cover design andphotograph bysusan c. dunn.exposure of lower gasconade dolomite, gunter sandstone...

Cover design and photograph by Susan C. Dunn.

Water Resources Report No. 351983

HYDROLOGY OF CARBONATE TERRANE NIANGUA, OSAGE FORK, AND GRANDGLAIZE

BASINS, MISSOURI

by

E.J. Harvey and John Skelton,U.S. Geological Survey

and

Don E. Miller,Missouri Department of Natural Resources,

Division of Geology and Land Survey

with a section on

Engineering Geology ofConns Creek Drainage System

by

Thomas J. Dean,Missouri Department of Natural Resources,

Division of Geology and Land Survey

G

MISSOURI DEPARTMENT OF NATURAL RESOURCESDIVISION OF GEOLOGY AND LAND SURVEY

Wallace B. Howe, Director and State GeologistP.O. Box 250, Rolla, MO 65401

Library of Congress Card Catalog No. 82-620024Missouri Classification No. MO/NR. Ge 9:35

Harvey, E.J., Skelton, John, and Miller, Don E., 1983, HYDROLOGY OF CARBONATETERRANE - NIANGUA, OSAGE FORK, AND GRANDGLAIZE BASINS, MISSOURI:Missouri Department of Natural Resources, Division of Geology and Land Survey, WaterResources Report No. 35, 136 p., 38 figs.• 35 pis.. 10 tbls.

ii

CONTENTS

Page Title

1 ABSTRACT

2 INTRODUCTION3 Purpose and Scope4 Definition of Terms and Conversion of Units6 Well Location System6 Methodology and Types of Data Collected

g DESCRIPTION OF THE AREA8 Climate8 Physiography and Land Use

17 Profiles of Streams20 Development of Karst Features26 Geologic Setting26 Stratigraphy28 Cambrian Rocks28 Ordovician Rocks28 Mississippian Rocks30 Alluvium, Colluvium, and Upland Residuum30 Structure

31 GROUNDWATER31 Description of Aquifers38 Groundwater Movement60 Relation of Well Yields to Topography and Subsurface Solution

Development61 Groundwater Quality

67 SURFACE WATER67 Magnitude and Frequency of Low Flows86 Seepage Runs92 Classification and Description of Streams94 Water Quality of Streams and Springs

99 GROUNDWATER-SURFACE-WATER RELATIONSHIPS99 Factors Affecting Relationships99 Groundwater Tracing

102 Vegetative Indicators of Hydrologic Characteristics102 Analyses of Groundwater Levels and Flow Patterns105 Osage Fork-Niangua River105 Dry Auglaize Creek-Goodwin Hollow-Niangua River107 Bear Creek111 North Cobb Creek111 Steins Creek-Parks Creek113 Drainage-Density Analysis116 Remote Sensing and Thermal Data

iii

Po,. Pille

11 lA-1C

12 2A·2B13 3A·3B

"4A·48

22 523 6A-582. 7A-7B25 832 9

33 1037 llA-llB

56 12A-12887 1397 14A·14C

100 15

106 16A106 168106 lBe109 17A109 178110 lOA110 188119 19A-198

Page Table

27 1

34 240 360 •62 5

71 696 7

117 8

122 912. 10

vi

PLATES (All photographs)

Wooded topography along the lower Niangua River

Distribution of woodland along Dry Auglaize Creekland clearing on slopes, valleys, and upland ridges in the Jakes Creek drainageModified dendritic drainage patternsAerial view of Grand Gulf. Oregon CountyAerial view of a large sinkhole northeast of Hahatonka SpringKarstie development in Goodwin HollowAerial view of Carroll Cave, Camden CountyExposure of Lower Gasconade Dolomite, Gunter Sandstone Member of the Lower

Gasconade and Eminence Dolomite at Hahatonka SpringNatural Bridge just east of Hahatonka SpringHi!J1-c.apacity well and fish ponds at Ozark FisheriesTwo views of Bennett $pring poolStream·f1C1oN measurement made as part of seepage run along Mill Creek, Camden CountyViM of Hahatonka and Sweet Blue SpringsCharcoal packets ("bugs") being collected and replaced at Ozarlc. Fisheries spring, CamdenCountyView of Dry Auglaize CreekPoor sorting of streambank gravels along Dry Auglaize CreekAerial view of Goodwin HollowView of dry reach of Bear Creek, Laclede CountyView of streambank gravels along dry ream of Bear Creek, Ladede CountyView of Bemtels Ford on Bear Creek, Ladede CountyView of Cliff Spring, Ladede CountyAerial views of Corms Creek, Camden County

TABLES

Stratigraphic column showing generalized lithology and hydrologic dlaracteristicsTransmissivities and storage coefficients of aquifers and specific capacities of wellsRecord of wells in the project areaWell statisticsAnalyses of water from selected wells in the Osage Fork, Grandglaize, and Niangua RiverbasinsHydrologic data at low·flow sitesWater-quality data for springs and streamsSoil temperature differences in flood plain soils of gaining and losing streams at a depthof 2.5 ftDye tracing of subsurface flow in Conns Creek basinValley cross sections in Conns Creek basin, June 6-10,1977

Abstract

ABSTRACT

A hydrologic study of an areacomprising three Missouri Ozark basins(Niangua River, Osage Fork, and Grandglaize Creek) and an analysis ofhydrologic methodology for study ofcarbonate terranes have shown thatthere are intricate relationships betweengroundwater and surface water and thatthese relationships can best be understood by using a number of studymethods. None of the methods, however, can be applied independently todescribe the hydrologic system.

The study area is underlain by about1800 ft of Ordovician and Cambrianrocks, largely dolomite, uninterrupted bya consistent confining bed. As a result,vertical percolation of water hasenlarged openings along joints and fractures throughout the section, allowingrelatively easy passage of water.

An important controlling factor onthe hydrology of Ozark basins is theamount and type of structural deformation of the rocks. Faulting and jointingdeflect streams, alter streamflows, anddirect the underground movement ofwater.

The measurement of streamflow, incombination with geologic mapping, isone of the most important tools inhydrologic studies of carbonate terranes.Seepage-run data provide excellentinformation about the magnitude anddistribution of low flows within andamong stream basins, information thatcan be related to distribution anddirection of faulting and jointing, anddevelopment of permeability.

Current and historical groundwaterlevel data are also essential hydrologic

tools in studying carbonate terranes.Well depths, water levels, and yieldsvary greatly within short distancesbecause of variable development ofpermeability in the rocks. The classicconcept of a water table is approximatedin only a few places in the study area;these are in alluvial material alongperennial streams such as the NianguaRiver and Osage Fork.

An effective way to studygroundwater-surface-water relationshipsis to construct basin profiles, usinggroundwater levels and streamflow datain conjunction with topographic,geologic, and structural information.Such profiles include much of thepertinent data for hydrologic analysis.

Dry Auglaize Creek and GoodwinHollow in the Grandglaize Creek basinare underlain by the most extensiveunderground drainage system in theproject area. Dye tracing has shownthat both are hydraulically connected tothe Niangua River, beneath a majordivide. Field observations have shown(J) that more storm runoff is diverted toNiangua River by Goodwin Hollow thanby Dry AugJaize Creek and (2) thatstream reaches and tributaries nearestthe Niangua River basin have the largestinfiltration capacities.

An engineering geology study inConns Creek basin was useful in relatinga si te study to the broader hydrologicrelationships of an entire basin. Testdrilling showed that the alluvial fill isincapable of transmitting large volumesof water after a rain and that conduits inbedrock are required to carry such flows.

HYDROLOGY OF CARBONATE TERRANE

INTRODUCTION

A complex hydrologic system hasevolved in the Missouri Ozarks, wherecrustal movement has occurred oftenduring the geologic past and where morethan a thousand feet of soluble rockexist with no continuous confining bed tointerrupt the vertical passage of water.Impose upon the system a hundred yearsor so of artificial development reflectingthe increasingly diversified needs of theinhabitants, allow those needs tointeract with a hydrologic system thathas matured over a few hundred millionyears, and a complexity results thatmust be clarified to achieve anunderstanding useful to the inhabitantsin making decisions on how to live inharmony with the natural environment.

The Ozark region of Missouri hasmany desirable features making itattractive for future intense development. For example, the weather isgenerally moderate; the area is notdensely populated; the perennial streamsof the area are clear, cool, and fed bynumerous springs; and groundwatersupplies are generally unpolluted andhave been adequate for most uses.

The prospect of extensivedevelopment has caused concern aboutthe future quantity and quality of waterresources. A primary reason for concernis that numerous streams and uplandareas in the carbonate terrane of theMissouri Ozarks recharge the groundwater system, which is used extensivelyfor water supplies and is the source ofthe many large springs in the region.

In areas with losing streams, anunderstanding of the hydrologic systemis needed to insure that streams andaquifers are not contaminated. In order

2

for responsible officials to manage waterresources wisely, they must haveinformation indicating areas wheregroundwater pollution could result fromaccidental spills or unwise location ofwaste-disposal facilities. For example, anew sewage-treatment plant is currentlyreleasing effluent into a losing reach ofDry Auglaize Creek. Highways, railroads, and pipelines can be scenes ofaccidents and, thereby, sources ofcontaminants.

This report contains the results ofhydrologic investigations in three basinson the Salem Plateau, about 45 minortheast of Springfield (fig. 0. Theproject area included the drainage basinsof Niangua River and Grandglaize Creekupstream from Lake of the Ozarks, andOsage Fork, with a combined drainagearea of approximately 1500 mi2

The natural features of the regionare similar in many respects to those ofcarbonate areas elsewhere in thetemperate zone and greatly influenceregional hydrology. A number of thestreams lose all or part of their flow tounderground drainage systems; there areareas of extensive sinkhole developmentand numerous caves, springs, and seeps.

The decision of the MissouriDepartment of Natural Resources, Division of Geology and Land Survey, and theU.S. Geological Survey to make thisstudy was prompted by the need todetermine the supportive characteristicsof the various types of data collectionmethods and the desire to learn moreabout the hydrologic system in karstterranes. The three basins chosen forstudy are considered typical of carbonate basins in the Missouri Ozarks.

Introduction

PURPOSE AND SCOPE

The primary purpose of this report isto present hydrologic information on theOsage Fork, Niangua River, andGrandglaize Creek basins, with emphasison distinguishing losing and gainingstream reaches and their relationship togroundwater movement. An importantfacet of this phase of the study was thedefinition of the low-flow characteristics of streams in the area in sufficientdetail to implement Missouri Clean

Water Commission regulations; that is,estimate the 7-day QlO low flow at asmany si tes as possible. A second purposeis to evaluate methods used in defininggaining and losing streams, and todetermine their relation to the flowsystem, the geology, and the physiography, thus permitting future basinstudies of this type to be done morequickly and efficiently.

A - Niangua BasinB - Grandglaize Creek BasinC - Osage Fork BasinD - Pomme de Ter~e RiverE - HahatonkaF - Grand Gulf

EXPLANATION

.~... --• •• 1M• •.. ,

.-\.j-{J_.-f"Ll+.~·'. t--1 f-'.--J--+-.-j . I .

-LJ-. ' . T--'. . ---j l,----l, ._ ..l,-

.-.J]-.!-, rr-+i: L.l- , I\.. A . IN 'C' (

? . Y'-'~"'\" .i .. r-'-r" I' ",-r~T . Ie

L~{- 'L ~.

L.

Aigure 1. Location of Niangua RIver. Osage Fork. and Grandglaize Creek basins. and other featuresmentioned in the report.

3


DEFINITION OF TERMS AND CONVERSION OF UNITS

1. Conversion of inch-pound units toInternational System of units:

7. Cubic feet per second (1t3 /s) - Theunit rate of discharge. One ft3/s isthe rate of discharge of a streamhaving a cross-sectional area of Isquare foot and an average velocityof 1 foot per second.1 ft3/s = 7.48 U.S. gallons per second=0.646 million U.S. gallons per day.

8. Dolomitization The processwhereby limestone is partly orcompletely converted to dolomite bypartial or complete replacement ofcalcium carbonate by magnesiumcarbonate.

9. Dye tracing - In this report, dyetracing refers to the use ofrhodamine WT 20-percent dye solution as a tracer in studyingunderground movement of water andtreatment-plant effluent, from losszones on the surface to points ofresurgence.

10. Evapotranspiration Movement ofwater into the atmosphere by thecombined processes of transpirationfrom plants and direct evaporationfrom the soil.

1L Fault - A rock fracture surface orzone along which there has beendisplacement.

12. Gaining stream or gaining streamreach - A stream that generallyincreases in flow with an increase indrainage area. Water levels andsaturated zones are very shallow insuch stream basins.

13. Graben - A crustal block, generallylonger than wide, faulted downwardrelative to the rocks on either side.

14. Hiatus - A "gap" in rock sequence, asshown by absence of geologicalformations present in other areas,because of nondeposition, or erosionbefore deposition of succeeding beds.

group offormation

lIQuere kilo_meter Ikm2)

cubic meter per58COnd (m3/sl

To obtain51 units

cubic meter1m 3)

meter lml

centimeter persecond lem/sl

kilometer (km)

0.02832

2.590

B,

0.3048

0.00035

1233

, .609

4047

Multiply inchpOlJnd units

mile{mi!

foot per dey(ft/d)

foot lit)

acre-foot lacre-ttl

cubic foot persecond (ft3 /s1

3. Aquifer - A formation,formations, or part of acapable of yielding water.

4. Artesian water _. Groundwater undersufficient pressure to rise above thelevel at which the water-bearingstrata are reached in a well.

To convert temperature in degreesCelsius (C) to degrees Fahrenheit (F),use the following equation:F = 1.BC+ 32

2. Anticline - An upfold or arch of rockstrata in which the beds dip awayfrom the axis.

5. Base flow - Sustained or fair-weatherflow.

6. Base level of erosion - "An imaginarysurface inclining slightly in all itsparts toward the lower end of theprincipal stream draining the area"(Powell, 1875). The level belowwhich a land surface cannot bereduced by the erosional action ofrunning water.

4

15. Horst - A crustal block, generallylonger than wide, faulted upwardrelative to the rocks on either side.

16. Hydraulic conductivity - The volumeof water at the existing kinematicviscosity that will move in unit timeunder a unit hydraulic gradientthrough a unit area, measured atright angles to the direction of flow.

17. Karst, karstic A term looselyapplied to solution features andphenomena in carbonate terranes.Generally includes a wide range offeatures, such as caves or otherunderground drainage, into whichsurface drainage is diverted bysinkholes, solution-enlarged crevices,and related phenomena.

1&. Lithofacies map - A map showing theareal variation in the lithology of astratigraphic unit.

19. Losing stream or losing stream reach- Stream segment that loses all orpart of its flow to undergroundsolution cavities.

20. National Geodetic Vertical Datum of1929 - A geodetic datum derivedfrom a general adjustment of thefirst-order level nets of the UnitedStates and Canada. It was formerlycalled tlsea level datum of 1929" or"mean sea level."

21. Permeability - A measure of therelative efficiency with which aporous medium can transmit a liquidunder a potential gradient.

22. Potentiometric surface (map) - Asurface (map) representing the statichead. As related to an aquifer, it isdefined by the levels to which waterwill rise in wells.

23. Reconnaissance mapping - Defined as"a general examination or survey of a

lnnoduction

region with reference to its mainfeatures, usually as a preliminary toa more detailed survey" (Howell,1957). Geologic maps for this studyare more detailed than reconnaissance maps, but not so detailed thatthey show all minor structuralfeatures or exactly define all facieschanges in the area. The mapsgreatly helped the project hydrologists understand the flow system.

24. Recurrence interval - The averageinterval, in years, between occurrences of a low fJow less than thatindicated by the data. Recurrenceintervals are averages and do notimply regularity of occurrencej forexample, an event with recurrenceinterval of 10 years might occur inconsecutive years or might not occurin a 20-year period. An event with arecurrence interval of Ja years has aprobability of 0.10 (or a la-percentchance) of occurring during any givenyear.

25. Residuum Material remainingessentially in place after all but theleast soluble constituents have beenremoved by rock weathering anddecompositionj also called regolith.

26. Seepage run - A series of dischargemeasurements made at numeroussites aJong a stream reach, during ashort period of time, to identifywhere gains or losses in flow occur.At each point, measurements oftemperature and specific conductance of the water provide supplementary reconnaissance information.

27. Silicification - The introduction of,or replacement by, silica, generaHyas fine-grained quartz, chalcedony,or opal; it may fill pores and replaceexisting minerals.

5


28. Sinkhole A surface depression,usually without surface outlets,occurring in regions of soluble rockand connecting with subsurfacedrainage networks. Sinkholes arecaused by solution and collapse orsubsidence of the underlyingformation(s).

29. Specific capacity - The rate ofdischarge of water from a well,divided by the drawdown of waterlevel or head in it. For example, if awell yields 200 gpm (gallons perminute), with a drawdown of 50 ft,its specific capacity is 200/50, or4 gpm per foot of drawdown.

30. Standard deviation - The square rootof the arithmetic average of thesquares of the deviations from themean.

31. Stromatolitic reef A structuremade up of stromatolites, laminated,variously shaped organosedimentarystructures (stratiform to columnar,nodular, or subsphericaI) produced bymicro-organisms, predominantly (atleast in the case of modern forms)blue-green algae (Cyanophyta).

32. Syncline - A fold in rocks in whichthe strata dip inward from both sidestoward the axis.

33. Transmissivity - The rate at whichwater of a prevailing kinematicviscosity is transmitted through aunit width of the aquifer, under aunit hydraulic gradient.

34. Water table - The upper surface of azone of saturation except where thatsurface is determined by impermeable overlying rock.

35. Wrench fault - A nearly verticalstrike-slip fault in which the net slipis partially in the direction of thefault strike_

36. X-day Qn - The average minimumflow for X consecutive days, with a

6

recurrence interval of n years. Forexample, the 7-day QlO is the 7-dayaverage minimum flow, with arecurrence interval of 10 years.

37. Zone of saturation - The crustal zonein which all voids are water filled.

WELL LOCATION SYSTEM

In this report, well locations arereferred to in accordance with thesystem of the Bureau of LandManagement Survey, using the followingorder: township, range, section, quartersection, quarter-quarter section, andquarter-quarter-quarter section (lO-acretract). The subdivision of a section isdesignated a, b, c, and d in counterclockwise direction, beginning in thenortheast quarter. If several wells are ina la-acre tract, they are numberedserially after the above letters, and inthe order inventoried.

METHODOLOGY AND TYPES OF DATACOLLECTED

One purpose of the project was to usea number of methods of investigationand determine to what extent resultsfrom each method supported the others.

Methodology and types of datacollected included the following:

1. Water-level measurements, includingconstruction of a potentiometric mapand groundwater profiles.

2. Streamflow measurements, includingseepage runs on all major streamsand on most of the tributaries.

3. Geologic mapping.

4. Identification of plant assemblages atall streamflow measuring sites.

5. Stream-profile analysis to definerelationships between streamflow,geology, and stream gradient.

6. Engineering geology study of soil,shallow bedrock, structural features,and streamflow in Conns Creekdrainage basin, a losing tributary ofWet Glaize Creek.

7. Dye tracing to determine subsurfacemovement of groundwater frompoints of loss to points of resurgence.

S. Soil temperature studies in the floodplains of streams with shallow(gaining stream) and deep (losingstream) water tables.

9. Analysis of drainage density and itsrelation to low-flow frequency.

Introduction

10. Analysis of physiographic development and its relation to runoff andsurface geology.

11. A study of well yields from theseveral aquifers to determinerelations between yield and topographic situation, producing formation, and location within a gaining- orlosing-stream valley.

12. Analysis of water-quality datacollected on wells, streams, andsprings. Potential usefulness of suchdata in basin-type studies wasevaluated.

13. An analysis of the practicality ofremote sensing and thermal-imagerydata for these studies.

7


DESCRIPTION OF THE AREA

CLIMATE

The project area has a humidcontinental climate, with changeableweather and extremes of temperatureand precipitation in some years. Theaverage temperature (all averages basedon 1941-70 data at Lebanon) is 56.1 0 F.The average for July, the hottest month,is 77 .2°F and for January, the coldestmonth, 33.40 F. The average annualprecipitation is 40.4 in. Usually, themaximum monthly precipitation occurs

in April (4.09 in.); the minimum, inJanuary (I. 78 in.).

During the current study, thevariability in the climate was evident,with some significant departures fromthe 1941-70 averages at Lebanon. Thefollowing table summarizes abnormaltemperature and precipitation during theperiod of data collection for this project:

Temperature and precipitation departures from 1941-70 averages at Lebanon, Missouri

(Data from National Oceanic and Atmospheric Administration)

Year Temperature departurefrom average

IF)

Precipitation departurefrom average

On.)

1974

1975

1976

1977(January - September)

PHYSIOGRAPHY AND LAND USE

-Kl.2

-Kl.5

-0.5

+6.5

+3.3

+2.3

·12.7

+9.6

The topography of the project area isshown in figure 2. The land surface isgently rolling in the central and southernparts, where much of the land iscultivated (fig. 3). Relief in the areaaround Lebanon is generally less than100 ft, and even along the streamsdraining from the Marshfield-Lebanondivide, relief is low.

Along the main stems of the OsageFork, Niangua River, and GrandglaizeCreek, relief is greater, especially alongthe lower half of the Niangua River inthe northern part of the area. Little of

8

the gently rolling land so prominent nearLebanon remains, and ridges betweentributaries are long and narrow. Slopesalong the lower Niangua River aremostly wooded (fig. 3 and plate O.Dolomite bluffs are 200 ft high in somereaches, and 100 to 150 ft high alongOsage Fork and Wet Glaize Creek.

Total relief along the Niangua Riverand Osage Fork ranges from 100 to300 ft. The character of the relief isdifferent, however, as shown by thedistribution of woods and cleared land.The amount of woodland remaining is

Description of the Area

93°00'00"

38°00'00"--+EXPLANATION

Contour lnter....ol: 200 Feet

~ 600-800

L:J 800· 1000

c:::::::J 1000 - 1200

1200 - 1400

_ 1400·1600

All el.....otlon. In Fut obo....eNational Geodetic VerticalDatum of 1929.

10 0 10 Mil••

ITII r::r;~l====rI==:::::J110 0 10 Kilometers

Bose from U.S. GeoloQlcol Sur ....eystat. bo.. mop, I' 500,000.

Figure 2. Topography of the Niangua River, Osage Fork, and Grandglaize Creek basins.

9

EXPLANATION

Note: Forest cover interpretedfrom ERTS photograph, waveband 5, December 15, 1972,Notional Aeronautics and SpaceAdministration.


93°00'00"

,aooo.oo..-t

Bose from U.S. Geologicol Surveystote bose mop, I: 500,000

10 0 10 Miles

b:::lI =;=::I:I:lt:::::::===!'===:J1I-J..l-1-l.l.ll I10 0 10 Kilometers

Figure 3. Areal distribution of forest cover.

10

•D Forest Cover

Cleared Land

Plate 1. Wooded topography along the lower Niangua River, showing the long, narrow ridgesbetween tributaries. Note accordance of topography in lA and lB. The broad, flat featureshown in the center of lC is the valley floor of the Niangua River near Sweet Blue Springin T. 36 N., R. 17 W. Photographs by James E. Vandike.

A

B

c


determined by the relief (plate 2). Inareas of high relief, cleared land ismainly in the valleys; in areas ofmoderate to low relief, it is on thedivides as well as in the valleys.

In recent years, cattle grazing hasgreatly increased (Missouri Crop andLivestock Reporting Service, 1976).Between 1941 and 1970, a moderateyearly increase in cattle grazing

A

B

Plate 2. Distribution of woodland is determined by relief. In areas of high relief, such as the viewnorthward in Dry Auglaize Creek basin, shown in 2A, cleared land is mainly in the valleys.View 28 shows clearing of moderate slopes in the area of an abandoned meander loopalong Dry Auglaize Creek. Photographs by James E: Vandike.

12


"ol!

"'" -:10<"\lr i. --.

'" ~... , ~, ,

">;~,

"," "-

'< ."1\' .\:\ .,{- • , -"'", .....

A

Plate 3. Land clearing on slopes, valleys, and upland ridges, resulting from increased cattle grazingin the area, is shown in 3A and 38. These are views of land clearing in the Jakes Creekdrainage, in sec. 34, T. 36 N., R. 18 W., Dallas County. Photographs by James E. Vandike.

occurred in all of the study area. In1975 an increase of 45 percent over 1970surpassed the average increase duringprevious 5-year periods. Concurrentwith this increase in cattle population,much land has been cleared, slopes aswell as uplands (plate 3).

Although there has been considerableclearing, some tracts have reverted toscrub timber growth. Cleared land andtimbered land would tend to counteracteach other in their gross effect onprecipitation as it becomes groundwaterrecharge and base flow, surface runoff,

13


Plate 4. Modified dendritic drainage patterns in the study area reflect strong structural control. ThegO-degree bends shown in 4A and 48, along the Osage Fork of the Gasconade River, inT. 33 N., R. 15 W., are examples of such control. Photographs by James E. Vandike.

or vapor. Figure 3 depicts forest coverin 1972; no doubt the future distributionwill differ in detail.

The hydrologic effect of smallchanges in land use is difficult orperhaps even impossible to measure, buta substantial conversion from woods topasture might allow a comparison ofhydrologic conditions before and afterthe change. However, records collectedsince significant conversion to pastureland are few and do not indicatesignificant effects on hydrology.

The modified dendritic drainagepattern in the area reflects the stronginfluence of fault and joint patterns.

14

Many 90-degree bends in main stem,tributaries, and divides occur throughoutthe area (plate 4); many short reaches ofstreams have straight northwest, north,and northeast segments that suggeststructural control. Solution alongfracture systems was important in theposition of valleys and divides. Forexample, the ridge that divides theNiangua and Osage Fork, extending fromMarshfield to Lebanon, is offset severalmiles to the northwest in the area wherea northwest-trending fault zone crossesthe upper ends of the two basins(compare figs. 2 and 4, in pocket). TheEast Fork of the Niangua is extendingheadward into the Osage Fork basin,offsetting the divide.


Plate 4 (continued)

B

Other topographic and hydrologicfeatures reflect structural control:

I. The southwestern boundary of theproject area forms an unusuallystraight linej the south corner, a 90degree angle.

2. The upper Niangua parallels anorthwest-trending fauJt zonej apronounced change in the gradient ofOsage Fork occurs at an altitude of1220 tt, in approx.imate alignmentwith the fault zonej and four springsat the Dallas-Webster County line,near the intersection of this fault anda northeast-trending fault, markedlyincrease the flow of the NianguaRiver.

3. Dry Auglaize Creek flows approximately 7 mi northwest in a graben(fig. 4, in pocket), a structurallycontrolled reach containing thejunction of Goodwin Hollow and DryAuglaize. After the junction, DryAuglaize Creek leaves the graben,flows north approximately 18 mi, andabruptly turns east to the junctionwith Wet GJaize Creek.

4. The Niangua River abruptly changesfrom a northwest to an easterlycourse just downstream from themouth of Greasy Creek (fig. 4, inpocket), continuing thus about 8 mibefore flowing north again.

15


.0

11~

~~

GJiii

EXPLANATION

Foull. wlt~ orrOWl indicatlIMJ uplhrownand Iklwnth.own eides.

Jelfenotl ClIy 00Ic....1I aMIColle. Dolomite

Roubkloull FQflllolion

Gole_de Oolomlll

30

•i!",•<,

o •o '"

•~••

'" 60 00

DlltOIlU, ill ",il.. , uplfreom from mout~.

o '0 30 '" 60 00

i! '0

'.0

Oiseho'Qe mea.uredAuou.t 23 - 26, 1976

Figure 5. Stream gradient and discharge, Osage Fork.

16

5. Probably the outstanding example ofstructural control on topography andhydrology in the three-basin area isillustrated by the relationship of thethree basins to each other. TheNiangua River reaches a commondivide with the Osage Fork flowingeast and the James River to thesouth, and the Grandglaize Creekbasin is cut off (fig. 2). The ridgeseparating the Wet Glaize from theDry Auglaize, paralleling the grabenin which the Dry Auglaize flows, andforming a part of the CamdenLaclede County line helped restrainheadward development of theGrandglaize basin. As a result,assuming the Grandglaize andNiangua began their southward basindevelopment more or less simultaneously before the last Ozark uplift(Bretz, 1965), the Grandglaizesystem, which includes the WetGlaize, Dry Auglaize, and GoodwinHollow, did not advance headward(southward) as rapidly as the NianguaRiver. As shown in subsequentsections of the report, only the WetGlaize basin presently (I 978)contributes continuous flow toGrandglaize Creek, and most runofffrom Dry Auglaize Creek basin isdiverted westward to the Nianguabasin.

Profiles of Streams

The main streams, such as OsageFork and the Niangua River, havemoderately smooth, concave profilesthrough the downstream 75 percent oftheir reaches (figs. 5 and 6). Theaverage gradients of Osage Fork andNiangua River are nearly the same: 3.6and 3.9 ft/mi, respectively. However,the rate of descent of the Niangua isgreater in the upper reaches than that ofthe Osage Fork, indicating greatercutting power along the upper part ofthe Niangua River.


In short reaches of the streams (figs.5 and 6), there are many irregularitiesthat may reflect lithology orstratigraphy; others are due to faultsthat may abut strong and weak beds.Still others result from substantialinflows or losses of water orcombinations thereof. Since runningwater is mainly responsible for shapingvalley profiles and for headwardextension of valleys, quantity andduration of flow are important factors;nevertheless, lithology and fracturing ofrock are overriding influences ondetailed sculpturing of profiles.

The contrast in gradients in the upperreaches of the Osage Fork (fig. 5) arethe most pronounced: 28.6 ft/mi and 7.4rtfmi in adjacent reaches. Thesteepened reach is near the southeastextension of a Niangua basin fault(fig. 4, in pocket) paralleling the mappedfault crossing the Osage Fork about 3 midownstream. Because several northwesttrending faults cross the area in thisvicinity, variations in lithology betweenadjacent fault blocks could cause thesegradient changes. No marked increase inflow occurs here.

Some of the best indications of apossible relation between spring inflowand gradient are evident in comparingthe profiles of three tributaries of theNiangua River and Osage Fork (fig. 7).Mill Creek, a spring-fed perennialstream, changes gradient markedly atsprings about J mi upstream from itsmouth. The profile of Mountain Creek, astream generally dry throughout itslength, is nearly featureless. NorthCobb Creek, an Osage Fork tributary,perennial in its lower reaches, has anormal concave profile to within 7 mi ofits mouth. In downstream reaches thegradient steepens as perennial flowbegins, and continues on a new concaveprofile to the mouth.

17


..0 •< •" of~

0 Of •.. •~i • 0

"'l> 0 •3 ~ h .. Q

~ "- •40 11 • • .!!;;; ~~ • w• • ~ - • :. •.. .. • .. .: - • - .::,. u <z • - •i u .. < 0 ..

j .. • • < ::• '. < .. • " " .:;• • i! < •~ ~• i • • ~ ::::~ 30 ~ ~

_." c ~ .:::.. ,':':

.t ::::::.. ::.:::{

.g :{:};• 20

:rf11~1~~1~

.3 .::;:;:;:;

10 ,;/::~:.,;;:;:::::::::::;:;.;.;::::.:.......•••... QR

10 20 30 40 30 60 70 BO 90 100Dlsfonce, I. miles, upstream from mouth.

0 10 20 30 40 30 60 70 00 90 100

100

~gu

1.-l....t."••u•• 10,;~••u•"

1.0 *[iJ~

II

EXPLANATION

Faull, with arrow. indicating upthrownand downthrown ,ides.

Jefferson City Dolomite andCotler Dolomite

Roubidoul. Formation

Gasconade Dolomite

Discharge mea luredAugust 24 . 26, 1976

Figure 6. Strecm gradient and discharge, Niangua River.

18


"'" •N

,!!! 0•- •0

~

E •Z 1300 Surface flow ~

~

<3 begins In this <

-- /.. reoch.

\,

"~

1200 •~

..I< )jlf

~

~;;1100~

0•"..<.2 10000 NORTH COBB CREEKz• (Osogl Fork bOlin)>0~ 9000.."-"".2 a 2 • 6;; 8 10 I.>• Distance, In mil•• , upstream hom mouth.

'"

Dlstonce, in mile., upstream from mouth.

MOUNTAIN CREEK(Niangua River bosln)Not.: Stream hal noflow Ilxc:ept during.torm•.

0ls10nce, In mil•• , upstream hom mouth.

MILL CREEK(Niangua RI'Ilr batln)

64

~--":>'~~~

80"Flow

2a

..N!!!;;E,

1100;;0

0."~

1000

.";;~0 900•";;<.2;; 800z•>0~0 700-'•

"••g"'S>•w

10864za

800

900

1100

1000

12.00

•"-""••

Figure 7. Stream profiles of typical valleys in the Niangua River and Osage Fork basins.

19


800 t~

J•;

1.-00 !

f'200 •

tI

•1100 f

j

1000

5•j•]

Ol,'anu. In IIIitn, 1l1l.lr.'III 'ralll LaU 01 III' O.arill.

/flood PlaIn P_"_'''~'__

l_------':-::::::::::-::=='=:::::::::::::::=;i~-;.~--:,...---100 _---1(.._.".. ""'"---1OO+----,---.---r---,--.-----.--,------.---.---,--...,..---+6oo

o ~ ~ ~ ~ ~ ro ~ ~ ~ l~ ~

'100

1000

Figure 8. Stream profile of the Niangua River.

A long, subtle flattening in the slopeof Niangua River begins near the mouthof Dousinbury Creek, extends to BennettSpring (fig. 8), and includes that reach ofthe Niangua River that changes directionabruptly from a northwest to an easterlycourse (fig. 4, in pocket). Where theflow increase of the stream is notsufficient to keep it at grade (the dashedline in fig. 8), the grade flattens. In thisreach of the Niangua River, tributariescontribute very little water, and there is1ittle increase in discharge in theNiangua itself. The profile begins tosteepen in the vicinity of Bennett Spring,reaching its projected normal profile inthe vicinity of Lake Niangua. Not untilBennett Spring Creek, Sweet BlueSpring, and other springs and tributariesin the downstream reach add theirdischarges does the gradient steepensufficiently so that there is a return towhat may be considered a "normaJ"gradient and profile.

In many cases, marked changes ingradient in short reaches along the mainstreams may be logically attributed todifferences in lithology or to structure,whereas the longer, more gradualchanges are due to discharge. Along thetributaries, either flow, lithology,structure, or a combination of thesefactors may cause changes in gradient.

Development of Karst Features

Sinkhole topography is prominent onthe level areas extending along thedivides radiating from Lebanon (fig. 9).The broad area underlain by theRoubidoux Formation lies between 1200and 1400 it above the National GeodeticVertical Datum (NGVD) of 1929, andcontains most of the sinkholes (comparefigures 2, 4 (in pocket), and 9). In thiskarst recharge area, dry or intermittentstreams are the rule and groundwaterlevels are deep. Between 1000 and

20


10 0 10 Miles

b::, ==::I:dt=:::=~==:::::J1j..l..l..U..I.. I

10 0 10 Kilometers

EXPLANATION

•

,

,,

,

••

•

•

Note: Geology from Figure 4.

Bose from U.S. Geological Surveystate bose mop, 1:500,000.

•"'....••

•

•

•

,"•"

•

••

•

•••

•

Gasconade Dolomite(Ordovician)

SInkhole

Cave,•

-

Figure 9. Areal distribution of caves and sinkholes.

21


1200 ft, there are fewer sinks in theRoubidoux, and as relief increases, theybecome even less numerous. Few liebelow 1000 ft or in the GasconadeDolomite, the formation generallycropping out at lower elevations.

Plate 5.Aerial view of Grand Gulf, Oregon County,showing an advanced stage of karst development in Ozark car~onate rocks. This sinkholeis approximately 200 ft deep and about onemile long. Drainage from Grand Gulf is toMammoth Spring, Arkansas. several miles tothe southeast. Photograph by Jerry Vineyard.

22

Sinks in the area are of two types:(1) shallow, broad, and open, and {2} deepand chimneylike. The shallow ones arecaused by steady subsidence, whereasthe chimneylike sinks are due to suddencollapse. A few have been observed inthe losing reaches of stream valleyswhere groundwater levels are 50 to 75 Itbelow flood plain. Although sinks. arecommon in the project area, theirpresence does not preclude a welJdeveloped surface-drainage network.Stream density, however, is less wheresinks are common.

Stages in development of karsttopography in the project area can bestbe appraised outside it. In Grand Gulf,Oregon County {fig. 1), the mostadvanced stage of development is acollapsed vaHey, a chasm approximately200 it deep and a mile long {plate 5}. Inthe upland bordering Grand Gulf, itwould probably be necessary to drillwells more than 200 it deep, as thewater level would probably be below thatdepth. Along Logan Creek in ReynoldsCounty ({ig. 1), an infrequently flowingintermittent stream, groundwater levelsare as much as 250 it below flood plainlevel. Sinkholes, representing an intermediate stage of karst development,occur on the flood plain along the valley.Just north of Hahatonka spring is a largesinkhole, spanned at its northeast end bythe natural bridge illustrated on plate10, that probably has some connection tothe spring system (plate 6).

tn the project area, in a lessadvanced stage, Goodwin HoJlow haswater levels 70 to 100 it below the floodplain, and the stream seldom flows(plate 7). In each case {Grand Gulf,Logan Creek, and Goodwin Hollow}, thesurface stream has been pirated, andeach feature represents a different stagein geomorphic development by corrosional work of underground waterreplacing much of the abrasive work of


A

B

Plate 6. Aerial views of a large sinkhole northeast of Hahatonka Spring, in sec. 2, T. 37 N., R. 17 W.,that probably has some connection to the spring system. Photographs by James E. Vandike.

Sinkholes and caves are surface andsubsurface manifestations of underground drainage. Both may have readily

surface streamflow. As subsurfacepirating encroaches from the NianguaRiver on the west, Goodwin Hollow mayeventually show more of thecharacteristics of Grand Gulf, and DryAuglaize Creek will assume more of the

topographicHollow.

character of Goodwin

23


A

B

Plate 7. Karstic development, less advanced than Grand Gulf, in Goodwin Hollow. 7A is an aerialview upstream in the headwaters, showing classic losing stream characteristics. 78, takenfrom a bridge on U.S. Highway 5, sec. 27, T. 36 N., R. 16 W., during a heavy rain, showswater moving into the subsurface and marking the farthest advance of surface-water flowduring a single storm event. Photographs by James E. Vandike.

accessible openings into the undergroundsystem at the land surface or theopenings may be completely hiddenbeneath the landscape (plate 8).

Much has been written about the roleof caves in a karst drainage system.

24

Stringfield (I 969) lists some of theinvestigators who have hypothesized onwhether development of caves andenlargement of fractures have occurredabove or below the saturated zone.Following is a tabulation of theiropinions on the subject:


Cavern development in relation to the saturated zone

Investigator Below Abo.. Near Remarks

Grund (1963) X

Matson (1909) X

Meinzer (19231 X Uplift

Swinnerton (1929) X

Dallis (19301 X Two-qcle; uplift

Piper 11932J X

Gardner 119351 X X

Theis (1936) X

Malott (19381 X

Moneymaker (1941) X

Thombury (1954) X Caves are giant nodes

Bretz (1956) X Three cycle; uplift and filting

Thrailkill (1968) ? ? Calles and sinks only indirectly related

Stringfield (1969) X

Plate a. Aerial view of Carroll Cave, sec. 20, T. 37 N., R. 14 W., Camden County. This cave, one ofmany in the study area, is one of the more spectacular karst features familiar to the public.Only a small fraction of subsurface open spaces resulting from karst development formslarge openings such as caves. Photograph by James E. Vandike.

25


It is apparent there are considerabledifferences in interpretation, influencedin each case, perhaps, by the part of theworld where studies were conducted.

The following outline presents ourinterpretation of the development of theNiangua River and Dry Auglaize Creekbasins:

1. Consequent streams initially.Differential headwater lengtheningof streams, the Niangua lengtheningmore rapidly than Dry AuglaizeCreek.

2. Fractures allow penetration of waterbelow the surface mantle. Movementof water and opportunity to descenddepend on development of adischarge area. Early solution rapidbut selective in zone of aeration;slower but more widespread and morecontinuous in the saturated zone.With increase in head differencebetween contributing area andreceiving area, movement becomesmore rapid, and there is increasingsolution near or above the zone ofsaturation as greater volumes ofwater are lost by the higher stream.It ·would seem, therefore, that theremust be solution both below andabove the saturated zone, butinitially more below than above.

3. Faulting, jointing, etc., mustinfluence direction of discharge.Assuming the Niangua River and DryAuglaize Creek began their headwarderosion contemporaneously on anemerged or rejuvenated land surface,many factors such as lithology of therock units, intensity of fracturing,and differential uplift determinedwhy one valley became a receivingarea, and another, a contributingarea. In this case, the Niangua Riverbecame the receiving area and DryAuglaize Creek, the contributingarea.

26

GEOLOGIC SETTING

Stl'"atigraphy

The project area is undedain by asmuch as 1800 ft of Ordovician andCambrian rocks, largely dolomite. Table1 lists the formations in the pl'"oject areaand describes their- lithologic andhydrologic characteristics.

The stratigl'"aphic section thatincludes the principal aquifers throughthe Potosi Dolomite is uninterrupted bya consistent confining bed. As a result,vertical circulation of water hasenlarged openings along joints andfractures, allowing freer passage ofwater from the surface through thePotosi Dolomite.

Pleistocene and Recent alluvial,colluvial, and residual deposits coverbedrock in the valleys and uplands.Except along the river bluffs, exposuresof bedrock are discontinuous over muchof the area.

The section can be divided into twoparts. One comprises the upper 1000 ftor so containing the important aquifersof this study, including the formationsdown to and including the PotosiDolomite; the other, those formationsbetween the Derby-Doerun Dolomite andthe Precambrian igneous and metamorphic rocks.

Much of the section below the DerbyDoerun Dolomite contains siliceousmaterial largely deposited in a deltaicenvironment. Those deposits above theDerby-Doerun, which constitute themajor part of the section containing theimportant aquifers, were mainly formedin a shallow carbonate platform environment to which only small quantities ofdetrital materials were supplied; hence,carbonates are the principal rock


TABLE 1

Stratigraphic column showing generalized lithology and hydrologic characteristics8y".... Gn,up, fo,"'otion, "''''''bof Thick..... Lithologic <lll>c,iption Hydml"llic ch..oct..;..ics

Oo.>OlI""ry Alluvium, ooll..ium, and ~, Une"",oIjd.lld unO., .ill".nd c1.y wi\h D... '0 1"90 froction 01 linoil,oined ""lOri.I,upl.,.j ,e>iduum "'9'1., '0 'oondo<! ctl<'1 "_n".:>o;1 "'0' 11>_ doPOl'" ",".lly h."" 1'00' w'\ll'·t:.ori"')

fil.. ",ulily cootlin, lrogipon '''''•. chorlC,",i"i",_

Mi..i..ippi.n BII~in\llon·Kookllk.No'th- ().l50m Che"y li"""t.......il"'on•••nd lI>in·bo<!dod Mi .. i..ippi.n wdimen'.'Y ,ocI<. h... limitld

vitw. Co<n!>''''' 1m., c,inoKl.llimellono. ..... eKtent; not impe,ton' •• 111 .quit., in

IIndi.ido<l "lIdy"e•.

COlte' Dolomi,. "'" Rol.,i••ly """""lfly••rg;II0ce0"'. thin- '0medium-t>eddod dol"",il'. Simil."o.nd Ho,i,onl" pe,meobili'y of Ih... uni" .ppe."loclily "'" di.lin~i",.bI.hom IIndo,lying 10 be quill low. yitl'" of wello f",iohed inJeffeBOn City Doiomilt. ColllhleU.""" Ci'y interv.llf. 2-35 gpm.

.Jeff."on City Oolomill ,·no Thin-_. fi... ly '0 modillm-<:,ys,.IHno. \h....,. being oppoKimol.ly 7 gpm.

orgjlllClO'" dolomi.. w,'h nll""'OII' in'.'v,l,Oboe...I;on·wIIi d.l. indicoII ••rticol pe,-

of Ihick't>od<led. m..,i". c....,ly. b,own .......,ility high .n<>Ugh 10 pe,m;t "dl.rge In

doIomi'., Sumo Ihin. inttrt>oddo<l g'otn ",.1. ..... who,. '"nofl i. nol "pid,

loc.lly po-...n!.

Roubi~K Formotion 0,'80 Finoly to medium-cry.IIlI; .... ,hin"o lI>ick- Modo..'o 10 good l>o,i,on,.11nd .."icol per-bedded. merry dolomi,. wi.h in"""" of Ii ... - ......biliry. Wt1I. yi.i<1 1·50 gpm. Pond> and'0 medillmil'o<nod dolomitic ..n<htono, I.k .. in 'hi. fo,m.,ion often do not hold

Ord""id'n LOCOlly dlllocteri,od by 'ipple mo'ko. m'" w,I,.. M.ny I..ing " ...m ._n" in thi.etlCk<, and b..cd. ,one._ lorm.,i ....

Uppe, Gosconodo Oolomi,. 0-1IlO Finoly 'oc<>l"oly cry"a1lin•. v"9ll'l, INS"".Ii~'·bfowni"'...-.. dolom',., .. Ioti .. ly ctl<"

Good ho,i'onlll.,.j .."icol pe...,.oI>lIl'y ..". W.11o finished in 'hi. inlo..01 yi8ld 2O-751lP'".L....., GISC... iIdo Oolomi,. 205-385 Finoly '0 medium-<:ry.ulli"". min- '0 mldium' RePO'" o! .itl"' .. hi~ .. 150 1lP""" not

beddod, morty dolomi ... C'YP""""" ,III IIncommon. bill ... un.ubsllllti.tod_ Uni..m......nd lI>in .ond"onc bodi..... ioo,lI. coo,.in numc,ou. c.... , .",i"9'. ond oth.."'.....,. k.", te.tur... llld ar" imPO<tIII' in ..a1l1lting

Gun.. , Slnd"ono mb'. "., Mtdium1l""'od _dttono will> dolomilic .u,f......" .. -lIrooo<!w.,<r ..1.,iornhipS i" the

co"",n,; b<com<' mort dolomi'ic in \h. basin ""'y or••_S"otigrop/lic.Uy. tho I......'

.....'.m prt't of ,t>c "udy ..... SondI'one unit CfUPPing <;<I' in tho It"'y .... is lOWl'conlon' v.. i<o be .....n 2Dl'.nd lOO'J(,_ G...,onodt Dolomil'.

Emi ...nc:o Dolomi'. 240-600(11 Modillm' '0 oo".. ly Cry"oIli"". medillm- Thi. unit not on im_,on' oqllifo, in tho .rudy

bedded '0 m...i•• dolomi... Sm.11 om"",," "vdy ''1'. Yi.ld, 10 _II. or, B-\OOgpm. the

of d>c" ",...n,. primo'ity in tho "I''''' plf' "". I>cing 11>011' 20 gpmof fo,mllion.

l'<>'OIi Oolomi,. 00·"" Fi .... ly '0 medium-ery.lIllino. m... i""ly Thi. unil on impot'on' oquif<, for well. in thebed<Ied bfowniol111"y <hofly <lolom;IO; con· ,,"dy ..... T.... indicotl yi.I<II of 80·750

I.i", obundon' qu.'" d",... IIPm I,om ... 110 finiol1od i" tho Pot..i. WI-.

..••, .. ","ifo" or. open '0' well. yillds ..

hi~ .. 500 g.pm ". po"ibl.

o.,by·Dot'un Oolomill 8OlII-215 Ala'n.ti"') thin· '0 medillm-bedded dolomi...lI>in-becIded .it",ono, and ",.I<;doIomill i.fi"" gnintd ••i1tv ond .r~IIIC"",,'.GI.uc""il'locolly j>fflIn' in 11>. IOWI' por' of fo'motion. Thi. in..,.,a1 i. not ;mPOt'on'" on oquOf" in

Cambl'i.n D•• i. Fo'''''I;o" 50-380(11 Silt>'one. fi""'9'oinod .",,<lo'''''', dolo",i". tho ",ooy .....

IIId "'01,. wi'h Iime.tono CO"'JI"""' .... 1"".lIypr...n,- Siluton< IIId .ondo'o"" coo,.inglouconi'._

Bonno'.... Formotion 85·200 Finoly '0 me<!illm-ery"a1li"". mcdillm-<>ed<lcd Inoonelll.i.... inform..i"" <:onoIming yiOI"'.dolomite Ind lim,"one. In .rudy oro•. limo- bII' in'.",.1 probably not '0 be comKII.... on

" ..... con"i..... 40% to 9Oll. of tho corbonote impo'tonl SOIl'OO of w... , in the ..udy " ...

ffoeti"" of the formotion, Uni' "1.,,••lym'" fr...

Lorno'.. Sandt,..... 14().JOO Fino- '0 medium-vro<ned .and""",,. Locolly Onl. 'h,.. _II. in 'ho It"'y .... pent,,.11

9' ..... I...'a1ly into Irk..ic m...,i.L Con- \hit unit;lInia f'om ..... Eminc""" \h'ough

g10m0Il'ic ma,..-i" loclily., buo. "",~yi"li Lomott.... II....-d. A.. ,ogc yi.I'" I.,.. "'"p.,,,,,,mb,i.,,. Thick..... of "klllic conlliom· L.mott, ..e 100-200gpm; 10tll y;"'" "om

er." '"'"9" f,om 0·00 ft. ",.110 ....ao·5(Kl\lP"l.

P,ecombr; ... Ignoo", and Mf,!lmOIPhrc No' importll'l'''' '00100 of w.tor in tho,~, "lIdy."._

27


material. At times, reefs formedlagoons in which detrital materials weredeposited and beds of sandstonealternate with reef deposits. In general,however, the depositional environmentthrough the Cambrian and Ordoviciancontinued to be one in which carbonateswere deposited, resulting in a rocksequence amenable to later widespreaddissolution, with few beds to interruptfree circulation of water to a depth of1000 ft or more.

Cambrian Rocks

Cambrian rocks are 1200 ft thick atlebanon and thin to about 700 ft at thewestern side of the area. They arepredominantly dolomite, with lesserthicknesses of limestone, siltstone, andsandstone occuring principally below thePotosi Dolomite. The Cambriandolomite above the shale of the DavisFormation is massive, with little shale orsandstone. Quartz druse is present inthe Eminence Dolomite and abundant inthe Potosij it usually indicatespermeable condi tions. Chert is lessabundant than in the overlyingOrdovocian formations. The DerbyDoerun Dolomite, at the base of thePotosi Dolomite, contains more siliceousmaterial here than elsewhere inMissouri; it constitutes the uppermostlimit of the predominantly clasticmaterials encountered in the Cambrian.The underlying Davis Formation containsthe only persistent confining shale bed inthe Cambrian section. The PotosiDolomite, the principal aquifer in theOzarks and the project area, is 250 ftthick at Lebanon and thins to lOa ft inthe western part of the project area.

Ordovician Rocks

The Gunter Sandstone Member, atthe base of the Lower GasconadeDolomite, is stratigraphically the oldestOrdovician rock unit in the study area.The lithofacies map of the Gunter (fig.

28

10) shows the percentage of sandstone inthe unit; it also indicates structuralcontrol of sandstone distribution,inasmuch as the northwest trend ofvariations in sandstone percentagesparallels faulting and axes of warping inthe area (Knight, 1954). The GunterSandstone is not exposed in the projectarea.

Although the Upper and LowerGasconade Dolomite are recognized asseparate units in well logs, they werecombined in mapping for this report. Aprincipal difference between them is theabundance of chert in the lower unit andits sparsity in the upper. Their combinedthickness is between 300 and 400 ft.

The Roubidoux Formation is oftenrecognized by the sandstone beds in it.In the project area, however, sandstoneis not as prominent as in some parts ofthe Ozarks. Much of the Roubidoux isdolomite and chert, the chert contentoften exceeding 20 percent of theformation (Carver, 1961). Where theRoubidoux does not crop out, it may beas much as 180 ft thick.

The Jefferson City and CotterDolomites are often separated in welllogs, but they were combined in arealgeologic mapping for this project.Sedimentary structures in the CotterJefferson City indicate frequentfluctuations of sea level, which led toformation of conglomerates, sedimentary pinchouts, lenses of cross-beddedsandstones, and mud cracks. TheJefferson City contains more clastic andsiliceous material than the Cotter, butthe latter is locally argillaceous; theircombined thickness in the project areaapproaches 400 ft.

Mississippian Rocks

Mississippian rocks are limited to thedivide in the extreme southern part ofthe study area and are unimportant to


60%

Laclede: Counl)'WruJIl! Cou:o;t~,'----

10 ::::I(nn'iIi0l=====r==:::::J'Y Milts1:1:I::DCb:', .'. f II. I', I I10 0 10 Kilometers

1

'<-=-~Lt" eoo-',,::,""71"'::'UI-~"",...1

Buffalo•

__"",---COmdtn CouMy

r/ oollos County

I

L

Figure 10. Lithofucies map of the Gunter Sandstone Member of the Lower Gasc-onade Dolomite. Contoursindicate sandstone percentages.

29


Residual soils developed on theRoubidoux are stonier, less plastic, andallow more efficient percolation thansoils on the Jefferson City. Chert bedsderived from the Cotter Dolomitelocally contribute to high permeabilityof Cotter-derived soils. The total soilcolumn on the Roubidoux consists ofalternating zones of gravelly, sandy day,and broken chert layers having a verylow clay content. Horizontal permeability, therefore, is also extremely high,particularly in the cherty gravel zones.

30

area hydrology. They lie unconformablyon the Ordovician sequences describedabove. Uplift and widespread erosion atthe end of the Silurian (Snyder, 1968)account for the lack of Silurian andMiddle and Upper Ordovician rocks inthe Niangua basin.

Uplift and removal of Mississippiansediments from much of the Ozarks andof Devonian rocks from the study area,antedated a Pennsylvanian submergence.Subsequent Pennsylvanian sedimentswere eroded without trace in the studyarea.

The most prominent structuralfeatures in the project area arenorthwest-trending faults, possibly withroots in Precambrian rocks, that arebelieved to have been active as recentlyas Middle Ordovician time (K.H.Anderson, Missouri Department ofNatural Resources, Division of Geologyand Land Survey, oral communication,1977) (fig. II, in pocket). VerticaJdisplacements along them range from 10it to as much as 400 ft. Several grabensand horsts were formed, of which themost noteworthy, hydrologically, is thehorst crossing Steins Creek in the OsageFork basin (fig. II, in pocket); another isthe graben containing the junction ofDry Auglaize Creek and GoodwinHollow.

Structure

Northeast-trending faults are lessprominent, younger, and were probablyactive between the Mississippian andPennsylvanian. They appear to be highangle faults with more horizontal thanvertical displacement (C.E. Robertson,Missouri Department of NaturalResources, Division of Geology and LandSurvey, oral communication, 1977).

Associated with the major faults arenumerous smaller, connecting faults andflexures produced when the majorstructures were formed. Displacementalong minor faults is small, rangingbetween 5 and 30 ft. Closure on flexuresis also low. Fractures and joints with noapparent displacement are abundant.Some of the fractures are related tomajor structural development in theOzarksj others may be the result oferosional unloading following uplift ofthe region (Currie, 1977).

Location and direction of majordrainage were influenced by warping,fauJting, and jointing. Streams were

UplandandColluvium,Alluvium,Residuum

Surface soils in the area areclassified as residual, alluvial, andcolluvial. Colluvial soil development onthe lower valley slopes is very limited.Alluvial soils are not extensive in thenarrow valleys in the project area.Residual soils developed on theRoubiduox Formation and the JeffersonCity and Cotter Dolomites in the uplandsusually have a fragipan 18-24 in. belowthe surface, a feature that retardspercolation of water to bedrock; it ismore continuous on the Jefferson Cityand Cotter Dolomites than on theRoubidoux. Water is transmittedhorizontally on top of the fragipanexcept where it is cut by gullies orvalleys.

deflected and misfits betweenstreamflow and basin size developed.Dissolution of the dolomitic rocks,leading to development of secondarypermeability, is another result of theshattering produced by movement. Typeof rock involved, strength and durationof deforming forces, chemical characterof groundwater moving through crevices,and position of each affected rock unitin relation to changing base levels oferosion are also contributing factors.

In the eastern part of the projectarea, the rocks have a northwardregional dip of 31 ft/mi; in the westernpart, they dip westward 25 ft/mi.

Erosional unconformities and hiatusesare important features in studyingcarbonate-rock hydrology, because whencarbonate sediments are subaeriallyexposed, dissolution removes some ofthem.

An erosional interval marks the closeof Cambrian deposition. It is

Groundwater

questionable, however, that significantdissolution occurred during this intervalin the project area. The actual time

.boundary (systematic boundary)undoubtedly is somewhere in the upperpart of the Eminence Dolomite andshould coincide with evidence ofstructural activity in Missouri (Snyder,1968). Difficulty in identifying. theboundary has led to adoption of the baseof the overlying Gunter SandstoneMember of the Gasconade Dolomite asthe stratigraphic base of the Ordovician.

An important period of erosion,lea.ding to extensive dissolution, is thelong interval when all post-EarlyOrdovician sediments were erodedbefore deposition of the Mississippianlimestones. Erosion began afterdeposi tion of these limestones, nowpresent only on the southern border ofthe project area (fig. 4, in pocket), and iscontinuing. Therefore, it seems probablethat much of the dissolution leading tothe karst character of the Ozarks waspost-Early Ordovician.

GROUNDWATER

DESCRIPTION OF AQUIFERS

All rock units listed in table 1 arelocally capable of yielding water to wellsin the area. Certain uni ts, such as theRoubidoux Formation, Lower GasconadeDolomite, Gunter Sandstone Member ofthe Gasconade Dolomite, and PotosiDolomite, are more productive thanothers and are therefore commonly used.They are readily recognized in outcrops

and in well cuttings. Springs arecommon where the units are exposed;depending on valley altitudes and thedepth to the zone of saturation, eitherlosing or gaining stream reaches canoccur in such outcrop areas.

Many domestic wells obtain waterfrom the Roubidoux Formatiol), UpperGasconade Dolomite, or upper part ofthe Lower Gasconade Dolomite, orcombinations of these units. Average

31


32

yields of wells completed in theseaquifers are 15 to 20 gpmj specificcapacities range from 0.10 to 0.40 gpmper foot of drawdown.

Wells penetrating the deeperaquifers, the lower part of the LowerGasconade Dolomite, Gunter SandstoneMember, Eminence Dolomite, PotosiDolomite, and Lamotte Sandstone yield

Groundwater

up to 750 gpm and have specificcapacities ranging from 0.90 to 20 gpmper foot of drawdownj wells penetratingthe Potosi have higher specificcapacities. The large springs in and justoutside the study area are in LowerGasconade and Eminence rocks (plate 9).Many other solution features, such ascaves, sinkholes, and natural bridges, arealso associated with these major springs(plate 10).

•Plate 9.Exposure of Lower GasconadeDolomite, Gunter SandstoneMember of the Lower Gasconade, and Eminence Dolomiteat Hahatonka Spring, sec. 2,T. 37 N., R. 17 W. Photographby James E. Vandike.

•Plate 10.Natural Bridge just east ofHahatonka Spring. The largesinkhole pictured in plate 6is on the other side of thebridge in this view. The rock;s Eminence Dolomite, withthe Gunter Sandstone Mem·ber of the Lower GasconadeDolomite near the top of thebridge, sec. 2, T. 37 N., R.17 W. Photograph by JamesE. Vandike.

33


TABLE 2

Transmissivities and storage coefficients of aquifers and specific capacities of wells

Owner or user Location Principal Static Yield Orawdown Specific Transmissivityaquifer water level (gpml lftl """'''' Ift2/dl

1ft) 19pm per ftof drawdownJ

Shell Pipeline Company 33-19-17cbd Roubidoux 105 29 3 9.7Robert StllllOns 34-15-2b<:d 150.3 36 7 5.1H.R. Grafton 34·19-33abd 145.1 11 48 .03James Sullivan 35-15-10add 94.6 10 40 .25Earl York 36-13-8dbd 90.3 7 30 .23lynn Bohannon 36-13-8<1ab 68 27 72 .39Bardette Carnes 36·13·19baa 75 20 60 .33E.R. Ravenscroft 38·13-30aba 170.3 15 40 .8Runell Hood 31-14-17ccc Gasconade 2002 25 40 .62Gordon Knight 32-17·10cbb 124.7 35 100 .35Conway High Schoo' 32-1 HlcOO 150.3 7.5 20 .39Peter Atkinson 33-17-7ddd 205-0 20 20 1»Robert Pruitt 34·15·22dad 288.1 21 30 .70Cliff Springs Camp 35·14-ladb 80.1 60 6 8.3L.H. Bryant 35·16·1Odaa 171.1 10 10 1»Archie George 36·16-23aaa 125 10 25 .4R-6 School 31·15-1788 Gunter 216.0 22 10 2.2laclede County PWSO 3, Wall 3 33·17-22da 327 80 120 , 230U.S. Civilian Conservation Corps 34·13-2Odaa 272-0 25 11 2'Frad Adams 36-18-31ba 90 1,140 22 52Ozark Fisheries IHurt Well) 37·15-25 Gunterl?l 39' 615 1862 3. 300Ozark Fisheries lAsh Well) 36-15-25bda 10.6 660 114 ,.City of Marshfield, Well 2 3O·18-3OOc Potosi 254.4 590 68.5 10 1,730City of Conway 32-17-8<1cc 172.8 183 104 "laclede County PWSO 3, Well 2 33-16-6aa 405.2 115 33.1 3.5 240laclede County PWSD 1, Well 31 33-17·1dd 604» 175 62.0 2. 510lllClede County PWSO 1, Weill 33-17·1ddd 359.0 185 35.0 5.3 720lllClede County PWSD 1, Well 2 34-16·200 167 46 M 1,200City of Lebanon, Well 4 34-16-3dcb 345.1 480 85 7.4Mid'America Dairy 34·16·1Odc 348.8 260 60 4.3Frisco Railroad 34-16·11bac 345 300 67 4.5City of lebanon, Well 3 34-16·11cad 335 495 160 3' 960City of lebaoon, WellS 34-16-14abb 383.2 500 122 4.1City of Buffalo, Well 2 34-20·26adb 172 205 53 3.City of Buffalo, Well 3 34-20·26aOO 186.1 200 68.3 a 410Minouri Highway Department 35-17-31bcc 14' 100 15 6.7

Rest StopCity of Richland, Wtll1 3S·13·7ccd 252.4 100 5 20City of Richland, Well 3 36·13-8 263.0 500 113.8 4.4 410City of Richland, Well 2 38-13-18abc 240 210 60 4.2Ozark Fisheries, Squirrel Well 36-14-6abc 52.7 753 45 17laclede County, PWSD 2, Well 1 36-14-31bad Potosi 263.3 68 94.3 • 270

1Storage coefficient equals 0.0002

34

Groundwater

The major streams in the study areahave cut only as deep as the lower partof the Lower Gasconade, and this only inthe extreme northern part of the area.It is possible that even though highpermeabilities might exist locally in theupper, less productive rocks, water is notpermanently stored in them, because ofdrainage to local streams. The LowerGasconade becomes less productivenearer its outcrop in the Nianguadrainage, as does the Gunter Sandstone

Member in outcrops just outside thenorthern boundary of the study area.One explanation of this phenomenoncould be a reduction in the secondarypermeabili ty of these rocks by deposi tionof CaC03 (calcium carbonate) in thepore spaces, because of a change ingroundwater gradients near the outcrop(Burdon, 1967). More study is needed toverify this change in permeability and itseffect on well yields.

Yields of many of the large-capacitywells in this area are lower than those ofcomparable depth in surrounding areas.Transmissivities of aquifers in theproject area range from 240 to 1730ft2/d (table 2); the higher transmissivities and specific capacities are inthe southwestern part and across thenorthern margin of the study area (fig.12 and plate II). Some evidencesuggests these productive areas resultedfrom uplift and erosion at the end of theMississippian. There are higher transmissivities in Cambrian-Ordovician rocksin Missouri, along such structural trendsas the Early Pennsylvanian Bourbon arch(D.L. Fuller, Missouri Department ofNatural Resources, Division of Geologyand Land Survey, oral communication,1977). The lowest specific capacitiesare in the south-central part of the studyarea (fig. 12).

the lowerinterrelated

higher yields ofresult from several

Theaquifersfactors:

l. The lower zones are brittle, massive,cherty dolomite with little silt orclay and fracture cleanly.

2. Residue from solution is small andcirculation is not impeded (Reesmanand others, 1975).

3. The productive zones are below thebase level of erosion and the presentzone of water-level fluctuation;hence, pore spaces are always:-aturated (Sokolov, 1967).

4. High hydrostatic pressure and mixingof water from more than one sourcepromote dissolution of dolomite andlimestone (Jakucs, 1977).

35


EXPLANATION

/!1 Roubldoux Formation .ell

• Potosi Dolomite .ell

C Ga'COl'lOde Dolomite .ell

+ Gunter Sand.ton Member .ell

~.BII(J3.3

I,)J10

MOBnfleld

52 + >8 \\

.•yr\ CI.O /I (-./

e6.7 / .74 ) /..I '.6. ~ ~ ~5.1

4.'·ct... "'\ 4.1e,.. Buffalo +2.32.' I f

2.':' ./9.7/!1

.-J,.,.5

93°00'00"

'.'OO'OO"-+-

• ~.3 Specific capacity In 9pm per Itof drowdown

10 0 10MIIn

tIl1 r:::r;(iiiiJmijI==~1===:JI10 0 10 Kilometer.

Bose from U.S. Geol09lcal Survey stolfibose mop, 1:500,000.

Figure 12. Areal variation in specific capacities of high-capacity wells. Yields greater than 30 gpm.

36

Groundwater

Plate 11. 11A is a view of a high-capacity well, with a capacity of 615 gpm and a transmissivity of300 h 2/day, in the northern part of the study area, at Ozark Fisheries, sec. 25, T. 37 N.,R. 15 W., Camden County. 118 is an aerial view of fish ponds, at Ozark Fisheries, filledwith water from high-capacity wells, springs, and Mill Creek. Photographs by James E.Vandike.

37

A

B


GROUNDWATER MOVEMENT

As a first step in collectinggroundwater information, logged wells inthe project area were inventoried andwater levels measured and plotted on amap of the area (fig. 13, in pocket).Obvious data gaps were filled byrevisiting unlogged wells and measuringtheir water levels. Recent data indicatethat configuration of the potentiometricsurface in the project area has changedvery little in the past 30 to 40 years,except for some lowering in areas ofmunicipal pumpage. Table 3 lists wellsthat provided data for this study; figure14 (in pocket) shows their locations.

There are advantages anddisadvantages in construction and use ofpotentiometric maps for carbonateaquifers. Contour shapes can indicateareas of significant water loss in surfacestreams like those in Dry Auglaize Creekbasin; however, areas where more subtlelosses occur cannot be detected fromcontouring alone, because contourintervals are usuaHy too large. Groundwater levels only a few feet belowstream level at the time of measurementresult from vertical groundwater movement and streamflow loss not reflectedin contouring.

Because water levels may differ inwells of various depths in any specificarea, potentiometric maps must beconsidered subjective if drawn only onthe basis of selected wel1s of specifieddepth or of wells completed in aparticular stratigraphic unit. Construction of such maps does not fully takeinto account areal variations of verticalpermeability, because groundwater maymove through condui ts at various anglesto the generalized flow pattern. However, these factors do not detract fromthe principal purpose of potentiometricmaps: to show the general direction ofgroundwater movement.

38

Figure 15 is a map constructed bydrawing flow lines on the potentiometricmap; arrows show direction of flow. Thefollowing conclusions can be drawn fromexamination of this map:

a. The groundwater divide as indicatedby the flow lines conforms approximately to the surface drainage dividebetween the Niangua River andOsage Fork.

b. Groundwater movement is generallytoward the principal streams in thearea: the Niangua River, Osage Fork,and Grandglaize Creek.

c. Runoff from the Niangua River isincreased by groundwater flowingfrom the upper Dry Auglaize Creekbasin and perhaps by a very smallamount from the Osage Fork basin.

d. As indicated by the southernmostflow lines, some groundwater flowfrom the drainage area of the OsageFork may be reaching the GasconadeRiver.

e. Groundwater and surface-water flowsystems of Ozark basins are interdependent; anything natural orartificial affecting hydrology in onebasin may affect it in others.

As shown in the following table,there appear to be at least three,perhaps four, separate potentiometricsurfaces in upland areas:

SeqUflnect of 'orm.tions R.nge in depth Avtlrage depthpen.tI.ted by w.11s to w.t.r, to w.ter,

in ' ..t In ' ..I

Jeffenon City Dolomite '.00 50Jefferson City Dolomile- 18-205 100RoubidoUK Formation

RoubidoUK Formation- 14-.300 '50Gesconllde Dolomit&

Eminene& Dolomite- 15407 200LemOlle Sanchtone

Groundwater

93000'00"

'8000'00'---J-

~ I~'=:====r=:=::Jlr Miles~ I

10 0 10 Kilometers

EXPLANATION

Generallud direction of 9roundwat., flow interpreted from FlQure13.

BaSI from U.S. GeoiOQlcol Surveystott boSi mop, 1:500,000.

re 15. Generalized directions of groundwater flow in the Niangua River, Osage Fork, and GrandglaizeCreek basins.

39

:I:-<0;0.. TABLE 3 0

0 gRecord of wells in the project area-<-, ""'-.... ""'"" O'lR-DllLS D.,. Allitu,," of ,.," "'0 - 1'0'.'... 1.... 0". Oltdl.tgo

-~"'Inci""" 0

1000"""'t>ot """,pnod land ,uri,.. 01 ....1 .~ &omo,,, (lnd ........ 1- lUltlon. ~.. -" oq.lI..,~

(IMI) (1_1 ,...., lind",,! -~ minlltol IlJlmlttl (")».10/1 ...... , C,R. mN Al8WOSB8Cl Wob<\O( ,~. 01/01/19.8 "." ~ .. • l1UlO 01Itll/1Bq: :J61CTTR

;0

'"Fritndshlp BIPtin Church T2QN A19WOtBOAl Wlt>lIO' ""'" 01101/1967 ,..,'" " • loe.oo 01/0111987 " 368JFRC §1

(loy". Tn..1 T30N R,5W 17AAAI W,igl>l 23216 01/01/1964 1616 '" '" • "00 01ml'9~ , J88JFRC

Hu"on, Mrs. e. T30N RI6W 1086Bl W,lgIIt "'" 01101,1987 ,.." ,~ ", ~OO (l1101I1007 , 368JFAC »

-<Bunn, Fl... noN Rl6W23AAAI 1'0"'9111 =" 01/01/1963 1568 ,~ " • 00.00 01/0"1917 • 368JFRC '"11011, E.W. T30N Rl6W 2U.BCl W,~" 25510 IH!0111ge7 1510 "'" , 3671190X -<S!l<rmon, Rov T30N R11W02 W.b.... 27640 01101/197\ ". 367RBOX '"Oycho. w.e 1JON RI7W058DAI W<I>UOl 20073 01/0111955 "'" '" "

, ~OO 01/0111917 " 368JFRC;0;0

Camp ....'owt>t.d T30N RHW 080AOI W.b"er ~" 01/0111962 "" "'" '", 12Ul0 01101/1002 " 3C7R80X »

P....o"'. l(..., PON R17W 358AC I Wob"o' IJ2C9 01/01/1854 ,.., ,~ " ,.~ 65.20 01/01l19flA JIl8JFRC ZMcV.~.l(tn T30NR!8W01A8Al W.bo'.. ,~" 01101/19fl7 "'" m "

, 18.00 01101/11Hl1 " 361R8DX '"Lotwfmon, P.ul TJON Rlaw0180BI WoboW 261~7 01/01/1961 '.,0 '" '" • "'00 01/01/1&61 " 366JFIlC

""".'. H.H. TJON R18W02DC W..,.,., 261U 01101/1968 1432 '" ", 57.10 01/O1110118 " JtIllJFRC

MarlhUof<l "2 r.lON Rl$W03CDC' Wobo'Ot 9765 12/O1/11147 "'" ,,,. ,~ " '"'00 '" /19" "'" 10.\ 367GNTR

St.""'fd 011 noN R18WlW;881 Wobo'.. 26552 01/01/1970 ..a9 "'" "'" , 00.'" 01/01/1070 '" 367RaOX

Mo''''';old 3 T30N IHaw 10 1'0'_0010, """ 01/01/1916 "'" m " 233.10 01/01/1916 311P01S

Mar,llliold .\ T30N RI6W 10ABSI Wlbo'.. 2114 "" 14B1 ~. '00 • ""'.00 1926 '" 367C,SCO

Con",1 P,......." l30N f\18W 1080Bl Wobo'O' "", 01/0111944 1486 ,,~ '" • 210.00 01/Q11H144 "'" 371POT'S

P....y Ool'y T.l(lN RIal" 118&1 1'0'10010' 2219 01/01/1930 ,.., 00. ", '0000 01/01/1930 "'" 387GNTR

Btll. Rov noN RIal" 110091 1'0'000,., "'" 01/01/1965 1433 ''" ", 95.00 01/01/1%5 " 368JFRC

Gr..... Ro~ T30N Rll1W 19CDCl 1'0'''''''' 25143 01/01/1967 "'" ,.. " • ".00 01/01/1967 • Jli8JFRC

Cr.w/ord. BUI TJON R181'1 22CM1 WOO"" 25108 01101/1967 ''''' '" ", 217.30 0110111981 " 368JFRC

Erl>. F.A. TJON Rll1W 25A.AAI Wlbo,•• 4512 01/0111\137 1135 ,~ " • 111.00 01/01/1937 368JFRC

lIndt,.H.W. lJON Alaw neC91 Wobo'" 25146 01/01/1987 "" .~ n , 180.00 01/0111951 " J67ABDX

MonlV"""'..... H.P. TJON R16W33CASl Wot>ou:, 27173 01/01/11Hlll "" '" '", ,"00 01/01/196/1 " 387RBDX

Hood. Au..1i TJ1N RIll" 17CCCI W'IQn' '"~. 01/01/1967 "" ~ .. ,"''''' 01/0111967 " •• 381GSCOL

Mood. Au ... 1i T31N RI4W 160CAI Wdlil" """, 01/01/1968 ,~ '" " • "00 01l01/19M '" 367RaDX

Hood. Au ...11 DH'l RIll" 198BAI 1'0"'111" 25246 01101/1961 1255 "" '", '0000 01/01/1961 " 367GNTA

Edl/l'lOfl. R.E T31NRI5W05DBBI W'IQn' 27192 01/01111159 "'" ~, '" • 171.30 01/01/19W " 361GSCOL

G.llnn.o."oll T31N R15W 050DCl W''II'" 11169 01101/1963 "" no " • 139.00 0l/OlIl!16.3 " 36J'GSCOIJ

Gulnn.J.D. DIN R16W08MOI W,~", """ 01/01/1969 m '", 110,40 01/01/1973 " 367GSCDL

GUltv>. V.lm.. DIN R15WDeADCl W,jg!1' :llnl 01/0"1963 ,,,. n. '" • 111.llO 0111)1/1963 '" 367GSCDL

B,."on. J.E. 131N RI5W 16ADBI W''II'" 26156 01/0111961 "". m '" • 240.80 0I/01/1~7 • 367C,SCOl

Robl""'n, Coyl. r:I1N RISW 18DCBl W''II''I 11810 0110111993 1128 '" ,n • 1~1.00 0110111963 '" 361RBOX

RB SeII".,1 0 .."",, TJ1N R16W 17M W'ig/ll "''''' 0110111981 ,"" ,~ '00 • 118.00 01101/1961 " " 371EMNC

KilTll4'.LJov<l DIN RI5W 17ACAI W'Ign, -, 01101/1963 ,~, n. " • "." 01/01/1963 '" 387GSCDU

w....,. ()w;~1 nlN RI5W naCBl W'~T 27101 01101/1069 1315 '" ", 165.90 0110111969 " 367GSCDL

Hmdo,,,,n. Tho."., l31N RI5W 16ADAI W,Ign, 251Cll 01/01/1967 1270 '" " • 100.30 01/01/1967 '" 367GSCOL

Pollard. E. T31N R15W lB9Ml W';g~, 27117 01/01/1968 """ "', '",

""''''' 01/01/1009 '" 387GSCDl

blow. T.C T3IN RlIiW2\CDDl W'Ig/l' ~""01101/19l1S 113' '" ..." 01101f19l16 , J67RaOX

Dittk•• lIabt'l T31N RI5W2BBACI Wrl;nl ,~. 01/0111965 ,,,. "" ", '"00 0I/o1I196r> '" 381R8DX

W.....n.c..ol l31N R16W32CBBI W,I~' 13812 01/0111955 1426 '''' ", ".00 0110111955 '" 367R80X

Now S/>o<llIy Chuf<:11 l31N RI5W33CDBI W,igh' 23140 01/01/1994 "" '" " 8.25 111.:10 OI/O!lllHl1 " 369JfRC

Millo,. c..OfIilO D1J'l R1BWOJ(;AAl ""-''11''1 15144 OllOlIl!lo61 "'" '00 ", "00 01/01/11167 ~ 361R9DX

Tob.. 3 (CDm;n.....)...., "'"'-- ~-ONR·OGU D.'. Alti'''''"01 ~.. "". ~~ W.'.. l.... D.'. Olooh••go Sptcilic Principal..... numbo' """'pi..... lond.url_ .~, -- di.....- (I...! ...' .. 1.... (VI'lI_po< -, oquil..

(I..d II..,! ,_, (incll••1 ......ur«l mi""'.!

Milam. P.ul T31N R16W06ACCI W.b"., 241112 01101/HI68 "'" ". " • 62.00 01101/1968 ~ 367RBOX

Ve.tol. Le"y T31N RI6W06BABI W.l>it., 2178B 01101/1963 "" '" " • .. 00 01101/1963 " 387RBDX

Geo<go.o..id 131N R16W09CCBl W.b..., ""'" 01101/1963 1373 '" ", ~.OO 01101/1963 " J68JFRC

Delli. N.T. 131N RI6W 12BCAI Wr;5I'>' ,~ 01101/1961 ,,~ .., 55.00 01/01/1987 • 361GSCOU

Williem•• .k>hn 131N Rl1W 20ACAI Wo"'.o, 01/01/1947 1375 '" " • 67.00 01101/1947 , J67RBOX

Nie"IrJa. CHy No. 131N R17W 20BCAI Wel>it., 24571 01101/1966 '«' ,~ ,~ , "".00 01101/1966 J71EMNC

Soll• .lame. 131N RI7W2OBCBl W_,., 24071 01101/1965 '''' ,.. " • 115.00 01/01/1965 " 367RBDX

MFA Exolla.. 131N RllW 20CABI ~I>i.., 23111 01/01/1964 '''' '" ,~ 4.15 B5.30 01/01/1964 " 367RBDX

Control. Horben T31N RI7W25DBDI Webl.., "'" 01/01/1963 ,~, '" ~ • ~.OO 01/01/1963 , J68JFRC

Hyder. Gen..1 131N Rl1W29CA W.b"., """ 01101/1964 1421 '00 " • 55.00 01/01/1964 , 368JFRC

Go_.John T31N RI8W06BDBI Wob".' 23151 01/01/1964 1278 "" ~ , 129.00 01101/1964 '" J61R8DX

Odell, Roy T31N R16W 22DDCl W.blt., 26163 01/01/1967 "00 '" ~ • 41.10 01/01/1967 .. 368JFRC

N.loon. Earl 131N RI8W25AAOl W.b"., 28740 01101/1967 1370 '" " • 86.10 01/01/1967 • 361RBDX

Jump. Robe't T31N RI8W 28CBOI W.b".' 24801 01/01/1968 "" "" ", 7B.2O 01/0111966 .. 36BJFRC

John""n . .l.l. 131N RI9WQ4CDBI W.l>it., '''''' 01101/1963 "" '" " • " J61RBDX

lloIIlonnon. Bust.. T31N RI9W IOCAC1 Wobl'or ,.... 01/0111966 1324 '" ", 42.30 01101/1966 • J6BJFRC

Hoboon. Glenn T31N RI9W 36CC W_tor 21101 01101/1974 '«' ... '00 • 22O.tO 01/01/1974 '''' 361GSCDU

Todd. Mel.in 132'1 R14W01BDBI ~.~ "'" 01/01/1963 1251 '" " • 123.90 01101/1963 " J67RBOX

Burd. Vi'g;1 T32N R15W01CBDl ~~ 22418 01/01/19&3 1121 '" " • 76.00 01/01/1983 '" J61RBDX

Humph, .... l.roy 132N RI5W04ACBl locl.de 21170 01/01/1969 ~, ~ , 221.10 01101/1969 • 361GSCDl

Me'edith. M.. T32N R15W 2ODAA1 Wrigh' 24114 01/01/1968 ,~,

'" .. • 121.20 01/01/1966 " 361GSCDl

Mo",O.R. T32N R15W 21BABI Wright 26150 01/01/1961 '''' n, '", 180.30 01101/'961 " 361GSCDl

Moore, .k>hn T32N R15W 21DCA1 Wright 23139 01/01/1964 ,~ '" "", 119.00 01/01/1964 ~ J67GSCOl

Si",mon•. CIIlU<!t T32N R15W 24AAC1 Wrigh' 11018 01101/1947 ,m '00 ", 45.00 0,101/1941 J6BJFRC

Park." R.y TJ2N R15W 24BCDI Wright 110BI 01101/1947 ,"" " • , , 36BJfRC

K........ Roy T32N R15W 2668Cl Wright ''I'" 01/01/1968 m '" • 233.80 0'101/'968 '" J61GSCDl

L.o<l;, Earl 132N R15W32AADI W'ight 26145 01/01/1961 1373 ~ n • 243.10 01101/1967 " 367GSCOL

Kn..l•. R.y T32N RI5W32DACI W,igh' 23158 01/01/1964 1375 '" 00 6.25 239.40 01/01/1964 " 361GSCDl.loch,,". Mar.in 132N RI6WO'CACI u~~ 01/01/1950 ".. '"

, 148.40 01/01/1911 368CNONKilburn.....nrv 132N R26W06ABAI ....~ 11002 01101/1947 '''' '" " 6.25 J67RBOXCompboll, Harold 132'1 R'6WOt;(;CCl ~,~ '''''' 01101/1963 ,m '" 6.25 116.90 0'/0111963 " J67GSCDlB..n. loor>ord 132N R16W06BBAI ~,~ 22135 01/01/1963 '''' "" ~ 6.25 116.20 01101/1963 " J67GSCDUMod"","-, Willi.", 132N R16W 19Dcal W.!>lto, 22331 01/01/1963 ,~, '" " 6.25 61.80 01/01/1963 " 367RBOXHil.man.D.G. 132N RI6W2iSDCl W'ight 2314, 0110111965 ,~, m ~ 6.25 110,20 01/01/1965 " J61GSCDlKotd>o"ide, C. 132N R,6W29AAAI Webitt, 24111 01/01/1966 ,~,

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Figure 13 (in pocket) was constructedusing an average water-level depth of150 ft. When compiling the map, greatcare was necessary to avoid includingwater levels from more than one aquifer.

The shallowest water levels weremostly obtained from wells in valleys;the deepest, from those on or near hills.All four potentiometric surfaces are notpresent in all areas; in most there areonly two or three. In some areas, suchas in the upper part of the GoodwinHollow drainage basin just west ofLebanon, only the deepest zone isgenerally present.

Groundwater in all the aquifersconstantly moves from areas of highhead to areas of low head. Thepotentiometric surfaces have gradientstoward points of discharge: seeps andsmall-volume springs along hillsides or insmall tributary valleys, and high-volumesprings in the large valleys. Thepotentiometric surface illustrated infigure 13 (in pocket) is locally influencedby structure associated with majorsurface drainage, and by large faultsystems.

The multiple water-level phenomenonand the relation of stratigraphy andgeologic structure to water levels in thestudy area are illustrated in figure 16, awest-to-east hydrogeologic cross sectionthrough the center of the study area.

Sokolov (I967), in describing a similarmultiple system, termed the higherlevels "suspended" karst waters. Hebelieves the main control upon suchwaters is nonuniform permeability of therock and the local presence ofimpermeable zones, and that the mostfavorable conditions for a multiplesystem are in uplifted areas with moistclimates.

Groundwater

Because of the predominance ofcarbonates, openings along beddingplanes and fractures have been enlargedby moderate to intense dissolution.Burdon (I967) believes that fissureenlargement is predominantly verticalabove the zone of saturation andhorizontal below it. Based on water-wellrecords, inflows of water often occurwhen a bedding plane or other horizontalopening is penetrated after drilling drythrough massive rock to a considerabledepth below the potentiometric surface.On the other hand, connection throughvertical openings between shallow anddeep zones is shown during pump tests,by the declining rate in lowering of thewater level in a deep well when thedrawdown data are plotted semilogarithmically, indicating drainage fromoverlying beds to the principal aquiferopen to the well.

Permeability produced by erosionalunloading and consequent solution alongbedding planes is probably much moreimportant than previously recognized.Snow (I968) believes that opening andclosing of these smaller horizontalfeatures in response to the "breathing"effect of flUid-pressure reversals orchanges is very important in increasingpermeabilities. He discovered horizontalpermeability increased with pressurefaster than vertical permeability. Ingeneral, solution channels providerelatively open, if not direct, conduitsfor water movement.

Significant local recharge to thesystem is proved by differences in headbetween the various aquifers.Observation-well records (fig. 17) in theLebanon area indicate a fairly rapidwater-level response to local rainfall.Water levels in wells completed in theshallow aquifers ("50-foot" and "100foot" water-level zones) have beenreported to rise within hours ofsubstantial local rainfall.

51


A.,; ~

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Figure 16. Hydrogeologic section showing multiple water levels and structure.

52

Groundwater

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EXPLANATION

Water level

---/

Derby - Doe Run Dolomiteand Davis Formalion

Control well.Numbers indicate location(see Table 3)

,/

Bonneterre Formation oIo 2

2 3 Miles

"3 Kilometers

Lamotte Sandstone

53


'00

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•

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".,.."""

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,~

,~

'"

Hydrographs of selected observation wells, compared to discharge of Bennett Spring a~precipitation at Lebanon.

,

I ,•i ••,, ,j •,{1 ,

."Figure 17.

54

-."

,,

•,,

,

The drought that affected groundwater levels during the current studyaltered expected seasonal trends. Longterm observation wells in other parts ofthe Ozark carbonate region showseasonal fluctuations of water levels,partly resulting from evapotranspiration,with highs in March or April and lows inOctober or November. Water levels inthe study area, however, maintained adownward trend during the investigation.Normal, or above normal, rainfall duringthe last year of this study (1977) did notreverse the downward trend ofgroundwater levels, but it did preventmuch lower water levels.

Water levels recovered during thelast part of June 1977 (fig. 17).Significant rainfall occurred during thefollowing months, and water levelsdeclined, but did not reach the downwardtrends established earlier in the year.This indicates a rather rapid movementof recharge water through large nearsurface conduits, with no significantrecharge of the small-diameter network.

The total volume of rainfall in akarst area such as this is not asimportant to recharge as the distribution, both spatially and chronologically,because the distribution controls thepercentage of annual infiltration(Kessler, 1967). The amount of infiltration or recharge is not directlyproportional to the amount of yearlyrainfall and may vary in the same areaby an order of magnitude (Kessler, 1958).

Recharge occurs In uplandinterstream areas by infiltration ofwater into residual material, then intobedrock. This direct infiltration can betermed "diffuse circulation"; it enlargesjoints by dissolution (Burdon, 1967). Theamount of infiltration in upland areasdepends on soil types and topographicsetting (Reesman and others, 1975).Gentle slopes favor increased

Groundwater

infiltration; steeper slopes, increasedrunoff and less diffuse infiltration.

The system is rapidly rechargedthrough stream losses and throughconduits in upland sinkholes. This typeof recharge, called "concentratedcirculation" by Burdon, is illustrated bythe recharge in the Goodwin Hollowarea.

Although much recharged water israpidly flushed through the shallow partof the system during a rainy period, asignificant amount penetrates to greaterdepths. This is illustrated in figure 17.After heavy rain in June 1977, the waterlevel in the Weaver well roseconspicuously, a significant reversal ofthe steep downward trend that ended inJune. The Vestal Courts well showed alarger immediate rise, but it alsodeclined to a level closer to that reachedduring the previous downward trend thandid the water level in the Weaver well.In addition, the discharge of BennettSpring (plate 12) increased significantlyby an amount commensurate with therise in the Weaver well, suggesting ..thatrecharge to the entire system issignificant, because the long-term flowcharacteristics of Bennett Spring dependon the water available from the entiresystem.

Fluctuations of water levels in allthese artesian aquifers result fromevents such as alternating periods withand without rainfall, and alternatingperiods of pumping and nonpumping ofnearby wells. Every drop of waterrecharged to the system tends toincrease the head throughout the system.In some instances, in response torecharge, water levels rise in wells thatare miles from recharge areas.

Fluctuations in water levels are morepronounced and of shorter duration inthe shallow, less productive aquifers

55


Plate 12A. View of Bennett Spring, looking southwest across the spring pool. Photograph by JamesE. Vandike.

than in the deeper, high-yield aquifers(fig. 17). Proximity to the land surfaceis the primary reason why shallowaquifers show greater water-levelfluctuations than the deeper aquifers.The deeper are primarily recharged bywater movement through shallow zones,so response to precipitation is usuallyslower but more sustained than inshallow aquifers.

At depth, seasonal f luctuations areusually smaller in areas with mUltipleaquifers than in those having directrecharge to deeper, high-yield aquifers(Sokolov, 1967).

56

A true artesian hydrologic system isimpossible under physical conditions likethose in the study area. Rather, allphases from true water-table conditionsto (but not including) true artesianconditions probably exist somewhere inthe study area.

In the previous discussion of karstrecharge and flow mechanisms, twoimportant aspects deserving furtherdiscussion were not mentioned: the rateof flow through the medium, and thechemical character of the water movingthrough the rock. During periods whenthe system is full after extended

Groundwater

Plate 12B. Aerial view of Bennett Spring; south is at the top. The spring pool is visible as a circularfeature in the stream, just left of the central upper part of the photo. Photograph byJames E. Vandike.

rainfall, flow is at a maximum, and inthe large conduits it is turbulent. Atthese times the concentration of calciumcarbonate in the water is low. Suchconditions contribute to increasingpermeability by solution. After initialflushing, residence time of water in thesystem is comparatively long, calciumcarbonate concentration is more nearlyin equilibrium, and the rate of solutionof material is reduced. Thrailkill (I968),however, states that even though waterintroduced by diffuse infiltration maybecome calcium carbonate saturatedafter movement through residual soilsand small secondary rock openings,

undersaturation of the water can resultfrom the increased pressure at depth,mIXIng of waters of differentcomposition, and changes in the rate offlow. Surface water is undersaturated,and when it is introduced into the systemthrough losing streams, solution ofcarbonate material is facilitated.

Caves are common in the area, butthese large conduits probably transportonly a relatively small percentage of thetotal underground flow. Mijatovic (I 968)indicates that spring discharges and wellhydrographs in carbonates show threedistinct stages follOWing periods of

57


preCipitation. The initial stage is whenspring discharge begins to recede, andwell hydrographs show a rapid decline, astage that represents drainage in thelarge conduits (3 ft or more in width).The second stage comprises a longerdecline in spring discharge and a lesssteep lowering on the well hydrograph, astage that represents drainage in thenumerous water-bearing cracks andcrevices (approximately 4 in. wide). Thefinal stage represents prolonged drainagein very small openings (less than 0.5 in.wide), a stage characterized by sustainedand relatively stable springflow andmoderate to very slight lowering ofwater levels in wells. The prolongedrecession indicates that these very smallopenings contain many times the storagecapacity of the larger conduits.Although masked somewhat by droughtconditions and by intermittent rainfall,these stages are discernible on hydrographs of observation wells measuredduring this study (fig. 17).

A semilogarithmic plot of waterlevel elevations versus well depths in thevicinity of Lebanon, Richland, andBennett Spring (fig. 18) shows that, inthe Lebanon and Richland areas, waterlevel elevations decline with increasingwell depth, and that, at Bennett Spring,they rise slightly as well depths increase.

At Richland and Lebanon, shallowwells are completed in the JeffersonCity Dolomite and Roubidoux Formation;deep wells, in the Lower Gasconade,Eminence, and Potosi Dolomites. AtBennett Spring, shallow wells arecompleted in the Gasconade Dolomite;deep wells, in the Potosi Dolomite.Richland and Lebanon were selected forcomparison with Bennett Spring, becausethey are the only places where asufficiently large cluster of wells existsnear a divide to warrant analysis.

58

The data plot for the wells in thevicinity of Richland shows that waterlevel elevations do not declinesignificantly below a depth of about 400ft. In contrast, the data plot for thewells in the vicinity of Lebanon showsthat water levels decline with deeperdrilling.

At Bennett Spring, the rising waterlevel trend in wells indicates they are ina discharge area and also suggests thatvertical permeability along fracturesresults in equalization of water levels.Friction loss as the water rises to thesurface along fractures from a depth of600 ft may also be a cause of the gentlyrising trend at Bennett Spring, comparedto the steeper trends at Lebanon andRichland. The steep trend of waterlevel elevations in the vicinity ofLebanon would seem to indicate poorervertical permeability between deepaquifers in a recharge area, because achange in trend like that at Richland isnot evident. The authors do not believethat the trend at Lebanon is due topumpage in that area, because modern(1972) water levels in the Lebanon areaare comparable to historical (1887-1947)data (Searight, 1955). The steep,uniform trend at Lebanon may be due tolowering of water levels in deepaquifers, by discharge along the NianguaRiver. If Bennett Spring and theNiangua River did not exist, perhapswater levels in deep and shallow wells atLebanon would have the same relation toeach other that they have at Richland.No large natural discharge of watercommensurate with that on the NianguaRiver exists near Richland.

As indicated by the scarcity ofshallow wells and the need to drilldeeper to obtain water, verticalpermeability increases west of Lebanon,between Goodwin Hollow and the

GroundwaterLOCATION MAP

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Spring..£1 850 fI

)

\

SCALE10 Mil..,o

ho 10 Kilom".,.

". -".

(1' 5 i Jin 'n' obove 'Not~OI Geodlli<: Vlrli<:ol 001 m of 1929.All elevOllOns

Well deplh, In feel

10 too 1000 to,ooo0300+----------'------------'----------.:.L

~ •~ EXPLANATION

"00,,B • 'Nells In lhe vlclnlly of Richlond

" , Wells In Ille vi<:inlly af Lebonon..j

,, , Wens In Ille vi<:lnlty af Senne" Spring

•.."00 ~ •

0 • •

i "• •, ,,

z • ,• , , ' ,

'000g •0 •.. • I'• •., ,i ,; • • ,

• •"'00 • • '.•

" • I:' • •• •• .. • t •• ,! •r

'000'00'oo,-l----------~--------~---------~

'0

~tl depTh, In fIoel.

Figure 18. Water-level elevation versus well depth for welts in selected areas,

59


Niang~a River. This increase and thecapacity of the rocks underlyingGoodwin Hollow to accept large volumesof surface flow during heavy rains,compared to the lesser capacity of DryAuglaize Creek (see subsequent sectionon groundwater-surface-water relationships), indicate increasing east-to-westvertical permeability.

The connection between Potosi wellsat Lebanon and the Niangua River, assuggested by figure 18, is not readilyapparent from the potentiometric map(fig. 13, in pocket). This suggests thatther~ is hydraulic connection throughconduits and fractur~s transmittingwater, a condition that cannot beadequately portrayed by water-levelcontours in such a heterogenous system.

RELATION OF WELL YIELDS TOTOPOGRAPHY AND SUBSURFACESOLUTION DEVELOPMENT

The large difference in the standarddeviation of the ratio of well depth toyield (O/Q) in various basins andtopographic situations (table 4)

correlates with results of other lines ofinvestigation, which show a relationshipbetween well-completion data, thepermeability characteristics of theformations, and topographic situations.An example will illustrate the matter.The mean discharge of wells in NorthCobb Creek basin is 17 gpm; in OryAuglaize Creek basin, 18 gpm.Similarly, the mean O/Q values for thetwo basins are comparable at 19.6 and22.8 ft/gal, respectively, but thestandard deviations of O/Q are 14.2 and28.5 it/gal, respectively. The area withthe greater standard deviation is thebasin in which solution has affected thebedrock more severely and developed amore hett:.fogenous condition. The relationship correlates with the evidence ofanomalous streamflow characteristics inthe Ory Auglaize Creek basin and themore normal characteristics of NorthCobb Creek basin.

Wells completed in the GasconadeOolomi te along the Marshfield-Lebanondivide and in the Ory Auglaize basin, arecharge area, have similar mean O/Qvalues, yields, and standard deviations.Along the Osage Fork, on the other hand,

TABLE 4

Well statistics

Ar••

Ifjg.4'

North Cobb Creele

Dry AUlI~il. ernie

Divide MershfoelcH.ebanon

Osage Fork

Divide Marshfield·Ubllnon

Osage Fork

Bennett Spring

Areawide

South Outcrop

1Ratio of well depth to Vield

60

FOrmf;tion

Gnconade Dolomn"

Roubidoull Formation

Guconaoe DOlomite

Potosi Dolomite

Jef1er$On City Dolomite

No.otw.,.

'""33lBlB1.I.22

24

Mean discttet9t. M..nDI0 1 StandardIlfPml Ift/e-ll dWimon.

Ift/v-ll

" 19. 142,. 22£ ,.,,. 25£ 2B'22

"lB

13 20 11.S

21 10.1 ".21 13.6 12

250 .. B.B

" 28 28.5

the values are quite different from thosealong the divide. Mean yields alongOsage Fork are a little higher and meanD/Q values and standard deviations aremuch lower than those along the divide(table 4). In other words, it is notusually necessary to drill as deeply alongOsage Fork to obtain the same quantityof water from the Gasconade Dolomite,and wells are more uniform. The higheraverage yields are probably due to moresaturated material, and higherpermeability resulting from solution ofthe dolomite. The same relation holdstrue for the Roubidoux Formation,except that standard deviations for bothtopographic situations are lower thanthey are for the Gasconade Dolomite.

Wells completed in the GasconadeDolomite in the vicinity of BennettSpring, a discharge area, have valuessimilar to those for other dischargeareas. The Potosi Dolomite, the highestyieldin~ unit in the section, has the best(lowest) D/Q value, the best mean yieldof all units investigated, and the loweststandard deviation. The Jefferson CityFormation, a silty dolomite, has thepoorest mean yield, the highest D/Qvalue, and one of the greatest standarddeviations for the areas sampled.

GROUNDWATER QUALITY

Analyses of water from selectedwells in the study area <table 5 and fig.19) show that mineralization ofgroundwater is typical of karstic, highcirculation groundwater regimes.Because of rapid recharge and relativelyshort residence and transi t time todischarge points, the water is not highlymineralized. Continual dilution isequivalent to rapid recharge.

Groundwater

Differences in mineralizationbetween aquifers are subtle and must beevaluated with respect to well depth, theproducing aquifers, location of wellswith respect to recharge and dischargeareas, and the time of the year.

Water entering the system in uplandareas, by seepage through residualmaterial, tends to become saturatedwith calcium and magnesium carbonatesrather quickly. In time, however, asmore and more carbonate is leachedfrom the residuum, less remains, andunsaturated water is able to penetratemore deeply. Thick residual mantles,such as those west and south of Lebanon,result from long periods of leaching offractured dolomitic rocks. Data fromwell logs show 40 to 80 it of residualmaterial at many sites in this area,which the potentiometric map (fig. 13, inpocket) shows is an important uplandrecharge area.

During periods of normal or abovenormal rainfall, thick residuumundoubtedly acts as a storage zone formuch water unsaturated with calciumand magnesium carbonates. Slowdrainage from residuum into bedrockdissolves soluble carbonates at the rockresiduum contact, leaving an insolubleresidue to perpetuate and thicken theresidual mantle (T.J. Dean, MissouriDepartment of Natural Resources,Division of Geology and Land Survey,oral communication, 1977).

Mineralization of groundwatercorrelates with movement of water fromrecharge area to discharge area. Figure20 is a map showing the totalmineralization of the water from 38 areawells completed at many depths in allwater-bearing units of Cambrian andOrdovician rocks.

61

TABLE 50:-<oi35'"-<o."n,.'"~,.-<'"-<'"'"'",.Z'"

Analyses of water from selected wells in the Osage Fork, Grandglaize, and Niangua River basins(Ojc = Jefferson City-Cotter Dolomite· Or :; Roubidoux Formation' 09 '" Gasconade Dolomite" Cp ". Potosi Dolomite). • .

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"

Groundwater

EXPlANATION

...

well location and _UMber(SM Tobie 5)

••

•

... from U.S. Geototkol Surve,note bo•• mop,':500,ooo.

• 9

'3

'3'

36

38'

'37

Camdenton.

/-~C~amd.n County-T-31. -~

, ~32 \I \ ,.-430, \ '28 7 25' __J

I ) ./I r 27'L-~1

"29 J fl.21 1.';'9 "7 I /( ......,.....,/ / .,.

I \ r'5.22 I I ) '16

, L~./

! ;;.""",.. Co,,," I{ Lo,"" Co","

;W.....,C..;;;'----;~ - ---1 W"."~~-

\• I/ ,Mor.h~f"::::''''VJ _, I,

II

Figure 19. Location of wells where water-quality data were obtained.

63


9~'OO"

58"00'00"-+e8.6

EXPLANATION

Bose from U.S GeoloQlcol Sumy"0" ba•• lftOp, ':500,000.

e 7.7 Total Ion. In ~ul,al.nt1

p.r fI''lIl1lon

D Atchclr9' ar.o

e8.4

'.2

o'0

fb':::I::I:i'~===r=1='y"u

"10 K llomet.,.

Figure 20. Ion concentrations in groundwater.

64

In the area along the divides in thecenter of the project area, the concentrations of total ions in milliequivalentsper liter (meq!O are generally lower andmore uniform than in surrounding areas.The potentiometric map shows th3.t thisis a recharge area. Wells within it are270 to 1625 ft deep and obtain most oftheir water from the GasconadeDolomite, Gunter Sandstone, and PotosiDolomite. The relative uniformity ofthe mineralization indicates vertical aswell as horizontal mixing of the waterthrough the section. The II ionconcentration values range from 6.9 to10 meq!l, the medium value is 7.7 meq!l.Twenty-five ion-concentration valuesoutside the central area range from 5.2to 17 meq/l; the median value is 11meq!l. The range in ion concentrationsin the circumferential area represents avariety of hydrologic conditions,inclUding recharge and discharge. Forexample, the low concentrations in theupper part of the Osage Fork basinprobably represent recharge conditions,whereas the high concentration atBennett Spring, in west-central LacledeCounty (13 meq/O, and threeconcentrations of 11 meq!l along OsageFork, in southeastern Laclede County,probably represent discharge conditions.

A divide area with a considerablerange in concentration values suggestsslower recharge and less mixing. Alongthe divide extending from Marshfield tothe southwestern corner of LacledeCounty, the sampled wells range from315 to 1050 ft deep and the values ofmineralization range from 8.0 to 15meq!l, with a median value of 12 meq!l.

Admittedly, the foregoing analysis ofthe data is very general because of thesmall number of analyses in relation tothe size of the area and the diversity ofthe recharge and discharge characteristics. Within a basin such as Osage Forkare many subbasins with widely varying

Groundwater

recharge and discharge characteristics.For a more comprehensive analysis ofthe relation of mineralization torecharge and discharge, additionalanalyses are needed; sampling locationsshould be determined by the flow systemas determined from streamflow, waterlevel, and geologic investigations.

In this respect, carbonate-saturationdata have been used successfully in othercarbonate terranes in the United Statesto show the movement of water fromrecharge to discharge areas and tocorrelate such movement with yields ofwells and springs (Norris, 1971; Feder,1970; Back, 1963). It seems certain suchstudies would strongly support thefindings of this project. For future basinstudies, some carbonate-saturation datashould be collected and evaluated.

Two wells on Bear Creek (25 and 27in table 5) were sampled to determine ifthere are any differences, in kind andconcentration of dissolved constituents,that might be associated wi"(h the flowsystem in the valley. Results of theanalyses are given in table 5, except forfecal coliform and streptococcus values,which were less than I colony per 100milliliters (col/lOO mO for both wells.

Well 27 is adjacent to a gaining reachof Bear Creek (fig. 21); well 25 is at adairy farm, downstream in a losing reachof the stream. The water level in Well27 stands above'the stream channel; thelevel in Well 25, about 40 It below thestream channel. Both wells are open inthe Roubidoux Formation and GasconadeDolomite and have similar lengths ofcasing. A sinkhole formerly used as agarbage dump lies midway between thetwo wells (fig. 21). It is not knownwhether the dairy operation, thesinkhole, or a combination of the two isthe source of the high nitrate, chloride,sulfate, and potassium concentrations inWell 25, but such concentrations do

65


0.5 2 Mil..

1---1,',--'-,---,-',I 1 1o I 2 :3 KIlometers

80.. from U.S. GeoloQlcol Survey 1:62,500 quodrangle15.

EXPLANATION

Sinkhole

0"

..... 'M

Figure 21.

66

Well ond number (See TobIe 5)

Sprlnll

Reoch of .treom with no turfaceflow during dry weather. Groundwoter levelt below streom channel.

Locations of wells in Bear Creek basin where water-quality data are indicative of groundwater-surface-water relationships.

indicate a source of pollution within thelosing stream reach.

The foregoing suggests that anysource of pollution in a recharge area

Surface Water

where materials at the surface can becarried downward to bedrock is apotential hazard to water wells in thatsame area. Since many streams in thestudy area lose their flow to bedrock,the potential for pollution is great.

SURFACE WATER

The basis of the surface-waterinformation in this report is a datacollection network of 1.34 stream gagingsites (figs. 22, 23, and 24), two of which,Osage Fork at Drynob, and BennettSpring at Bennett Spring in the NianguaRiver basin, are continuous-recordstations, used in this study as indexstations for estimating low-flowfrequency characteristics. The othersare partial-record stations and miscellaneous sites where periodic observationsof streamflow, temperature, and specificconductance were made.

The purpose of surface-water datacollection was to provide basic information on flow characteristics (primarilylow flows) for all streams in the area.These data were then used to study therelationship between spatial andtemporal patterns of surface-water andgroundwater flow.

MAGNITUDE AND FREQUENCY OFLOW FLOWS

The low-flow frequency data forstreamflow stations and springs, asshown in table 6, were computed byprocedures described by Skelton (1976)and provide reliable estimates of medianvalues (the 2-year recurrence intervaI),with somewhat less reliable estimates

for more extreme events. There is noway, however, to evaluate mathematically the magnitude of the errorsinvolved in these procedures.

The frequency data shown in table 6are the 7-day Q2' 7-day Q,o' and 7-dayQ2(}l the values most frequentlyrequested. The 7-day QlO is of specialinterest, because it has been designatedby the Missouri Clean Water Commissionas the maximum flow for design ofwaste-treatment facilities. For the twocontinuous-record stations in the area(figs. 22 and 23, map nos. 23 and 31),values for 1, 3, 14, 30, 60, 90, 120, and183 consecutive days can be obtainedfrom the Missouri district office of theU.S. Geological Survey, Rolla, Missouri.

In some cases there are differencesin the low-flow frequency values ofstreams of comparable size in adjacentbasins, and the values sometimesdecrease downstream. This is primarilybecause of differences in infiltrationrates in losing or non-gaining reaches ofthe streams. In this report, discussionsof structural trends and effects on flowpatterns are contained in the sectionsStructure and Groundwater-SurfaceWater Relationships; variations in floware discussed under Seepage Runs.

67


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OEld'ldQe

i

'"~o

\I

,

(37°W-

Figure 22. Data-collection network and seepage-run measurements in the Niangua River basin.

66

Surface Water

)

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............ " ~"""'.....-.

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\,

Figure 23. Data-collection network and seepage-run measurements in Osage Fork and Bear Creekbasins.

69


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Figure 24. Oata--eollection network and seepage-run measurements in Grandglaize Creek basin.

70

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" -- SWll. NE" Me. 12. T. JJ N~ R. 19W~ .. briclwt on 31•• 5-20-75 .~ '" ~. ~. 0 0 •CountyH~ JJ. 7 n'Ii _"'-s. olllufl.... 0 ..... ..." ,~ ". ~.

<-" J·11-75 .~ = ""8-:lS-75 0 ~ "'011·\J·]5 ,... '" 10.01·:1'5-71 010-'8-711 0

" N..... II,_ SWXSWll. __ 28.T~N•• R Il1W_ .............. ,,, ..., ... ~O " .. "s,_ If........ 31. 7% .... _. ollkltlolo. 0 ..... 7·13~ '4.7

<-" So21-e2 .U ~O.,., 11.5 nD10-2-43 111.5 111.011·5-113 1lI.3 12.010-21~ 15.2 ~ 11.0 ,~

11-22-111 31.S "" n.o..., ~o ~ 1\1.08-3\.70 "'.. "" 24.5 NO11-28-11 ".. "'" 23.0 ",6 ... ·75 611 '" n.o1·111-15 "'.. ... ~.o

8·25·15 19.3 ... ".8·25·18 ... "" 2l.59-918 11.11 ... 18.010·1876 "'., ... 10.5 13.5

'·25-77 21.9 ~ n.o 26.5.. G<...y OHk NW" NW" lee. 20, T.]oI N.• R. 19 W.••l l<><d "" ... 6·5·15 '.87 ... no"

,..<"""IV ~'9"'''IY. III m, --mUll of 8uUtlo. OoU.. 1·111·15 1.52 ... "'0,""0" 825·76 '''' '" n,

10·18·16 " ... 11.0 14,0

Surface Water

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0S....m"_d", tow·llow hoq................ "Mop no. s,,""'" ".... Loeo.ion Oni...,. Om Dhd,_ Sp.,dl'" w.... A<, An""oIlow.flow nn ~hllo, -<... (1,3/.1 cor>!luetan.. tomp...WtO tempo""''' 7 con_uti.. d.".. Of indi..,1II! 0Iml 21

-"'~1°C) 1°C) ,"curren.. In"..,1 lin v••nl ~

at 250C) ," ro n,.

(till< n. contl.n'lf<ll NIANGUA RIVEA 8ASIN Ico",'m.oe<ll '"'"" NI.ngw Ri... Icon•.! SE~ SEll. .... 25. T. 35 N•• R. 18 W.. \""",i"""'1 ". 10.'.·70 on "0 16.0 02·\1).71 '" "'" '.0 Z• .(S.]. '" ,~ 11,0 ~8-4·71 '" >a, m.~72 '" '00 12.0 -<11·14·n :).5040 '" 10.0 '.0 m6·2-15 "" .. 11.5 '"8·25·76 '" ." 19,0 '",.

" OI~""C,rek Nw1I SW% l.OC. 30. T. 35 N. R. 17 W.O II ''''d on .2 6-2-75 0 0 0 0 Z""""tv htghwlV. hIlt. "".. notttl 01 6on.... tt Sfl';ng, 11·14-75 0 mL~e<I.Co...."I. 8-26-78 0

" Llltl. OIl1"'V.'<I C,..k NE% NWII _. 30. T. 35 N" R. 17 W.," lord o<l " 8·2·Th , 0 , ,COlli'" high...y, 1 ",1""'1Il ot ao"noll Sprong, 11·'.·75 ,LW.d< Co""l•. 8·28·76 0

" NI""iI" RI"" NW% NEll. lOC, 1, T. 3S No, R, 18 W.. " old bridlJl.", .~ 6·2·/5 '" ~ '8.0county h;glowav. 411 ",I no<tn...., 01 8oMo1\ SIlr!.... 8·26·]6 '" ~ 16.0Doll.. e""n.....

" /.lou,,,,;,, C,."" SW:I. SW4 OK. " T. 36 N •• A. 17 w.. ., ford "'" eoutolV 28,1 B·NS .. , 0 0h~w,V. 41\ mi .ootn","1 01 EldtldQI. Loolll<!o 11·a·16 0County. 11-2&-18 0

n H....VHoIlow SEll. SEll. _. 35, T 36 N.. R, 18 W"" 10«1 on <""nlv '.0 8·2.15 '''' 0.'h'IIh........ 8 m, "",u..." or Tun... 0.11.. Countv. 11·20·15 ,ro ." "2·25·16 "" '00 ...

8·26_76 .'" "'" "'.,'" t<1-.gut RI .., SWlo:NEI' ..c.30.T 36N.• R 17W......... ot""'ynty "" 6-2-15 '" .. 21.0

ni9:'w.~.5m; ..." aI Eldtldgo, lAC""" County, lI-2&76 '"" 5_. 01... 50""'! SE" NE% ..c. 30. T. 36 N., R. 11 W,," f,"',"lI ,.."'I, 6·NS 47.2 .ro 13.5 " "5 "'i " ..., 01 EldddlPo. locl.d. Counly. 11-28·76 n.s 15.C10-21-76 n .• .~ 14,0 '2,58·2(·71 ro.' .'" ".5

" J.l<o,C,..k NE~ NWY. ""'. 33, T. 36 N.• R, 16 W.. " 10«1 at 000 pf 18.' 5·2H5 M ", 21.0 24,0 0 0 0Count. High...... YY, 5 m, .""tt..." ot Tun... 001,•• &3·75 " ",0 21.0-,. 7·1&.15 0

11·20·15 00 "" ..,2-25·16 '.00 ,,,

'08-21>-75 ,11).19-16 ,

M;lIC,..~ SEll. NE'4 ooc. 10. T J6 N .. A. 18W...1 ford on ""unt. '" 8-3·15 11.8 .'" 19.0 .0 "''''';,1'''' n"tt'..." 01 T~. 0011.. CounlV. n·1O·15 10.0 .W 10.08-26·16 ,." '00 "'.,8-24-11 2,13 ." 21.5

l Mo"u",m."u "'., ~,. <1>0""" ""''" "'_ du,ing_p"9" ,~"', Min. 0.............ilobl. ,n file< ot til. U~;. Go<>IOg'OOI Su,... ", R"tl., Mo.

TobI.61_,tin_1

S"....f1ow<l.... t..o..·f1ow h"'l'-'CY <loto

Mop no. Stram nom. lOCO'Kln D,.t_. D.,. Di""'_ s-m< W.,.. AI. Ano,,", low·llo.. (In nJ/d 10'... lnJ/d .ond"",..- ,_,.w,. tempo<"U" 7 ..,._ti•• <I..... tt ;"(li,,.'t<llml 21 (;.",,"0/= (OCI '"'' ' ••" .......,. In'....tl lin va")

., ~"CI ,'" ro

Uig. 22. oo."lnoedl NIANGUA RIVER BASIN 1C<WI,lnueel)

~ Ni"'9ua RI .., SWll. Nwll. 1tC_ ". T, 36 '1_. R. 18 W.. oI>ou' 200 1, - 9-29-11 '" .., 23,0 28,0 '" ,~

do.....n'..m from Mill C,"~ inflo... 1 ml nOI1I>o.. , of 6-3·15 '" "" ro,Tuna•• 0.11.. County, 1·16·15 '" ". 23.0

8·26-16 ".9-8-16 "" "" 22.510-19-18 '" "" 10.5 ."3-24-11 '" "" 24_0

~ Wool ..y CfH" NEll. NEll. .ec. 36. T. 31 'I .. R. 18 W......" mouth. 18.9 3-28·16 , , , ,2 ml ooulll of Tun... , Dom. Camden County.

" B.ood", B,..c:Il SW'4 NEll. .... 23. T. 31 "I .. R. 18 W.. allord 011 10.2 8-3·75 ,,, .." 21.0 , , ,.ounty hivt>....... 8 ml ooutto..., 01 Mook. CfHk. 11·1<·75 ,.'" ." 120C.....dtn County. 3-26-16 ,

" W......, CfHk SE" NE" ..t. 7. T. 31 "I .. R. 11 W.. 11 010,,1"9 ..... " 8-3·15 " .00 21.0 , , ,lIl. moulll. <\40 ml south...., of Camelln1on. Camden 8·26·16 .'" "" 28,0County.

" 8.nk B,.ndl SEll. SW% 1tC_ 3. T. 31 "I .. R_ 11 W.••l t>rld~ on •• 8-3-75 <.<0 ... 19.0 ,, ..County Highway 1(. 2\40 m, 'OUlllWfll of Camd.nlO11. 11·1<·18 '00 '" 11.0Camd.n County. 3-26-16 .00 ~ "'''

" SponoorC,etk NEll. SE14 lie. 30. T. 37 "I,. R. 16 W... , ford on county 10·15-11 .., 13.5 • • ,~~wlly. 1\40 mi norm_l 01 Decllu",III. Clmden 8-26-16 •County.., S_ce.C,ook SWll. NEll. lie. 13. T."R "I .. A. 11 W.. obeUl 2000 It 10·15-11 • • • •upOl••.., f.om Tu,k.ypen Hollow. Camden County. 3-26·16 •

" Spencer Crook NW% "IE" sec. 1<. T_ 31 'I .• R, 11 W.,,' ford on 10-15-11 .00 • • •""""ty hiIJllw.Y. 1\\ mi ",lIt!> of CounlY H~wlly 11-14·15 .00 '00 10.5O,CtrndenCounty. 8-26·16 • ~ 19,5

" S!>tnce' Crook SE" se"...,. 3. T. 31 "I .. A. 17 W.. II bridge 011 ,,. 6-3·15 1.69 .." 210 , • ,County Hlllhwily O. 2 ml sou'h.....' 01 Camden,OII, 11-14·15 '.00 •• 11.0Camden County, 6-26-16 •

" H""onka Sp,lng ' Can'.r .... 2. T. 31 "I" R. 11 W.," H.t.. ,,,,,kl. 2 mi 8-26-16 'H .00 14.0 .. .,00II111 of C..,den<on. C.-nden County, 10-21-16 65.5 "" 14.0 11.5

3-8-11 ~. 1<,05-25-11 86,5 14,08-23-11 51,3 "" 1<.0

1119.2<1 GRANOGlAIZE CREEK BASIN

Dry AU\llalze C...k2 "IEI' SEll- 'oc_ 2, T_ 34 N_. R. '8 W_,.t b,idgo "" 6-2-1& 1.28 "" 22_0

""""lY hi9hw'V.t n"""" ..l eel"" of leb..."". 8-25-15 '" .." 26.0lKlede County_ 11·5·15 '" "" 16,5

2-24-16 .00 M' ••3-24-16 .00 ". 11,58-19·16 '"... lM...ure,...n" lIllIl'" ohOWll_.. mlde duri"9 ...... ",n._ M.ny o'h.".,....lloblo In fl,.. of lIl. U .5_ GoololJicol Survey II Rolla. Mo.

'" 2F,eqUOflC'V ..llm.t.. nol p",.ibl. bee&uot of ..';lbI. effecl of ....age·t'.ltment plen, outflow.

"TobilII lconllnuodl

C>SUO.ntl_tla.. Lo-tl.... l,oquUlCY d......~. S1..... n..... LOCIli_ Dr';..."" O~ Dlld>",,,, """. W...., Ai. Ann...1!_·ltow (In ril,.) ro<... U~/.I-~ 'a_ow'" IOrnp"'OW," 1 """......u••~ rt b.,l1",,""

(m~l lIJrnlu""'" '"'" (OCI '.cu,...... m'....ll;" V"").. 25"C1 ,

" ~

I!I~ 2", CCWl~n..edl GRANOGLAIZE CflEEK BASIN 1...",lnutdl

"'",,_.-u.._, SEll; "'£1'..,..;. 2. T. ~ N.. R. t6W ••, nol1:l1 ••" ""to H4·76 ,.~ "'" 12.f,~."t _.nZ (Ilnl 01 L.tIOn"". LI<lod. C""n..... &-6·76 ,.~ "'" 16.0IloQM <JIlefatln~ In I.te 8·19·711 '.00 ." \B.OFtll.....V 1976), Dry AlIQloi .. C,••k'2 NW'ji NW>I sec. 31, T. 36 N.• R, 15 W.• "'o<d "" 6-2-16 ." ~O 22.0

ooun,,,, 01<11...... 1% ml no<1"'", 01 LOll"""", 8·26·16 ." .~ ".Lad.". Co,,"''!. 11·5-15 .00 '00 165

2-24·711 .00 ." '.03·24·7l1 '.00 "'" 11.5s,e·78 '" ." ".B·I9-16 '00 "'" 20.0, Dry ""III';", c.,,,,,2 NWW; NE% _. XI. 7.35 N., R. 15 W•••tlol'd on 6-2·7!i O.lil '" 21.0

""'""IV It"",".v, '2 mi _'~WltIt 01 $1"1*. lodtd. 8-25·75 .~ = 27.0-.. 11~75 ..,0 ~, 15.51.24·76 .00 m '.0J·24-15 2.lll "'" ".4·2-16 '''' .W 11.0

&-6·76 4.50 OW ...11·3·111 '" ~O 1&.0

8·24-17 ,." '" :M.O ,,.• D,V AlIQIOI.. Cro.k2 On 11".I>O_n ...... 18 on<l 111, T. 36 N.. R. 15 W., 01 &'2·'1!i 0

b'la(,JO "'" .....nty hlgllw.... , 111 ...1_.1 01 51.po" g.25-71i 0LKlodt Coun'v. 11·1i·75 0

2-24·76 03·24·76 .'" '00 12.04-2·76 .00 '" •••&-tH6 ." .'" Is.1i6·111·76 ,11·3·78 ,

• Drv ""lII0I.. Crwk3 SWIIo NWll. -:. 8, T. 31i N" R. lliW" 01 b,idgo.", g.HIi ,.§ '" n.' , , ,C""nty H~w.... F, 2 ...' nort!1wnl 01 51.._. l.-e:loodo 8-25·76 0County. 11-l1·7s .~ no 18.0

2·24·16 .~ "" ,..3·24·76 ." '" 12.04·2·78 .00 '" 11,5

6-11·16 .00 '" 17.08·111·1& ,12·21·76 0

• Willi .......... 6,..<:h NWli: SWl' _. 4. T. 35 No, R 15 W" o,fortl ..... co""lV 6-2-75 0 , 0 ,hlgllw.... , 21' ...1n"'th 01 SletPO', L..I.... COIlnl\l. 8·25-75 0

11-5·75 0!t-6·16 08·19-76 0

2F'OQ""ncv ."i....... not p""IIll. bee...... "I • .,lob" .fleet "llOwOll"-'nlotmon, ....n' OIl'~OW.

30.",,_ I'''''' ,,_·'nt.uno", pi.., I. di••" ... 10 Ni0"9". RI,or b ..ln ""0'" ~ndo'9'_....~tioo <llonnol. ~l'It"'orn !,"'" ",1••1... 1St. 'ul 10' <10<011.\

T..... 8C_~n.... l

S......._do.. Low-t_'....--.. d...Mop ..... S....... n_ C_ 0'_ o..

0_ ...... W.... AA ........... _·11_ Hn tt3/tl I",... ltt3hl - .._.ou.. .._.'u'" 1 -..oculi........,. .,__

1..,;21_.....

0"<' 0"<1 __ in..",.. tin,...,.1., 250CI ,

" ~

tlit. 2•. contin..... GII,tJlOGlAIZf CAEEK BASIN I<>an_J

D<v Auglol .. CIwI< SWll; Sf'>' OK. 29. T. 36 N~ A. 15W...1bridto .... 8-3·15 , , , ,....... tv h.......OV. 5"" ...st 01 Stoud_.~ 8-25-15 ,0..". 11·5-75 ,

3·'''''',

8-10-18 ,• Drv ............ CIwI< SEX $WX Me. III. T. 36 101.• R. '5V1...' 1___ 8-3·15 , , , ,

......... County High...... BB. 6X ......, of fldrldlo. 11·5-15 ,~County. 2·~1B ,

3-2H8 ,",1-1B ,

• 0.., ...~.... Cooek On .... bo...... ...,..13_2•• T.3BN..A.1BVI.••, 8-2·15 , , , ,__btidlIt ..........ty ......OV.6 ... _ ... 11~15 ,of E........ l_County. 8-1.16 ,

" O"' ........ Cooek NWlt. SEl' ...... I•. T. 3B N~ R. 16W~fl_. __ 8-1-1'5 , , , ,bridto ........nty .........,. 5 ..._.t 01 Eldt.... "'0-111 ,ledodo County.

" ~--NElr. NElr. ..... 20. T.:)oI 101, R. IIIVI,.' tIondge ... 8-2-15 , , , ,

SUW Highwov 32. IX mi _., of L_. lus-n ,lododo County. IUO·}1I ,

" Gooifwin H,,"- NWlt. SEX ........ T.:)oI N~ A. IIIVI.• 01 bridge ... S.... 8-2-15 , , , ,High...... fIol. hoi'. __I <1/~.l_ 11-25-15 ,0..". 3-26-111 ,

..»16 ," -- On .... _IOCI.28_33. T.:l6N~ A. IIIVI.... 11-'·15 , , , ,

..... ""_ty........,.3..,;_ofL-.. 8-25-15 ,~,"",,",. 3-26-111 ,

8-»111 ,.. --- NElr.Nwlr.OK.21. T.35N~ A. 16V1~ .. ""'", 8-'·15 , , , ,-..tyh.......OV. 5 ...._Iof~. LKI_ 8-25-15 ,0..". 8-20-111 ,

" ~Hollow SWX SWI' Me. 21. T. 36 101 .. A. " w...'bIi<l9o'" 8-US , , , ,Stnt H;ghway 5. 3"'; NIl or EkIhclge. L.._ 8-25-15 ,0..". 8-»18 ,

" 0", "'ugI.,..e- o. lin< bo_n lOCI. I I _ I•. T. 3B 101 .. R. '8 W.• II 8-2·15 , , ,low......, b.... on county highwlV. 5.,., ",1 __, 11·5-150' EkIr". lKlodo C<->ty 8-20-16

" D<v .......Ii.. C_ NEll. NE'>' OK. 35. T.31 101 .• R. 16W.... 1__.., '''·15 ", , ,

..... on .....nty hivhwov. 2\\ "'; ••t or O'U'.....III•. 8·20-76 ,Cerndof, Coun'v.. Drv ....uglli .. CrHk NEll. SE'>'_. 22. T.31 101.• R. ISW.... I_-w..., ~·15 , , ,..... on county hivhwIII. 2"" ......"'••, 0' Dee.o...... 8-20·16 ,

~.111•• Cemd'" Covnty,

"'" '"'" n•'"..~

I-<"'"Tobl. 6 lconlinued) 0

~ ....'" 0

S~",fl_d.tt Low·flowff«J....,cy d... ClMop no. 5......" ••_ LocatiOfl D'''n. 0 •• 01"",,0'11" Specific W...r ., Annu" low.flow lin It='/sl lor -<

.r•• 1tt3/ol e<>nductan". ""-'0"" ..mPOtOtu," 7 oo......,u" .. doy. ot Indl<.t..:l 0Imi2) II<mho/om (OCl (OCI ,"u"e." in...... lin ye.n) ~

ot 250(:1 ,'" ~ ",.

{fig. 24, contlnuedl GAANDGLAIZE CREEK BASIN (continuedl '"'"" P,nijolln Ii<>ll"", SWll SEll ~c. 14. T. 37 N., R. 16 W., ot low-water 64·75 0 0 0 0 0Zbridge on coynty hijllwoV. 4 mi IOUthwe" of 8·20·16 0 ,.

Moo".. I, Camden County. --;~ Dry AU\lI.i,. Creek NEI> SEll ..c. 35, T. 38 N" R. lew" 01 b';dllf on 5-22-15 '00 ~ 21.5 0' "'St.t. Highw.~ 7, 3% mi no<thwtOl 01 Mont,..I, 6-4-75 '00 '" 23.0 --;

"'Camden Coontv_ 7-15.-75 .~ ". 25.5

'"11·5.-15 '.00 ,~ 15.5

'"2-2H6 2.70 = 10.5 ,.3·24·76 '.00 ,~ 12.5 Z5-5·16 '.00 "']-He .~ ,~ 22.08-21H6 .~ = 23.010-19-76 " ,~ 12.0 '0

" Soli." Hollow NWlI SWY. .e<:. 5. T. 37 N., fl. 15 W.• ot low·wa.., 6-4·15 ." ~. 23.5 0 0 0Dridlll' on StOle H~w,y 7, 1 mi wo" of Mon...... 6·20·76 •ComdOfl Coun.~.

" Dry AU~laizo C...~ NW'4 SW% .ec:. 17. T. 3S N,. R. 16 W,. It low-wa"', &'21·15 0 0 0 0bri~ on county hlghway.4 mi nor1h of Mon"aa1. 6-4·75 0Camoon Coun.y. 1·15·15 0

11·&'75 0 = 19.02-24·76 01016-76 0

" Dry Au~lai.. C,ook Nw% SW% soc. 22. T, 36 N.. R. 15 W.. allow-w..., 6-4·75 '" '" 22.0 0 0b<idge on county highw.... , 21' mi noftlloa" of Mon· 7·1&'75 0 ,~ 17.5...... Ctmelen County. 11·&'76 .~ ,~ 10.0

2·24-76 1,708-2076 08·9·77 0

" Dry Augl .... C...k 'lE'4 NW% .OC:. 23. T. 3S N.. A. 15 W., 0' bridllO on "" 5·21·15 4.23 "" 26.0 27.0 ., 0County Highwov A. 2 mi north...... 01 TO,OnIO. 6-4·15 ,." "" 23.5Camdan County. 7'15-75 1.14 "" ~.

11-&.75 ,~ ,~ 19.08·2076 ..10·19·76 ." "" 11_0 •••6-23-77 .~ '" 30.5

" Sh.ko'09 C..... NE'4 NE'4 100, 26, T. 36 N.. R. 15 W.. a. low-wa.o, 6·3·76 0 0 0 0bri<lgo on County Highwoy H, 1'4 mi northwest 01 8-18-76 0S,outlar>d, Camdon Coonty_

'" Rook~ Hollow SE'4 SWII sec. I, T. 36 N.. R. 15 W.... forn on ooun.~ 6'3-75 0 0 0 0higl'lwOV. 4'4 mi no,th of S.outland, C_n Coon,~. 8-19-76 0

" Soli... C'ook NE% NE'4 '00. 31, T. 37 N.. R. 14 W.• at brid..,. 00 ~ 6·3·76 9,02 '" 22,0S'". Highway 7. 6 mi north..... ' of Riml.nd. Camden 8-19-76 4_39 '" 23,0County. 11-29·77 2_75

Ma~ 1\(1. D...

5"-..11,,.. dOl.m_g. S_lnc

Itt3/o) "","",uc,""co

WmhoJ....•• :s"C)

W".rIImpo.... ,"

lOCl

Lo,....f1ow'nq_ d...

Ann••II<>w·llawlin tr31.I'o<7 <on'Iocutl.. <loy Indleo.od

...,.. ......,. In, lin flO")

l 10 lO

GRANOGLAIZE CIlEEK BASIN (conti""od)

,

,

,

,

,

,

"

,

,

,

•

,

•

,

"

,

•

,

,

,

,

,

..,

"

..,

260

..,

27.026,0

21.0

••

21.0

21.0

'"24.029,0

•••

".."'..

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'"

'"

,..

'"".'"'"m

'"".

".",

",,••••

9.025.16•.915,01,,,,'",,,

1),610,5.2>..'"),19,."3.19,,

11.5.m4.19

••32,3

/1-3·157·15·768·11P6

6-)·7&8-19-76

6-3-158·19-165-2S·7111-29·11

6-3-758·19-16S·2S·71"·:29·71

6-3·158-19·165-25·1]11·:29·1]

6·22-166-3·157·15·158-19-1610·20·165-25-1111-2!1-11

/1-3·158-19-16

6·3-756-19-76

6·)·768·19·7611·2\1·11

6+75a.19·76

"

"

"

'"

NEl< NW"'-_.4. T, 36 N.• R. 14 W.. 01 b"<kIo ""5t.to Ilighw.v 1.• mi ""'til....., of RidJl....d. e."d.n

Coun'v.

SWI> NWI>_, 11, T, J6N .. R. 15W•••, lK~ an.altM'Y hlgllw.V. 4 ml ""'"Ill...." 01 5,,,,,,1.'><1. Comd..,0..,.

SWy' SWY. let. 25. T.31 N" R. 15 W, ot lKldgrr anS.... Hlfl ..... 7, 4)1; mllOUth.... of Man"o", Comd,n0..,.

SW% NE% ... , 27,T 31N.. R.1I'W"'lb"dlltltMcoun'v h"'>ny•• m, _"',... 01 M"""nl, CtmdonC"""ty.

SE" Se1' ..e:. 14. T, 37 N., R. IS W..., bridvo "" Stoto111;;. ..... 1,3\0 ml "''''h.... 01 M"""..I, Comd.n0..,

NW\I SWY.MC lB. T.37 tL R. 14W low...."',l>ti<lll< an ••,"'''V IoI",wty,. ml """", , of M",,~".Corn<Iof, C"'-"'.V.

SE% NWY. Ml;. 7. T. 31 N.. R. 14 W...' law....'"b'i<!vo "" """nly hlgt1,...•• , 5 mi _"'.... of M""'.....C....,denC"""ty.

NW% NEIO _. 6. T. 31 N.• R. 14W... llow........b<idgo an .""nl'/ hlgt1wty, 5 ml nOfth.... of Montr..1,

Comdon CounlV.

SW%SEI' ...., 11. T 31 N•. R. ,.W.... low-w...'

t><idge "" ",",,"tv hl;;.w..... 2:<. mi "ar"'....' 01 W..Gloiu. e."don CaYntv.

NEll. NWI' """" 29. T, J7 N.. R. 14 W",' I -w... 'l>tldge on CUUMIV h~w,V. Sy; ml Mrl..Ih ' of Ri<:l1-lor><l, Com<;\"" Ca<lnw.

On Hn. b,l1w..n loe1. 10 on<! IS, T. J6 N,. fl, ,4 W., 0'bridge "" c""n,V lo~w..... 1 ml ....., 01 RidJlon<I.C,""",n CaltMty

Mill Cr.....

Murphv C_k "Tom'"",

o..l,llolluw

MiIIC,..k

W., GI.I,. C,..k

We. Glol'" Crook

"

0) Tobie 6 (o;on,;nuodl0

St,._ll... ",,~ low-flow INquoonq dot.

",",PRO. S"..", no",. l_ti"" D,ol_ DOlO Dischar!i'" Spocifi. W..., ., Annual I"",.flow lin ttl",! tor.,.. (till,) C<l"dl>ClanOl ,,,,,,,,,,,.tur• ..."pt.Olu•• 1 co......,..\i•• doy. ot I...IA....

Imi 2) lil.molcm <'« lOCI '","u'"'''' Into.... Hn v....1•• 25OCl ,

'" ~

(fi9_ 24••on,inuodl GAANDGLAIZE CREEK BASIN (continuodl

" We, Gloi,. Creek NE'4 NWJ; He, 31, T, 38 N.• A. 14 W., It bridge on '" 5·22-62 35.2 '" " "Coonty Hi!llw..,. A. 7 mi .",,11> of !l,umlty. camden 7·10-62 "" 24.0

County. 1l·1J.t12 21.2 10.0,.., 17.11().S63 14.8 18.0 n,10-&63 15.2 '00 14.0 ""10·23-64 11.0 .~ 12.0 16.09-8-67 16.8 '" 21.09-1-70 24.' ~ 24.C1 35.0l().I5·11 24.3 15.0 ".5&-22-15 51.9 ,~ "'., 24.56-4·15 33.5 '" 21.57·15-75 n.ll '" 24.08·19-16 16.1 '" 28.510·19·16 16.7 .~ 11.5 "8·2J.77 19.7 '" 25.5

" e"r>tll H<>Ilow NW\I SE;; ,0<. 25, T. 38 N" R. 15W._ It bridgo on 6-4·75 , , , ,County llighw.V A. ~.U. mil. oou'" of To,,,,,'o, 8·20·76 ,Camden Counr.. 8·23-77 ,

" O'.... C...k. NE% NE% 1eC. 34. T, 38 N.. R. 14 W,... low......' " 8-4·76 ." on ~, , , ,brOlgo on .O'>or. highww. 4l!< "" .ou...... , ot 2·24-76 ,..,

~ 10.0Toron'o. Comdon CO!Jnty. 8·21H6 ,

" Do.... C'Hk. SE% NE% <oe. 2B. T. 38 N.• R. 14 W.• lllow.....11O< ~ 6-4·76 ." ." ~., , , ,bridyt on eounr. b;gt>w..... 3l!< mi 1.1 of To<onto. 2·24·76 .~ '" 11.0c.ndtn County. 8-21).76 ,

" Dun"C...1< SW% SWI' 1eC, 2(1. T. 38 N .. R. 14 W.• II IOW.....Il.r " 6·1-75 2.43 '" no , , ,bridyton eounw highw..... I%m; n"' .....' of 2·24·76 10.0 '" 10.6To'onl0. Candon CO~"lV 8·21).76 ,

« Do.... C'HI< NE% NE% <0£. 18, T. 38 N • R. 14 W.. at brid9' on ~ 9·1-70 , , ,County HighWay C. 3\\ mi wuth 01 B,umlOy. Mill", 6-4·75 2.79 '" 22.0,-, 2·24·76 11.0 '" 10.0

8·20·76 ," 8,uml~ C'Hk NW% <0£, 7, T. 38 N.• R. 14 W.. ot mouth. 3\\ m; ,outh· 7-4·34 , , , ,

....it 01 B'uml ••• 1\11,11.. C"",nty. 7·26-35 "9·'·67 ,9·11).69 ,9·'·70 ,g.3Q·71 ,8-11H8 ,10·2(1·76 ,

:I:-<o(5g-<o~

n,."~z!.<"'~

""~"'

St..omflow date low·llow froq....,,,,, dot.Mol'no. St...m nom. l ....tion D"';~ ,.. D"dl"'go Spocific W.,., Ai, Annuol low·flow lin n3"1 fo<

•• 1n31Jl -- lOmp.,otu.. ..m_.tufO 1 C<K1N1:IIti .. d..,.••t indi<o..-tImi 2! l/!mho/"", lOCI ,"0, roc<l'fOnm in.., ... (in V""!

.t 25"'C! ," "

(fig. 24. continuodl GIlA~DGlAI2ECREEK OASIN !<:ontin""").. G,.,dvloizo Crook NW~ <eo. 7. T. 3D N.• fl, 14 W.• ju" ""w",troom f,om '00 ,.~ 10.0 " " "O'uml.v Cre.k. 31\ ml .<>Uth_" 01 B,uml.v. M;II., 11-2-34 ~,

~". '2·28-34 ".3·1H5 '.0005·20-35 '.0005-29-35 8.1707-25-35 ,~

7·30-35 75.610-13-35 ~,

12·5·35 '"1~·36 '"4·23-35 40.74·23,35 ".,6·2-36 23.6,.~ 16.49·7~1 ".,9·1D-6ll 00.' = 18.0 17.59·HO 40.5 '" 23.0 27.09·30·71 57.6 '" 22.0 ",6-5·75 00.' '" 22.01·15·15 41.3 '" 22.00-20-76 ", '"10-20-76 '" ." 10,5 "

Ifjg.23l OSAGE fORK AND OEAR CREEK BASINS

Os. Fork NW% NW% <eo. 22, T. 30 N.. R. 17 W, ••t br'dgo "" 11.2 6-2-75 1.16 '" 24,0 ", ,

Suro H;';'w.V 38. 51> mi "",th<.., 01 M.nhli.,d, 8-25-75 .00 '" 27,5Wtb".. CoU"ty. 11--4·76 ''''' '00 16.5

8-2]·76 '" '"9·16·76 ." "" 21.0, 0sa90 ForI: T,ibu..", NEil SW" tee. lB. T. 30 N.. R. 17 W.. It brld'l" on " 0·2-75 ." '" 22.0 , , ,5'.... Highw" 3B. 21> mi "",th••, 01 MonI11iold. 0-26-75 ,Wob.lOr County. 0-23-76 ." '" 21.0

9-18-76 .'" = 23.0, 0.. Fork On Ion. botw..n ...,.. 5 ond 8. T. 30 N.• R. 11 W,." '" 5-2·75 5.14 '" '", , ,

b<id!l' or> County H;gtlw..,. 00. 3 ml not 01 Monh· 8-26-75 ~ "" 29.0fi.ld. Webstt, County. 11--4-75 '00 '00 16.5

8-23·76 lA' ". 22.09,'6·76 ." '00 22_0

• 0u90 Fork SE\< NE% ..c. 33. T. 31 N.. R. 17 W..., low.w.,.. " 6·2-7'5 6.75 '00 25.0 ,.. ,b'ldgo On c<>Unty ~Ighw"", 51> mi north••t of M.,sIt· 8·25-15 .~ '" 31.0li'ld, Web"., Countv. It-4·75 '3.0 ". '6.0

8·23-76 '.00 ". n. V>0

9·16·76 ." '" 24.0 "'" '"- n•.,~•

J:-<

"'"ex> 0

"...

Ttbl. 6 (oon~"uodf g5"..mll.... <l0\.. lo",·lIowl,oqUln""d." -<

Mop no. s"........... locolion Droln"",.. Disd>orgo Specific W.tt. Ai, A""~" low'llow lin 1~/ollo. 0

•• Ut3"1 ""nductonco t.mpera,u," tomporttu" 7 ""n>ocuti.. doy••t indi..,od ~

Im;2) l~""'o/cm ." (OCI ,,,,,,,,once into,nl fin y.. ,,) n" 250(:)

, '" ~ »'"I/ig, 23, continued) OSAGE FORI< AND BEAR CREEl< BASINS (""",inue<ll '"0, 0.." For~ SE% Sf\:'. ooe. 22. T. 31 1'1.. R. 17 W.••t o,id90 "" .. 9-1]-53 "' 23,0 ., "Z»

County HighwOy M. 211 mi ..., 01 1'1101>\1"', 1'1.1»"" 5-3-75 '" "'" 21,0 -<County. 8-25-75 .. '" ~., m

11-<1-75 18.5 '" 15.5 -<8-23-76 '00 ,~ 24.0 m9-16-76 ." "" 24.0 '", '", CoMroll Cr..k NEil. NEl> IOC. 30. T. 31 1'1 .. R. 161'1.• at Md9" on " 7·17-53 .'" ,. »

County HighWay M. 51\ mi ..., of NiangUl, Webs,.. a·HS 10.6 '" 19.5 ZCo<Jnty: 8·25-75 1.01 "" '" m

2·26·16 '00 "" 14.0

8·23-75 '.00 ~" "."9·16·16 ." 23.0, HVdoC,..k SWl< NWIl. ,0<:. 2lI, T. 31 1'1 •• R. 16 1'1.• 01 b<idgo "" " 9·17.53 ,m ,.,County Highw.... M. 7 mi ..,,01 NioJ>g\>l, Webster 6·3·75 3.67 '" 16.0County_ 8·25·75 " .~ 27.5

2·26·16 '00 ~" l~.O

6·23·16 .~

8-16-16 .00 "" ~"

• C.nt,,11 C,oe~ SE'4 SEl'<..c. 12. T. 31 'I .• R_ 17 1'1 .... Iow·...t., " 5-20-75 11.6 "" "" 23.0 U "bridge on county ~i~....... 41> mi no<tho..t of Ni*"ilu1. 6-3-75 16.2 '00 21.5Webs.. , Count';. 1-17-75 2.51 "" 21.0

2-26-76 11.0 "" 12.08·23·76 1.26 "" 23.09·16·76 " '" 24.010·18·76 1.27 .00 11.0 11.5

• o..Fol1< SEll SWl> ..c. 12. T, 31 N.• R. 17 1'1 .• " low-wa.., '" 6-3·15 "., '"' 23_0 .. ,bfjdge on County Hi\t1 ...y F. ~Y..mino<th"Slof 8·23-16 '.00 ~,

~"Nionguo. W.b.te, County, 9·16·16 " '"" 2~.0

'" 9owt1n C".k NEl:I SW'4 SO<:_ 2. T. 31 N_. R_ 17 1'1_," lord on county " 6-3-75 2.07 ." 25_0 ,.,~i~w ..... ~ mj nonh...t of Njangu•• We!>ster CO-Un1y, 8·23·76 '" '" 28_0

9·11·76 "' "" 21.0

" Littl. Bowen Cro.k SEll NWlI. >0<:. 2. T. 31 N.• R, 17 1'1.• " lord on cOUntv ,., 6-3-75 " '" 24_0 ,highw..... ~ mi nonh..., of Nionll"'. W.bste, Co-unty. 8-23-16 .'"

9-12-76 00 '00 ~."

" o..FoI1< NWlI NElli <eo. 2. T. 31 N.. R. 11 1'1" at low'w"" '" 6-3·75 28.B "" 23.5 ,., •b,idll" on county hj~w..... 3Y.. mi soumWfl' of Rode,. 8-23-16 ,.'" ""Webs"',Co,"""y, 9-17-76 .~ '" ~"

" My." B,andl NW% 51'1% 'oe, 29. T, J2 '1_, R. 161'1" at low·..... , ,. 6-3·75 1.21 "" 22.0 ," "b'idge on Co-unty Hi\t1way N at Rode,. Wab<te, 9·2J.16 ,

County. 11--17-76 , "" ~."10·18·76 ,

,-- Str__lI_do"

Ditcll... Spoofic W•••,(ttJIol __ _,......

"""""ofu>l lOCI.'Z5"'cl

l.ow·ft_ ftOCl~d...AI, __.ft_llrltt3I1)""

__.IU.. 7 _ .. cI*TO Ollndicotod

l"C1 ........- In....... (In , ....)

2 10 ZO

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u

u

••

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..,

"

..

15.0

".".,

,..••".

".

19.018.511.0

22.0w.,

11.0

".18.5n.'

12.5n •".".

".'"n.n.".,,.w.w.n...,'un.'".

n,""~,""

""""

""""

'"'"""

""""""•w."

""''''""""

'"'"'"".

""'"""""..~.""

19.•18.319.187.826.3,~

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1.l6

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.~

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••13.1

n.'~

'.n

".","..u,.,...,...".,".......m,.,.."",.,..ro

11·17·537·tH"9-1·&016"'·758-2.·16

6.. ·758·2.·16

Q-28-J'1-31·"s.20-J5",."'·"·711'4HSam..111g..n·JlIlOollHlIll-14·n..25-11

ll-lo.J5e.n1lQ-1HlI

...·75&-23-711-11-71

~.""2]"71• 11·71

.11-63....8-20-11"'18-"•.e."lHI-"...·758-2..,5'·11-71

t-11.f3... ·7511-6-758-'4·711

31.7

"

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,..

...

...

".

OSAGE FORK AND BEAR CREEK BASINS l<:ontin_l

sn, SWl/. OK- 7, T. 32 N. A. 1$ W bridgo onCounty H9>woy Y. ,'" mi _ of Morgon,

l_Countv.

On 1.... _ ..... 111_ n, T.32N.• R.ll1W~ ..-.btidgo "" ........., ".......,. 2111i __•

01 MorP>. I.adodo Cowl..,.HElIoSE" '1. T. 32 N_ A. lew. "'--t",,,

twIdgo"" ty~. 'l!ollli_'" of....,.,.Led... County.

SE!li SWlho". 14, T. 32 N~ II. I'W~ rttw\dtO ""-"'..,higt>wwy.l"'mi_of-.....~

<-•.HW\I;.SWJI,._. 7, T. 32 N.• R. 15W. 0' bridponCow!ty H.....II¥' ". 2 mi __I of Moovon. l..odo6o

<-•.

SEll; NEll; Me. 30. T. 32 N., A. 111W~ •• btidgo onCowl.., H~oy U.t Rodof, W.tIt... CowIt'(.

'lEI' NEl' __ 6. T. 32 N.• R. 15 W.• I~ bed of OoogtFOfI< _ J m, nonh..., of Morll'l'. L_ County.

SWlfo SEX we. 31. T. 33 N., R. 15 W.. at low-w.....bri. ""county hi\trW.v. 2\1 mj norlhoOl' of M0'9"'.lO<!f<lo County,

8""'" C,"k

"

"

"

"w

"

"

NE% NW4 ""'. 36. T. 33 N,. R. 16 W.• ot l_oWot.,b.klgo 00 ooonty hilll1w,V. 2 mi nol1!1..., of M",~,Lododo County,

'M••u.....ntlltl.t ... "'own we,. modo during ••~ runo. M.nv otl1." Of••"ilobl.ln fil•• of the U,S, Geolog;<ol Su, ....... Roll•• Mo.

..

:I:-<"'"

~0C"

Tobl. & l-.tinuedlg-<

51..."nOW ....1I low-llow I'"""on.... dotl 0Mop no. S"........... lOCllbon DroinOgt ,.. Olodltrgo Spocilic WIll, -, Annu.llow·llo.. lin tt3hllor ~

• oo 1tt3/d _due_oo tomper",Uf. to"""" ..."• 7con....,...'; •• d ..... Of indl«"" ()

(mi21 (jlmho/cm (OCI (OCI NCU'....OO inll,..1(in yo.nl »ot 250Cl ,

" ~ '"'"0(fig. 23, """,inuodl OSAGE FORI< AND BEAA CReeK BASINS loontin""dl Z

" 0"," F"k NW14 NW14 sec. 33. T. 33 N .• R, 15 W.• It b<i~ on '" 9·17·53 16.9 180 " " " '<StlU Hi~w"" 5. 3 ml-.t of 0'1., loci",," County. 10·12·61 31.6 en

5·21-(12 ".. ...,8·2-62 31.9 no en9·3-63 19.8 25.0 '"'"9·31).G3 18.5 10.0 »114·63 19.0 "" 12.0 Z10·21)·64 ~, "" 130 14.0 en9·5-67 22.8 ,~ 19,08-31-70 ~, "" no ".~27-71 37.2 '" 2',0 26.05-20·75 m no 20.0 23.584·75 ~, ~, 2l.57·17·75 40.7 '00 22.08·24·75 24,2 '" ~o

1().18·76 ~. '00 10,0 10.5

" ...... '~ On lino botwoon IKI. 25 on<! 25. T. 3:1 N., R. 15 W._ It ~, 8··H5 ~, '" 22.5 " " "br~ on oo.,,"y hi~w.V It O~" Loclodo County. 8·24-76 '" "" 23.0

" S,.ln,C...k '1E% '1E% soc. 10. T. 32 'I .• R. 15 W.. I\ lor<! on " 11-6·15 ,~ '00 1],5 0' " "C"'-"ty H;ghw.... O. 2 m; IlOUm.." 01 0.11. lIdt<le 2-2&-16 ,~ ~o 15.5County. 1·2-16 '00

&-24·16 "J.7·11 '"9-9·11 "'SIt;n, C,"k NW%NW%soe.36. T.33 N.• R. 15W.. 1t b,ldgoon 00 9-1H3 0 " " 0ooun!~ hlg/l....y, hill I m;11 ,oum...t 01 0.11. Laolod. &-4-15 0County. 11-6-15 "2·26·16 "1·2-16 0

3-1·11 09-9·11 0

" 0"11' f",k SE% NW% soc. 1. T. 33 N.. R_ 14 W.. I! MdlIO on '" 6-5·15 95.1 '" 22.5 " .. "County Hil/hwIY 8.1 mi n",m••, 01 0.11. lIelodo 8·21·16 24.1 '" 25.0County,

" 0u\I0 F",k 'IEI' NW% soe, 16. T. 33 N.. R. 11 W.. tt bddllt on 8-21-76 "." ~" 25.5county hil/hwty.11I m; nO<1hol" 01 0';1. LaolodtC"'-"ty,

" CobbC_k SE% '1W% soc. 21. T. 33 N.. R. 11 W.. It MdlIt on " 11-6-15 ,.. "" 16.0 0 0 "C",-"ty I-I;I/h"'". B.I mi n",m.." 01 00-11. Lldodo &-21·16 "C",-"l'y.

'" L;tlI. Cobb C,eek SW% NE% 00<:. 22. T. 33 N_. R_ 14 W_.I' b';d!l" on .. 11-6-75 ,~"

16.5 " 0 "county ~il/hwIY. 5 mi normo..! of 0<1•• Laolt<le B·21-16 0"...

T_ •.-I

,.........- Lo-.fIow'- _...- -- l __

D..... 0_ -- ....~ W_ ~ _ '-.flow I... tt3"1 ""- 1tt3"1 -- -- - 1-.I......... at iooIica-.:I

""-_...

1"<1 l"CI _ "'l>WWIlin_""..-c ,

" '"(fi9. 23.....,...,..1) OSAGE FDIII<: AND BEAll CIlEEI<: BASINS 1......-)

" o..,..F"",1 NWllO NE14_. 21. T.~ H.• II. 14 W••• b.... "" ... 5-70-15 '" " .. "$1._ H......... 32. 0.1 mi ....._., 01 Orynab. ..~ ,..l_County. lContlnuou_ ....1.... 1. 1·11·75 0... "0 ~O

6-24·76 "'.0

" ",,"0- SE\O Hev. _. 23. T. 34 "I .• II. 14 W.... 1_........, 8-6·75 0 0 0 0b'idllt .... oount> hill"'t...y. I ml .." g! Orynob. 8-2H6 0llldodo Co",,'y.

" N.mIl C_C_~ HEllo HW\O .... 26. T. 34 No, II. 14 W., IIllI'ldgIO .... 52.0 5-20-75 ,." "0 21.5 24.5 .,SUI. MIs;.wov 32. Il!o "I! -., g' DrylNli>. loe'- .." ... ~O ~o.,..•. 1·11-75 ... '" ~>

11~75 ...0 ~, 11.02·26-76 ...0 ~ 12.56-24-76 ."lD-lIHIl ,.

"" H '.0

~ 0..,.. F..~ SW1l. HEX-. 17. T. 34 N_II 14 w_ .. twIdp ... ..~ "' '" n,ea-... H.--., AC.IIllo .... _101 l--..~.,....

'" -,~ sex Hev. __ 5. T. 34 N_ II. 14 w~ III_oter &.-24-7' ... ~, ~>

"'.. on -..... I!o¢w... I1 ... _.01 L__.L.-do Co<ottv.

" Mill-=- SWX "lev. -. 5. T. 34 H_ R. 14 W_., """,""" 'U &s-15 ,.,'" n. 0 0 0

ea-... Hith.... N. 8 ..1_,oll._. l.Id«Io 8-24-76 0.,...." G_III.., SE\O NEl' IOC. 23. T. 35 "I" II. 14 W,,",1_ lHl-75 '" "" 26,0

1lI'1dgo ... coun.v hlltlwlV. 1\1 ",I_"'wn. of Maul·11'_. Lodldo Cou~lv.IU""""" lrem mou'" ofOugo Foo-kl.

0 ......... 111_1 SEll: SEII'.-e. IS. T. 35 "I" II. 14 W.. I' t:N\dv< on I~'..• 1,250 .~~,,,

'" ~.O .. '" "".to Hi5t>wOV". 1\1 ..1_. 0' H..."'...... Lod_ 1-17-75 ,~ "" ~.O

County. 'Con'in~<l" tN' 0110 1921P'1 8-28-76 ...,Q.20-76 ".. ~ .. ••

" e..,c.nI< SW14 NO. IE. 6. T. 34 H" II. 15 W" .. "'-' "" ..~ 0 0 0 0Countv Hq.w....... 2\1 ..._. 01L_ 3--3711 0L.-do Counov.

~ ...- NWl' "IE" __ 28. T 35 N" II 15W.... btId;o .... .." 0 0 0 0....... _ .. Int<n..uH.._".I",;lOUthol 3--75-76 0~.~CDunov.. ...- SIn $WIl. -. II. T.35 "1 .• 11. 15W~ .1II\dvI .... .." 21 '" ~> 0 0 0_tv ............ "';_"Sir""II..a. Udod< 3--376 U. "" "..,... 6-2.·16 0

g.I8-16 0 ~0

00 "'" 1_.".nt< "'at a.. """"" ..oro rna du""ll_ "'.... Manv 0Il1011 .....a;lobll i~ filet of",_ u.s. Gaol...... Suo_ II Rolli. Mo.

il'"•'"•11


SEEPAGE RUNS

A new sewage-treatment plant forLebanon began operation in February1976, in the upper reaches of the basin.The plant, with an average discharge ofabout 1.1 mgd (million gallons per day),replaced two faciJities active for someyears on Dry Auglaize Creek andGoodwin Hollow (fig. 24). In the projectarea, this reach of Dry Auglaize Creek isthe only place where urban effects onstreamflow are significant. Because ofvariable discharges from the sewagetreatment plant, frequency estimatescould not be shown for several stationsin the upper reaches of Dry AuglaizeCreek (table 6).

Most of the seepage-run data werecollected during periods of minimumstreamflow 10 the summer and fall, butdata collected in the winter and spring(during periods when there is no stormrunoff) can supply valuable informationabout areas of significant water loss innormally dry channels. In many cases,streams that lose flow to bedrock willstill be dry during the winter and spring"wet" seasons, whereas streams that are

Data from seepage runs are amongthe best sources of informationconcerning magnitude and distribution oflow flows and anomalies within andamong stream basins. If several flowmeasurements are made at seepage-runsites during the course of aninvestigation, the data can also be usedto estimate low-flow frequency characteristics at those sites (plate 13).Seepage runs in small areas (figs. 25 to28) are of special interest, because datacollected from them can be used instudying the interrelation betweengroundwater and surface water.

o

o

o

•

o

o

,

o

o

000

I I I I I I I I I I I I ~ I I I I I

o

o

• l!j I I I •• I I I I HI. II

!u

•I •

;i

til'':!..• Ii E.-

I•~

86

Plate 13. Taking stream-flow measurements along Mill Creek, sec. 36, T. 37 N., R. 15 W., CamdenCounty, as part of a seepage run to detennine stream losses or gains. Photograph by JamesE. Vandike.

normally dry during hot, rainless periodsof high evapotranspiration will beflowing. Discharge measurements in theflowing reaches can pinpoint zones ofwater loss that would be otherwiseunnotedj these zones can be related togeologic and structural features,vegetation, topography and slope, andgroundwater levels.

Conclusions based on seepage-rundata are as follows:

l. Big Spring, near Morgan (fig. 23),contributes about 60 percent of theflow of Osage Fork during Jow baseflow conditions and about 40 percentduring high base-flow conditions.

2. Bennett Spring, at Bennett SpringState Park (fig. 22), contributesabout 60 percent of the flow of theNiangua River during low base-flowconditions and about 50 percentduring high base-flow conditions.

3. The Osage Fork basin contains moretributaries with base flow duringmost of the year than either theNiangua River or Grandglaize Creekbasins, The greater numbe"r of drytributaries in the latter two suggeststhat more of the precipitation fallingin these basins is stored, to bedischarged later and at a moreuniform rate from the several largesprings along the main stems.

87


,,."'-

110.1 1,_ U.S. G+oIotkal Su....y1'62,500 quad.afl4ln.

EltPL.AHATIOH

;.,.......~ .... .."..,-u../io \wMnl.howRlll _, R_bw./ I..F~ 22. a.... Tab" 6.

-¥i, 0lM. II....... II dIIdoot9Il1cubkfMt,.._.

I .5 0 I Wills",,,'11.1,1,0,1 0 '

t 5 0 IK......*l

Figure 25, Seepage-run measurements in the upper Niangua River basin, November 11·12, 1975,

88

Surface Water

~I

Ell.PLANATIOH

*0..... 1119 olio, Uppof " ...,,",(..h.,••~,,"ll. mop ftum",f,om Fill"" zt o"d Tobl. 6.O'h., "umb., II dllc~'Il' I"cub1c 1.11 PO' l.cO!lCl

I ,~o I lIliltl""U""~','''A~'''I.,\~I_,=,'

I !i 0 i ~Ilamo''''

r".

",--...

<'

I"••!....~.,

~__&/ .J!.

I!"*IO"V ..r~.

)

___ _ _ ~- CoIIn.!! _

Dalla. eov." I Loclodo Coull!)

I

II

II

----,/

I

J

Figure 26. Seepage-run measurements in the lower Niangua River basin, August 25-26, 1976.

89


Ell:PLIoHATIOH

_ ..... Ille.~. """'"~._~I~_".......t>..

m.. ",w.. 2.! 'filii lob" 6Otl.,....._ I. dlKlloft4 100culllcfwl __

'c..,~...., ..tr./h!,,\l.j...ff---,-'=,' .....1.5 0 I~

I ... ".oo U.I. _,1<.1 50.... "61,~OO .~•• ,••,lo.

Figure 27. Seepage-run measurements in the Steins Creek basin, July 2, 1976,

90

Surface Water

/r...~

ji{I

"'--'"

..///

......,//"

//'

'.0

0.40 1.40

.~

r..··llovtJ-.ot,1/ 1/......... I..\

\

.--r./ /... /

·'iP'-'~I'..-,"".'r,tl---~--'·i'-,~-_--.J! ..I ...." 0 1 I .110.......

[KP\.A.NATION

~ Mtoturlno tile. N~IIl"r I.tl~1.&0 In cubk IM!,...-.d,

o

"OTES:

"-.••

!

1J .. _..,t;~od ''('';.-I,.O..._.t CoMIC'" 0............ -by _ l. 0.0- 10< ._I"•• ~.... ,,_ ot~_ .......__'''CoM,C'''_.,

'I!_io_'_'''~I ...... _.2.,31It'''''l'-'__"'__ """_.tW"O~.. c..ol<_~_'"""___ SoorinI·

'I_....... O I.3 t __ _ ...

_JO.lt7e.IOo _' ""' _ ......_....._.IDlrioo"......,t"ro-_ .. "'.__ t... _ .. _

_ to.2"o.liftlhl"eo.-~ ........ _01___ 1I__ o--r,~100__ 100011____... C.... ~,_lo",,___....-........-....-.

."""

Figure 28. Seepage-run measurements in the Coons Creek basin, April 1, 1976.

91


Stream name Tributary Known springs Contributions along Total flowcontribution contribution main stem (percent)

(percent! (percent!

Hi!ll base flow, June 1975

Osage Fork 27 36 37 100Niangua Riller 8 62 30 100

Low base flow, August 1976

Osage Fork 11 61 28 100Niangua River 4 68 28 100

4. The tributaries contribute only asmall proportion of the total baseflows of the main stems; most of thewater is contributed along the valleysby springs. The preceding tableshows the proportions of total flowscontributed by tributaries, knownsprings, upwelling of groundwater inthe bed of the streams, groundwaterdischarge from any alluvial fillsbordering streams, and along themain stems by small springs thathave not been inventoried. Flow andincrements of groundwater dischargeare much better sustained along theNiangua River than along the OsageFork, because, in the case of theformer, more precipitation is stored,to be discharged at a more even ratethroughout the year.

.5. Streams draining the Jefferson CityDolomite often lose their flowshortly after reaching the RoubidouxFormation. Once the zone ofsaturation has been intersected bythe stream valleys, however, largerbase flows can be expected [rom theRoubidoux Formation than from theJefferson Ci ty and Cotter Dolomites,because the Roubidoux is topographically lower and has greaterstorage capacity.

6. Discharges of principal streamsincrease markedly when they enter

92

the Gasconade Dolomite i [ the zoneof saturation intersects the valleys.In a few places where streams crossthe formation, however, there is flowonly after heavy rains.

CLI\5SIFICATION AND DESCRIPTIONOf STREAMS

On the basis of continuity of flow(fig. 29), streams in the project area andin other areas of carbonate-rock terranecan be divided into four types:

Type I streams are characterized asgaining from headwaters to mouth; thisdoes not imply, however, that they willflow continuously during the year.Evapotranspiration may deplete thewater in storage, so that none is left forstreamflow, but groundwater levels willbe shallow beneath the valley; BroadusBranch in the Niangua basin is anexample. Two reaches along the OsageFork and one on the lower Niangua Riverhave small decreases in flow at lowstages. Decreases are small comparedto total flows, however, and areconsidered diversions through bedrockchannels to downstream points ofdischarge; for this reason, the two riversare classified Type 1.

Type 2 streams have low water levelsthroughout their Jengths and generally do

Surface Water

Type No. Stream Narrw Basin

NianguaNianguaWet GlaizeNianguaNianguaNianguaNianguawet Gla;ze

NianguaNianguaWet GlaizeOsage ForkWet GlaizeNianguaWet GlaizeWet GtaizeOsage Fork

Osage ForkOsage ForkWet GlaizeWet GlaizeOsage ForkOsage ForkOsage ForkOsage ForkOsage ForkOsage ForkOsage ForkNianguaNianguaNianguaNianguaNianguaNianguaWet GlaizeWet GlaizeNianguaNianguaNianguaOsage ForkOsage ForkOsage ForkGasconadeWet GlaizeOsage Fork

NianguaOsage ForkNianguaNianguaNiangua

Jones CreekBennett Spring CreekDry Auglaize CreekSteins CreekConns CreekEast Fork Niangua RiverGoodwin HollowDeberry CreekParks Creek

Brush CreekCentrell CreekGarman HollowWet Glaize CreekPanther CreekHyde CreekBowen Creeklittle Bowen CreekNorth Cobb CreekCobb CreekLittle Cobb CreekDousinbury CreekMill Creek - NianguaJak.es CreekHalsey HollowDurington CreekIndian CreekDeane CreekMill CreekGreasy CreekBanks CreekSpencer CreekMyers BranchSmith BranchCore CreekBear CreekMurphy CreekMill Creek

West Fork Niangua RiverOsage ForkBroadus BranchJugtown HollowNiangua River

Mountain CreekFour Mile CreekBarnett HollowCave CreekWoolsey CreekHawk Pond CreekGivins BranchTraw Hollow

2.

4.

Up~nd Surface

3.

1.

GAIN

~",,",:~~:;;':G~,~.~unctwot.r L....I

'-s'reOM Bed

LOSS

..............~GA1N

~.

I.

3.

2.

Figure 29. Flow patterns of streams based on continuity of flow.

93


not flow in any reach except after heavyrainsj Mountain Creek in the NianguaRiver basin is an example.

Type 3 streams are characterized byan upstream gaining reach followed by alosing reach, a pattern that may berepeated several times in some streams.For example, Dry Auglaize Creek hasfour gaining reaches alternating withfour losing reaches. The lengths of eachsegment in a particular stream vary, sothat the upstream gaining reach mayextend far downstream or for only ashort distance.

Most of the streams are Type 4, inwhich the upper part of the basin is alosing reach followed by a gaining reach.The upper part is considered a rechargearea, and the zone of saturation is belowthe stream channel, which is dry exceptafter rain. At some point downstream,the zone of saturation intersects thelevel of the flood plain and flow begins.As in Type 3 streams, the pattern maybe repeated several times. Because ofthe potential of unsaturated storage inthe flood plain of a receiving stream,surface flow may disappear when smalltributary streams reach the flood plainof the receiving stream.

WATER QUALITY OF STREAMS ANDSPRINGS

A good understanding of movementof water through the flow system ofcarbonate rocks aids in identifyingsources of pollution and areas wherewells, springs, and streams may beaffected; hence, dye traces, seepageruns, geologic mapping, and water-levelcontouring contribute to the interpretation of water-quality data anddetermination of sites where repetitivesampling would be useful to verifyanomalous values.

94

All water in the system, whether wellwater, springflow, or streamflow, is ofthe calcium-magnesium-bicarbonatetype. Sodium, potassium, sulfates, andchlorides are present in small amounts.During a base-flow period, bacterialcounts were measured and chemicalquality samples taken at seven springsand nine streamflow si tes (fig. 30 andtable 7).

Fecal coliform and fecal streptococcus counts for springs were lowerthan those for streams, but counts forboth springs and streams were notinordinately high. The moderately highcounts for Dry Auglaize Creek, nearSleeper, are due to effluent, whichaccounts for most of the flow, from thesewage-treatment plant at Lebanon. Ashort distance downstream from thesampling point, the creek goesunderground and the water reappears inSweet Blue and Hahatonka Springs(Skelton and Miller, 1979). Dilution bygroundwater and bacteria die-off reducethe concentration in the springflow, sothat counts are no higher than those ofother sampled area springs.

It is difficult to account for thepollution of Dry Auglaize Creek atToronto (fig. 30, map no. 15), as fewpeople live in the valley or on theadjacent uplands, and the stream beginsto flow only about 3.5 mi upstream. Apossible source is an area near Montreal,about 4 mi southwest of the site, whichcontains a rather unusual cluster ofbroad sinkholes, where a number offamilies operate turkey farms. Thecluster is unusual, because few sinksoccur within miles of this locality.Wastes from septic tanks and turkeyfarms can be carried down through thesinkholes, but northwest-trending faultssuggest a more likely route, parallel tothe fault system. On the other hand, if anortheast-oriented system of intense

&ffalo

\

\.--;:;:::;

RiV61'

5

/

8 Roder

Surface Water

---- 36°00'00"

Note: Structure from Flllur. II.

10 a 10 MUe.l~I--'--'-t'T''r+'r~~'h'-'rll-------,,----"11111 1111 I

10 a 10 Kilometers

EXPLANATION

,'" SprlnlJ lampllng ,It, (numbers 1-7)

.,. Stream sampllnlililte (numbers 8-16)

.... from U,S. Geoloolcol Survey state bOH mop, 1'500.000.

@ Sinkhole aru

\...- Foult

Figure 30. Water-quality sampling sites for streams and springs.

95

'"-<0'"TABLE 7 0....0

Water-quality data for springs and streams "(data in milligrams per liter except as indicated)-<0~-- s___

"'. -- - ,_,'''''' ... lli_. 0--- ... ... ,.. ..~ """ ,.. ... n:>

lilt- 301 -- tttJ"'l .- "'"1__1

"000,' '00,' "- -.. - -- •., - m_'"•• l!o"C.l '01 '" '~I "'" \aDlI1 00 ••11 ""00 _, '"0, Lan. 5<><.... "25-17 " '" " " ", , ,... ,... " " ,... , • z:>, crill Son"t Inn " .., '" " ~

, .. .. .. ~ ,.. ," -<, BlwHoIoSc><..., "23-77 ,.

"" " " "",

." .. " " ,... • " '"" "

-<""""$<1<,... • 2'17~ '" " " ~ , u ... v " ,." '",

~ .....• :loin " ." " " '"

," '" .. " 1.1)7 • ~ '"'"• s.-, 81... SlH'..., • 2. 77 " ." '" ,." ""

, .. " .. " 1.07 " • :>,Hoh'l""~' Sp,I,. 8-2)-77 ~ "" " " "" • " ... " " 1.03 "

Z

'"• o..q. f ... ~ nU' .2577 " In " .. '", .. ... " " '.00 ~ ",

0.', 01.1I9O f"'k "".. 8U·n .. ", " ,.. '00 ," ... " " '" '" "O'VAllb

'. ~lonQ<J' A,,,", Mar Bn·n 20 VI ~. ,.. ,.. ,'" ." " " ... .. '"'_m

" ffi ..... R"...... 82!H7 " "" " .. ~, , ... ~ " ~ I.Gl .. ""8uH....

" ""..... R_ •• ':M 11 ", n. ~ .. '",

" ~ " " '00 ,'",-

" Mol.e... ",..... "2' 77 " '" '" .., "'", >- • .,

" ,... m '"" o.............C_ 82'·77 U "" ~ •• ~ ,

" .. .. '" U, ~ ,....m_'

" o.v .......,.e-. ."" ., n• '" •• m , ... ~ " " ,.. ,m ,m.. I",.....

" WIll G/....e- .. ." n '" '" ". .. ,.. ," m .. ~ ,.,

'''' ...-' Artoc\lOdb<t_"'.... _U.._,lltooo.

jointing intersected the fault zone, sucha cluster of sinkholes could develop andunderground drainage could be directedto the site. At present (1978), thesource of the pollution is unknown, butrepetitive sampling and selection ofadditional sites on Dry Auglaize Creekshould help identify it.

Bacterial counts in the Niangua andOsage Fork basins are highest in theupstream reaches and decline down-stream. Because of the largecontribution of groundwater fromBennett, Sweet Blue, and other springs inthis reach, the decline is greatest on theNiangua River, between Buffalo (fig. 30,map no. 11) and Tunas (fig. 30, map no.12). Similarly, the counts are reduceddownstream on Osage Fork (fig. 30, nos.8 and 9), but not to the degree that theyare along the Niangua River.

Even scant water-quality data canprovide clues to sources of pollution in

Surface Water

the hydrologic system. For example,when springflow which normally containsa phosphorous content of 0.01 to 0.02mgl (milligrams per liter) carries small,though abnormally high, amounts ofphosphorus, it may be due to capture ofwaste-laden streamflQw. On August 24,1977, Sweet Blue Spring had an unusuallyhigh phosphorus content (0.12 mgl)j onAugust 23, 1977, Hahatonka Spring, asmaller, though stHI unusually high,content (0.06 mgl) (plate 14). It shouldbe noted that the norm for streams wasabout four times that for springs. A dyestudy (see GroWldwater Tracing) showedthat the flow lost from Dry AuglaizeCreek, downstream from the Lebanonsewage-treatment plant, reappeared inthe two springs; therefore, the highphosphorus content may indicate thepresence of treatment-plant effluent.Since Hahatonka Spring has a greaterflow than Sweet Blue Spring, dilutionprobably accounts for the smallerphosphorus content in Hahatonka Spring.

Plate 14A. Hahatonka Spring. Water issues from an opening at the base of the Eminence Dolomitebluff behind the gravel bar shown in the center of the photo. The water from this springhas slightly higher than normal phosphorous concentrations. Photograph by James E.Vandike.

97


B

cPlate 14. 146 is a view of Sweet Blue Spring. Water from this spring had hi~er concentrations of

phosphorous than Hahatonka Spring, due to less total dilution of the pollutant fromincreased discharge. The dye trace mentioned on page 99 showed dye emerging from thesetwo springs. 14C is an aerial view of Sweet Blue Springs, showing its relation to the NianguaRiver (view toward southwest, with Niangua River on right and the spring just left of thebridge). Photographs by James E. Vandike.

9B

Groundwater-Surface-Water Relationships

GROUNDWATER-SURfACE-WATERRELATIONSHIPS

FACTORS AFFECTING RELATIONSHIPS

In Ozark basins, a number of relatedfactors variably affect groundwatersurface-water relationships:

1. How saturated is the system? Antecedent conditions must be consideredduring any study of groundwatersurface-water relationships. Climatic extremes before an investigationmay significantly alter hydrologicconditions and influence conclusions;this is a temporal factor.

2. How open is the system? Rockfracturing and subsequent solutioncan range from negligible to intense.The difference in altitude betweenthe point of loss and the point ofresurgence and their proximity toeach other are factors that alsoinfluence the rate of solution and theresulting volume of storage.

3. How soluble are the rocks? Becauseof variable lithology, this is adifficult factor to evaluate.Brittleness and solubility determinethe development of secondary permeability.

4. How large is the system? The areacontributing flow to the point of lossmay be large, contributing more tothe loss area than it can take, exceptin dry weather. On the other hand.the contributing area may berelatively small compared to the lossarea, so that aU flows, except thoseresulting from intense storms, can beaccommodated.

5. What part of the basin is involved?The geographical position of the lossarea within a basin may also besignificant, i.e., whether it is locatednear the headwaters, midway to the

mouth, or near the mouth, a factordirectly related to altitude andproximity of contributing andreceiving areas (item 2 in this list).tn general, the greatest depths to thewater table have been observed inthe upper and middle reaches oflosing Ozark streams. In the projectarea, water levels are as much as 70to 100 it below flood plain along theupper parts of Steins and DryAuglaize Creeks, and 10 to 20 itbelow it along their lower reaches.In Ozark locations outside the projectarea, water levels may be as much as250 ft below flood plain.

To study these factors, application ofthe methods described below wasinvestigated. Following these descriptions, results of the studies of several ofthe basins in the project area arepresented.

GROUNDWATER TRACING

The use of fluorescent dyes tocompute travel times and observedispersion patterns in surface streams iswell-established, dependable, and useful(Wilson, 1968). For the current study,however, the relationship betweensurface water and groundwater wasemphasized, especially in basins wheresurface flow is lost.

Groundwater tracing experimentsusing rhodamine WT dye (20-percentsolution) were made in the Dry AuglaizeCreek basin from May 1976 to April1977. The results of these experimentsare described in a paper by Skelton andMiller (l979); a brief summary of theirfindings is presented herein in order toevaluate the usefulness of groundwatertracing.

99


The location of the dye-injectionsite, dye-sampling sites, and thedirection of underground dye movementare shown in figure 31 and plate 15. Thedye was injected into Dry AuglaizeCreek at site 1, where most streamflowduring rainless periods consists ofoutflow from the Lebanon sew~ge

treatment plant (approximately 2 ftJ(s).Between si tes I and 2, the flowdisappears into the streambed, resurging

in two large springs (sites 4 and 5,fig. 31) in the Niangua River basin.

The following is some of theinformation obtained from the dye study:

1. The upper Dry Auglaize Creek basinis one of the sources of recharge toSweet Blue and Hahatonka Springs inthe Niangua River basin.

Plate 15. Charcoal packets ("bugs") being collected and replaced at Ozark Fisheries spring, sec. 25,T. 37 N., R. 15 W., Ccrnden County, as part of a dye trace of groundwater movementdiscussed on page 99 (Dye sampling site ,*8). Photograph by Jcrnes E. Vandike.

100

Not.: For control purposes,Orynob site 12 w(]s located on Big

Piney River, 19 mile' eastof lIte II.

EXPLANATION

1::1.1

Dye-Injection site and number

1;.2 Dye-sampling slle and number

• New treatment-plont site

IliI Old treatment-plont sit.

~ SprlnQ

""'~ DIrection of dye movement

Grou nd water-Su rface-Water Rela t ionsh ips

IPulaski County

+-_-f_Loclede County -LWright County

Grof1dg!o;zeJ.--......Creek-

6

_Camdenton

Conway

-Niangua

Lake of ,,,. 010'''~93°00'00"

38000'00"-+

I Suffaloe

Camden Coun'y

~,;;;C",oI,

I

Marshfield.

I

In--- +~..,......J.'- --=-'V"'I"=Ll-

IWebster County

_---..J

II

1

~ a 10 Mile,

WilLLL.tI.rI'I-I/TI+1"I~rllTl, 1----'1.----"10 0 10 Kilometers

o Stream-goglng station

.. from U.S. Geologlcol Survey stote bose map. 1:500,000. From Skelton and Miller, 1978.

Figure 31. Location of dye-injection site. dye-sampling sites, and direction of dye movement.

101


2. The underground travel rate, basedon straight-line distance from dyeinjection point to resurgence points,was approximately 0.4 to 0.6 mild.

3. Geologic structure appears to controldirection and rate of groundwatermovement.

4. Studies of groundwater levels,streamflow patterns, and geology areinsufficient to define resurgences oflosing streams in carbonate rocks;they only indicate possible areas ofresurgence.

5. Late fall and winter particularlyfavor successful groundwater tracingexperiments using rhodamine WT dye,because background fluorescence isthen lower and more stable.

VEGETATIVE INDICATORS OF HYDROLOGIC CHARACTERISTICS

Study of the relationships betweenhydrology and bottomland vegetation inthe project area (Harvey and Skelton,1978) has shown that identification ofplants and plant assemblages is helpful inthe study of carbonate hydrology. Thefollowing are some of the conclusionsreached during the study:

1. Plant assemblages indicate gainingand losing conditions in Ozark streamvalleys.

2. A change from one plant assemblageto another in a stream valley notrecently altered or cleared,especially if the change is abrupt,suggests a marked change in depth tothe saturated zone.

3. Plant assemblages indicative ofdiffering hydrologic conditions can beused in any season (but not as readilyin winter> to help evaluate low-flowcharacteristics of streams and

102

groundwater-surface-water relationships.

Vegetation is most helpful incarbonate hydrology studies when used inconjunction with other information, suchas groundwater levels, geology andstructure, and seepage-run data.Vegetation, however, can beindependently useful in defining areas ofabrupt hydrologic changes.

ANALYSES OF GROUNDWATERLEVELS AND FLOW PATTERNS

The top of the saturated zone is aconcave surface extending from thedivide on either side of a basin to astream and sloping downstream fromheadwaters to the mouth. Surface flowusually begins at places where thissurface intersects tributary streams, atvarious distances upstream from theirmouths.

Stream profiles, using groundwaterlevels, streamflow data, and topographicand geologic information are useful instudying the relationship of groundwaterto surface water. The profiles in figure32 illustrate the groundwater-surfacewater relationships and complement thepotentiometric map (fig. 13, in pocket).

In constructing profiles, water-leveldata were generally obtained from wellswithin a mile of the stream. In somecases where control could not beestablished near the stream, water levelswere projected I or 2 mi from theuplands, resulting in a water-levelprofile probably somewhat higher ingaining reaches of the stream than theactual water level in the valley. Inreaches of abnormally low water levels,almost all wells used were within a mileof the stream.

Groundwater-Surrace-Water Relationships

Dry Auglalze Creek-Goodwin HollowNiangua River

Goodwin Hollow and Dry AuglaizeCreek (type 3, fig. 29) are generally dryalong most of their lengths and have themost extensive reaches of lowgroundwater levels in the area (fig. 32).Both streams flow only after intenseraif'.lstorms; they cease flowing within afew hours to a day or two. In dryweather, pools of water are morecommon along Dry Auglaize Creek thanalong Goodwin Hollow, indicating a moreopen underground drainage system -in theGoodwin Hollow basin (plate 16).

Further proof of the greaterinfiltration capacity of Goodwin Hollowwas obtained on March 31 and June 22,1977. Following a rainstorm on March28 and 29, in which 2 to 3 In. of rain fellin the area, landowners reported thatDry Auglaize Creek stopped flowing byMarch 30. However, a field reconnaissance for high-water marks showedthat Goodwin Hollow had not flowed atall in the reach from mile 45 to thejunction with Dry Auglaize Creek atmile 29, although there had been someflow in the creek upstream from mile 45.High-water marks indicated that rises of1 to 2.5 ft occurred along Dry Aug1aizethroughout its length. In addition, alltributaries entering Dry Auglaize Creekfrom the east, between the mouth ofGoodwin Hollow at mile 29 and mile 14,had trash lines and small flows or poolsin their channelsj those entering fromthe west, however, were dry, with nopools or trash lines. The undergrounddrainage system of Goodwin Hollow andwestern tributaries of Dry AugtaizeCreek wi11 accept more storm runoffthan Dry Auglaize Creek and its easterntr ibutar ies.

Osage Fork-Niangua River

The Osage Fork and Niangua Riverare perennial streams (type 1, fig. 29)for most of their lengths (fig. 32).Except for several short reaches,average groundwater levels stand aboveflood plain in each basin. Nowhere inthe Osage Fork basin are groundwaterlevels more than 20 ft below flood plain,and in virtually the whole Niangua basin,water levels are above flood plain.

In the Osage Fork basin, water levelsare at shallow depth below flood plain, inthe reach from about mile 35 to mile 48,where Big Spring, the largest in thebasin, is located. This suggests thatthere has been karst development, andthat the wells supplying data may havebeen drilled into bedding planes orfractures filled with water having alower head than that in the stream.During the drought of the mid-1950's, a2-mi reach of Osage Fork upstream fromBig Spring had no surface flow.Furthermore, as shown in figure 32,there is some decrease in surface flow ina lO-mi reach just downstream from BigSpring during years when base flows arenormal. Thus, this reach of the OsageFork, though perennial, does not conformto the pattern of continuous pickup alongthe rest of the main stem.

As noted by Harvey and Skelton(1978), the Osage Fork and NianguaRiver have similar vegetative patternsindicative of perennial flow conditions inOzark streams. In the headwater areas,sandbar willow (Salix interior), Ward(Ward's) willow (So caroliniana), stiffwillow (So rigida), sedges and rushes,watercress (Nasturtium officianale), andtouch-me-nots (Impatiens spp.) graduallydisappear and are replaced downstreamby tall black willows <S. nigro), boxelders, maples, sycamores, ashes, andelms.

More conclusivefollowing heavy rains of

observations,3.5 to 6 in. on

103


·• ·i. •0 r • .;• • •""" < ! • •• • • •~.

B

•., • " ; •• i v • ,~ i 3 3~oo ~ .I J i

"'00

'.

0000 • ·t. 0 I I

• Upland Su.faee'. - , .-Flood Ploln -_':._- ___ =_iC

~800 -.·Pol,nllo,...I,le Su.foe, >0- -~"

'.

o3070 60 50 40Mil" up,lreo... f.om lI'IO\I111NIANGUA RIVER

8090

600 Olttl>org,,' Aug, 24 -26, 1976. Ground_oil, In,l, , 1976 - 1977

"0

•N•

•20

o

"

>0

''''"•

30

•

!

"

"

L..Jn""H eo... JI'd_lopment---'.1"!,

."20"30

lit

6O~504540

Mil" uPllreo... f.OM moult>OSAGE FOflK

"

..

Mile, uPlI.-o... 1.__IIIGOODWIN HOLLOW - DRY A!JGLAIZE CREEK

23-261976. Ground_'-...~,I, 1976-1977.

•, ~.•~5••• -j.!l

1Il~~•

11l f Ill~! jr,j ~r ••

••

Ir

~C:I::I'1c Su'Ioe,V-·_~t~_:::'i----:::.=.ttr~t;;;f'f;;iu~":."'~~:'~'r":·~\'I 0 !' _ ,J.

Aug 19-20,1976 Gtou~l... ""'11 1976-

800

800 Ol'thO. , A

80 "

'000

''''''

1400

"00

Figure 32. Profiles of streams showing relation between groundwater levels. streamflow. and faults.

104

Groundwater·Surface·Water Relationships

''''''

CJCJ

I

EXPLANATION

•Ground"oli' 1'.'ls Nlo," flood ploln •

G,O.. oo..Oltr ...el, above flood plain *Well. Heo~y lin. ,heM, d'pth 01well•.

Faull. A"o.... thow dlftcllon of mo••menl

.-upland Surlac.

600 Olscha, II' May 2~, 1976. Gtound....1et 1...1.' Summer 1977. 600 Olscho,g..' No•. 6.197~. Groundwater leYel., 1976.

20 15 10 !5 0 I 10 !5Mil.. up,lflam from fnO\Olh

NORTH CoeB CREEIC

'000

800PotentiometricSu.fac:.

,..,Plgln

BEAR CREEK

800

o

--_~_ .....UPlond Surlan,,FloodPlain

000

Uplond Surfon

"00,

-, -,Pol.nllomlol'lc} --- 0, , .

"'1" •'"" - "

"S..,Ia.e.

0000

'600

'000

j•

,'0

800 OlsthorQu: No.6, 1915 GroundWOI,. 1,.,1" 1976

"o800 Dilello.",.., J..,y 2, 1976. G,oundwot•• 1.....1" Summt. 1977.

20 151041,-. "PII"om f,om mol,llh

STEINS CREEK PARKS CREEK

Figure 321continuedl

105


Plate 16.16A is a view of Dry Auglaize Creek, sec. 22,T. 37 N., R. 16 W., Camden County, showingdry creekbed and pools remaining from arecent rain. 16B shows poor sorting of gravelsin the streambank along Dry Auglaize Creekat this site; angular chert fragments indicatelittle rounding by stream action (pencil nearcenter of photo indicates scale). 16C is anaerial view of Goodwin Hollow, showingabsence of pool s. Photographs by James E.Vandike.

106

A

c

June Ig to 22, 1977, confirmed the largedifference in infiltration capacity ofGoodwin Hollow and Dry AuglaizeCreek. Data from a number ofmunicipal and private rain gages in theLebanon area showed that the heavyrainfall was general in the two basins(fig. 33). Goodwin Hollow and DryAuglaize Creek flowed along their entirelengths, and rises on the two streamswere commensurate, ranging from 3 to 5ft. Peak flows had passed by the timeflow conditions were observed in the twostreams on the morning of June 22.Measurements of flow and site locationsare shown in figure 33.

The volume of storm runofftransmitted to underground storage wasmuch greater in Goodwin Hollow than inDry Auglaize Creek. Furthermore, thetributaries entering Dry Auglaize Creek,downstream from the mouth of GoodwinHollow, had not flowed, and theyrevealed the same relationship theyshowed after the March rain. BothGoodwin Hollow and Dry Auglaize Creekare therefore losing streams. GoodwinHollow, however, is more deficient inflow than Dry Auglaize, and the streamreaches and tributaries nearest to theNiangua River have the largestinfiltration capacities.

An underground dye trace during thisproject (Skelton and MUler. 1979) hasshown that the Niangua River isreceiving flow from the upper reaches ofDry Auglaize Creek. Earlier dye studiesreported by Vineyard and Feder (1974)and Dean and others (969) revealed thatGoodwin Hollow is also hydraulicallyconnected to the Niangua basin; thus,interbasin stream piracy has been wellestablished.

Harvey and Skel ton (I978) observedthat the vegetative patterns in GoodwinHollow and Dry Auglaize Creek aretypical of those in losing Ozark streams.

Groundwater-Surface·Water Relationships

Plants prominent in perennial streambasins occur only sporadically; these arefound in the few reaches wheregroundwater levels are shallow andstreamflow is perennial, or occasionallyat the base of bluffs along dry streams.In such cases, however, the variety,abundance, and continuity of waterloving plants are lacking, and a stronglylocalized water-saturated conditionseems ·to be indicated.

Bear Creek

As shown in figure 32, Bear Creek(type 4, fig. 29) has two dry and two wetreaches. The upper dry reach extendsfrom the headwaters to about mile 10.5.Near this point, surface flow begins andextends downstream to about mile 7.5.From this point to mile 4.0 the stream isdry (plate 17). The downstream reachfrom mile 4.0 to the mouth has a shallowgroundwater level, and there is usuallysome surface flow in the reach.

The lengths of the four reaches varywith the season and weather. In dryweather the wet reaches shortenconsiderably and the dry reacheslengthen, but the wet reaches alwayshave at least a trickle of flow in them.

Groundwater levels in the two dryreaches stand below the level of thestream channel; in the gaining reachesthey stand at or above it. There is thesame relationship along Dry AuglaizeCreek and Goodwin Hollow.

In the reaches of Bear Creek wherethere is no surface flow and water levelsstand at some depth below flood plain,water that leaves the stream moves outof the basin to the Gasconade River.This was demonstrated when dye wasinjected at Bechtel's Ford in 1977 andrecovered in Cliff Spring (plate 18 andfi~. 21). Downstream from mile 7.5

107


".'.•Ca••

92°4!l'OO"

370 4!l'OO"-+ i 2.

'''x6.0", II

•.6bL.bonon

13.EXPLANATION

StreomfJo. IMOlllr1ft9 11M. NllmbetIndicates flow 11'1 Cllbk: feet per .econd.

RolnfolllMOllUrlng IHe. Nllmbet Indlcot..rall'lfollll'l Inche. dllrlft9 period Jl,ine 1822, 1977.

Note: An .treamflow !MOIllrem.,,"mode Oft MOrnlftt af Jllne 22, 1977.

Bo.. 'rom U.S. Geological SlIr..,1:250.000 qllodroftCJleL

o !l 10MI~sI----.,--L'-r, .J,o !l 10 Kllo"'eter.

Gray. "",I..10 ",Ue. sou'" of Lebanon

Figure 33. Streamflow patterns in Goodwin Hollow and Dry Auglaize Creek following heavy rainfall.

108

Grou ndwater-Su rface-Water Relationsh ips

A

Plate 17.17A is a downstream view along a dry reach ofBear Creek, sec. 5, T. 35 N., R. 14 W., LacledeCounty, downstream from Bectels Ford. 17Bshows sorting (or lack thereof) of gravels instreambank just left of view in 17A. Photographs by James E. Vandike.

B

109


A

B

Plate 18. 18A is a view of Bectels Ford on Bear Creek, sec. 7, T. 35 N., R. 14 W., Laclede County.Dye placed in the stream at this point was lost to subsurface flow a short distance down·stream and emerged at Cliff Spring, sec. 9, T. 35 N., R. 14 W., Laclede County. Flow fromthe spring shown in 18B depends almost entirely on flow in Bear Creek, at Bectels Ford.Photographs by James E. Vandike.

(fig. 32), there is a steep gradient in thegroundwater level. In effect, thereexists a large depression in the waterlevel profile, extending to the gainingreach that begins about 4 mi upstreamfrom the mouth.

"0

Willows and other water-lovingvegetation are scattered along the dryreaches of Bear Creek. They do notbecome prominent until perennialgroundwater discharge and shallow waterlevels occur. The gaining reaches of the

stream have a diversified suite ofabundant water-loving plants; the losingreaches, on the other hand, have lessvariety and abundance.

North Cobb Creek

The longitudinal profile of thealtitudes of the upland, flood plain, andaverage groundwater level in North CobbCreek basin (fig. 32) shows that about6 mi upstream from the mouth,groundwater levels begin to stand abovethe stream profile. At this point thestream (type 4) becomes perennial asshown by the flow measurements(fig. 32). Water levels always standclose to the ground surface even thoughevaporation depletes the groundwaterinflow, 50 that in late summer the flowmay be reduced to a trickle betweenpools.

Upstream from the point whereperennial flow begins, there is a markedchange in stream gradient, and thestream profile and groundwater profilediverge toward the divide, with anincrease in the available volume ofstorage between the upland surfaces andthe zone of saturation. In a large part ofthe upstream section of the basin, theRoubidoux Formation underlies thesurface (fig. 4, in pocket). Here theJefferson City Dolomite has been erodedaway, sinkholes are common, and therock and soil sections of the entireRoubidoux outcrop area are conducive toinfiltration and storage of precipitation.

Within the reach where the streamgradient steepens downstream, waterloving plants become more prominent.Between this point and the mouth of thestream, no stream losses occur as theflow gradUally increases to the mouth.Thus, groundwater levels, streamflow;topography, and vegetation combine todefine the low-flow characteristics of

Groundwater·Surface-Water Relationships

the stream. Vegetation upstream usuallydoes not include water-loving types, butsmall colonies of willows and sedges mayexist where the stream runs along thebase of bluffs.

Steins Creek-Parks Creek

Steins Creek, an interrupted stream(type 3, fig. 29) tributary to Osage Fork,is an example of a stream whose lack offlow is probably related to faulting andsolution along a fault system. Twoparallel faults forming a horst cross thebasin midway between the headwatersand the mouth, where the GasconadeDolomite is at the surface (figs. 4 (inpocket) and 32). There is no flow inSteins Creek (except for a trickle in theheadwaters) until it crosses the horst;from there it is perennial until it reachesa point near its confluence with OsageFork.

Parks Creek (type 3), in the adjacentbasin to the west, is somewhat smallerthan Steins Creek, but exhibits similargeology. The base flow of Parks Creek,however, is larger than that of SteinsCreek in the downstream reach (fig. 32),and it is possible that flow from theupstream reach of the latter is beingdiverted to the downstream reach ofParks Creek, along or in the fault blockshown in figure 34, a possibilitysuggested by decreasing groundwaterlevels to the northwest.

An alternative to northwestsubsurface discharge from Steins Creekis northeast discharge to the GasconadeRiver. Groundwater levels also declinetoward the Gasconade basin.Groundwater movement in that directionis possible; in fact, contours on thepotentiometric map {fig. 13, in pocket}suggest discharge in that direction.

A comparison of elevations along thetwo streams also helps to show why

111


-T't-_T;.'>Z N---; T31 N

~ f"0,-o

){(

8a.e from Missouri HI;"wo, Departmentcounty "IQllwoy map., 1'2SO,OOO.

20

1<;

, ~~

~.,\ 6.0

1~

0.0

Nat., 2.S to 3 Inch.. minimum wa.recorded ot Grove Sprlno and Lebanonon March 28~29.1977.

EXPLANATION

Fault

Streamf~ mealurln; lIt•. Number.Indicate flaw In cubic IMt per ..cond.

o 2! 4 Mil••L~'rlfr\ITt-""T...L..--,l.'-,---"----"I II I I I

I 0 2 3 4 Kllam.t.r.

Figure 34. Streamflow in Steins and Parks Creek basins, March 30, 1977.

112

hydrologic conditions in the two basinsmay differ. The II OO-ft elevations ofboth streams are at about the samelatitude, and each stream reaches thedivide at nearly the same elevation0540-1560 ft). Downstream from thedivide, at the latitude where theelevation of Steins Creek is 1300 tt, thatof Parks Creek is about 1230 ft.

The relationship between theseadjacent basins was further studiedfollowing 2.5- to 3-in. rains on March 2829, 1977 (fig. 34). Note that the flowfrom the smaller, Parks Creek basin wasstill somewhat larger than that of SteinsCreek in the lower reaches and that theflow in Steins Creek, even undersaturated conditions, was apparentlyinfluenced by the structural featuresshown in figure 34. Even under differinghydrologic conditions, less flow iscontributed from the upstream part ofSteins Creek basin than from thesmaller, Parks Creek Basin.

The distribution of water-lovingplants and their relation to streamflowand groundwater levels in the SteinsCreek basin have been described byHarvey and Skelton (978). In ParksCreek basin, vegetation patterns similarto those along Steins Creek wereobserved. Plant diversity is limited by~he lack of adequate water in the upperreach of Parks Creek, where flow isintermittent. Near the mouth, whereflow is perennial and water levels areshallow, plants are more diversified.

Similar relationships betweengroundwater levels, streamflows, andvegetation can be anticipated fortributaries not described here. Theobservation of dry-weather flow in themiddle reach of a valley does notpreclude a dry streambed between thatpoint and the mouthj nor does theobservation of a dry streambed in mid-

Groundwater-Surface-Water Relationships

valley preclude a perennial reachupstream. Observation of streamflowcondi tions can be used to predictvariations in groundwater levels in abasinj conversely, observation ofgroundwater levels can be used topredict streamflow characteristics.Vegetation is a key to both. In addition,observation of anomalies in these threeelements may suggest that more detailedgeologic mapping is warranted.

Using all available hydrologic data,the authors classified areas of rechargeand discharge along streams in thethree-basin region, as shown in figure 35.The illustration is a generalizedpresentation intended to show arealdistribution of recharge and discharge; ineffect, it summarizes many of theconclusions presented in the report.

Drainage-Density Analysis

Using a method described by Trainer(1969), drainage densities were computedfor a number of streams in the projectarea and for several Ozark streams inother parts of southern Missouri todetermine the usefulness of the methodas an indicator of low-flowcharacteristics. Trainer1s studies wereuseful in sandstone, shale, andmetamorphic rock terranes in theinvestigation of groundwater dischargeand its relation to the development ofthe drainage network. Figure 36 is aplot of drainage-densi ty values for Ozarkstreams, versus the 7-day median lowflow (7-day Q2). Because of excessivescatter, the data plot in figure 36 did notprove conclusive.

Because of development ofunderground drainage, the drainagedensity-low-flow relationship is not clearin karst terranes such as the Ozarks.Originally a drainage network was

113


EXPLANATtoN

ReCMrte Area

DiKl'Ior98 Area

to 0 10 Wile,L..L'--L...Lj/Y,'~'Tt..,tf,'eJl----,-----J,I ill I i fj I

to 0 to Kllomele,..

BaH from U.S. GMI091co1 Survey ,lotibaH fnGp,':500.ooo.

Figure 35. Recharge and discharge along streams, based on hydrologic data.

114

Groundwater-Surface·Water Relationships

0..

•i•~••I

1l 0.1

iii!; QOO•••••I,N

•I,,

0.01

[KPLANATION

ED StrMM Itl Project AreoX Ozorlls StJ'MM 11\ southern MIssouri.. In4ko,," .-0 ''ow• Golnlno streaML Louno streaM

X·

X·ED·

"ED

•

"X

X·•

·X ED"

ED"L L L,.. , • •• •••

Droll\olje density. In Miles per ..,ore Mlle.

Figure 36. The relation of ]-(j;jV Q2 to drainage density.

'15


established on a surface with little or nosolution development, underlain bydolomite. As dissolution of the dolomiteadvanced, the surface-drainage networkcontinued to exist, but groundwaterdischarge to the stream declined orremained at a high level, depending onthe amount of diversion taking placebetween basins. As a result, two streamnetworks with nearly the same densitycan coexist in the same area, with littleor no correlation with groundwaterdischarge.

The authors have concluded thatthere may be a range of drainagedensities that typify losing or deficientstreams, and that there also may be afamily of drainage-density curvescharacteristic of perennial streams.However, because of the time requiredto make a comprehensive drainagedensity study of Ozark basins, and theavailability of other methods, consideredmore reliable, in defining gaining andlosing streams, the authors haveconcluded that drainage density may notbe useful as a predictive hydrologic toolin carbonate karst terrane.

REMOTE SENSING AND THERMALDATA

Satellite imagery may be useful indefining gross hydrologic differencesbetween large basins like the DryAuglaize Creek and Niangua Riverbasins. The terrain in the areacomprising Goodwin Hollow, upper DryAuglaize Creek, and the adjacent part ofthe Niangua River basin has acharacteristic drab appearance on colorenhanced imagery, distinguishing it fromother areas where groundwater levelsare shallow. The drab appearance of thearea is believed to be caused bymoisture-stressed vegetation; howeverJ

these gross hydrologic differences werealready known before the project was

116

begun. After examining availableimagery, the authors decided anevaluation by other methods would yieldspecific data more significant to theproject.

In a recent study in Missouri, lowaltitude thermal imagery was shown tobe useful in distinguishing betweenrecharge and discharge areas alongstream valleys on the Salem Plateau(Harvey and others, 1977). Based on theresults of that study, the authorsconcluded that low-altitude thermalimagery of losing streams like DryAuglaize Creek and Goodwin Hollow,Conns Creek in the Wet Glaize Creekbasin, Jones Creek in the Niangua basin,and Steins Creek in the Osage Fork basinshould exhibit thermal characteristicssimilar to those of Logan Creek, a losingstream in the Black River basin (fig. O.

Low-altitude thermal imagery andcomputer evaluation of the data are veryexpensive; in addition, obtainingsignificant data requires precise timing{time-of-day and season) and good flyingweather. The authors have concludedthat it would be necessary to havelocally available equipment, which couldbe used within a few hours notice, tocollect low-altitude thermal dataeffectively.

Because thermal data are recognizedas potentially useful in distinguishingbetween gaining and losing streams, itwas decided to use thermocouples toobtain shallow-depth temperature data.A previous investigator (Cartwright,196&), discovered that soil temperaturesabove water-filled sand and gravel lensesin glacial till were generally higher inwinter and lower in summer than soiltemperatures elsewhere in the till. Healso found that diurnal fluctuations ofair temperature did not significantlyaffect soil temperatures at depthsexceeding 1.5 It (Cartwright, 1968).

]

'"N'0t•••L~ I::"",8''5 I- .....c=• •8'''

co 'c: ~~ &~.. ~ .

o I~H

.. C.-iiI

H.. ;C 0.,- E

~~~

;..•

tE••

N•

~iti'C

~"••-"

~

"-

0.,'",.

~

~

'",

Grou ndwater-Su rface·Water Re lationsh ips

"Thermocouples were installed 2.5 itbeneath ground level at three locationsin gaining and losing reaches of Bear,Dry Auglaize, Conns, and DeberryCreeks in the Lebanon area. A controlset of thermocouples was installed onBenton (gaining) and Norman (losing)Creeks in Phelps County, near Rolla (fig.1), where more frequent measurementscould be made.

T'able 8 lists observed soiltemperature differences. Winter tem.peratures (January 19 to March 18) forBenton Creek and the wet reach of BearCreek averaged 2.90 C warmer thanthose of Norman Creek and the dryreach of Bear Creek. In spring (March24 and June &) the average temperatureof the wet reaches was O.gOC higherthan that of the dry reach. In Augustthe average of two values for the wetreaches was still O.150 C higher than thatof the dry reach. In winter, whenvegetation was dormant, temperatures inthe wet reaches were always higher thanthose in the dry reach, a findingconsistent with results obtained duringlow-altitude flights (Harvey and others,1977).

Noting the vegetative cover at thetime of the measurements, it becameapparent that cover greatly influencedthe temperature levels in the summer.As Cartwright (I968) observed, "temperature variations caused by changes invegetation and shade were the two mostdifficult problems faced in the field."By June 7, 1977, the pasture and hayfieldat the gaining site on Bear Creek hadbeen cut, but the cover was still fairlythick at the losing site, where a goodcover of weeds and grass remained. Th'etemperature was slightly lower at thegaining than at the losing site. OnAugust II, 1977, the losing site was alittle cooler than the gaining site. Coverat the losing site was a fairly tall, thickstand of weeds; that at the gaining site,scattered straw and a few clumps ofweeds.

117


On June 1, a similar temperaturereversal was noted in comparing Bentonand Norman Creeks and the differencewas more pronounced. Just before JuneI, the hay had been cut at Benton Creek,but that at Norman Creek had not beencut.

A thermocouple in a losing reach ofDeberry Creek became progressivelymore shaded as the year advanced.Although the water table was deeper onDeberry Creek than in the gaining reachof Conns Creek, the Conns Creek siteremained warmer during the summerthan Deberry Creek, probably duelargely to shade and thick cover at theDeberry Creek site. Thin pasture grasscovered the Conns Creek site throughthe summer.

Fromconcluded

these observations it isthat changes in vegetative

cover during the summer monthsmeasurably affect ground temperatures,even at 2.5-ft depths, thus complicatinginterpretations.

In summary, soil temperaturemeasurements obtained in the wintershould be more conclusive than thoseobtained in the summer, because shadingand the insulating effect of vegetationare not problems. The temperatureprofile in the ground is radically alteredby hay cutting, heavy grazing, orremoval of plant cover. As a tool tosupport the findings from other lines ofinvestigation, shallow-depth soiltemperature measurements are useful,but the method is neither as practicalnor as specific as other methods, such assurface-flow and groundwater-levelmeasurements, in identifying infiltrationcharacteristics.

ENGINEERING GEOLOGY OFCONNS CREEK DRAINAGE SYSTEM

Thomas J. Dean

An engineering geology study ofConns Creek, in the Grandglaize Creekbasin, showed that such a study can bevery useful in relating site evaluation forwaste disposal, water impoundment, orfoundation investigation on a smalltributary or stream reach to theinvestigation of an entire basin. Testdrilling showed conclusively that thealluvial fill is incapable of transmittinglarge volumes of water after a rain andthat conduits formed in bedrock bysolution are required to carry such flows.

Conns Creekpercent of the

118

represents about 7Grandglaize Creek

drainage area (plate 19). Its geologicsetting is typical of surface andsubsurface condi Hans in much of theOzarks; therefore, the basin was chosenas one that could serve as a prototypefor future engineering geology work inthe Ozarks.

Conns Creek, with a drainage area ofabout 25 mi2 , rises in the city ofRichland and flows approximately & mito its confluence with Wet Glaize Creek(fig. 37). Deberry Creek, a principaltributary, drains approximately 9 mi2 .

Engineering Geology ofCoons Creek Drainage System

Plate 19. 19A is an aerial view westward of Conns Creek, sec. 22, T. 37 N., R. 13 W., CamdenCounty. Note the very broad, well-defined valley, a type present even in severely losingOzark stream reaches, such as the reach of Conns Creek pictured in 19B. This aerial viewof Conns Creek shOW's the stream immediately downstream from its junction withDeberry Creek. Photographs by James E. Vandike.

The main stem of Conns Creek follows Faulting may have affected thethe local northwesterly bedrock dip of geomorphic development of the Connsabout 19 it/mi. In ascending order, Creek drainage system, as indicated bybedrock formations at the surface are the parallelism between Conns Creek,the Roubidoux Formation, the Jefferson subsurface flow, and a major northwest-City Dolomite, and the Cotter Dolomite. trending fault {fig. 37} that nearly

119

A

B

25

Base from U.S. GeologIcal Survey I: 62,500 quadrangle,

/'. ) .'V

.' ./." J#I.l.<...., /\"~,---... ""C:.../

OJ' "'",--

~~~.,,,.~'''"' '''~'.

'"

.. ', Ojc s

,\\\\\

Cross section for flight auger boring Inflood plain {see Table 101.

StrtlOm reach where flow Is perennial or&oturoted lone Is very shallow.

Stream reach where surface flow Islost to bedrock.

EXPLANATION

lnnrn!d faull

Soli thickness, In feet.

Location of charcoal pockets for dyelrocl'"il nperlment (see Table 9).


"",,,,,,,,,,

x

Ojc Cotler Dolomite and Jefferson City DolomIte.

[Q!] RoubldouJ. Formation3 0

Figure 37. Geologic and hydrologic data and data-collection sites for engineering geology study inConns Creek basin.

120

bisects the basin and appears to becontinuous, although it is difficult totrace in the thick residuum at theeastern edge. Other mapped faults crossthe lower part of the basin, and mappingsuggests the existence of additional,though minor, faults. Blue Hole Spring,approximately three-fourths of a miledownstream from the junction of ConnsCreek and Wet Glaize Creek, liesadjacent to a northwest-trending fault.

In ascending order, the RoubidouxFormation consists of massive chertyreefs, fine- to medium-grained chertydolomi te, and massive coarse-grainedsandstone. The reefs are exposed in thelower reach of Deberry Creekj thecherty dolomi te, along Conns Creek,where it forms low bluffs; and themassive sandstone, on both sides of thevalley, near the mouth of Conns Creek.

Where the Roubidoux is exposed,rugged topography results fromdissolution and varying lithology, andfrom joints, which create a very highpermeability, attested to by theabundance of sinkholes and slumpfeatures, in the shallow subsurface.Lateral movement of water alongfractures in drainage divides is ascommon as leakage from impoundments.The Roubidoux outcrop is a rechargearea in many places.

The residual soils developed on theRoubidoux Formation are 10 to 40 ftthick and permeable, particularly wherethe bedrock contains much chert, andmassive sandstone beds. The total soilcolumn comprises alternating zones ofgravelly sandy clay and broken chertlayers. Horizontal permeability isextremely high, particularly in thecherty gravel zones.

The residual soils of the Roubidouxare classified in the Unified SoilClassification System as GC <U.S. Army


Corps of Engineers, 1960). The Atterburg classification of the fine fraction(less than 0.03 in.) is ML te rl , with aclay content of between and 25percent. Vertical permeability ofundisturbed samples of the stony clayportion of the soil column is estimatedto be approximately 2.8 x 10.2 to 2.8 x10.3 It/d.

The soil normally has a low pH,ranging from 5 to 6, a result ofprolonged leaching. Soil formation inzones of intense faulting and fracturingis promoted by percolation of waterthrough the acid soil. The highly pinnacled soil-bedrock contact influencesthe direction of shallow groundwatermovement.

The Jefferson City Dolomite isprincipally a thin-bedded, fine- tomedium-grained, clayey dolomite withthin, discontinuous beds of chert. Theoverlying Cotter Dolomite normallycontains little chert elsewhere in theproject area, but in the Conns Creekbasin its residuum is very cherty. TheJefferson City is exposed in the uplandsin most of the basin, whereas the Cotter1s recognized only in study of residualmaterials in drill cuttings from wells inthe upper part of the basin.

Residual soils developed on theJefferson City and Cotter Dolomitesrange from 20 to 45 it thick (fig. 37).The soils of the two formations aresimilar, except that the Cotter soilcontains much more chert than theJefferson City soil, approaching 50percent in some locali ties. Both have aUnified Classification of gravelly clay,CL to CHj permeabilities range from 2.8x 1&2 to 2.8 x 10-4 it/d. Their fabric isuniform, compared to residual soils onthe Roubidoux Formation.

Permeabilities of the residuum on theRoubidoux Formation and Jefferson City

121


and Cotter Dolomites have a similarrange. Because of the heterogeneity ofthe soils derived from the Roubidoux,compared to the more homogeneous soilsderived from the Jefferson City andCotter Dolomites, values based on coredeterminations do not completelyrepresent the permeability of theRoubidoux. The cores represent a verysmall sample of the soil characteristics.

Soils on the Jefferson City andCotter Dolomites do not readily allowrapid recharge of groundwater. Surfacerunoff and horizontal, rather thanvertical, movement of water in the soilis prevalent, especially where a fragipanexists. Where excessive fracturing andsolutioning of the underlying RoubidouxFormation have caused slumping andfracturing of the Jefferson CityDolomite, infiltration is promoted.

Where residual soils are thin, thebedrock sheds rather than absorbs water.The low infiltration capacity of theJefferson City and Cotter contrasts withthe high infiltration capacity of theRoubidoux. Stream-channel development is well defined in areas underlainby the Jefferson City and CotterDolomi tesj the streams are gainingrather than losing. Farm ponds and lakesconstructed in the residual soils of theJefferson City and Cotter pond waterreadily.

Figure 37 shows the gammg andlosing reaches of Conns Creek (type 3,fig. 29), as defined by streamflowmeasurements and water levels in wells.The upper reach of Conns Creek is againing stream to a point near itsjunction with Deberry Creek.Downstream from this point, surface

TABLE 9

Dye tracing of subsurface flow in Coons Creek Basin

(Two pounds of fluorescent yellow injected on March 23, 1977, at 1530 hours in Coons Creek, 100 yards upstreamfrom junction with Deberry Creek. Dye extracted from charcoal packets by elutriating with 5 percent potassiumhydroxide in ethyl alcohol and detected by observing solution with high-intensity lamp)

Site location (fig, 371

Wet Glaize Creek at low-water crossing

Wet Glaize Creek upstream from Blue Hole Spring

Blue Hole Spring

122

Date ofobservation

3-14-773-25-773-30-774-5-774-7-77

3-14-773-25-773-30-774-5-774-7-77

3-14-773-25-773-30-774-5-774-7-77

Visual results

Negative

Packets lost in flood

Negative

Negative

Weak positiveVery positive

"


flow is lost to bedrock (plate 19B).Similarly, Deberry Creek gains in itsupper reaches, and loses in the lower.

abundant upstream, butdownstream from the ConnsDeberry Creek confluence.

absentCreek-

In March 1977, fluorescent dyeplaced in Conns Creek where water lossoccurs at its confluence with DeberryCreek was recovered at Blue HoleSpring, on Wet Glaize Creek (table 9 andfig. 37), but did not appear in Wet GlaizeCreek farther upstream.

In June 1977, after the dye trace,exploration holes were drilled on ConnsCreek flood plain to determine if waterwas carried in the alluvial fill. The holeswere drilled along sections perpendicularto the creek, in both losing and gainingreaches (table 10). Cross sections 1, 2,and 3 are located in the losing reach ofthe stream and show dry alluvium tobedrock (fig. 37). A marked differencein depth to bedrock between sections 1and 2 correlates with faulting mappednear the mouth of the creek, suggestingdeeper weathering at section 1. Crosssection 4 is in the gaining reach andconfirms the existence of water in thebasal 3 to 4 ft of the alluvial material onthe bedrock. With available equipment,holes could not be drilled in bedrock inthe valley bottom.

A profile along Conns Creek (fig. 38)shows the position of the water table inrelation to channel and flood plain. Theprofile of the water table, based on awater-level measurement in a dug wellabout 1 mi above the confluence withDeberry Creek, and water levels in twowells at Seven Springs Hollow, showsthat the water table declines beneaththe channel, in the vicinity of theconfluence with Deberry Creek. Thisconfluence is the point at which thewriters and a former landowner haveobserved dry-weather flow to ceasenumerous times. In addition, willowgrowth, an indicator of perennial surfaceor shallow subsurface water flow, is

A cross section of the valley at SevenSprings Hollow (fig. 38) shows thedecline in water level between two wellsat the edge of the flood plain and theprojected altitude of the water tablebeneath the flood plain. These datasuggest that the water level is about 10to 20 ft below the bedrock surface in thelower reach of Conns Creek, near SevenSprings Hollow.

The streams and gulleys tributary tothe main stem of Conns Creek, at andbelow the Roubidoux-Jefferson Citycontact, exhibit very poor channeldevelopment. No sustained flow afterrainfall is indicated or was observed.Vegetation growing in the channel, verylittle to no sorting of alluvial fines, andvery weak channel development areindicators of vertical water loss fromthe alluvium into the underlying bedrock.

The water-holding capacities of sixfarm ponds and small lakes in theuplands bordering Conns Creek, andstream inflow characteristics before andafter rainfall were observed during theperiod of investigation. None of thelakes or ponds maintained stable waterlevels within several days after inflow.One small lake has a drainage area of330 acres, yet had no inflow and was d,"yduring a period when heavy rainfall hadproduced considerable runoff in ConnsCreek and Deberry Creek.

In the gaining reaches of Conns andDeberry Creeks, water is discharged intothe stream system through springs andseeps and contributes to perennialstreamflow. In the losing reaches of thetwo creeks, the general absence ofsprings and seeps indicates that thewater percolating into the soils and

123


TABLE 10

Valley cross sections in Conns Creek Basin, June 6-10, 19n(see fig. 37 for location of cross sectionsl

Fli!tlt Auger BoringSection 1. Aver.elevetion 790 ft above Netionalllllodetic vertical detum of 1929

Hole no.

2

3

4

•

6

Loeation

100 ft north of chennel

250 It north of chennel


500 ft north of channel


850 h north of channel

Depth 1ft)

0-4.54.5·77~

9·14.514.5

0-22·1212

O~

3-15

"15-16

0-22·1414-1515-17.5

0-1515-2323-2424

0-22~

9-2121-2424

Description of materiel

SiltGravelly clayBouldery siltBouldel'$; gre....1 {58ndstone?)Dolomite -demp

SiltGrll\Iel; boulders; clayey (dry)Refu581 on boulders (wet)

SiltGre....1 (clayey)Bouldel'$Dolomite - soft lwet)

SiltGrevelly. silty clayHerd {chert?)Soft dolomite· dry

Brown silty cleyGrewlly clay - sliff . plasticChert bedRefusel

SiltGravelly clay lsome lenses of gravel}Stiff, dry dey (no gravellGravel and bouldersRefusal (probably chert zone)

S&ction 2. Aver. elevetlon 800 ft Ibove Natlonal geodetic: vertical datum of 1929

Hole no.

2

3

4

124

Loeation

Chennel bottom

150 it south of chennel on lowterrace

300 ft south of channel

400 It south of chennel

Depth (ftl

0-44

0-1010-'0.510.5-11

0-77~

8

O~

3-77~

8

Desc:ription of materiel

GravelDolomite (dry I

Brown 58ndy siltGravelly c1eyDolomite (dryl

Brown sandy siltBouldel'$Dolomite (dry)

Brown siltGravel (dirty)Silt, brown, dryDolomite (smallemount of weter;

100 it to south valley waUl

Engineering Geology ofCoons Creek Drainage System

Table 10 (continued)

Right Auger Boril'l9

s.etion 3. A........~on810 ft __ Netion.. ,.oUtic ...niC8l deblm of 1929

Hole no.

2

3

•

5

5

Loution

170 tt soliltl of Mw channel(bedrock on north lice» of_....,

320 ft south of n_ chenne!

520 It south of new channelIn old channel

630 ft south of new ch8llnel

780 h south of n_ chennel

980 h KlUth of new ctoennel(75 h 10 IOUth \/IIllr;' welll

o.pth (tt)

0-77

0-77

O~

5

O~

5-77

0<.~

5.9·1212·1.

"0-22-101().1212-1.

"

Description of met.rial

Soulderl, gre...1 (dry!AefuUol on chen

Soulders, gra.."lldry)Dolomite (dry)

Gre..,,1 (wet but no free weterlDolomite

Boulders, gre..,,1 (dry)Large bouldersDolomite. tine grtin~ (dryl

Brown 1111

Grevel (drylSilty...ndy e1IYGra...erty deyBouldersDOlomite (dry!

SiltGravelly. boulOery (dry!8rown Illty. sandy cley (plasticlSoulden. grtlll'lAefUIII on chert

Hole no.

2

3

•5

Loution

50 h ~th of chennel

200 ft IOlJth of chennel

150 ft nontl of chltrtnel

350 h north of channel

500 h nontl of chennel

o..,th ltd

0·1010-11

o.e.e0-77

O~

5

DeKrlption of mlterial

Silly. g... \/II1Iy cllyDolomite; wlter lwlter rOM! to 7 ft

below lend lurlece in 1 hour; U1m1l

It 24 hours]

Herd. dry. gravelly tiltSoft-wet Ilravel1y cley (wetedDolomite (250 ft north of south

Yelley weill

SillY; sandy gr.velly cleyGre....1end bouldery e1IY (weter)Dolomite

eo.... boulden, minor grlvelAefUIII on chef-t (dry!

Bouldery;gr_lIv (dry!Aefusal on chert

125

8edroe~ __ ?

-?-----p.------------:::-.:. 6123171Iflow III ctIo ......)- -- ----?----~/2~mIHoflo.l


,,•.!

<I_It._0 ... ; •• 0

Conn. Cr..~ Clw:!11...1

1.,-:.

"

i 100

l"

j 800•

o '000Dlltgnu, III ,..,

••••.!•

r

'''''' 2000

j 100

j-o , , • • •

Dllronea, ill mllll, u~lIrlOm hom III. lnOulll

Figure 38. Profile and cross-section of Coons Creek showing groundwater-surface-waterrelationships.

126

bedrock of the Roubidoux Formationenters the valley as groundwater flow.

The total flow that the shallowbedrock in the valley bottom cantransmit can be estimated fromdischarge observations. Figure 28 showsthe flow pattern during a seepage run onApril 1, 1976, when the loss was8.2 ft 3/s in the lower reach of thecreek. On another occasion, March 31,

Summary and Conclusions

1977, Conns Creek flowed continuously,headwaters to mouth. Streamflowmeasurements on the main stem were asfollows: 10.5 ft3/s, 100 ft downstreamfrom the junction with Deberry Creek;8.5 ft 3/s, 100 ft upstream from themouth of Seven Springs Hollow; and0.5 ft3/s, near the mouth of ConnsCreek. The capacity of the subsurfacebedrock conduits, therefore, is estimatedto be about 8 to 10 ft3/s.

SUMMARY AND CONCLUSIONS

1. Using most of the availablehydrologic data, the authorsclassified areas of recharge anddischarge along streams in the threebasin region.

2. The evaluation of availablemethodology for hydrologic analysisin carbonate terranes led to thegeneral conclusion that a combination of methods will always beneeded; no single method cancompletely define the hydrologicconditions.

3. The most important controllingfactor on the hydrology of Ozarkbasins is the amount and type of rockstructural deformation. Northwesttrending faults are older thannortheast-trending faults; hence,there has been more time fordevelopment of northwest-trendingsolution channels.

4. Reconnaissance geologic mappingshould be available early in a projectin order to determine where detailedmapping may be helpful whenhydrologic data reveal an anomalouscondition.

5. An appraisal of the differences inelevation between streams inadjacent basins offers definite cluesto the flow characteristics of theentire system.

6. The latest 7Y2-minute topographicmaps were extensively used instudying the hydrology of the area.Field observations showed that theactual incidence of perennial andintermittent streams in the tributaryareas may differ from that shown onthe maps.

7. A study of groundwater levels, inconjunction with other hydrologicdata, can define areas of significantrecharge and discharge.

8. The classic concept of a water tableis approximated only along some ofthe perennial streams, such asNiangua River and Osage Fork, andrarely along others, such as GoodwinHollow, where the aquifer isextremely heterogeneous throughdissolution.

9. Except for small declines atmunicipal well sites, the potentiometric surface has changed verylittle in the past 30 to 40 years.

10. In upland recharge areas, depth towater increases markedly with welldepth, whereas in discharge areaswater levels in deep wells are only alittle higher than in shallow wells.

11. In wells deeper than 400 ft, waterlevel elevations are more uniformthan in shallower wells.

127


12. It is not advisable to dispose ofsewage or industrial waste in streamsor construct impoundments in valleyswhere groundwater levels areanomalously deep. Water-levelelevations should be compared withstreambed elevations In order todetect stream reaches where surfaceflow is lost to bedrock.

13. Where surface-water data arelacking, analysis of groundwaterlevels may lead investigators topredict where perennial flow mightbegin. Abnormal decline ingroundwater levels along a streamvalley may indicate streamflow loss,suggesting solution along zones ofintense fracturing. Adjacent basinsshould then be considered areas ofpossible resurgence.

14. Well depths necessary for adequatewater supplies are more uniform In

valleys than uplands, a correlationrelated to the premise that valleysare zones of weakness and the linesof least resistance for draining anareaj thus, they are the locus ofgreater intensity of fracturing andpermeability.

15. Yields of wells completed in allformations above the PotosiDolomite range from 9 to 35 gpmjhowever, a few wells reaching theGunter Sandstone Member, at thebase of the Gasconade Dolomite yield100 gpm. Yields of wells completedin the Potosi Dolomite range from100 to 750 gpm. Penetration offormations below the Potosi does notimprove yield.

16. Studies of potentiometric maps,streamflow patterns, and geology areinadequate to pinpoint areas ofresurgence of water from losingstreams in carbonate-rock terrane.Groundwater tracing showed thatupper Dry Auglaize Creek in

128

Grandglaize Creek basin is one of thesources of recharge to Sweet Blueand Hahatonka Springs, in theNiangua River basin. The travel ratemeasured approximately 0.4 to 0.6mild. The direction of dye travelshowed that geologic structurestrongly influences direction ofgroundwater movement.

17. Measurement of streamflow atnumerous sites during a short periodof time (seepage runs) is one of themost important available methods instudying the hydrology of carbonateterranes. Seepage-run data collectedin the winter and spring (duringperiods when there is no stormrunoff) can supply valuable information about losses in streamreaches normally dry during summerand fall.

18. Stream profiles are generallyconcave, but irregularities in shortreaches may have lithologic orstratigraphic significance. Someirregularities are due to faults thatmay abut strong and weak bedsjothers may resul t from substantialinflows or losses of water.

19. Analysis of flow lines on thepotentiometric map shows that theprincipal drainage divide between theOsage Fork flowing to the east, andNiangua River and Grandglaize Creekflowing to the north approximatesthe groundwater, divide. Within thesetwo systems, however, are numerousgroundwater diversions betweensubbasins. In a carbonate terranesubject to a long period of dissolutionresulting in considerable topographicrelief, groundwater and surfacedrainage divides become lessconformable.

20. The engineering geology study inConns Creek basin was useful 10

relating a site study to the broader

hydrologic relationships of an entirebasin.

21. Ozark soils are 40 it or more thick inmany places and store largequantities of water. In futurestudies, more comprehensive soilthickness data should be used inhydrologic analyses of basins.

22. Identification of plants and plantassemblages common to gaining orlosing stream reaches is useful instudying carbonate hydrology andaids in identifying areas of abrupthydrologic changes.

23. Thermocouple measurement ofwinter soil temperatures showed thatgaining stream valleys remainedwarmer than losing stream valleys.As a tool to support the findings fromother lines of investigation, thesedata are useful, but the method is notas practical or as specific as othermethods, such as surface-flow andgroundwater-level measurements.

24. Only one water-quality sample wascollected at most stream, well, andspringflow sites selected for study.One set of samples can be useful inidentifying areas with potentialproblems, or areas where moredetailed data are needed, but severalare required to explain data, fromother lines of investigation, thatsuggest anomalous conditions.

25. Water analyses for wells showedgross correlation between areas oflow mineralization and rechargeareas on the one hand and highmineralization and discharge areas onthe other.

26. Analyses of data from two wells inBear Creek basin, one in a gainingreach and one in a losing reach,showed that wells in losing streamreaches are more susceptible to

Summary and Conclusions

pollution than those in gainingreaches.

27. Analyses of single water samplesfrom Sweet Blue and HahatonkaSprings in the Niangua River basinrevealed low, but neverthelessabnormal, phosphorus contents suchas might result from sewagetreatment plant effluent. Althoughthese single samples were useful forhydrologic analysis, they would nothave sufficed to identify the sourceof the phosphorus, without verification by groundwater tracing.

28. Land clearing for cattle grazingincreased moderately between 1941and 1970. Between 1970 and 1975,the cattle population increased 45percent, resulting in extensive landclearing. The scant streamflow andsediment data available preclude ananalysis of the effect of land clearingon stream characteristics.

29. Drainage density may not be helpfulas a predictive hydrologic tool incarbonate terrane for the followingreasons:a. There is excessive scatter in

graphical plots of drainagedensity versus the 7-day Q2,indicating that there is littlerelationship between drainagedensity and low-flow characteristics.

b. Considerable manual labor isrequired to compute drainagedensity from topographic maps.

c. Field work is required afterdrainage-density computationsare completed, in order toanswer the most importantquestion: Is a stream gaining orlosing flow?

d. Other methods, considered morereliable, are available.

129


ACKNOWLEDGMENTS

The information in this report isbased on data collected by the MissouriDepartment of Natural Resources,Division of Geology and Land Survey,and the U.S. Geological Survey. Thereport was prepared under the directionof Wallace B. Howe, State Geologist andDivision Director, and the late AnthonyHomyk, District Chief of the MissouriDistrict of the U.S. Geological Survey,who was succeeded by Donald L. Coffin.

We thank the following geologists andsupport staff of the Missouri Departmentof Natural Resources, Division ofGeology and Land Survey: Ira

Satterfield, Larry Stout, KennethAnderson, and Ardel Rueff for reconnaissance geologic mapping identifyingmajor structural featuresj Thomas J.Dean, who made an engineering geologystudy in the Conns Creek basin; SusanDunn and Gary Clark, for drafting andlayoutj and Betty Harris for typesetting.We also thank Leroy R. Korschgen,senior research biologist, MissouriDepartment of Conservation, foridentifying plants and plant assemblages.We are grateful to the many landownersand businessmen of the area forinformation and for permitting access totheir property.

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cover design andphotograph bysusan c. dunn.exposure of lower gasconade dolomite, gunter sandstone...

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