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USGS

for a changing world

Depositional Environment, Stratigraphy, and Vertical 

Hydraulic Conductivity of the St. Francois Confining 

Unit in the Fristoe Unit of the Mark Twain National 

Forest, Missouri

£oa X *M«°

Water-Resources Investigations Report 00-4037

Prepared in cooperation with the

U.S. Department of Agriculture, Forest Service,

U.S. Department of the Interior, Bureau of Land Management,

U.S. Environmental Protection Agency, and

Missouri Department of Conservation

U.S. Department of the Interior 

U.S. Geological Survey
Cover Photograph: Carbonate and shale rock core samples from exploration holes in the Fristoe Unit of 

The Mark Twain National Forest
U.S. Department of the Interior 

U.S. Geological Survey

Depositional Environment, Stratigraphy, and Vertical 

Hydraulic Conductivity of the St. Francois Confining 

Unit in the Fristoe Unit of the Mark Twain National 

Forest, Missouri

By Michael J. Kleeschulte1 and Cheryl M. Seeger2

Water-Resources Investigations Report 00-4037

In cooperation with the

U.S. Department of Agriculture, Forest Service,

U.S. Department of the Interior, Bureau of Land Management,

U.S. Environmental Protection Agency, and

Missouri Department of Conservation

Rolla, Missouri 

2000

U.S. Geological Survey 

2Missouri Department of Natural Resources
U.S. Department of the Interior

Bruce Babbitt, Secretary

U.S. Geological Survey

Charles G. Groat, Director

The use of firm, trade, and brand names in this report is for identification purposes only and does 

not constitute endorsement by the U.S. Geological Survey.

For additional information write to: Copies of this report can be purchased

from:

District Chief

U.S. Geological Survey U.S. Geological Survey

1400 Independence Road Branch of Information Services

Mail Stop 100 Box 25286

Rolla, MO 65401 Denver, CO 80225-0286
CONTENTS

Abstract.................................................................................................................................................................................. 1

Introduction ........................................................................_^ 3

Purpose and Scope....................................................................................................................................................... 7

Study Area..................................................................................................................;................................................ 8

Exploration Borehole Data.......................................................................................................................................... 8

Rock Classification According to Depositional Texture ............................................................................................. 8

Geohydrologic Units.................................................................................................................................................... 10

Lead-Zinc Deposit Exploratory History...................................................................................................................... 10

Acknowledgments....................................................................................................................................................... 11

Depositional Environment...............................................................................................................^^ 11

Stratigraphy ...............................................................................................................................................................^ 13

Precambrian Rocks...................................................................................................................................................... 16

Lamotte Sandstone ...................................................................................................................................................... 16

Lamotte Sandstone-Bonneterre Formation Transition Zone....................................................................................... 17

Bonneterre Formation.................................................................................................................................................. 17

Davis Formation.......................................................................................................................................................... 20

Derby-Doerun Dolomite.............................................................................................................................................. 22

Vertical Hydraulic Conductivity............................................................................................................................................ 27

Methodology................................................................................................................................................................ 27

Evaluation of Results................................................................................................................................................... 28

Summary and Conclusions.................................................................................................................................................... 32

References Cited.................................................................................................................................................................... 34

Contents
FIGURES

1. Map showing location of study area, Viburnum Trend, Precambrian-rock outcrops in the St. Francois

Mountains, and the prospecting area.................................................................................................................... 4

2. Simplified cross section from western Howell County to eastern Shannon County across the prospecting

area....................................................................................................................................................................... 6

3. Well-numbering system........................................................................................................................................ 9

4. Dunham rock classification.................................................................................................................................. 9

5. Schematic section of depositional conditions and lithologies showing facies development in the

Viburnum Trend................................................................................................................................................... 12

6.-12. Maps showing:

6. Location of exploration borehole................................................................................................................. 14

7. Structure of the top of the Lamotte Sandstone............................................................................................. 18

8. Structure of the top of the Bonneterre Formation........................................................................................ 21

9. Structure of the top of the Davis Formation ................................................................................................ 23

10. Structure of the top of the Derby-Doerun Dolomite.................................................................................... 24

11. Thickness of the St. Francois confining unit................................................................................................ 25

12. Net shale thickness of the St. Francois confining unit................................................................................. 26

13. Boxplots showing the vertical hydraulic conductivities of formations and rock types in the Fristoe

Unit and Viburnum Trend .................................................................................................................................... 29

TABLES

1. Core log analysis data ................................................................................................................................................. 39

2. Porosity, vertical permeability, and vertical hydraulic conductivity data ................................................................... 61

IV Contents
Depositional Environment, Stratigraphy, and Vertical 

Hydraulic Conductivity of the St. Francois Confining Unit 

in the Fristoe Unit of the Mark Twain National Forest, 

Missouri

By Michael J. Kleeschulte1 anc/Cheryl M. Seeger2

Abstract

The confining ability of the St. Francois 

confining unit was assessed in six townships (T25- 

27N and R03-04W) of the Fristoe Unit of the Mark 

Twain National Forest in Oregon and Shannon 

Counties of southeastern Missouri. This was 

accomplished by describing the depositional environment and stratigraphy of the confining unit, and 

quantifying the vertical hydraulic conductivity of 

rock core samples from the confining unit using 

laboratory techniques. Stratigraphic data for this 

study were obtained by analysis of 238 exploration 

borehole core logs and rock core from exploration 

boreholes that typically described a 600- to 800- 

foot interval from near the bottom of the Potosi 

Dolomite into the Lamotte Sandstone or Precambrian basement rock.

Faulting created a Precambrian highland 

area (St. Francois Mountains) and basins; erosion 

gave the Precambrian igneous knobs an irregular 

shape. This erosion and a marine transgression 

with continued deposition of clastic material led to 

the accumulation of sediments that formed the 

Lamotte Sandstone. Transgression caused shelf 

drowning and gradual development of a large 

intrashelf basin with a narrow, discontinuous rim 

(lowermost Bonneterre Formation) which allowed 

the carbonate-dominant facies to form. The transiU.S. Geological Survey 

^Missouri Department of Natural Resources

tion from shaley deposits with a limited stromatolite zone to carbonate with more frequent 

stromatolites suggest a general shallowing of the 

sequence as the Bonneterre Formation was deposited.

The Bonneterre Formation-Davis Formation contact denotes abrupt intrashelf basin development that was filled during cycles of 

transgression and shallowing. The intrashelf basin 

likely had a wide, continuous shelf rim producing 

the shale-dominant Davis Formation. The DerbyDoerun Dolomite was formed during a pair of carbonate depositional cycles. The basal shaley 

sequence represents a transition with the Davis 

Formation.

Thirty-three exploration holes penetrated 

Precambrian knobs that appear to intercept two 

linear structures or ridges that trend northwestsoutheast. These knobs generally protrude less 

than 200 feet above the surrounding Precambrian 

basement rock; however, some knobs along both 

of these ridges extend more than 500 feet above 

the surrounding basement rock.

The greatest thicknesses of the Lamotte 

Sandstone are 50 to 60 feet and it is present 

throughout the study area, except where it pinches 

out against some Precambrian knobs. The depth 

from land surface to the top of the Lamotte Sandstone, where present, ranges from 1,552 to 2,450 

feet with an altitude ranging from a high of 502 

feet below sea level to a low of 1,600 feet below 

sea level. Both of the Precambrian ridges can be

Abstract 1
identified as prominent structural high features or 

domes.

Algal reef zones in the upper part of the 

lower Bonneterre Formation are common and are 

well-defined digitate stromatolites; reef zones 

reach thicknesses of 100 feet. The depth from land 

surface to the top of the Bonneterre Formation 

ranges from 1,358 to 2,002 feet, and the altitude of 

the top of the formation ranges from 278 below sea 

level to 1,152 feet below sea level. The formation 

generally dips to the south or southeast. Evidence 

for the two Precambrian ridges in the study area 

can again be observed as domed features.

The Davis Formation is composed of interbedded shales and carbonate, with both shale- and 

carbonate-dominant sequences and ranges from 

less than 50 to more than 300 feet thick. The Davis 

Formation carbonates primarily are limestone, 

with dolostone^at the top and base of the forma- . 

tion. The shales restricted the flow of dolomitizing 

fluids from reaching most Davis Formation limestones. The depth from land surface to the top of 

the Davis Formation ranges from 1,171 to 1,692 

feet and the altitude of the top of the formation 

ranges from 200 to 878 feet below sea level. The 

structure map is similar to that of the top of the 

Bonneterre Formation, with the presence of the 

two linear highs in the study area and the dip of the 

formation to the south.

The Derby-Doerun Dolomite is composed 

of mudstones, grainstones, and mudstone-matrix 

boundstones. Thin shales are present throughout 

but shale content and bed thickness increases near 

the contact with the Davis Formation. The depth 

from land surface to the top of the Derby-Doerun 

Dolomite ranges from 970 to 1,598 feet, and the 

altitude of the top of the formation ranges from 18 

feet above sea level to 788 feet below sea level. 

The Derby-Doerun Dolomite structure map is similar to that of the Davis Formation with the two 

structural highs in the study area and the general 

slope of the formation to the south.

The thickness of the St. Francois confining 

unit generally ranges from 250 to 375 feet in the 

study area. The net shale thickness of the St. Francois confining unit ranges from less than 50 feet in

the northeast part of the study area to more than 

150 feet in the southwest.

Laboratory vertical hydraulic conductivity 

and porosity analysis were performed on 88 core 

samples primarily representing the various rock 

types present in the St. Francois confining unit of 

the Fristoe Unit and the Viburnum Trend. Vertical 

hydraulic conductivity ranged from 8.70 x 10"8 

foot per second for one sample to less than 3.17 x 

10 foot per second (the reporting limit) for 39 

samples. The porosity values ranged from a high 

of 17.47 percent to a low of 0.36 percent. There did 

not appear to be a strong correlation between the 

vertical hydraulic conductivity and porosity.

There is no significant difference (p-value = 

0.375) between the ranked vertical hydraulic conductivity of samples collected from the DerbyDoerun Dolomite and Davis Formation in the Fristoe Unit. The interquartile range of vertical 

hydraulic conductivity shown for the DerbyDoerun Dolomite samples has more than an order 

of magnitude greater span than the interquartile 

range shown for the Davis Formation samples.

In the Viburnum Trend, there is a statistically significant difference (p-value = 0.006) 

between the ranked vertical hydraulic conductivity 

of the Derby-Doerun Dolomite and Davis Formation. Although the vertical hydraulic conductivity 

of both formations is small, the median vertical 

hydraulic conductivity of the Derby-Doerun Dolomite is more than an order of magnitude greater 

than the median vertical hydraulic conductivity for 

the Davis Formation.

There is no statistically significant vertical 

hydraulic conductivity difference (p-value = 

0.790) in ranked samples from the Fristoe Unit 

containing carbonate or shale or both rock types. 

This is also true when comparing ranked samples 

containing carbonate or shale or both rock types 

from the Viburnum Trend (p-value = 0.412), even 

though carbonate rocks have more than an order of 

magnitude greater median vertical hydraulic conductivity than shales.

The net shale thickness is not the single controlling factor that determines the effectiveness of 

the confining unit. Because the vertical hydraulic 

conductivity of the carbonate rocks and shales in

Depositional Environment, Stratigraphy, and Vertical Hydraulic Conductivity of the Mark Twain National Forest, Missouri
the confining unit are similar, the entire carbonateshale thickness is important in determining the 

effectiveness of the confining unit.

The estimated range of effective vertical 

hydraulic conductivity for the St. Francois confining unit in the study area was calculated to be a 

maximum of 1 x 10" 12 foot per second and a minimum of 3.0 x 10" 14 foot per second. These vertical 

hydraulic conductivity values are small allowing 

the St. Francois confining unit to effectively 

impede the flow of ground water between the 

Ozark aquifer and the St. Francois aquifer, unless 

preferred-path secondary permeability has developed along faults and fractures.

INTRODUCTION

Lead and zinc exploration in the Fristoe Unit of 

the Doniphan/Eleven Point Ranger District of the Mark 

Twain National Forest (hereinafter referred to as the 

Fristoe Unit) in southeastern Missouri has been ongoing since the 1960s. In the late 1970s and early 1980s, 

the search intensified, resulting in several hundred 

exploration holes being drilled in the Fristoe Unit. This 

exploration focused on a possible southern extension of 

the Viburnum Trend (fig. 1) ore deposits located about 

20 miles to the north.

In 1983, as a result of the exploratory drilling, 

two Preference Right Leases were submitted for areas in 

the Fristoe Unit. After the Preference Right Leases were 

submitted, the U.S. Department of Agriculture, Forest 

Service (Forest Service) and the U.S. Department of the 

Interior, Bureau of Land Management (BLM) made the 

decision to prepare an Environmental Impact Statement 

(EIS). The EIS study area was enlarged to include 

119,000 acres of the Fristoe Unit that had reasonable 

potential for mineral leasing proposals (U.S. Department of Agriculture, Forest Service and U.S. Department of Interior, Bureau of Land Management, 1988).

After the EIS was completed, mining companies 

focused their attention on a smaller area of the Fristoe 

Unit (prospecting area; fig. 1), south of Winona. The 

prospecting area lies within a larger region of welldeveloped karst terrain with an extensive network of 

solution-enlarged fractures ranging from small channels to large conduits. The two largest springs in Missouri are in this area Big Spring, which has an annual 

mean discharge of 447 cubic feet per second [(ft3/s); 

Hauck and others, 1997], and Greer Spring which has

o

an annual mean discharge of 346 ft /s (Hauck and others, 1999). Discharge from these springs helps sustain 

flow in two nationally designated streams; Big Spring 

flows into the Current River (Ozark National Scenic 

Riverway) and Greer Spring flows into the Eleven 

Point River (Eleven Point National Scenic River). The 

potential for lead-zinc mining in this environmentally 

sensitive karst area has concerned the Forest Service 

and BLM in regard to possible impacts that mining 

may have on the water resources of the area. The concerns include but are not limited to the effects that mine 

dewatering may have upon shallow water resources.

Predominantly carbonate rock sequences of the 

Lower Ordovician and Upper Cambrian Series (Jefferson City Dolomite to the base of the Lamotte Sandstone) 

overlie the igneous granites and rhyolites of the Precambrian basement rock in the study area (fig. 2). The formations from the Jefferson City Dolomite to the Eminence 

Dolomite are predominant at land surface; these rocks, 

together with the Potosi Dolomite, form the Ozark aquifer, which is a primary source of water for private and 

public-water supplies and major springs (Imes and 

Emmett, 1994). The St. Francois confining unit lies 

beneath the Ozark aquifer and consists of the DerbyDoerun Dolomite and the Davis Formation. This confining unit impedes the circulation of water between the 

overlying Ozark aquifer and the underlying St. Francois 

aquifer, which consists of the Bonneterre Formation (the 

potential host formation for lead-zinc deposits; Wharton, 

1975) and the Lamotte Sandstone. Little is known about 

the hydrology of the St. Francois aquifer because the 

shallower Ozark aquifer is a reliable source of ground 

water for the area. The geologic names used in this report 

follow the nomenclature used by the Missouri Department of Natural Resources, Division of Geology and 

Land Survey (DGLS).

The Bonneterre Formation is the potential host 

formation for lead-zinc deposits in the prospecting 

area. This formation is part of the St. Francois aquifer 

and the top of this formation is at depths greater than 

1,300 feet in the prospecting area. Before potential 

lead-zinc deposits can be extracted, the mine area will 

have to be dewatered. If the overlying St. Francois confining unit is leaky, mine dewatering could result in 

lowering water levels in the shallow Ozark aquifer. 

Because the prospecting area is a possible extension of 

the Viburnum Tend, where lead-zinc mining is currently (2000) active, the geology and depositional environment in these two areas during Late Cambrian time 

when these formations were deposited may be similar.

Introduction
91°30' 90°30'

37°30'

Base from U.S. Geological Survey digital data, 1:100,000, 1994 

Universal Transverse Mercator projection, 

Zone 15

10 15 20 25 MILES

0 5 10 15 20 25 KILOMETERS

EXPLANATION

H ST. FRANCOIS MOUNTAINS

^m PRECAMBRIAN-ROCK OUTCROP

[3D PROSPECTING AREA

A A' TRACE OF SECTION (section shown in figure 2) 

VR ,, . BOREHOLE AND IDENTIFICATION

NUMBER (table 1) 

LEAD MINE

Figure 1. Location of study area, Viburnum Trend, Precambrian-rock outcrops in the St. Francois Mountains, and 

the prospecting area.

4 Depositional Environment, Stratigraphy, and Vertical Hydraulic Conductivity of the Mark Twain National Forest, Missouri
91°25'

37°00' -

36°55'

36°50' -

28 N.

27 N.

26 N.

T. 25 N.

T. 24 N.

R. 05 W. R. 04 W. R. 03 W. R. 02 W.

Figure 1 . Location of study area, Viburnum Trend, Precambrian-rock outcrops in the St. Francois Mountains, 

and the prospecting area Continued.

Introduction 5
I

o"

O 

o

a 

c 

o

1,000-

Jefferson City Dolomite (200-300 feet)

Roubidoux Formation (125-200 feet

Gasconade Dolomite (250-300 feet)

Eminence Dolomite (150-300 feet)

Potosi Dolomite (250-300 feet)

Derby-Doerun Dolomite (100-200 feet

Davis Formation (125-225 feet)

 " Area ';

of potential | 

lead-zinc i 

deposits../

Precambrian knob

or 

Precambrian high Bonneterre Formation (300 feet)

Lamotte Sandstone (0-500 feet)

-t- Precambrian rock 

TD 2692

0 5 10 KILOMETERS 

VERTICAL SCALE GREATLY EXAGGERATED

POSSIBILITY OF OR POTENTIAL FOR KARST FEATURE

Modified from U

Forest Service a

Bureau of Land 

(20-40 feet) TYPICAL THICKNESS OF FORMATION

Figure 2. Generalized geohydrologic section from western Howell County to eastern Shannon County across the prospectin

in figure 1).
Extensive studies performed in the Viburnum Trend by 

Palmer (1991) and Thacker and Anderson (1979) indicate the environment that existed when the St. Francois 

confining unit was deposited affects the mud content of 

deposited sediments, which in turn affects the confining ability of the formations.

In 1990, the first of several consecutive geohydrologic studies was started in and adjacent to the Fristoe Unit. As a result of these studies, baseline 

hydrologic information was collected (Kleeschulte and 

Sutley, 1995) to help understand the natural flow rates 

of streams, water quality in surface and ground water, 

ground-water level fluctuations, and ground-water 

flow in the aquifers. Ground-water-level mapping and 

dye-trace studies have shown the presence of a groundwater trough between Hurricane Creek, which is adjacent to the prospecting area, and Big Spring. This indicates the possible presence of a large-permeability 

conduit system in the area that supplies water to Big 

Spring from the Hurricane Creek Basin (Imes and 

Kleeschulte, 1995).

In 1995, the U.S. Geological Survey (USGS) and 

the DGLS began a study in the prospecting area that 

supplements the geohydrologic studies that have 

already been completed in the Fristoe Unit. This study 

was preformed in cooperation with the Forest Service, 

BLM, U.S. Environmental Protection Agency, and the 

Missouri Department of Conservation.

The purpose of this study was to determine the 

depositional environment, stratigraphy, and vertical 

hydraulic conductivity of the St. Francois confining 

unit to assess the confining ability of the confining unit 

in an area centered on the prospecting area. However, 

the scope of the project was expanded to include the 

formations of the St. Francois aquifer. The Bonneterre 

Formation (part of the St. Francois aquifer) has a transitional contact with the overlying Davis Formation of 

the St. Francois confining unit. By including a description of the formations of the St. Francois aquifer, the 

entire interval from the Precambrian basement rock to 

the Davis Formation was considered. A better understanding of the effectiveness of the confining unit in the 

area was obtained by also analyzing the vertical 

hydraulic conductivity of rock core from five boreholes 

(VB1-VB5; fig. 1) in the Viburnum Trend. The results 

of these analysis were used for comparison purposes 

with the results of the core analysis from the study area.

The overall confining ability of the confining 

unit could have been obtained by performing aquifer 

tests. However, because of the expected small hydraulic conductivity of the confining unit, the excessive 

depth of the confining unit, and the resulting installation costs for pumping and observation wells, this was 

economically prohibitive. Therefore, the alternative 

laboratory hydraulic conductivity analysis method was 

selected. It is understood that there are inherent restrictions associated with the results of the laboratory 

hydraulic conductivity analysis, such as the inability to 

account for the effects of secondary permeability features (faults and fractures) that may be present in the 

subsurface of the study area.

Purpose and Scope

This report assesses the confining ability of the 

St. Francois confining unit in six townships (T25-27N 

and R03-04W) of the Fristoe Unit of the Mark Twain 

National Forest in Oregon and Shannon Counties of 

southeastern Missouri. The first objective of this report 

was to describe the depositional environment of the St. 

Francois confining unit. This information was interpreted from descriptions on mining company borehole 

and water well logs, and from detailed logging of five 

borehole cores from the study area on file at the DGLS 

McCracken Core Facility in Rolla, Missouri. This discussion was expanded to include the St. Francois aquifer.

The second objective of the report was to 

describe the stratigraphy of the St. Francois confining 

unit. This not only included describing physical rock 

characteristics but also geologic structure and formation thickness. After the stratigraphic data were compiled, structure maps were prepared depicting the 

altitude of the top of formations in the St. Francois 

aquifer and confining unit. Other maps show the thickness of the St. Francois confining unit and the areal distribution of cumulative shale thicknesses (net shale 

thickness) in the confining unit.

The third objective of this report was to quantify 

the vertical hydraulic conductivity of rock core .samples from the St. Francois confining unit in the study 

area. This was achieved by performing laboratory vertical permeability analyses on rock cores from exploration holes. Ground water obtained from the Bonneterre 

Formation was used as the transmitting fluid during the 

analysis, allowing the vertical permeability to be converted to vertical hydraulic conductivity.

Purpose and Scope
Study Area

Data for this report were collected from a fourcounty area of southeastern Missouri. However, the 

area of intense data collection (study area) for the core 

log and laboratory vertical hydraulic conductivity analysis consists of six townships (T25-27N andR03-04W) 

in the Fristoe Unit of Shannon and Oregon Counties. 

Core log data also were collected beyond the study area 

perimeter to aid in contouring formation structure; this 

expanded area included part of western Carter County 

(fig. 1). For comparison purposes, laboratory vertical 

hydraulic conductivity analysis also were performed on 

rock core samples from boreholes in the Viburnum 

Trend area in Shannon and Reynolds Counties.

Exploration Borehole Data

Several hundred exploration holes have been 

drilled by numerous mining companies during the 

decades of exploration for lead-zinc ore in and near the 

Fristoe Unit. Two hundred thirty eight exploration 

borehole core logs from in and near the study area were 

made available for study (table 1, at the back of this 

report) by the BLM, DGLS, and the Doe Run Company. The BLM receives copies of core logs from all 

exploration holes drilled on Federal lands, DGLS was 

donated copies of logs from several mining companies, 

and currently the Doe Run Company owns and operates all of the active mines in the Viburnum Trend. 

These sources have obtained copies of many of the 

exploration core logs from the various mining companies that have performed exploratory drilling in the 

study area. These logs provide general information 

such as location of the borehole, land surface altitudes 

at the borehole, depths to formation tops, and total 

depth of the hole. In some cases, the logs also provide 

detailed lithologic descriptions of the formations 

encountered from near the bottom of the Potosi Dolomite into the Lamotte Sandstone or Precambrian basement, typically an interval of 600 to 800 feet. These 

core logs along with a detailed study of core samples 

from five Amax Exploration, Inc. boreholes drilled in 

the study area (801-002, 801-009, 801-010, 801-016, 

and 801-031; table 1) provided the primary source of 

the detailed stratigraphic data contained in this report. 

Considerable interpretation was necessary in defining 

stratigraphy in some of the logs because of transitional 

lithologies and variable stratigraphic nomenclature that 

has been applied in the area.

In this report, the location of exploration boreholes is shown as the local well number (table 1) and 

follows the General Land Office coordinate system 

(fig. 3). According to this system, the first three sets of 

numbers of a hole location designate township, range, 

and section. The letters that follow indicate quarter section, quarter-quarter section, and quarter-quarter-quarter section. The quarter sections are represented by 

letters A, B, C, and D, in counterclockwise order, starting in the northeastern quadrant. Two or more exploration holes in the same division are numbered serially in 

the order they were inventoried.

Rock Classification According to 

Depositional Texture

Carbonate mud constitutes the bulk of many carbonate rock sequences. Sediment type and depositional 

environment (sediment deposited in calm water versus 

sediment deposited in agitated water) are two factors 

that influence the confining ability of rocks that are 

formed from these sediments. According to Larsen 

(1975), one way of classifying depositional environments is to focus on fine material that remained at the 

deposition site. In calm water, mud (particle size less 

than 20 microns) settles to the bottom and remains 

there, so mud-rich rocks are categorized differently 

than mud-free rocks, regardless of the amount and size 

of coarse-grained material in the rock.

Dunham (1962) defined five textural classes of 

carbonate rocks (fig. 4). These classes distinguish 

between mud-support, grain-support, and components 

that were bound together during deposition of the carbonate rock. These classes include:

Mudstone Mud-supported carbonate rocks primarily composed of fine-grained carbonate mud and 

containing less than 10 percent grain-sized particles 

(quantity at which the grains become noticeable). The 

significance of mudstone is that it implies a calm-water 

or low-energy environment.

Wackestone Mud-supported carbonate rocks 

in which grain-size particles are in excess of 10 percent, but are not so abundant as to support one another.

Packstone Mud-rich carbonate rocks with 

grains so abundant they support one another (generally 

more than 65 percent grain-size particles). Grain support generally is a property of rocks deposited in an agitated-water or high-energy environment. Rocks 

exhibiting properties of both high- and low-energy 

depositional environments are peculiar. The unusual

8 Depositional Environment, Stratigraphy, and Vertical Hydraulic Conductivity of the Mark Twain National Forest, Missouri
R. 06 W. R. 05 W. R. 04 W. R. 03 W.

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properties may simply be a result of compaction of 

wackestone (especially where interstices are completely filled with mud), may indicate the introduction 

of mud-rich sediments into an area occupied by previously mud-free sediment, or may indicate the abundant 

production of grains in calm water.

Grainstone Mud-free carbonate rocks that are 

grain-supported. Some grainstones are current laid, some 

are the result of mud being bypassed while locally produced grains accumulate, and some are the result of mud 

being winnowed from previously deposited mud-rich 

sediment. The class name merely denotes the absence of 

mud and that the grains are supported by each other.

Boundstone Carbonate rocks that exhibit signs 

that the original components were bound together during 

deposition. These components exhibit intergrown skeletal matter (corals), lamination contrary to gravity (laminations of algal stromatolites), and cavities present on 

sediment floors that are too large to be interstices.

"Whiterock" is an additional term used in the 

lithologic descriptions and facies discussions in this 

report. The term originated during lead mining in 

southeastern Missouri and denotes back-reef (area 

between barrier reef structure and the exposed land 

mass) facies composed of planar algal stromatolites 

interbedded with burrowed carbonate sands and muds,

with localized soft green clay (Howe, 1968). Both algal 

stromatolites and carbonates are bleached, dolomitized, and recrystallized to varying degrees. The 

back-reef facies is interpreted as representing a lowenergy zone above wave base in shallow water with 

restricted tides and circulation (Lyle, 1977). Whiterock 

horizons are present in much of the Upper Cambrian 

Series (Eminence Dolomite through the Lamotte Sandstone) of southern Missouri.

DEPOSITIONAL TEXTURE RECOGNIZABLE

Original components not bound 

together during deposition

Contains mud (part cles 

of clay and fine silt size)

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Packstone 0

9>. 

in Lacks mudandis grain-supported

0 CD CD o c 

Original ^ bound components were 

21 together duringeposition

3 CD

(Dunham, 1962)

Figure 4. Dunham rock classification.

Purpose and Scope
Geohydrologic Units

Delineation of geohydrologic units is based on 

hydraulic properties and the hydrologic relation of each 

unit to adjacent geohydrologic units at a regional scale. 

The terms aquifer and confining unit, as defined 

regionally, may not adequately describe the hydraulic 

properties of a sequence of rocks locally because of the 

variation in water-yielding capability of the same 

sequence from one area to another.

The lowermost geohydrologic unit is the Basement confining unit which is dominantly granite and 

rhyolite. Imes (1989) states that this confining unit is 

virtually impermeable. In areas where extensive faulting and fracturing has occurred Imes reports the basement confining unit can yield small quantities of water. 

In areas where the unit crops out, well yields are less 

than 10 gallons per minute.

The St. Francois aquifer (Imes, 1990c) overlies 

the Basement confining unit and consists of the Bonneterre Formation and the Lamotte Sandstone. In areas 

of southeastern Missouri near the St. Francois Mountains where this aquifer is close to land surface, it yields 

adequate supplies of water for domestic and small 

capacity public-supply wells. The thickness of the St. 

Francois aquifer can vary considerably because of the 

rugged surface of the underlying Precambrian basement rocks.

The Derby-Doerun Dolomite and the Davis Formation form the St. Francois confining unit (Imes, 

1990b) that overlies the St. Francois aquifer. Imes and 

Emmett (1994) state in their regional s.tudy of the 

Ozark Plateaus aquifer system that substantial secondary porosity and permeability have not developed 

regionally in the St. Francois confining unit. The finegrained nature of the formations indicates they have 

minimal permeability, even in areas containing little or 

no shale. The physical and hydraulic characteristics of 

the unit generally impede the circulation of ground 

water between the overlying Ozark aquifer and the 

underlying St. Francois aquifer (Imes and Emmett, 

1994).

Common indicators of the effectiveness of a confining unit are the thickness and the shale content (usually a minimally permeable material) of the unit. 

Whereas these normally are good measures of the confining ability of a unit, other physical properties of the 

unit may alter the confining ability, including the 

degree of cementation of the rock and secondary permeability features that development in the rock such as 

solution channels, fractures, and faults (Imes, 1990b).

Because of the depths at which these units are found in 

the study area, the presence of the secondary permeability features in the units could not be assessed.

Although the characterization of the Ozark aquifer is not within the scope of this report, a general 

description of the unit is provided to show the significance of the unit in regard to the underlying confining 

unit. Being the uppermost geohydrologic unit in the 

study area, the Ozark aquifer (Imes, 1990a) consists of 

rocks from the top of the Jefferson City Dolomite to the 

base of the Potosi Dolomite (fig. 2). This predominantly carbonate aquifer is made up of dolostone and 

limestone with some sandstone and is the most widely 

used aquifer in southern Missouri. Ground water in the 

aquifer generally occurs under water-table conditions, 

which means the upper surface of the aquifer is at 

atmospheric pressure, and the water is not confined by 

less permeable rocks.

Lead-Zinc Deposit Exploratory History

The Bonneterre Formation is the prominent host 

formation for the major lead-zinc deposits located in 

southeastern Missouri. During the prospecting and 

mining of lead in eastern Missouri, the close correlation that exists between the ore deposits and stratigraphic traps, structural highs, and "reef structures 

was discovered (Wharton, 1975). This relation provided the rationale used during the exploration for new 

ore bodies in the Viburnum Trend. As the ore deposits 

in the Viburnum Trend were being discovered and 

mined, the data gathered from extensive drilling and 

mapping provided new information about the depositional history and regional facies relation of the formations. Exploration in the Fristoe Unit in Shannon and 

Oregon Counties was directed at a potential extension 

of the Viburnum Trend (fig. 1). Much of the extensive 

geologic information that has been collected in the 

Viburnum Trend probably is transferable to the Fristoe 

Unit, especially information concerning the general 

description of the regional geologic setting and the depositional environment of the formations. A basic understanding of these factors gives insight as to the 

hydrologic characteristics of subsurface structural features and facies, which influence the confining ability 

of geohydrologic units.

10 Depositional Environment, Stratigraphy, and Vertical Hydraulic Conductivity of the Mark Twain National Forest, Missouri
Acknowledgments

A special acknowledgment of gratitude is 

extended to Glenn Adams of the Doe Run Company for 

his assistance in obtaining rock core samples and for 

access to the core logs on file at the Doe Run Company. 

Much of the data in this report could not have been 

obtained without his cooperation.

DEPOSITIONAL ENVIRONMENT

The Late Cambrian depositional environments 

can be described only in general because of the extreme 

variability in the core descriptions and unequal core 

distribution (fewer data are available for the western 

one-third of the study area). For example, descriptions 

of the Bonneterre Formation (the target formation for 

mineral exploration) by different core loggers vary 

from brief one line descriptions to detailed descriptions 

several pages in length. Formations other than the Bonneterre Formation are typically described by no more 

than a few lines per formation. Also, various carbonaterock classification systems such as Dunham (1962) and 

Folk (1959) were used. Classification of carbonates as 

either packstone or grainstone often is difficult without 

extensive petrographic work in even slightly altered 

limestones. Often the limestone and dolostone were not 

differentiated within individual cores because these 

data were not necessary for the mining geologist. Relogging of cores with consistent terminology would be 

required for a thorough characterization of depositional 

environments and confirmation of the interpretations 

provided herein.

Faulting created a Precambrian highland area 

(St. Francois Mountains; fig. 1) and basins, and parts of 

this terrane underwent extreme erosion before deposition of Upper Cambrian alluvial and marine sediments. 

This erosion gave the more resistant Precambrian igneous knobs an irregular shape. They typically have steep 

sides, but are separated by broad flat valleys and where 

these Precambrian knobs are present, overlying formations can be thin or missing.

The overlying Upper Cambrian sediments are 

composed of alluvial and fluvial elastics that grade 

upward into marine sandstones and carbonates and are 

characteristic of intershelf basin areas. These sediments were deposited during repeated cycles of marine 

transgressions (spreading of the sea over land areas) 

and subsequent shallowing. The intershelf basin was a 

large basinal feature that formed on the regional shelf.

The intershelf basin covered much of southeastern 

Missouri, including the study area and the Viburnum 

Trend (Palmer, 1989). The deposited rock sequence in 

this intershelf basin area includes the following formations (in ascending order): Lamotte Sandstone, Bonneterre Formation (including the Sullivan Siltstone and 

Whetstone Creek Members), Davis Formation, DerbyDoerun Dolomite, Potosi Dolomite, and Eminence 

Dolomite. This sedimentation in southeastern Missouri 

was controlled by pre-Late Cambrian uplift and erosion 

of the igneous basement rock, and by faulting during 

the Late Cambrian Epoch. Most of southern Missouri 

was uplifted repeatedly throughout the Paleozoic Era, 

which includes the Cambrian and Ordovician Systems. 

This is evidenced by unconformity-bounded sequences 

between and within nearly every system in the Paleozoic Erathem (Palmer and Seeger, 1998).

The St. Francois Mountains (located about 45 

miles to the northeast of the study area; fig. 1) and Precambrian knobs affected mineralization in the Viburnum Trend. During the Late Cambrian, the 

Precambrian highland area was east of the Viburnum 

Trend and a shallow water basin was to the north and 

west (fig. 5). The exposed Precambrian knobs in the 

basin were a major influence on the marine depositional environment in the area and affected the formation of island complexes. These island complexes were 

conducive for the development of algal reefs which 

were covered by sediments that later formed the Bonneterre Formation. A simplified schematic section of a 

typical buried reef structure (fig. 5) in the Viburnum 

Trend area, shows features that probably are common 

to the prospecting area.

Erosion of the Precambrian highlands and a 

marine transgression with continued deposition of clastic material led to the accumulation of sediments that 

formed the Lamotte Sandstone. The Lamotte Sandstone basal conglomerate is associated with fan deposits (alluvium deposited where streams flowed onto a 

lowland from the Precambrian knobs) (Houseknecht 

and Ethridge, 1978; Yesberger, 1982). These deposits 

can be divided into debris flows (sandstone matrix conglomerates) and mudflows (clay matrix conglomerates). Both types of fan deposits are described in the 

borehole logs. Coarseness of the alluvial deposits generally decreases with distance from the Precambrian 

highland area. Palmer (199la) interpreted arkosic sections as gravel-based channel deposits, sandbars, laminated sheet-flood deposits, and overbank deposits 

(from bottom to top through each fining-upward

Depositional Enviroment 11
WEST EAST

Derby-Doerun Dolomite

Davis Formation

Shale

and

Mudstone

Bonneterre Formation

Mudstone

CreekjyiejTiJpej^-^..^^--^ _-^^^ ^-^^ -=--^- = 

(High energy)

Grainstone __^ Whiterock 

Oo% _ M .__

Digitate Back reef 

stromatolite (low energy) 

Foreshore 

Offshore 

(low ener

Taum Sauk 

Limestone Member

Precambrian rock

Island in 

Cambrian sea

Planar 

stromatolite

Figure 5. Schematic section of depositional conditions and lithologies showing facies development 

in the Viburnum Trend.

sequence). Arkosic deposits are also present near Precambrian knobs and generally these deposits thin with 

increased distance from knobs.

Conglomerate and arkose facies are conformably 

overlain by well-sorted, well-indurated (hard), fine- to 

medium-grained quartzose sandstone. Some cross-bedding and burrows are present in these facies. These 

facies are interpreted as normal marine sandstone, and 

may have been a near shore barrier and shallow tidal 

flat complex (Palmer, 1989, 199la, 1991b).

Transgression caused shelf drowning and gradual development of a large intrashelf basin (Central 

Missouri Intershelf Basin) (Palmer, 1989). Interbedded 

sandstones and marine carbonates of the Lamotte 

Sandstone and Bonneterre Formation are included in 

sediments deposited in the transition zone where fan 

deltas were still active and discharged into tidal flats or 

shallow marine areas (Hayes and Knight, 1961; Yesberger, 1982). Differences between sandstone- and carbonate-dominated facies probably indicate distance 

from the clastic source (Precambrian highland area), 

with carbonate-dominant facies likely deposited farther 

from the source of the clastic material.

The lowermost shaley carbonate sequence of the 

Bonneterre Formation also suggests intrashelf basin 

deposition, when the basin margin was likely a narrow, 

discontinuous rim, allowing the carbonate-dominant 

facies to form. Interbedded shales are indicative of 

increased elastics coming into the basin, which periodically suppressed algal stromatolite growth. Stromatolitic zones indicate periods of limited clastic 

deposition and possible limited sedimentation. 

Between the lower shale-rich carbonates and the upper 

coarse crystalline dolostones, Bonneterre Formation 

rocks are mostly non-argillaceous (lacking clays and 

shales) and oolitic. The texture and alterations to the 

rock make identifying algal constituents in this 

sequence difficult and the rock is described as cryptalgal "reef dolostones and grainstones. The transition 

from shaley deposits with a limited stromatolite zone to 

carbonate with more frequent stromatolites suggests a 

general shallowing of the sequence, with possible 

channel development. Oolitic horizons (indicative of 

near-shore, high-energy wave-action environment) 

with possible shoaling.

12 Depositional Environment, Stratigraphy, and Vertical Hydraulic Conductivity of the Mark Twain National Forest, Missouri
Arkosic zones (up to 4 feet thick) may be interpreted in several ways. If the zones are interbedded 

with whiterock (indicative of shallow or subaerially 

exposed rock) or oolitic rocks, they may be a near shore 

facies and suggest proximity to a Precambrian knob. 

Alternately, if interbedded with only white- rock, the 

environment may have been alluvial channels. Finally, 

if they are interbedded with dark-colored mud-rich 

dolostones, they are more likely to be grain flows 

(small debris flows that moved farther offshore during 

storm events). Most core descriptions are not in sufficient detail to determine which depositional environment was present.

Several rock sequences show a cyclic pattern of 

deepening, then becoming shallow with whiterock 

present at the top of the shallowing-upward cycles. The 

whiterock thins toward the basin area. Reddened hematitic (iron oxide) patches remain in many whiterock 

sequences and grade outward to pale olive-green clayrich coarse-crystalline dolostone, suggesting that reddened limestones were the precursor to whiterock dolostone (Palmer, 199la). Dissolution of the precursor 

limestones suggests that these areas were subaerially 

exposed. The Sullivan Siltstone Member is a transgressive clastic-dominated facies that occurs where the 

shelf surface was inclined at steeper angles. This may 

have been accompanied by southeastward-directed 

shelf subsidence that was filled with sediments that 

lessened the steeper angle shelf area (Larsen, 1977; 

Palmer, 199la). Intraclast refers to sediments that were 

"torn up" by erosion, reworked, and then redeposited in 

the same basin to form a new sediment. Intraclast conglomerate beds are interpreted as possible storm-generated debris flow deposits that moved down slopes of 

only a few degrees (Palmer, 199la). One core description in the northern part of the study area notes siltstone 

intraclasts, interpreted to have been formed where they 

were found; carbonate clasts in cores to the south are 

considered to have moved down slope from the source 

area and deposited.

The Bonneterre Formation sequence may change 

to nearly all limestone or all coarse crystalline dolostone in short distances. Retention of limestone in the 

basal part suggests that the southern and extreme northwestern parts of the study area were deeper offshore 

environments because generally near-shore carbonates 

are dominated by vuggy coarse-crystalline dolostone.

The Bonneterre Formation-Davis Formation 

contact denotes abrupt intrashelf basin development. 

The intrashelf basin continued to be filled during cycles

of transgression and shallowing. The facies is a clastic 

sequence deposited within a.regional carbonate shelf. 

The intrashelf basin likely had a wide, continuous shelf 

rim, as is suggested by the shale-dominant Davis Formation, unlike that of the basal Bonneterre Formation 

basin which had a narrow, discontinuous rim and carbonate-dominant facies. Horizontal burrows in the 

Davis Formation are suggestive of slow periodic deposition in a marine subtidal setting, where the shelf 

underwent gradual drowning during a slow transgression. Intraclast conglomerate beds can be interpreted as 

storm-generated flow deposits that presumably moved 

down slopes of only a few degrees or less. Individual 

cores with more abundant intraclast conglomerate layers suggest that those locations are near the intrashelf 

basin margin and consequently nearer to the source of 

the conglomerate. These facies tends to thin towards 

the geographic center of the shale depositional basins 

where there was less deposition.

The Derby-Doerun Dolomite was formed during 

a pair of carbonate depositional cycles. The formation 

includes sequences of thinly layered carbonate rock of 

differing composition (ribbon rock) that change upslope to sequences with thinner mudstone beds and 

thicker grainstone or packstone beds. Intraclast conglomerate beds (storm-generated debris flow deposits) 

presumably moved down slopes of only a few degrees. 

Abundant intraclast beds in individual cores may suggest that those locations were near the basin margin. 

The basal shaley sequence represents a transition with 

the Davis Formation.

Arkosic and porphyry conglomeratic material 

throughout the section indicates Precambrian highlands remained exposed during the Upper Cambrian 

carbonate deposition. Continued exposure of the Precambrian highlands may have been caused by the original height of the highlands, or be the result of 

continued uplift on fault-related structures.

STRATIGRAPHY

The 238 exploration boreholes from which the 

stratigraphic data were obtained (fig. 6) ranged from 

1,478 to 2,590 feet deep. The borehole location 

recorded on the core log was determined either to the 

nearest quarter-quarter-quarter section or in feet from 

the north/south and east/west section line. Land surface 

altitudes were determined at the time of drilling using 

altimeters or topographic maps. The reported altitudes 

were verified during this study using USGS 7.5-minute

Stratigraphy 13
37W

36°55'

36°50'

T. 28 N.

T. 27 N.

T. 26 N.

T. 25 N.

T. 24 N.

R. 05 W. R. 04 W. R. 03 W. R. 02 W.

EXPLANATION

I PROSPECTING AREA

BOREHOLE AND SITE NUMBER Solid black symbol represents

borehole completed in Precambrian basement rock 

1 o Amax Exploration, Inc. 

200 A St. Joe Lead Company 

168V Asarco/Amselco 

178 D Cominco American, Inc./Phelps Dodge Mining Company

Figure 6. Location of exploration boreholes.

14 Depositional Environment, Stratigraphy, and Vertical Hydraulic Conductivity of the Mark Twain National Forest, Missouri
36°54' -

36°52' -

T. 26 N.

T. 25 N.

R. 04 W.

0.5 1 KILOMETER

Figure 6. Location of exploration boreholes Continued

Stratigraphy 15
topographic maps that generally had contour intervals 

of 20 feet, making the land surface altitude accurate to 

about 10 feet (one-half the contour interval). In a few 

instances, the reported land surface altitudes on the 

core log did not agree with the land surface altitudes 

shown on the topographic maps for the given location. 

When this situation occurred, the altitude shown on the 

topographic map at the borehole location was used. 

The altitudes used in contouring the formation tops of 

the Lamotte Sandstone, Bonneterre Formation, Davis 

Formation, and Derby-Doerun Dolomite were determined by subtracting the depth of the formation top 

reported on the core log from the land surface altitude. 

The thickness of the St. Francois confining unit also 

was mapped.

Because shale content usually is a good indicator 

of the effectiveness of a confining unit, core logs with 

detailed descriptions of lithologies were used to determine the net shale thickness of the Derby-Doerun 

Dolomite and the Davis Formation. These logs typically divided the cored section into small intervals in 

which the lithology had similar characteristics. The 

rock was described as to color, texture (mudstone, 

wackestone, packstone, grainstone, or boundstone), 

grain size, physical features present in the rock (algal 

stromatolites, vugs, and staining), and the percentage 

of each rock type (shale, dolostone, and limestone). Net 

shale thickness was calculated by multiplying the 

reported percent shale in an interval by the thickness of 

the described interval. The net shale thicknesses of all 

intervals were then summed to determine the total net 

shale thickness at that borehole location. Because most 

of the cores were not logged in sufficient detail to 

extract all the needed information to make a net shale 

thickness determination, these data are not as extensive 

as the data describing the altitude of the formation tops.

The Upper Cambrian sequence in the study area 

is a complex series of dolostones, limestones, shales, 

sandstones, and siltstones, with minor arkosic and conglomeratic layers. The lithologic summaries presented 

below are necessarily brief and focused on lithologic 

features that potentially affect hydraulic properties. 

Palmer (1989) contains a detailed discussion of the 

lithologic framework of the Upper Cambrian strata in 

southeastern Missouri. The Dunham classification system for carbonate rocks (Dunham, 1962) was used in 

this report where the Dunham system was applied by 

the core logger. Many dolostone "grainstone" may be

"packstone", or should be termed "packstone-grainstone". Logs reported using other classification systems are described using Dunham classification terms.

Precambrian Rocks

Thirty-three core logs analyzed as part of this 

study described exploration boreholes that penetrated 

Precambrian knobs (fig. 6). The locations of these 

boreholes define two linear structures or ridges that 

trend northwest-southeast. One ridge is located along 

Sycamore Creek in the northeastern part of the study 

area and the other extends through the central part of 

the study area. The knobs generally protrude less than 

200 feet above the surrounding Precambrian basement 

rock; however, some knobs along both of these ridges 

extend more than 500 feet above the surrounding basement rock.

Structural evidence of the Precambrian knobs or 

ridge in the central part of the study area appears to 

extend as high as the Roubidoux Formation. Based on 

altitudes of the contact between the Roubidoux Formation and Gasconade Dolomite, a structural dome was 

identified during geologic mapping of the area conducted in 1996 by the USGS (R.W. Harrison, U.S. Geological Survey, oral commun., 1996). In other areas 

where buried Precambrian knobs occur, structural 

domes have been mapped in overlying strata as high as 

1,000 feet above the buried knobs. One explanation as 

to why the existence of Precambrian knobs can be indicated so far up in the geologic section is that younger 

horizontal sediment layers originally buried the Precambrian basement rocks in southeastern Missouri. 

Over time, loading on the buried sediments caused 

compaction and subsidence. Thick sediments deposited away from and on the flanks of the buried knobs 

subsided more than the much thinner sediments deposited directly over the knobs, creating the mappable 

structural domes (R.W. Harrison, oral commun., 1996).

Lamotte Sandstone

The Lamotte Sandstone is present throughout the 

study area, except where it pinches out against some 

Precambrian knobs. The greatest thicknesses of this 

formation indicated by borehole data are 50 to 60 feet. 

Most cores penetrated the Lamotte Sandstone (if 

present), but were terminated before the complete section was drilled.

16 Depositional Environment, Stratigraphy, and Vertical Hydraulic Conductivity of the Mark Twain National Forest, Missouri
The Lamotte Sandstone is a white to light tan or 

gray, well-sorted, well-indurated mature quartzose 

sandstone. It generally varies from fine- to mediumgrained, but can be very coarse-grained. The sandstone 

has locally abundant burrows and small fossils (type 

not identified). Sandstones are dolomite-cemented in 

the upper part of the formation. Some dolostone is 

bleached, recrystallized, porous, and vuggy. Minor secondary calcite fracture fill and calcite- and dolomitelined vugs are reported.

Several cores contain Lamotte Sandstone that is 

all or partially arkosic or conglomeratic. Clasts are 

detrital porphyry fragments, and are supported by 

poorly sorted and angular feldspathic quartzose sandstone; clast size is up to 1 foot in diameter. The thickest 

conglomerate section is 33 feet; the thickest arkose section is 31 feet. Some clasts are scattered in thin beds 

throughout the sandstone, suggesting continual shedding of moderately worked material by erosion and/or 

continued uplift of the Precambrian highland area.

The depth from land surface to the top of the 

Lamotte Sandstone, where present, ranges from 1,552 

to 2,450 feet, with an altitude ranging from a high of 

502 feet below sea level (borehole 212, 1.5 mile north 

of the study area) to a low of 1,600 below sea level 

(borehole 236; 0.7 mile south of the study area) (table 

1, figs. 5, 6, and 7). The general dip of the formation is 

to the south or southeast. Both of the Precambrian 

ridges can be identified as prominent structural high 

features or domes. Along these ridges are several Precambrian knobs that protrude above the top of the surrounding Lamotte Sandstone. Superimposed on the 

dome structure in the central part of the study area are 

several local highs. A smaller structural high evident in 

the southeastern part of the study area (based on two 

boreholes) is adjacent to a structural trough that trends 

to the south. This trough is also a distinct feature on 

structural maps of overlying formations.

Lamotte Sandstone-Bonneterre 

Formation Transition Zone

The contact between the Lamotte Sandstone and 

Bonneterre Formation is marked by a transition zone. 

This transition zone is comprised of tan or light to 

medium gray medium-grained quartz sandstones with 

minor dolostone grainstone lenses. The sandstones 

exhibit some cross-bedding and mottling, have locally 

abundant glauconite that may be pelletal (fecal pellets),

and are cemented by fine-grained brown dolostone. 

Several logs note scattered green to dark-green and 

dark-gray crepey (crinkled appearance) shale partings.

In several core intervals, the transition zone is 

pale to medium gray or tan to grayish-brown dolostone 

with localized sandstone lenses. The dolostone is shaley to sandy, fine to medium crystalline and fine- to 

medium-grained. Dolostones are grainstones, wackestones, and mudstones; the sequence appears to coarsen 

upward. Some mudstones are interbedded with grainstones, and scattered whiterock is reported. The dolostone is sometimes mottled, burrowed and bioturbated 

(sediment disturbed or agitated by organisms), and 

nodular. Secondary calcite and dolomite vug fill and 

calcite fracture fill is present. Irregular, wavy, dark 

gray-green to greenish-gray or dark gray argillaceous 

partings as much as 1 -inch thick are present. Dolostone 

porosity is noted, but no description of type or degree 

is given. Both sandstone- and dolostone-dominant core 

intervals contain detrital igneous lithic fragments.

Bonneterre Formation

Because of the importance of the Bonneterre 

Formation as the host rock for potential ore deposits, 

the formation is studied and described in much more 

detail in logs than the other formations. The Bonneterre 

Formation is dominantly carbonate, with several shaley 

horizons and a siltstone (the Sullivan Siltstone Member). The formation is missing from several cores 

because it pinches out against Precambrian knobs. The 

lower Bonneterre Formation is subdivided into a basal 

part composed of carbonate with interbedded shale and 

an upper part composed of dolostone with occasional 

shale layers or partings. Several logs note a basal 

sequence of the Taum Sauk Limestone Member (fig. 

5).

The Taum Sauk Limestone Member is a light 

gray-white to greenish gray-white and red-mottled 

limestone with some dolostone. Where noted, the unit 

is generally found in the vicinity of the reef structures 

and is 20 to 40 feet thick. It is fine- to medium-grained 

and moderately argillaceous with red and green shale, 

and is locally burrowed.

The basal part of the lower Bonneterre Formation primarily is dolostone. Limestone is preserved in 

the southern and extreme northwestern parts of the 

study area. The basal unit ranges from 30 to more than 

300 feet thick. The dolostones are comprised of mudstones to grainstones with mudstone-matrix boundstratigraphy 17
91°25' 91°20'

37W

36°55'

36°50'

EXPLANATION

I__I PROSPECTING AREA

 -900 STRUCTURE CONTOUR Shows altitude of 

the top of the Lamotte Sandstone. Dashed 

where approximately located. Contour 

interval 100 feet. Datum is sea level

BOREHOLE Solid black symbol represents borehole

completed in the Precambrian basement 

o Amax Exploration, Inc. 

A St. Joe Lead Company 

V Asarco/Amselco

n Cominco American, Inc./Phelps Dodge Mining 

Company

Figure 7. Structure of the top of the Lamotte Sandstone.

18 Depositional Environment, Stratigraphy, and Vertical Hydraulic Conductivity of the Mark Twain National Forest, Missouri
stones and vary in color from gray to gray-tan, and tan. 

Argillaceous zones are pale green. Bleached zones suggest that parts of the section are whiterock. The dolostones are fine to medium crystalline, fine- to mediumgrained, and have interbedded quartzose-rich to arkosic 

layers (as much as 4 feet thick), primarily near the base 

(transition zone). Dark greenish-gray and gray to black 

shale is present in beds as much as 21 feet thick, and as 

wispy partings. Dolostones occasionally are mottled 

and have common bioturbation and burrowing. Algal 

structures are digitate (finger-like appearance) stromatolites as much as 1 foot high, occasional crypt-algal 

laminates, and minor hummocky algal forms. Grains 

are oolites and fossil fragments (type not specified); 

several logs note edgewise carbonate conglomerates. 

Minor porphyry conglomerate layers are noted in some 

core intervals. Structural features include infrequent 

scattered subvertical fractures, locally disrupted bedding, and, in one log, a 100-foot vertical slump structure. Solution features include scattered stylolites, and 

vugs partially to completely occluded by calcite spar 

and pink dolomite. Vugs are the most common form of 

visible porosity and often are reported in algal zones. 

Noted porosity generally is 5 percent or less.

Limestone core intervals range from 100 to 260 

feet thick. They are more lithologically heterogeneous 

than equivalent dolostones, being comprised of mudstones and grainstones, with interbedded wackestones 

and mudstone-matrix boundstones. They are light gray, 

tan and pale greenish-gray, and are fine crystalline and 

fine- to medium-grained. The limestones commonly 

are burrowed, mottled, sparsely to moderately glauconitic, and contain carbonate intraclasts, fossil fragments (type not noted), oolitic layers, and digitate 

stromatolite zones. They have rare vugs and pores that 

are partially to completely occluded by pink dolomite 

and calcite spar. Occasional, thin dolostone layers are 

reported. Dark greenish-gray thin wavy-bedded shales 

are interbedded with the limestone. Shale percentages 

are higher in the limestones than in the dolostones; the 

shales probably restricted the movement of dolomitizing fluids. Dolostones similar to those described above 

bound the top and base of the limestone core intervals, 

and range from 20 to 70 feet thick.

The upper part of the lower Bonneterre Formation ranges in thickness from 40 to nearly 250 feet. It is 

composed of interbedded dolostone grainstones, mudstones, and grainstone- and mudstone-matrix boundstones, with occasional wackestones. The top of the 

unit generally is a grainstone underlain by whiterock.

The dolostones are fine- to medium-grained and fine 

through coarse crystalline. The coarse crystalline dolostones and reported bleached zones probably are whiterock. Color ranges from light to medium gray, gray-tan, 

pale greenish-gray, and brown. The dolostone often is 

mottled and is sometimes irregularly banded. Algal 

reef zones are common and are well-defined digitate 

stromatolites with infrequent hummocky algal features; reef zones reach thicknesses of 100 feet. Burrowing is also common in the unit. Clastic material 

includes occasional shale partings, and quartzose, arkosic, and porphyry conglomeratic layers. Solution structures include stylolites, possible solution breccias, and 

vugs partially to completely occluded by calcite spar 

and pink dolomite. Several descriptions note porosity, 

but are not specific as to type and nature. Scattered subvertical fractures sometimes are partially healed by calcite and/or dolomite.

The whiterock is comprised of fine- to coarsegrained dolostone with green to greenish-gray intercrystalline clay. It ranges in color from white to light 

gray, pale brown-gray, light tan, and light blue gray. 

Where clays have not entirely occluded intercrystalline 

pores, the dolostone appears very porous or vuggy. 

Matrix dolostone grains are sometimes visibly overgrown by medium-grained pink or white dolomite.

The Sullivan Siltstone Member (fig.5) is in the 

upper Bonneterre Formation, is 2.5 to 50 feet thick, and 

is composed of light to dark gray or brown, finely laminated, well indurated, fine- to medium-grained quartzose siltstone to sandstone. The unit thickens to the 

west and south. Siltstone is interbedded with thin dolostone lithoclast conglomerates, grainstone beds (primarily in the southern part of the study area), and scattered 

thin dark green to dark gray wavy shale partings. The 

siltstones have varying amounts of siliceous and dolomitic cement. Dolostones are tan, fine crystalline, and 

sometimes mottled, glauconitic, fossiliferous (type not 

noted), oolitic and/or porous. Solution vugs and brecciation are common in some dolostones. Brecciation is 

most commonly reported as soft-sediment deformation. Vugs have calcite, and contain trace sulfide mineralization which is most common in brecciated zones. 

Cores suggest that an incipient facies change to dolostone may be present in the north-central part of the 

study area.

The Whetstone Creek Member (fig. 5) ranges 

from 30 to 150 feet thick. The unit is dolostone with 

some limestone and limey dolostone, especially in the 

northwestern part of the study area. Color ranges from

Stratigraphy 19
light to medium gray and grayish brown to tan, light 

blue gray, and greenish gray. Carbonates are fine to 

medium crystalline, fine- to medium-grained mudstones and grainstones, with wackestone-packstones 

and mudstone-matrix boundstones. Grainstones and 

wackestone-packstones are oolitic, fossiliferous (type 

not specified), and contain intraclasts. All carbonates 

are mottled, burrowed, and glauconitic. Mottled and 

finely laminated dolostones alternate. Unlike most 

Whetstone Creek Member sections in other areas of 

southeastern Missouri, these logs do not show abundant pelletal glauconite. Digitate stromatolites and 

crypt-algal laminates are noted; digitate stromatolites 

are more common to the north and laminate stromatolites to the south. Crypt-algal laminates are underlain 

by mottled dolostone, which is underlain by laminated 

dolostone. Solution features are stylolites and vugs 

with dolomite. Fracturing is present, but not common. 

Where reported, fractures generally are subvertical, 

with rare medium-angle fractures. Some fractures are 

healed by calcite. Porous zones are noted but extent and 

type are not described. Some whiterock is noted and 

reported bleached zones likely are also whiterock. 

Arkosic and igneous-conglomeratic layers are noted 

throughout the unit. Silt content is greater in the lower 

Whetstone Creek Member, near the contact with the 

Sullivan Siltstone Member.

Dark green shale partings are present throughout 

the Whetstone Creek Member. A prominent shale (1 to 

27 feet thick) at the base of the unit is informally known 

as the False Davis (fig.5). Core descriptions are inadequate to determine if the False Davis is present 

throughout the study area. The shale is often interbedded with dolostone grainstones; the dolostones contain 

fossil fragments (type not identified), oolites, and occasional pyrite.

Based on 234 data points, the depth from land 

surface to the top of the Bonneterre Formation ranges 

from 1,358 to 2,002 feet. The altitude of the top of the 

formation ranges from 278 feet below sea level (borehole 179) to 1,152 feet below sea level (borehole 236; 

table 1, figs. 6 and 8) and generally dips to the south or 

southeast. Evidence for the two Precambrian ridges in 

the study area can again be observed as domed features. 

Also, the previously mentioned trough structure in the 

southern part of the study area is evident. The structure 

map of the top of the Bonneterre Formation indicates 

problems associated with using core logs from various 

sources to map formation tops. The fingering effect of 

the contours in the southern part of the prospecting area

may be caused by different criteria used during core 

logging for identifying the top of the Bonneterre Formation, as opposed to the presence of structural features.

Davis Formation

The Davis Formation is composed of interbedded shales and carbonates, with both shale- and carbonate-dominant sequences. It ranges from less than 50 to 

more than 300 feet thick. The thinner core intervals are 

over Precambrian knobs. Shales generally are light to 

dark green, with some gray to dark gray beds. Individual shale layers range from partings to 5 feet thick. 

Shale-dominant sequences can be as thick as 50 feet, 

and contain as much as 90 percent shale. Limestonefilled burrows comprise the only carbonate in some 

shale layers. Carbonate layers in shale-dominant horizons vary from less than 1 inch to several feet thick. 

Carbonate-dominant zones may be 70 feet thick or 

greater. Shale percentages in these zones can be as 

much as 50 percent or less than 10 percent. Shale interbeds in carbonate-dominant zones vary from partings 

to several feet thick.

Davis Formation carbonates primarily are limestone, with dolostone at the top and base of the formation. The shales restricted the flow of dolomitizing 

fluids from reaching most Davis Formation limestones. 

The limestones are mudstone, grainstone, and mudstone-matrix boundstone, with some wackestone and 

occasional packstone. They are light tan to brown or 

gray to dark gray and light gray-tan in color. They are 

fine- to medium-grained and fine to medium crystalline. The limestones contain pellets, fossil fragments 

(type not specified), oolites, glauconite (some are pelletal), relict crypt-algal laminates and infrequent digitate stromatolites. Mudstones are sometimes 

bioturbated; burrows are horizontal and may be selectively dolomitized. Some layers are composed of carbonate intraclast conglomerate. Scattered vertical 

fracturing is present, but is less common than in formations above and below. Solution features include horizontal and vertical stylolites, and local solution and 

slump breccias. Scattered arkosic or porphyry conglomeratic layers are present.

The dolostones are similar to the limestones 

described above. Coarse crystalline dolostone is 

present, especially in the upper Davis Formation, 

where it is sometimes medium to pale gray or green 

whiterock. Some gray mottling is present. The dolo20 Depositional Environment, Stratigraphy, and Vertical Hydraulic Conductivity of the Mark Twain National Forest, Missouri
91°25' 91°20' 9T15'

37°00' -

36°55'

36°50' -

D PROSPECTING AREA

 -900 STRUCTURE CONTOUR Shows altitude of the 

top of the Bonneterre Formation. Dashed where 

approximately located. Contour interval 100 

feet. Datum is sea level

EXPLANATION

BOREHOLE Solid black symbol represents borehole 

completed in the Precambrian basement. Gray 

symbol with contour represents borehole with 

data dissimilar to that in surrounding boreholes 

o Amax Exploration, Inc. 

A St. Joe Lead Company 

V Asarco/Amselco

D Cominco American, Inc./Phelps Dodge Mining 

Company

Figure 8. Structure of the top of the Bonneterre Formation.

Stratigraphy 21
stone has more vugs and is more porous than the limestone; vugs are partially occluded by calcite and dolomite. Core descriptions report limonite coatings in vugs 

in the upper part of the Davis Formation; this coating 

probably is a very ferroan (containing ferrous iron) 

dolomite.

Based on 227 data points, the depth from land 

surface to the top of the Davis Formation ranges from 

1,171 to 1,692 feet and the altitude of the top of the formation ranges from 200 feet below sea level (borehole 

212) to 878 feet below sea level (borehole 229,0.6 mile 

south of the study area) (table 1, figs. 6 and 9). The 

structure map is similar to that of the top of the Bonneterre Formation with the presence of the two structural highs in the study area and the general dip of the 

formation to the south.

Derby-Doerun Dolomite

The Derby-Doerun Dolomite is composed of 

light gray to gray or light tan to brown mudstones, 

grainstones, and mudstone-matrix boundstones, with 

some wackestones and wackestone-matrix boundstones. Dolostones are fine to coarse crystalline and 

fine- to medium-grained. Whiterock is scattered 

throughout and some mottling was reported. Bedding is 

thin to massive; thin disturbed beds may be burrowed. 

The dolostones contain fossil fragments (type not specified), oolites, and carbonate lithic clasts. Digitate stromatolites and crypt-algal laminates are present. 

Occasional scattered porphyry clasts are present. Thin 

black to dark gray and green shales are scattered 

throughout; shale content and bed thickness increases 

near the contact with the Davis Formation.

Glauconite is present near the base, where dolostones are interbedded with shales. Dolostones vary in 

visible porosity from none to extremely vuggy. Unlike 

the overlying Potosi Dolomite, the Derby-Doerun 

Dolomite contains only minor chalcedony and quartz 

vug linings. Highly fractured zones are present, 

although not ubiquitous; some fractures are healed by 

dolomite and calcite. Breccias are present, but are in 

part healed by the same cements. Some fractures have 

minor to abundant iron oxide staining on the fracture 

surface. Many mining companies did not begin coring 

until they had already penetrated the Derby-Doerun 

Dolomite; consequently, complete core intervals of the 

Derby-Doerun Dolomite are not equally distributed.

The Derby-Doerun Dolomite is the uppermost 

formation mapped during this study. Based on the data 

from 212 control points, the depth from land surface to 

the top of this formation ranges from 970 to 1,598 feet, 

and the altitude of the top of the formation ranges from 

18 feet above sea level (borehole 221, 1.5 miles north 

of the study area) to 788 feet below sea level (borehole 

229, table 1, figs. 6 and 10). The Derby-Doerun Dolomite structure map is similar to that of the Davis Formation with the two structural highs in the study area 

and the general slope of the formations to the south.

The St. Francois confining unit thickness as 

determined by core logs ranges from 173 to 656 feet 

(table 1; fig. 11) in the study area. Most boreholes in 

which the confining unit was logged at more than 400 

feet thick had abnormally thick Derby-Doerun Dolomite sequences. Eight boreholes [boreholes 162, 199, 

216, 218, 219, and 230 (fig. 6) are shown on figure 11; 

boreholes 221 and 236 (fig. 6) were slightly outside the 

study area boundary] were logged with abnormally 

thick confining unit sequences. This may have been a 

result of different criteria being used to define the 

Potosi and Derby-Doerun Dolomites and consequently 

part of the Potosi Dolomite near the conformable contact may have been logged as Derby-Doerun Dolomite. 

Typically the confining unit has a thickness ranging 

from 250 to 375 feet thick (table 1; fig. 11) in the study 

area.

The net shale thickness of the St. Francois confining unit also was mapped (table 1, fig. 12). The 

thickness ranged from less than 50 feet in the northeastern part of the study area to more than 150 feet in the 

southwest. This is consistent with the current understanding of the environment at the time these formations were deposited. The deeper part of the basin 

would have been to the west of the prospecting area. 

This would have been a low-energy setting allowing 

the deposition of the silts and clays and the formation 

of shale deposits.

These conclusions are consistent with Fletcher 

(1974) who states that the clastic (includes sand and 

shales)-to-carbonate ratio in the Davis Formation 

increases westward from the presently exposed Precambrian highlands in the St. Francois Mountains east 

of the Viburnum Trend (fig. 1). Thacker and Anderson 

(1979) also show the clastic-to-carbonate ratio in the 

Davis Formation increasing to the west of buried Precambrian knobs identified by Fletcher (1974) in the 

Viburnum Trend. The decrease in thickness and clastic/ 

carbonate composition of the Davis Formation can

22 Depositional Environment, Stratigraphy, and Vertical Hydraulic Conductivity of the Mark Twain National Forest, Missouri
91°25' 91°20'

37°00' -

36°55'

36°50'

EXPLANATION

PROSPECTING AREA

- -600 STRUCTURE CONTOUR Shows altitude of the 

top of the Davis Formation. Hachures indicate 

depression. Contour interval 100 feet. Datum 

is sea level

BOREHOLE Solid black symbol represents borehole 

completed in the Precambrian basement. Gray 

symbol with contour represents borehole with 

data dissimilar to that in surrounding boreholes

O Amax Exploration, Inc.

A St. Joe Lead Company

V Asarco/Amselco

D Cominco American, Inc./Phelps Dodge Mining 

Company

Figure 9. Structure of the top of the Davis Formation.

Stratigraphy 23
91°25'

37W

36°55'

36°50'

EXPLANATION

| | PROSPECTING AREA BOREHOLE Solid black symbol represents borehole

completed in the Precambrian basement. Gray

 -400 STRUCTURE CONTOUR Shows altitude of the symbol with contour represents borehole with 

top of the Derby-Doerun Dolomite. Contour data dissimilar to that in surrounding boreholes 

interval 100 feet. Datum is sea level ° Amax Exploration, Inc.

^ St. Joe Lead Company 

V Asarco/Amselco

Q Cominco American, Inc./Phelps Dodge Mining 

Company

Figure 10. Structure of the top of the Derby-Doerun Dolomite.

24 Depositional Environment, Stratigraphy, and Vertical Hydraulic Conductivity of the Mark Twain National Forest, Missouri
91°25' 91°20'

37°00'

36°55'

36°50'

n

EXPLANATION

PROSPECTING AREA BOREHOLE Gray symbol with contour represents 

borehole with data dissimilar to that in surrounding 

 400 LINE OF EQUAL THICKNESS Shows thickness boreholes

of the St. Francois confining unit. Contour interval o Amax Exploration, Inc. 

100 feet. Datum is sea level A St. Joe Lead Company

V Asarco/Amselco

d Cominco American, Inc./Phelps Dodge Mining 

Company

Figure 11. Thickness of the St. Francois confining unit.

Stratigraphy 25
91°25' 91°20'

37°00'

36°55'

36°50'

EXPLANATION

PROSPECTING AREA

 100 LINE OF EQUAL THICKNESS Shows net 

shale thickness of the St. Francois confining 

unit. Dashed where approximately located. 

Contour interval, in feet, is variable. Datum 

is sea level

BOREHOLE

o Amax Exploration, Inc. 

A St. Joe Lead Company 

V Asarco/Amselco

n Cominco American, Inc./Phelps Dodge Mining 

Company

Figure 12. Net shale thickness of the St. Francois confining unit.

26 Depositional Environment, Stratigraphy, and Vertical Hydraulic Conductivity of the Mark Twain National Forest, Missouri
reduce the ability of the confining unit to impede flow 

between the Ozark and St. Francois aquifers near the 

Precambrian knobs.

VERTICAL HYDRAULIC CONDUCTIVITY

Laboratory testing was used to determine the 

vertical hydraulic conductivity and porosity of various 

rock types present in the St. Francois confining unit. 

Shale typically has a smaller permeability than carbonate rocks (Freeze and Cherry, 1979). By determining 

the thickness of the confining unit, the net shale thickness of the unit, and the vertical hydraulic conductivity 

range of the various rock types present in the unit, the 

data are available to quantitatively estimate the confining ability of the unit. Permeability is a function of the 

medium (rock core) alone and is not dependent on the 

fluid used or the force field causing the movement of 

the liquid (Lohman and others, 1972). Hydraulic conductivity is a measure of the ease with which a specific 

fluid can be transmitted through a porous medium, and 

is a function of the medium and of the density and viscosity of the fluid being transmitted. The transmitted 

fluid used during the permeability tests was similar to 

water that flows through the confining unit in the study 

area. This allowed representative vertical hydraulic 

conductivities to be determined from laboratory core 

permeability results.

Rock cores from both the study area and the 

Viburnum Trend were sent to the Core Petrophysics, 

Inc. laboratory in Houston, Texas, for vertical hydraulic conductivity analysis. Samples from the Viburnum 

Trend were collected and analyzed for comparison with 

the results of the core analyzed from the study area. The 

potential lead-zinc deposits in the prospecting area 

probably have formed in a similar geologic depositional environment and by the same processes that 

formed the deposits that are currently (2000) being 

mined in the Viburnum Trend. The vertical hydraulic 

conductivity of the confining unit in the Viburnum 

Trend is minimal, allowing effective dewatering and 

mining. A comparison of the vertical hydraulic conductivity of the confining units in the two areas can give 

insight as to the potential of the confining unit in the 

prospecting area to inhibit ground-water flow between 

aquifers.

Rock core samples that represent the entire St. 

Francois confining unit sequence were selected and 

sent to the laboratory for analysis. Sixty-four core samples were selected from 11 boreholes in the Fristoe Unit

and 24 samples were selected from 5 boreholes in the 

southern part of the Viburnum Trend (table 2, at the 

back of this report). Twenty-six core samples were 

from the Derby-Doerun Dolomite and 59 samples were 

from the Davis Formation. One sample (sample number 35, table 2) was logged as the Derby-Doerun Dolomite, but after further inspection, the core was 

determined to probably be from the lower Potosi Dolomite; two samples (sample numbers 6 and 29, table 2) 

after further inspection were determined to be from the 

upper Bonneterre Formation.

Methodology

Vertical permeability and porosity were determined in the laboratory for the rock core samples using 

methods described by the American Petroleum Institute (1998). The test conditions simulated the in situ 

conditions at the depth from which each core sample 

was collected. The permeability of a medium is 

inversely proportional to the net confining stresses to 

which the medium is subjected. A net confining stress 

[calculated using a pressure gradient of 0.758 pounds 

per square inch (psi) per foot depth] was applied to 

each core sample during the permeability analysis (Jim 

Scale, Core Petrophysics, Inc., written commun., 

1999). A water sample collected from the city of Viburnum public-water supply, which pumps water from an 

abandoned lead mine in the Bonneterre Formation 

about 50 miles north of the study area was sent with the 

core samples to the laboratory. The transmitting fluid 

used in the laboratory vertical permeability analysis 

had similar density and viscosity properties as the 

water sample from Viburnum; this allowed the laboratory-derived vertical permeability to be converted to 

vertical hydraulic conductivity.

The following procedure was used to prepare 

each core sample at the laboratory. Upon receiving the 

88 core samples, the cores were trimmed to right-angle 

cylinders using air as the bit lubricant. The samples 

then were extracted with methanol to remove any precipitated salt, then oven dried for 24 hours at a temperature of 240 degrees Fahrenheit. The bulk volumes of 

the cores were determined by fluid displacement 

(Archimedes' principle). Dry weights were recorded 

and the grain densities calculated. Helium porosity of 

the rock core at room conditions was obtained by measuring a grain volume using Boyle's Law (Jim Scale, 

Core Petrophysics, Inc., written commun., 1999).

Vertical Hydraulic Conductivity 27
The core samples were evacuated and pressure 

saturated at 1,000 psi with the simulated Viburnum 

water. Saturations were verified gravimetrically upon 

removal from the saturation cell. The core samples 

were then placed in individual coreholders and the calculated net confining stress was applied. The differential flow pressure, time, and water volumes produced 

were recorded. When the permeability was below the 

reporting limit, the test was allowed to conclude after 

48 hours. The effective vertical permeability of the 

rock core was calculated using the following equation 

(Jim Scale, Core Petrophysics, Inc., written commun., 

1999):

k = A(Pu-Pd)

k = effective permeability, in darcies (1 darcy =

9.87 x 10 centimeters squared) 

Q = flow rate, in cubic centimeters per second 

jj, = fluid viscosity, in centipoise (1 centipoise =

0.01 gram per centimeter-second) 

L = length, in centimeters 

A = area, in square centimeters 

Pu = upgradient pressure, in atmospheres 

Pd = downgradient pressure, in atmospheres 

Hydraulic conductivity is related to permeability 

by (American Petroleum Institute, 1998):

K =

K = hydraulic conductivity, in centimeters per

second

k = effective permeability, in darcies 

p = mass density of the fluid, in grams per

cubic centimeters 

g = acceleration of gravity, in centimeters per

second squared

ILI = fluid viscosity, in centipoise 

After substitution, the conversion of vertical permeability in darcies to vertical hydraulic conductivity 

in foot per second (ft/s) becomes:

K = (3.17) x \0~5 k

Evaluation of Results

Vertical hydraulic conductivities ranged from 8.70 

x 10"8 ft/s for one sample to less than 3.17 x 10" 14 ft/s (the 

reporting limit) for 39 samples (table 2). The porosity 

values ranged from a high of 17.47 percent to a low of

0.36 percent. There did not appear to be a strong correlation between the vertical hydraulic conductivity and 

porosity.

With the outliers, the reported vertical hydraulic 

conductivity values span six orders of magnitude; this, 

compounded with the large number of values below the 

reporting limit, cause the mean and standard deviation 

statistic values for this data set to be strongly distorted. 

Therefore, box plots (fig. 13) using logarithmic scales 

are used to present the results.

Figure 13 shows the variation in vertical hydraulic conductivity of different formations and different 

rock types within the Fristoe Unit (A and C) and the 

Viburnum Trend (B and D). The variation in vertical 

hydraulic conductivity between similar formations and 

rock types in the Fristoe Unit and the Viburnum Trend 

is also shown on figure 13 (E-J).

The Lilliefors (two-tailed) test for normality 

(Iman and Conover, 1983) showed the vertical hydraulic conductivity data are not normally distributed. 

Because these data are not normally distributed, the 

data were ranked. All of the statistical analysis used to 

evaluate the significant differences between data sets 

were performed on the ranked data. The WilcoxonMann-Whitney rank sum test (two-tailed) was used 

when comparing two data sets and an analysis of variance was used to perform multiple-comparisons when 

more than two data sets were evaluated (Iman and 

Conover, 1983).

In all of the statistical analysis, a level of significance (a-value) of 0.05 was used to test the null 

hypothesis which states, the vertical hydraulic conductivity of the data sets being compared are equal. The 

attained significance level (p-value) is a probability 

value determined by the data (Iman and Conover, 

1983). The null hypothesis was rejected for all analysis 

with p-values for the pooled data that were less than 

0.05.

No significant difference (p-value = 0.375) 

exists between the ranked vertical hydraulic conductivity of samples collected from the Derby-Doerun Dolomite and Davis Formation in the Fristoe Unit. The 

similarity is also visually expressed (fig. 13A), by the 

considerable overlap of the two boxplots and the similarity of the median values of the two data sets. However, the interquartile range (the range between the 

upper and lower quartiles) of vertical hydraulic conductivity shown for the Derby-Doerun Dolomite samples has more than an order of magnitude greater span 

than the interquartile range shown for the Davis Forma28 Depositional Environment, Stratigraphy, and Vertical Hydraulic Conductivity of the Mark Twain National Forest, Missouri
rr LU 

a.

LU 

U_

Z

Q

O 

O 

O

Q

X

cc

LU 

>

10

10 r

io'

10lu

t 10

10

io'

10'

1Q10

(1)

Fristoe 

Unit

(18)

(43)

Viburnum 

Trend

| (16)

Potosi Derby- Davis Bonneterre

Dolomite Doerun Formation Formation

Dolomite

FORMATION

DerbyDoerun 

Dolomite

Davis 

Formation

Fristoe 

Unit

(33) (16)

Viburnum 

Trend

(11)

T(7>

Carbonate Shale Both carbonate 

and shale

Carbonate Shale

ROCK TYPE

Both carbonate 

and shale

i« rt; r

rLnoP 1 9

EXPLANATION

* DATA GREATER THAN 90TH PERCENTILE

90th PERCENTILE 

|(8) NUMBER OF SAMPLES

75th PERCENTILE (UPPER QUARTILE)

50th PERCENTILE (MEDIAN)

25th PERCENTILE (LOWER QUARTILE) 

 10th PERCENTILE

DATA LESS THAN 10TH PERCENTILE

Figure 13. Boxplots showing the vertical hydraulic conductivities of formations and rock 

types in the Fristoe Unit and Viburnum Trend.

Evaluation of Results 29
10

io'8

ID'9

io-10

ID'"

io'12

io 13

Q in"14 

Z 10

O -7

FEET UCTIVITY, IN PERSC

°i 0,.

a

o io" o

g 

I 10'12

DC

£

* »"

I 

CC -14

£ 10

10 ?

io 8 

io'9 

io-10

10"

io"2

io-13

10'"

i * 1 E

E All samples _

: * =

: * :

'- (64) J(24) :

= -

J

-

= ~ ~=

\

!

= - - | E

f G Derby-Doerun ~i 

: Dolomite :

: (18) ;

" T (8) -

- I -

- -

i

E I E

1 / Davis | 

- Formation

; " * i

r (43)

r ._... .' (16) -

I I : _

 -5

+

Fristoe Viburnum 

Unit Trend

E T I E

_ F Carbonate

E Jf E

r i

1 (33) T :

1 ^~\ 1 <6) r i :

i __ i

t

=~ -=

i

= 1 E

f H Shale i

T< 16>

I Tm =

ET -=

I

1 J Carbonate [ 

: and shale ;

: * ;

: J(n> :

r T(15) -

=- -|

+

Fristoe Viburnum 

Unit Trend

Figure 13. Boxplots showing the vertical hydraulic conductivities of formations and rock 

types in the Fristoe Unit and Viburnum Trend Continued.

30 Depositional Environment, Stratigraphy, and Vertical Hydraulic Conductivity of the Mark Twain National Forest, Missouri
tion samples. The samples collected from the Potosi 

Dolomite and the Bonneterre Formation are shown for 

comparison purposes, although they are of no importance in evaluating the St. Francois confining unit. The 

samples from the upper Bonneterre Formation have a 

low vertical hydraulic conductivity, possibly related to 

the transitional nature of the contact between the Davis 

Formation and the Bonneterre Formation.

In the Viburnum Trend, there is a statistically 

significant difference (p-value = 0.006) between the 

ranked vertical hydraulic conductivity of the DerbyDoerun Dolomite and the Davis Formation. Although 

the vertical hydraulic conductivity of both formations 

is small, the median vertical hydraulic conductivity of 

the Derby-Doerun Dolomite is more than an order of 

magnitude greater than the median vertical hydraulic 

conductivity of the Davis Formation (fig. 13B).

In the Fristoe Unit, there is no statistically significant (p-value = 0.790) vertical hydraulic conductivity 

difference in ranked samples containing carbonate or 

shale, or both rock types. This is shown visually (fig. 

13C) by the interquartile range of the box plots having 

considerable overlap and the median values being similar.

In the Viburnum Trend, there is no statistically 

significant (p-value = 0.412) vertical hydraulic conductivity difference in ranked samples containing carbonate or shale, or both rock types. Visually (fig. 13D), the 

carbonate rocks have more than an order of magnitude 

greater median vertical hydraulic conductivity than 

shales. The Derby-Doerun Dolomite contains primarily carbonate rocks and the Davis Formation contains 

primarily shale, this relation is also observed in the 

Viburnum Trend formation vertical hydraulic conductivity comparisons (fig. 13B). Also, samples from the 

Viburnum Trend that contain both carbonate and shale 

have a larger vertical hydraulic conductivity variability 

than samples from either individual rock type. Samples 

containing both rock types span the same vertical 

hydraulic conductivity range as the carbonate and shale 

together.

The interquartile range of vertical hydraulic conductivity for individual formations and rock types in 

the Fristoe Unit was compared with those in the Viburnum Trend. A larger variability of some core samples 

from the Fristoe Unit was observed (fig. 13, F-I). The 

cause of this variability can be attributed to the carbonate rock samples from the Derby-Doerun Dolomite, 

which have more than two orders of magnitude greater 

range in vertical hydraulic conductivity than the

Derby-Doerun Dolomite in the Viburnum Trend. In 

spite of this variability, the vertical hydraulic conductivity of rock samples from the Fristoe Unit are similar 

to those from the Viburnum Trend.

One conclusion that can be drawn from the vertical hydraulic conductivity measurements on different 

rock types in the Fristoe Unit (fig. 13C) is that the net 

shale thickness is not the single controlling factor that 

determines the effectiveness of the St. Francois confining unit. Because the vertical hydraulic conductivity of 

the carbonate rocks and shale in the confining unit are 

similar, the entire carbonate-shale thickness is important in determining the effectiveness of the confining 

unit.

Using the results of this study, the range of estimated effective vertical hydraulic conductivity values 

for the St. Francois confining unit in the Fristoe Unit 

was calculated. A typical thickness of the confining 

unit of 300 feet (fig. 11) was used in the calculations. A 

net shale thickness of 50 feet was used for the minimum effective vertical hydraulic conductivity of the 

confining unit calculation and 150 feet was used for the 

maximum (fig. 12). Vertical hydraulic conductivities as 

represented by the upper and lower quartiles range from 

about 1 x 10" 12 to 3 x 10" 14 ft/s for the carbonate rocks 

and 9 x 10' 13 to 3 x 10' 14 ft/s for shale in the Fristoe 

Unit.

The effective vertical hydraulic conductivity of a 

unit composed of several layers aligned in series, with 

each layer having different vertical hydraulic conductivities can be calculated using the formula:

K. K, K.,

dt = total thickness of the confining unit 

d|, d2, d3 , dn = thickness of layer 1, layer 2, layer

3, and layer n 

Kt = effective vertical hydraulic

conductivity of unit

K|, K2 , K.3, Kn = vertical hydraulic conductivity of 

layer 1, layer 2, layer 3, and layer n 

By using appropriate extreme values of net shale 

thickness and vertical hydraulic conductivity, the range 

of effective vertical hydraulic conductivity for the confining unit in the study area was estimated to be a maximum of 1 x 10" I2 ft/s and a minimum of 3 x 10" 14 ft/s. 

These vertical hydraulic conductivity values are small, 

allowing the confining unit to effectively impede the 

flow of ground water between the Ozark aquifer and

Evaluation of Results 31
the St. Francois aquifer, unless preferred-path secondary permeability has developed along faults and fractures.

This report assesses the confining ability of the 

St. Francois confining unit in six townships (T25-27N 

and R03-04W) of the Fristoe Unit of the Mark Twain 

National Forest in Oregon and Shannon Counties of 

southeastern Missouri. This was accomplished by 

describing the depositional environment and stratigraphy of the St. Francois confining unit, and quantifying 

the vertical hydraulic conductivity of rock core samples from the confining unit using laboratory techniques. Stratigraphic data for this study were obtained 

by analysis of 238 exploration borehole core logs and 

rock core from exploration boreholes that typically 

described a 600- to 800-foot interval from near the bottom of the Potosi Dolomite into the Lamotte Sandstone 

or Precambrian basement rock.

The Upper Cambrian sediments are composed of 

alluvial and fluvial elastics that grade upward into 

marine sandstones and carbonates and are characteristic of intrashelf basin areas. These sediments were 

deposited during repeated cycles of marine transgressions and subsequent shallowing. This sedimentation 

was controlled by pre-Late Cambrian uplift and erosion 

of the igneous basement rock and by faulting during the 

Late Cambrian Epoch. Faulting created a Precambrian 

highland area (St. Francois Mountains) and basins; erosion gave the Precambrian igneous knobs an irregular 

shape. This erosion and a marine transgression with 

continued deposition of clastic material led to the accumulation of sediments that formed the Lamotte Sandstone, which is interpreted as a near shore barrier and 

shallow tidal flat complex. Transgression caused shelf 

drowning and gradual development of a large intrashelf 

basin with a narrow, discontinuous rim (lowermost 

Bonneterre Formation) which allowed the carbonatedominant facies to form. The transition from shaley 

deposits with a limited stromatolite zone to carbonate 

with more frequent stromatolites suggest a general 

shallowing of the sequence as the Bonneterre Formation was deposited. Several rock sequences in the Bonneterre Formation show a cyclic pattern of deepening, 

then becoming shallow. Retention of limestone in the 

basal part of the Bonneterre Formation suggests that 

the southern and extreme northwestern parts of the 

study area were deeper offshore environments.

The Bonneterre Formation-Davis Formation 

contact denotes abrupt intrashelf basin development 

that was filled during cycles of transgression and shallowing. The intrashelf basin likely had a wide, continuous shelf rim producing the shale-dominant Davis 

Formation. Horizontal burrows in the Davis Formation 

suggest a slow periodic deposition in a marine subtidal 

setting, where the shelf underwent gradual drowning 

during a slow transgression. The Derby-Doerun Dolomite was formed during a pair of carbonate depositional cycles. The basal shaley sequence represents a 

transition with the Davis Formation.

Arkosic and porphyry conglomeratic material 

throughout the section indicates Precambrian highlands remained exposed during Upper Cambrian carbonate deposition. Continued exposure of the 

Precambrian highlands may have been caused by the 

original height of the highlands, or be the result of continued uplift on fault-related structures.

Thirty-three exploration holes penetrated Precambrian knobs. These boreholes appear to intercept 

two linear structures or ridges that trend northwestsoutheast. These knobs generally protrude less than 

200 feet above the surrounding Precambrian basement 

rock; however, some knobs along both of these ridges 

extend more than 500 feet above the surrounding basement rock. Structural evidence of the Precambrian 

knobs or ridge in the central part of the study area 

appears to extend as high as the Roubidoux Formation.

The Lamotte Sandstone is preserit throughout the 

study area, except where it pinches out against some 

Precambrian knobs. The greatest thicknesses of this 

formation indicated by borehole data are 50 to 60 feet. 

The depth from land surface to the top of the Lamotte 

Sandstone, where present, ranges from 1,552 to 2,450 

feet with an altitude ranging from a high of 502 feet 

below sea level to a low of 1,600 feet below sea level. 

The general dip of the formation is to the south or 

southeast. Both of the Precambrian ridges can be identified as prominent structural high features or domes. A 

structural high is evident in the southeastern part of the 

study area and is adjacent to a structural trough that 

trends to the south. This trough is also a distinct feature 

on structural maps of overlying formations.

The lower Bonneterre Formation is subdivided 

into a basal part composed of carbonate with interbedded shale and an upper part composed of dolostone 

with occasional shale layers or partings. Algal structures present in the basal part are digitate stromatolites 

as much as 1 foot high, occasional crypt-algal lami32 Depositional Environment, Stratigraphy, and Vertical Hydraulic Conductivity of the Mark Twain National Forest, Missouri
nates, and minor hummocky algal forms. Grains are 

oolites and fossil fragments (type not specified). The 

upper part of the lower Bonneterre Formation is composed of interbedded dolostone grainstones, mudstones, and grainstone- and mudstone-matrix 

boundstones, with occasional wackestones. Algal reef 

zones in this upper part are also common and are welldefined digitate stromatolites with infrequent hummocky algal features; reef zones reach thicknesses of 

100 feet. Dark green shale partings are present throughout the Whetstone Creek Member of the upper Bonneterre Formation and a prominent shale (1 to 27 feet 

thick) at the base of unit is informally known as the 

False Davis.

The depth from land surface to the top of the 

Bonneterre Formation ranges from 1,358 to 2,002 feet 

and the altitude of the top of the formation ranges from 

278 feet below sea level to 1,152 feet below sea level. 

The formation generally dips to the south or southeast. 

Evidence for the two Precambrian ridges in the study 

area can again be observed as domed features. The 

trough structure in the southern part of the study area is 

also evident. The structure map of the top of the Bonneterre Formation indicates problems associated with 

using core logs from various sources to map formation 

tops. The fingering effect of the contours in the southern part of the prospecting area may be caused by different criteria used during core logging for identifying 

the top of the Bonneterre Formation, as opposed to the 

presence of structural features.

The Davis Formation is composed of interbedded shales and carbonates, with both shale- and carbonate-dominant sequences and ranges from less than 50 to 

more than 300 feet thick. Shale-dominant sequences 

can be as thick as 50 feet, and contain as much as 90 

percent shale. The Davis Formation carbonates primarily are limestone, with dolostone at the top and base of 

the formation. The shales restricted the flow of dolomitizing fluids from reaching most Davis Formation 

limestones.

The depth from land surface to the top of the 

Davis Formation ranges from 1,171 to 1,692 feet, and 

the altitude of the top of the formation ranges from 200 

feet below sea level to 878 feet below sea level. The 

structure map is similar to that of the top of the Bonneterre Formation, with the presence of the two linear 

highs in the study area and the general dip of the formation to the south.

The Derby-Doerun Dolomite is composed of 

mudstones, grainstones, and mudstone-matrix boundstones. Digitate stromatolites and crypt-algal laminates 

are present. Thin shales are present throughout but 

shale content and bed thickness increases near the contact with the Davis Formation.

The depth from land surface to the top of the 

Derby-Doerun Dolomite (the uppermost formation 

mapped) ranges from 970 to 1,598 feet and the altitude 

of the top of the formation ranges from 18 feet above 

sea level to 788 feet below sea level. The Derby - 

Doerun Dolomite structure map is similar to that of the 

Davis Formation with the two structural highs in the 

study area and the general slope of the formation to the 

south.

Typically the combined thickness of the DerbyDoerun Dolomite and Davis Formation (St. Francois 

confining unit) ranges from 250 to 375 feet thick in the 

study area; however, the confining unit was logged at 

more than 400 feet thick for several boreholes. Most of 

these boreholes had abnormally thick Derby-Doerun 

Dolomite sequences. This may have been a result of the 

Potosi Dolomite near the conformable contact with the 

Derby-Doerun Dolomite being logged as DerbyDoerun Dolomite. The net shale thickness of the St. 

Francois confining unit ranges from less than 50 feet in 

the northeast part of the study area to more than 150 

feet in the southwest.

Laboratory vertical hydraulic conductivity and 

porosity analysis were performed on 88 core samples 

primarily representing the various rock types present in 

the St. Francois confining unit of the Fristoe Unit and 

the Viburnum Trend area. The vertical permeability 

values were converted to vertical hydraulic conductivity. Vertical hydraulic conductivity ranged from 8.70 x 

10"8 foot per second for one sample to less than 3.17 x 

10" 14 foot per second (the reporting limit) for 39 samples. The porosity values ranged from a high of 17.47 

percent to a low of 0.36 percent. There did not appear 

to be a strong correlation between vertical hydraulic 

conductivity and porosity.

There is no significant difference (p-value = 

0.375) between the ranked vertical hydraulic conductivity of samples collected from the Derby-Doerun 

Dolomite and Davis Formation in the Fristoe Unit. The 

interquartile range of vertical hydraulic conductivity 

shown for the Derby-Doerun Dolomite samples has 

more than an order of magnitude greater span than the 

interquartile range shown for the Davis Formation 

samples.

Summary and Conclusions 33
In the Viburnum Trend, there is a statistically 

significant difference (p-value = 0.006) between the 

ranked vertical hydraulic conductivity of the DerbyDoerun Dolomite and the Davis Formation. Although 

the vertical hydraulic conductivity of both formations 

is small, the median vertical hydraulic conductivity of 

the Derby-Doerun Dolomite is more than an order of 

magnitude greater than the median vertical hydraulic 

conductivity for the Davis Formation.

In the Fristoe Unit, there is no statistically significant (p-value = 0.790) vertical hydraulic conductivity 

difference in ranked samples containing carbonate or 

shale or both rock types. This is also true when comparing ranked samples containing carbonate or shale or 

both rock types from the Viburnum Trend (p-value = 

0.412), even though carbonate rocks have more than an 

order of magnitude greater median vertical hydraulic 

conductivity than shales. Also, samples from the 

Viburnum Trend that contain both carbonate and shale 

have a larger vertical hydraulic conductivity variability 

than samples from either individual rock type. Samples 

containing both rock types span the same vertical 

hydraulic conductivity range as the carbonate and shale 

together.

The net shale thickness is not the single controlling factor that determines the effectiveness of the confining unit. Because the vertical hydraulic conductivity 

of the carbonate rocks and shale in the confining unit 

are similar, the entire carbonate-shale thickness is 

important in determining the effectiveness of the confining unit.

The range of estimated effective vertical hydraulic conductivity for the St. Francois confining unit in 

the study area was calculated using the results of this 

study. The calculations used 300 feet as the typical 

thickness of the confining unit; 50 and 150 feet as the

19 lower and upper net shale thickness ranges; 1 x 10 

to 3 x 10" 14 foot per second as the upper and lower vertical hydraulic conductivity range (upper and lower 

quartiles) of the carbonate rock; and 9 x 10" 13 to 3 x 

10~ 14 foot per second as the upper and lower vertical 

hydraulic conductivity range (upper and lower quartiles) of the shale. Resulting estimates of effective vertical hydraulic conductivity were calculated to be a

1 0

maximum of 1 x 10 foot per second and a minimum 

of 3 xlO" 14 foot per second. These vertical hydraulic 

conductivity values are small, allowing the confining 

unit to effectively impede the flow of ground water

between the Ozark aquifer and the St. Francois aquifer, 

unless preferred-path secondary permeability has 

developed along faults and fractures.

REFERENCES CITED

American Petroleum Institute, 1998, Recommended 

practices for core analysis: Washington, D. C. 

American Petroleum Institute, 195 p.

Dunham, R.J., 1962, Classification of carbonate rocks 

according to depositional texture, in Ham, W.E. 

ed., Classification of Carbonate Rocks a Symposium, Tulsa, Oklahoma: American Association of 

Petroleum Geologists Memoir 1, p. 108-121.

Fletcher, C.S., 1974, The geology and hydrogeology of 

the New Lead Belt, Missouri: University of Missouri-Rolla, unpublished M.S. thesis, 91 p.

Folk, R.L., 1959, Practical petrographic classification 

of limestones: American Association of Petroleum 

Geologists Bulletin, v. 43, p. 1-38.

Freeze, R.A., and Cherry, J.A., 1979, Groundwater: 

Prentice-Hall, Inc., Englewood Cliffs, New Jersey, 

604 p.

Hauck, H.S., Huber, L.G., and Nagel, C.D., 1997, 

Water resources data Missouri water year 1996: 

U.S. Geological Survey Water-Data Report MO96-1, 292 p.

 1999, Water resources data Missouri water year 

1998: U.S. Geological Survey Water-Data Report 

MO-98-1, 434 p.

Hayes, W.C., and Knight, R.D., 1961, Cambrian System, in Koenig, J.W., ed., revised 1995, Thompson, T.L., ed., Stratigraphic Succession in 

Missouri: Missouri Geological and Water 

Resources, v. 40, second series, p. 14-20.

Houseknecht, D.W., and Ethridge, F.G., 1978, Depositional history of the Lamotte Sandstone of southeastern Missouri: Journal of Sedimentary 

Petrology, v. 48, no. 2, p. 575-586.

Howe, W.B., 1968, Planar stromatolite and burrowed 

carbonate mud facies in Cambrian strata of the St. 

Francois Mountain area: Missouri Geological Survey and Water Resources Report of Investigations 

No. 41, 113 p.

Imes, J.L., 1989, Major geohydrologic units in and 

adjacent to the Ozark Plateaus province, Missouri, 

Arkansas, Kansas, and Oklahoma Basement 

confining unit: U.S. Geological Survey Hydrologic Investigations Atlas HA-711-B, 1 sheet.

34 Depositional Environment, Stratigraphy, and Vertical Hydraulic Conductivity of the Mark Twain National Forest, Missouri
Imes, J.L., 1990a, Major geohydrologic units in and 

adjacent to the Ozark Plateaus province, Missouri, 

Arkansas, Kansas, and Oklahoma Ozark aquifer: 

U.S. Geological Survey Hydrologic Investigations 

Atlas HA-711-E, 3 sheets.

 1990b, Major geohydrologic units in and adjacent to the Ozark Plateaus province, Missouri, 

Arkansas, Kansas, and Oklahoma St. Francois 

confining unit: U.S. Geological Survey Hydrologic Investigations Atlas HA-711-D, 3 sheets. 

 1990c, Major geohydrologic units in and adjacent to the Ozark Plateaus province, Missouri, 

Arkansas, Kansas, and Oklahoma St. Francois 

aquifer: U.S. Geological Survey Hydrologic 

Investigations Atlas HA-711-C, 2 sheets.

Imes, J.L., and Emmett, L.F., 1994, Geohydrology of 

the Ozark Plateaus aquifer system in parts of Missouri, Arkansas, Oklahoma, and Kansas: U.S. 

Geological Survey Professional Paper 1414-D, 

127 p.

Imes, J.L., and Kleeschulte, M.J., 1995, Seasonal 

ground-water level changes (1990-93) and flow 

patterns in the Fristoe Unit of the Mark Twain 

National Forest, southern Missouri: U.S. Geological Survey Water-Resources Investigations Report 

95-4096, 1 sheet.

Iman, R.L., and Conover, W.J., 1983, A modern

approach to statistics: John Wiley and Sons, New 

York, New York, 497 p.

Kleeschulte, M.J., and Sutley, S.J., 1995, Hydrologic 

data for the Fristoe Unit of the Mark Twain 

National Forest, Southern Missouri, 1988-1993: 

U.S. Geological Survey Open-File Report 95-106, 

106 p.

Larsen, K.G., 1975, Stratigraphic and facies nomenclature of the Viburnum Trend, southeast Missouri, in 

Vineyard, J.D. ed., Guidebook to the geology and 

ore deposits of selected mines in the Viburnum 

Trend, Missouri: Rolla, Missouri Division of 

Geology and Land Survey, Report of Investigations 58, p. 15-19.

 1977, Sedimentology of the Bonneterre Formation, southeast Missouri: Economic Geology, v. 

72, p. 408-419.

Lohman, S.W., and others, 1972, Definitions of 

selected ground-water terms-Revisions and conceptual refinements: U.S. Geological Survey 

Water-Supply Paper 1988, 21 p.

Lyle, J.R., 1977, Petrography and carbonate diagenesis 

of the Bonneterre Formation in the Viburnum

Trend area* southeast Missouri: Economic Geology, v. 72, p. 420-434.

Palmer, J.R., 1989, Late Upper Cambrian shelf depositional facies and history, southern Missouri, in 

Gregg, Jay M., Palmer, James R., and Kurtz, Vincent E., eds., Field guide to the Upper Cambrian of 

southeastern Missouri: stratigraphy, sedimentology, and economic geology: Department of Geology and Geophysics, University of Missouri at 

Rolla, p. 1-24.

Palmer, J.R., 199la, Distribution of lithofacies and 

inferred depositional environments in the Cambrian System, in Martin, J.A., and Pratt, W.P., eds., 

Geology and mineral-resource assessment of the 

Springfield 1° x 2° quadrangle, Missouri, as 

appraised in September 1985: U. S. Geological 

Survey Bulletin 1942, 115 p.

 1991b, Stratigraphy and porosity characteristics, uppermost Lamotte Sandstone, Bonneterre 

Formation, and basal Davis Formation, in two 

closely spaced drillcores; Greer 7.5 minute quadrangle, Oregon County, Missouri: Unpublished 

report, Missouri Department of Natural 

Resources, Division of Geology and Land Survey, 

16 p.

Palmer, J.R., and Seeger, C.M., 1998, Synsedimentary 

tectonic features in southeast Missouri, in Seeger, 

C.M. ed., Syndepositional tectonics during the 

Late Upper Cambrian: Association of Missouri 

Geologists 45th Annual Meeting and Field Trip, 

September 25-26,1998, Farmington, Missouri: p. 

27-48.

Thacker, J.L., and Anderson, K.H., 1979, Preliminary 

carbonate lithofacies maps of the Cambrian Davis 

Formation, Rolla 1° X 2° quadrangle, Missouri 

1:250,000: Rolla, Missouri, Division of Geology 

and Land Survey, 2 sheets.

U.S. Department of Agriculture, Forest Service, and 

U.S. Department of the Interior, Bureau of Land 

Management, 1987, Environmental Analysis Doe 

Run Exploratory Drilling Project: Rolla, Missouri, 

U.S. Department of Agriculture, 98 p.

U.S. Department of Agriculture, Forest Service, and 

U.S. Department of the Interior, Bureau of Land 

Management, 1988, Final Environmental Impact 

Statement, Hardrock Mineral Leasing Mark Twain 

National Forest: Rolla, Missouri, U.S. Department 

of Agriculture, 129 p. with appendices.

U.S. Department of Agriculture, Forest Service, and 

U.S. Department of the Interior, Bureau of Land

References Cited 35
Management, 1991, Environmental analysis Doe num Trend, Missouri: Rolla, Missouri Division of

Run Exploratory Drilling Project, Bureau of Land Geology and Land Survey, Report of InvestigaManagement permits ES 19219 and ES 19220: tions 58, p. 3-14.

Rolla, Missouri, U.S. Department of Agriculture, Yesberger, W.L., 1982, Paleoenvironments and deposi70 p. with appendices. tional history of the Upper Cambrian Lamotte

Wharton, H.M., 1975, Introduction to the southeast Sandstone in southeast Missouri: unpublished

Missouri lead district, in Vineyard, J.D., ed., The M.A. thesis, University of Missouri at Columbia,

geology and ore deposits of selected mines, Vibur- 287 p.

36 Depositional Environment, Stratigraphy, and Vertical Hydraulic Conductivity of the Mark Twain National Forest, Missouri
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Core log analysis data 39
Table 1. Core log analysis data Continued

[YYYYMMDD, year, month, day; DDMMSS, degrees, minutes, seconds; all units for depth, altitude, and thickness are in feet; depth and altitude 

positional En

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8

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12

13

14

15

16

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18

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20

21

22

23

Derby-Doerun

Depth

1,425

1,171

1,445

1,284

1,375

1,345

1,335

1,405

1,397

1,382

1,478

1,230

1,405

1,354

1,235

1,525

1,335

1,370

1,346

1,384

1,348

Altitude

-403

-271

-439

-398

-413

-525

-500

-625

-382

-487

-493

-335

-445

-449

-600

-620

-555

-420

-426

-409

-368

Dolomite

Thickness

70

59

50

61

81

85

49

76

66

43

24

61

58

66

59

62

57

85

58

97

Thickness of St. 

Davis Formation Francois confining unit Bonneterre Formation

Depth

1,495

1,230

1,495

1,345

1,456

1,430

1,384

1,481

1,463

1,425

1,502

1,291

1,463

1,420

1,298

1,294

1,587

1,171

1,427

1,431

1,442

1,445

Altitude

-473

-330

-489

-459

-494

-610

-549

-701

-448

-530

-517

-396

-503

-515

-468

-659

-682

-581

-477

-511

-467

-465

Thickness

212

196

241

218

290

192

260

219

304

210

266

191

261

256

210

238

225

250

255

194

246

260

Total

282

255

291

279

371

277

309

295

370

253

290

252

319

322

297

287

183

312

279

304

357

Net shale Depth

1,707

1,426

71 1,736

1,563

1,746

1,622

1,644

1,700

1,767

82 1,635

84 1,768

1,482

1,724

1,676

1,508

1,532

125 1,812

1,421

1,518

1,682

1,625

1,688

33 1,705

Altitude

-685

-526

-730

-677

-784

-802

-809

-920

-752

-740

-783

-587

-764

-771

-678

-897

-907

-831

-738

-732

-705

-713

-725

Thickness

405

395

404

325

427

375

408

345

374

299

363

392

399

431

427

445

422

381

397

399

Lamotte 

Depth

2,112

2,131

1,967

2,071

2,049

2,019

2,108

2,112

2,009

2,067

2,087

2,068

1,907

1,963

2,239

1,866

1,940

2,063

2,085

2,104

Altit

-1,09

-1,12

-1,08

-1,10

-1,22

-1,18

-1,32

-1,09

-1,11

-1,08

-1,12

-1,16

-1,07

-1,32

-1,33

-1,27

-1,16

-1,11

-1,11

-1,12
Table 1 . Core log analysis data Continued

[YYYYMMDD, year, month, day; DDMMSS, degrees, minutes, seconds; all units for depth, altitude, and thickness are in feet; depth and 

o

0

3

6"

(Q

a>

2L

V)

v>

a.

0)

sr

A

Site 

number

(fig. 6)

24

25

26

27

28

29

30

31

32

33

34

35

36

37

38

39

40

41

42

43

44

45

46

Date drilled 

(YYYYMMDD)

19791008

19791020

19790728

19791207

19790927

19790921

19790830

19791002

19791011

19800206

19791026

19791113

19791112

19791210

19791031

19791106

19791127

19800123

19791213

19791218

19800215

19800111

19791228

Latitude 

(DDMMSS)

365820

365543

365214

365543

365541

365442

365424

365301

365536

365619

365500

365449

365443

365437

365526

365518

365410

365510

365646

365406

365430

365545

365543

Longitude 

(DDMMSS)

911143

911825

911302

912159

912038

911915

911949 ^

912114

911825

911915

911739

911907

911746

911753

911831

911841

911639

911729

912338

911802

911758

912057

912115

Mining company 

borehole 

identification

AM AX 80 1-024

AM AX 80 1-025

AM AX 80 1-026

AM AX 80 1-027

AM AX 80 1-028

AM AX 80 1-029

AM AX 80 1-030

AM AX 80 1-031

AM AX 80 1-032

AM AX 80 1-033

AM AX 80 1-034

AM AX 80 1-035

AM AX 80 1-036

AM AX 80 1-037

AM AX 80 1-038

AMAX 801 -039

AM AX 80 1-040

AMAX 801 -041

AM AX 80 1-042

AMAX 801 -043

AMAX 801-044

AMAX 801 -045

AMAX 801 -046

Local well number

T27NR02W29CDA1

T26NR03W 17BAB1

T26NR02W31CDC3

T26NR04W 14BBA1

T26NR04W 13BAA1

T26NR03W 19ABC1

T26NR03W 19CBB1

T26NR04W35AAC1

T26NR03W 17BAC2

T26NR03W07ACB1

T26NR03W 16CCB1

T26NR03W 19ABA1

T26NR03W20AAD1

T26NR03W20ADB1

T26NR03W 17BCA1

T26NR03W 17CBB1

T26NR03W21DDA1

T26NR03W 16CBD1

T26NR04W04DCC1

T26NR03W20DCD1

T26NR03W20ADC1

T26N R04W 1 3BBB 1

T26NR04W 14AAB1

A

la
6

</>

itional Environmen

»*

sB> <5*

B> O

*C 

fit

a

o'

SL

z

a.

fit

C

lie Condi

^

o 

<\

0

<D

2

0)

1

3 

Z

D>

1

0)

S1 

3

(0

S55'

8

Table I.Corel 

[YYYYMMDD,

og analysis data Continued 

year, month, day; DDMMSS, degrees, minutes, seconds;, all units for depth, altitude, and thickness are in feet; depth and altitude 

Thickness of St.

Site 

number

(fig. 6)

24 

25

26

27

28

29 

30

31

32

33

34 

35

36

37

38

39

40

41

42 

43

44

45

46

Derby-Doerun Dolomite

Depth

1,270 

1,351

1,405 

1,396

1,430

1,427 

1,366

1,465

1,371

1,287

1,373 

1,336

1,372

1,414

1,349

1,192

1,307

1,418

1,506 

1,368

1,297

1,358

1,284

Altitude

-540 

-411

-430 

-406

-445

-507 

-486

-545

-451

-407

-443 

-456

-402

-379

-429

-362

-327

-458

-526 

-463

-327

-418

-454

Thickness

63

64 

120

62

67 

88

77

34

78

38

47

25

66

74

63

58

54

79 

97

63

69

71

Davis Formation Francois confining unit Bonneterre Formation

Depth

1,414

1,469 

1,516

1,492

1,494 

1,454

1,542

1,405

1,365

1,411 

1,383

1,397

1,480

1,423

1,255

1,365

1,472

1,585 

1,465

1,360

1,427

1,355

Altitude

-474 

-494 

-526

-507

-574 

-574

-622

-485

-485

-481 

-503

-427

-445

-503

-425

-385

-512

-605 

-560

-390

-487

-525

Thickness

212

233 

202

207

204 

208

222

214

205

220 

213

214

205

217

206

260

213

228 

202

188

224

212

Total

189

275

297

322

269

271 

296

299

248

283

258 

260

239

271

291

269

318

267

307 

299

251

293

283

Net shale Depth

1,459 

1,626

30 1,702 

1,718

1,699

1,698 

1,662

80 1,764

1,619

94 1,570

61 1,631 

1,596

1,611

1,685

1,640

1,461

1,625

1,685

71 1,813 

.46 1,667

1,548

1,651

49 1,567

Altitude

-729 

-686

-727 

-728

-714

-778 

-782

-844

-699

-690

-701 

-716

-641

-650

-720

-631

-645

-725

-833 

-762

-578

-711

-737

Thickness

397 

420

388

348

375 

426

416

412

369

481 

413

370

437

360

413

315 

419

348

358

Lamotte 

Depth

1,856 

2,046

2,106

2,047

2,073 

2,088

2,180

2,031

1,939

2,112 

2,009

2,055

2,077

1,821

2,098

2,128 

2,086

1,999

1,925

Altit

-1,12

-1,10

-1,11

-1;06

-1,15

-1,20

-1,26

-1,11

-1,05

-1,18

-1,12

-1,02

-1,15

-99

-1,13

-1,14

-1,18

-1,05

-1,09
Table 1 . Core log analysis data Continued

[YYYYMMDD, year, month, day; DDMMSS, degrees, minutes, seconds; all units for depth, altitude, and thickness are in feet; depth and al

o

o

3

6"

CO

a> 

SL

(A

w

0. 

0)

8

.&

Site 

number 

(fig. 6)

47

48

49

50

51

52

53

54

55

56

57

58

59

60

61

62

63

64

65

66

67

68

69

Date drilled 

(YYYYMMDD)

19800418

19800606

19800229

19800503

19800328

19800328

19800314

19800319

19800416

19800326

19800409

19800716

' 19800228

19800207

19800125

19800408

19800220

19800628

19800425

19800503

19800813

19800905

19800512

Latitude 

(DDMMSS)

365104

365654

365818

365410

365147

365310

365222

365129

365249

365041

365206

365307

365642

365555

365549

365121

365540

365618

365152

365511

365513

365543

365424

Longitude 

(DDMMSS)

911854

912315

911808

911649

911813

911301

911306

911837

911413

912102

912150

912106

912147

911853

911855

911436

912000

912620

911515

912057

912055

912221

911958

Mining company 

borehole 

identification

AM AX 80 1-047

AMAX801-048

AM AX 801 -049

AM AX 80 1-050

AM AX 80 1-051

AM AX 80 1-052

. AM AX 80 1-053

AM AX 80 1-054

AM AX 80 1-055

AMAX801-056

AM AX 80 1-057

AM AX 80 1-058

AM AX 80 1-059

AM AX 80 1-060

AM AX 801 -061

AM AX 80 1-062

AMAX801-063

AM AX 80 1-064

AMAX801-065

AM AX 80 1-066

AMAX801-067

AM AX 80 1-068

AMAX801-069

Local well number

T25N R03W 08BCB 1

T26NR04W04DAD1

T27NR03W32BAA1

T26NR03W21DDB1

T25NR03W05ACD1

T26N R02W 30CDB 1

T26NR02W31CDB1

T25NR03W05CDB1

T26NR03W36BCA1

T25NR04W 12CCB1

T25NR04W02BAC1

T26NR04W35AAA1

T26NR04W02CDD1

T26NR03W07DDA1

T26NR03W07DDC1

T25NR03W02DDD1

T26NR04W 13AAA1

T26NR04W07BCA1

T25NR03W02BDC1

T26NR04W 13CBC1

T26NR04W 13CBD1

T26NR04W 15AAB1

T26NR03W 19CBB1

A

lan
Table 1 . Core log analysis data Continued

[YYYYMMDD, year, month, day; DDMMSS, degrees, minutes, seconds; all units for depth, altitude, and thickness are in feet; depth and altitude 

positional Em

^

13

w

3

Q>

3-

0)

3

a

o'

2L

X

a.

5

o' 

O

o

a.

c

o

i

9

2

Q>

H

D) 3'

z

Q)

5'

3

~

3 

u>~

255'

(0

o

Site 

number 

(fig. 6)

47

48

49

50

51

52

53

54

55

56

57

58

59

60

61

62

63

64

65

66

67

68

69

Derby-Doerun Dolomite

Depth

1,455

1,337

1,455

1,355

1,430

1,459

1,452

1,470

1,235

1,451

1,487

1,488

1,317

1,297

1,284

1,567

1,348

1,366

1,497

1,430

1,417

1,375

1,382

Altitude

-560

-447

-425

-395

-590

-469

-467

-550

-440

-531

-507

-568

-332

-432

-429

-557

-368

-386

-547

-515

-472

-475

-497

Thickness

71

131

55

65

62

66

50

64

72

63

64

82

73

63

72

70

67

99

65

71

112

77

88

Thickness of St. 

Davis Formation Francois confining unit

Depth

1,526

1,468

1,510

1,420

1,492

1,525

1,502

1,534

1,307

1,514

1,551

1,570

1,390

1,360

1,356

1,637

1,415

1,465

1,562

1,501

1,529

1,452

1,470

Altitude

-631

-578

-480

-460

-652

-535

-517

-614

-512

-594

-571

-650

-405

-495

-501

-627

-435

-485

-612

-586

-584

-552

-585

Thickness

278

194

202

203

254

195

255

286

180

283

293

202

237

190

193

238

217

240

237

220

199

187

205

Total

349

325

257

268

316

261

305

350

252

346

357

284

310

253

265

308

284

339

302

291

311

264

293

Net shale

106

96

57

77

100

58

72

88

51

162

80

71

59

79

Bonneterre Formation

Depth

1,804

1,662

1,712

1,623

1,746

1,720

1,757

1,820

1,487

1,797

1,844

1,772

1,627

1,550

1,549

1,875

1,632

1,705

1,799

1,721

1,728

1,639

1,675

Altitude

-909

-772

-682

-663

-906

-730

-112

-900

-692

-877

-864

-852

-642

-685

-694

-865

-652

-725

-849

-806

-783

-739

-790

Thickness

424

350

387

427

432

468

390

428

444

436

383

416

330

402

422

441

360

441

399

308

.394

420

Lamotte 

Depth

2,228

2,012

2,099

2,050

2,178

2,188

2,147

2,248

1,931

2,233

2,227

2,188

1,957

1,952

1,971

2,316

2,065

2,240

2,120

2,036

2,033

2,095

Altit

-1,333

-1,122

-1,069

-1,090

-1,338

-1,198

-1,162

-1,328

-1,136

-1,313

-1,247

-1,268

-972

-1,087

-1,116

-1,306

-1,085

-1,290

-1,205

-1,091

-1,133

-1,210
Table 1 . Core log analysis data Continued

[YYYYMMDD, year, month, day; DDMMSS, degrees, minutes, seconds; all units for depth, altitude, and thickness are in feet; depth and alt

o 

o

<36"

(Q

Q>

3

2L

(055'

Q. 

Q)

sr

Site 

number

(f>g. 6)

70

71

72

73

74

75

76

77

78

79

80

81

82

83

84

85

86

87

88

89

90

91

92

Date drilled 

(YYYYMMDD)

19800523

19800520

19800530

19800614

19800618

19800723

19800718

19800826

19800819

19800725

19800623

19800628

19800703

19800714

19800718

19800806

19800801

19800812

19800903

19801025

19801103

19801107

19801124

Latitude 

(DDMMSS)

365004

365531

365536

365115

365430

365433

365906

365533

365521

365543

365536

365539

365542

365544

365538

365201

364934

364950

365601

365302

365243

365254

365231

Longitude 

(DDMMSS)

911633

911831

911827

911329

911941

911929

912210

912053

912058

912014

912044

912032

912045

912055

912026

911516

911722

912044

911841

911256

911254

911302

91 1302

Mining company 

borehole 

identification

AM AX 80 1-070

AM AX 80 1-071

AM AX 80 1-072

AM AX 80 1-073

AM AX 80 1-074

AM AX 80 1-075

AM AX 80 1-076

AM AX 80 1-077

AMAX801-078

AM AX 80 1-079

AM AX 80 1-080

AM AX 80 1-081

AM AX 80 1-082

AMAX801-083

AMAX801-084

AMAX801-085

AM AX 80 1-086

AM AX 801 -087

AMAX801-088

AMAX801-089

AM AX 80 1-090

AMAX801-091

AM AX 80 1-092

Local well number

T25NR03W 15BDC1

T26N R03W 1 7BCA2

T26NR03W 17BAC1

T25NR03W 12AAA1

T26NR03W 19BCD1

T26NR03W 19BDC1

T27NR04W27AAD1

T26NR04W 13BCA1

T26NR04W 13BCC1

T26N R04W 1 3AAB 1

T26NR04W 13BAC1

T26NR04W 13BAD1

T26N R04W 1 3BAB 1

T26NR04W 13BBA1

T26NR04W 13ABC1

T25NR03W02BAC1

T25NR03W21BAA1

T25NR04W 13CDB1

T26NR03W08CBC1

T26NR02W30CDD1

T26NR02W31BDA1

T26NR02W31BAC1

T26NR02W31CAB1

Alt

land 
*; Table 1. Core log analysis data Continued

[YYYYMMDD, year, month, day; DDMMSS, degrees, minutes, seconds; all units for depth, altitude, and thickness are in feet; depth and altitude 

positional Em

 ^

I

(D

3

CO

Q>

(5*

 o

Q>

3

a.

so'

2L

I

"a

m

o' 

O

0

3

a

c

0

f

(D

Q>

?

0>5'

z

a>

6'

3

2L 

 n

o

(0 

(0

2

(0 

O

Site 

number 

(fig. 6)

70

71

72

73

74

75

76

77

78

79

80

81

82

83

84

85

86

87

88

89

90

91

92

Derby-Doerun

Depth

1,159

1,354

1,358

1,562

1,393

1,299

1,538

1,453

1,442

1,340

1,450-

1,393

1,374

1,345

1,351

1,562

1,413

1,496

1,288

1,471

1,477

1,454

1,502

Altitude

-519

-424

-428

-572

-493

-469

-448

-468

-502

-390

-475

-433

-419

-425

-431

-642

-723

-606

-418

-471

-507

-474

-512

Dolomite

Thickness

66

73

72

71

87

80

109

66

63

61

65

74

78

64

74

59

75

57

63

68

70

71

86

Thickness of St. 

Davis Formation Francois confining unit

Depth

1,225

1,427

1,430

1,633

1,480

1,379

1,647

1,519

1,505

1,401

1,515

1,467

1,452

1,409

1,425

1,621

1,488

1,553

1,351

1,539

1,547

1,525

1,588

Altitude

-585

-497

-500

-643

-580

-549

-557

-534

-565

-451

-540

-507

-497

-489

-505

-701

-798

-663

-481

-539

-577

-545

-598

Thickness

237

206

198

213

202

208

158

204

213

204

198

202

203

207

208

204

210

269

186

226

236

231

248

Total

303

279

270

284

289

288

267

270

276

265

263

276

281

271

282

263

285

326

249

294

306

302

334

Net shale

71

54

43

74

72

62

50

62

62

98

63

143

87

44

47

Bonneterre Formation

Depth

1,462

1,633

1,628

1,846

1,682

1,587

1,805

1,723

1,718

1,605

1,713

1,669

1,655

1,616

1,633

1,825

1,698

1,822

1,537

1,765

1,783

1,756

1,836

Altitude

-822

-703

-698

-856

-782

-757

-715

-738

-778

-655

-738

-709

-700

-696

-713

-905

-1008

-932

-667

-765

-813

-776

-846

Thickness

439

465

425

496

416

414

337

342

407

396

354

398

387

352

402

437

445

408

410

342

400

399

383

Lamotte 

Depth

1,901

2,098

2,053

2,342

2,098

2,001

2,142

2,065

2,125

2,001

2,067

2,067

2,042

1,968

2,035

2,262

2,143

2,230

1,947

2,107

2,183

2,155

,2219

Altitu

-1,261

-1,168

-1,123

-1,352

-1,198

-1,171

-1,052

-1,080

-1,185

-1,051

-1,092

-1,107

-1,087

-1,048

-1,115

-1,342

-1,453

-1,340

-1,077

-1,107 

-1,213

-1,175 

-1,229
Table 1 . Core log analysis data Continued

[YYYYMMDD, year, month, day; DDMMSS, degrees, minutes, seconds; all units for depth, altitude, and thickness are in feet; depth and a

o 

o

(D

0 

(O

£tt

SL

CO55'

Q.

3

^

Site 

number 

(fig. 6)

93

94

95

96

97

98

99

100

101

102

103

104

105

106

107

108

109

110

111

112

113

114

115

Date drilled 

(YYYYMMDD)

19800823

19801003

19800919

19800910

19800927

19800919

19800912

19800920

19800927

19801011

19801018

19801002

19801211

19801209

19801122

19801018

19800000

19801108

19801111

19801112

19801217

19801230

19801230

Latitude 

(DDMMSS)

364902

365150

365051

365417

365406

365358

365512

365519

365528

365444

365524

365532

365203

365156

365543

365510

365502

365456

365604

365559

364850

365546

365542

Longitude 

(DDMMSS)

912047

911716

. 911701

912028

912031

912042

912046

912041

912040

911914

911836

912026

911304

912231

912132

911843

911849

911858

911945

911942

911907

912139

912125

Mining company 

borehole 

identification

AM AX 80 1-093

AM AX 80 1-094

AM AX 80 1-095

AM AX 80 1-096

AM AX 80 1-097

AM AX 80 1-098

AM AX 80 1-099

AM AX 80 1-100

AMAX 801-101

AMAX 801 -102

AMAX 801 -103

AMAX 801 -104

AM AX 801 -105

AMAX 801 -106

AMAX 801 -107

AMAX 801 -108

AMAX 801 -109

AMAX 801-110

AMAX 801-111

AMAX 801-112

AMAX 801-1 14

AMAX 801-1 15

AMAX 801-1 16

Local well number

T25NR04W24CAC1

T25NR03W04ACC1

T25NR03W09DAB1

T26N R04W 24DBC1

T26NR04W24DCC1

T26N R04W 25BAB 1

T26NR04W 13CAC1

T26N R04W 1 3CAB 1

T26N R04W 1 3BDB 1

T26NR03W 19ABC2

T26NR03W 17BCD1

T26N R04W 1 3ACB 1

T25NR02W06BAB1

T25NR04W03ACD1

T26NR04W 14ABB1

T26NR03W 17CBC1

T26NR03W 18DDA3

T26NR03W 18DDC1

T26NR03W07CBC1

T26NR03W07C 1

T25NR03W 19DDC1

T26NR04W 14BAA1

T26NR04W 14ABA

A

lan
g Table 1. Core log analysis data Continued

[YYYYMMDD, year, month, day; DDMMSS, degrees, minutes, seconds; all units for depth, altitude, and thickness are in feet; depth and altitude r

o

CD

positional Em

^

3

3

(0

3

S5

£to'

2 o

0)

3

a

(D

o'

SL

I

Q.

2

o' 

0

o

a

C

a

!

1

s

0)

H

0)5'

1

§

SL 

 n

o

3

</>

255'

(0

o

C

Site 

number 

(fig. 6)

93

94

95

96

97

98

99

100

101

102

103

104

105

106

107

108

109

110

111

112

113

114

115

Derby-Doerun Dolomite

Depth

1,193

1,279

1,505

1,429

1,399

1,385

1,387

1,381

1,413

1,390

1,291

1,334

1,467

1,533

1,412

1,221

1,237

1,296

1,301

1,308

1,564

1,412

1,393

Altitude

-613

-639

-675

-519

-509

-545

-487

-481

-453

-480

-351

-434

-497

-547

-462

-381

-327

-396

-421

-378

-639

-452

-448

Thickness

97

67

78

63

87

72

59

67

75

70

65

68

70

99

85

60

75

63

61

56

44

83

83

Thickness of St. 

Davis Formation Francois confining unit Bonneterre Formation

Depth

1,290

1,346

1,583

1,492

1,486

1,457

1,446

1,448

1,488

1,460

1,356

1,402

1,537

1,632

1,497

1,281

1,312

1,359

1,362

1364

1,608

1,495

1,476

Altitude

-710

-706

-753

-582

-596

-617

-546

-548

-528

-550

-416

-502

-567

-646

-547

-441

-402

-459

-482

-434

-683

-535

-531

Thickness

221

213

196

203

200

213

206

197

212

189

185

206

217

209

197

192

180

191

152

195

266

197

198

Total

318

280

274

266

287

285

265

264

287

259

250

274

287

308

282

252

255

254

213

251

310

280

281

Net shale Depth

1,511

102 1,559

1,779

74 1,695

77 .1,686

89 1,670

73 1,652

73 1,645

1,700

1,649

1,541

41 1,608

1,754

104 1,841

1,694

57 1,473

1,492

1,550

1,514

1,559

114 1,874

1,692

1,674

Altitude

-931

-919

-949

-785

-796

-830

-752

-745

-740

-739

-601

-708

-784

-855

-744

-633

-582

-650

-634

-629

-949

-732

-729

Thickness

437

427

438

424

418

413

418

407

405

417

413

406

422

412

398

239

382

426

430

407

398

Lamotte 

Depth

1,948

1,986

2,217

2,119

2,104

2,083

2,070

2,052

2,105

2,066

2,021

2,160

2,263

2,106

1,871

1,731

1,932

1,940

2,304

2,099

2072

Altitu

-1,368

-1,346

-1,387

-1,209

-1,214

-1,243

-1,170

-1,152

-1,145

-1,156

-1,121

-1,190 

-1,277

-1156

-1,031 

-821 

-1,032 

-1,060

-1,379

-1,139

-1,127
Table 1 . Core log analysis data Continued

[YYYYMMDD, year, month, day; DDMMSS, degrees, minutes, seconds; all units for depth, altitude, and thickness are in feet; depth and al

o 

o

(D

6"

(O

0)

SL

(055'

Q. 

0)

sr

^

Site 

number 

(fig. 6)

116

117

118

119

120

121

122

123

124

125

126

127

128

129

130

131

132

133

134

135

136

137

138

Date drilled 

(YYYYMMDD)

19801229

19810116

19810110

19810122

19810130

19810207

19810226

1 98 1 0305

19810307

19810311

19810313

19810321

19810321

19810330

19810416

19810406

19810416

19810417

19810425

19810504

19810727

19810606

19810613

Latitude 

(DDMMSS)

365207

365155

365205

365041

365233

365136

365210

365250

365809

365543

365543

365111

365131

365114

365602

365601

365612

365505

365235

365255

365642

365031

365640

Longitude 

(DDMMSS)

912203

912215

912103

912015

912044

912133

911920

911915

912214

912107

912146

912035

912206

912128

911933

911950

911928

912114

911930

912030

912204

912320

911910

Mining company 

borehole 

identification

AMAX

AMAX

AMAX

AMAX

801-

801-

801-

801-

AM AX 801-

AMAX

AMAX

AMAX

801-

801-

801-

AMAX 801-

AMAX

AMAX

AMAX

AMAX

AMAX

AMAX

AMAX

AMAX

AMAX

AMAX

AMAX

AMAX

AMAX

AMAX

801-

801-

801-

801-

801-

801-

801-

801-

801-

801-

801-

801-

801-

801-

117

118

119

120

121

122

123

124

125

126

127

128

129

131

132

133

134

135

136

137

138-

139

142

Local well number

T25N

T25N

T25N

T25N

R04W02BBC1

R04W03ADD1

R04W01BBC1

R04W 12DDB1

T26NR04W36CAC1

T25NR04W02DCB1

T25NR03W06AB1

T26N

T27N

T26N

T26N

T25N

T25N

T25N

T26N

T26N

T26N

T26N

T26N

T26N

T26N

T25N

T26N

R03W31ACB1

R04W34ADA1

R04W 14AAA1

R04W 14BAB1

R04W 12BDA1

R04W02CCC1

R04W 11ABD1

R03W07C 2

r

R03W07CBC1

R03W 07DBB 1

R04W 14DDB1

R03W31CAD1

R04W36ACB1

R04W02CCCI

R04W 16AAA1

R03W06DCC1

Al

lan
g Table 1. Core log analysis data Continued

[YYYYMMDD, year, month, day; DDMMSS, degrees, minutes, seconds; all units for depth, altitude, and thickness are in feet; depth and altitude 

positional Em

 ^

3

3

(D

3

5

£<5'

S o

3-

0)

3

Q.

o'

SL

I

"o.

i

o' 

O

O

Q.

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f

i

D)

i5'

z

o>o'

3

SL 

 n

o

3

(A

255'

(0

o

c

2.

Site 

number

(fig. 6)

116

117

118

119

120

121

122

123

124

125

126

127

128

129

130

131

132

133

134

135

136

137

138

Derby-Doerun

Depth

1,532

1,521

1,546

1,528

1,518

1,523

1,519

1,485

1,481

1,396

1,434

1,544

1,404

1,481

1,283

1,303

1,374

1,456

1,524

1,498

1,340

1,246

1,390

Altitude

-553

-561

-586

-608

-578

-593

-584

-585

-461

-451

-444

-604

-549

-591

-413

-418

-424

-496

-644

-593

-415

-566

-440

Dolomite

Thickness

94

112

67

70

97

110

98

70

74

68

88

81

98

74

72

49

68

74

73

70

89

67

66

Thickness of St. 

Davis Formation Francois confining unit Bonneterre Formation

Depth

1,626

1,633

1,61.3

1,598

1,615

1,633

1,617

1,555

1,555

1,464

1,522

1,625

1,502

1,555

1,355

1,352

1,442

1,530

1,597

1,568

1,429

1,313

1,456

Altitude

-647

-673

-653

-678

-675

-703

-682

-655

-535

-519

-532

-685

-647

-665

-485

-467

-492

-570

-717

-663

-504

-633

-506

Thickness

214

198

224

223

199

192

207

216

203

201

197

214

201

219

201

201

200

198

203

201

204

222

196

Total

308

310

291

293

296

_

302

305

286

277

269

285

295

299

293

273

250

268

272

276

271

293

289

262

Net shale Depth

1,840

1,831

1,837

1,821

63 1,814

75 1,825

79 1,824

76 1,771

60 1,758

66 1,665

1,719

1,839

1,703

1,774

1,556

1,553

1,642

64 1,728

1,800

82 1,769

1,633

1,535

1,652

Altitude

-861

-871

-877

-901

-874

-895

-889

-871

-738

-720

-729

-899

-848

-884

-686

-668

-692

-768

-920

-864

-708

-855

-702

Thickness

400

415

409

428

425

417

425

378

400

400

427

424

426

376

361

390

412

428

417

388

405

395

Lamotte 

Depth

2,240

2,246

2,246

2,249

2,239

2,242

2,249

2,136

2,065

2,119

2,266

2,127

2,200

1,932

1,914

2,032

2,140

2,228

2,186

2,021

1,940

2,047

Alti

-1,26

-1,28

-1,28

-1,32

-1,29

-1,31

-1,31

-1,11

-1,12

-1,12

-1,32

-1,27

-1,31

-1,06

-1,02

-1,08

-1,18

-1,34

-1,28

-1,09

-1,26

-1,09
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Core log analysis data 51
en Table 1. Core log analysis data Continued

[YYYYMMDD, year, month, day; DDMMSS, degrees, minutes, seconds; all units for depth, altitude, and thickness are in feet; depth and altitude 

positional Env

o

I

3

W

I

(O

S

T3

D)

3

Q.

s. o'

SL

X

'o.

c

o' 

O

O

a

c

o

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(D

2

0>

5-

I

3 

Z

Q)

5'

3

SL 

 n

o

(D

wj*

S55'

(0

o

c

Site 

number 

(fig- 6)

139

140

141

142

143

144

145

146

147

148

149

150

151

152

153

154

155

156

157

158

159

160

161

Derby-Doerun

Depth

1,388

1,269

1,358

1,286

1,506

1,528

1,488

1,390

1,322

1,563

1,404

1,420

1,421

1,507

1,542

1,306

1,507

1,498

1,390

1,540

Altitude

-408

-416

-438

-486

-551

-608

-578

-415

-457

-579

-529

-510

-576

-472

-615

-371

-577

-568

-450

-580

Dolomite

Thickness

73

69

66

68

87

88

86

69

79

74

79

80

90

93

68

144

57

69

80

63

Thickness of St. 

Davis Formation Francois confining unit Bonneterre Formation

Depth

1,461

1,338

1,424

1,354

1,593

1,616

1,574

1,459

1,401

1,637

1,483

1,500

1,511

1,600

1,610

1,450

1,564

1,567

1,470

1,603

Altitude

-481

-485

-504

-554

-638

-696

-664

-484

-536

-653

-608

-590

-666

-565

-683

-515

-634

-637

-530

-643

Thickness

197

194

198

195

214

203

200

203

199

208

195

202

213

192

206

206

141

170

194

152

Total

270

263

264

263

301

291

286

272

278

282

274

282

303

285

274

350

198

239

274

215

Net shale Depth

1,658

1,532

1,622

1,549

85 1,807

1,819

1,774

1,662

1,600

1,845

125 1,678

99 1,702

74 1,724

90 1,792

104 1,816

1,656

1,705

1,737

1,664

1,755

1,713

1,555

1,714

Altitude

-678

-679

-702

-749

-852

-899

-864

-687

-735.

-861

-803

-792

-879

-757

-889

-721

-775

-807

-724

-795

-693

-445

-689

Thickness

412

416

418

401

402

419

420

397

365

341

403

422

404

430

363

374

391

392

Lamotte 

Depth

2,070

1,948

2,040

1,950

2,209

2,238

2,194

1,997

2,210

2,019

2,105

2,146

2,196

2,246

2,019

2,038

2,104

2,106

Altit

-1,09

-1,09

-1,12

-1,15

-1,25

-1,31

-1,28

-1,13

-1,22

-1,14

-1,19

-1,301

-1,16

-1,31

-1,08

-1,09

-1,08

-1,08
Table 1 . Core log analysis data Continued

[YYYYMMDD, year, month, day; DDMMSS, degrees, minutes, seconds; all units for depth, altitude, and thickness are in feet; depth and al

o 

o

Jo

6"

(O

Q>

3

9L

ww'

Q. 

Q>

ST

en

Site 

number 

(fig. 6)

162

163

164

165

166

167

168

169

170

171

172

173

174

175

176

177

178

179

180

181

182

183

184

Date drilled 

(YYYYMMDD)

19800508

19800829

19801024

19801104

19810303

19810319

19810523

19810415

19810506

19810604

19840709

19840730

19840816

19841200

19810916

19820513

19810512

19791129

19800106

19800125

19631007

19631119

19631231

Latitude 

(DDMMSS)

365618

365602

365603

365638

365701

365741

370148

365753

365557

370140

365622

365825

365838

365552

370007

365630

365742

370145

370150

370127

370121

370101

370037

Longitude 

(DDMMSS)

911655

912000

912034

912144

911402

912131

912117

912054

911319

911926

912012

912055

912054

912035

911656

911232

911539

911902

911832

911821

911803

911731

911801

Mining company 

borehole 

identification

ASARCOPK-14

ASARCO PK- 15

ASARCOPK-17

ASARCO PK- 18

ASARCO PK-26

ASARCO PK-27

ASARCO PK-28

ASARCO PK-30

ASARCO PK-32

ASARCO PK-35

AMSELCO PK-42

AMSELCO PK-43

AMSELCO PK-44

ASARCO PK-46

COMINCO SF-25

COMINCO SF-28

COMINCO SF-6

COMINCO WN-21

COMINCO WN-22

COMINCO WN-23

PH DDG 068689

PH DDG 068689

PH DDG 068691

Local well number

T26NR03W09ACA1

T26NR04W 12DAD1

T26NR04W 12CAD1

T26NR04W 11BAB1

T26NR03W01BDC1

T27NR04W35DCB1

T27NR04W 11ABA1

T27N R04W 36CBB 1

T26N R02W 07DBB 1

T27NR03W07BCA1

T26NR04W 12ADB1

T27N R04W 25CCC2

T27NR04W25CBC1

T26NR04W 12CDD1

T27NR03W 16DCC1

T26NR02W06DCD1

T27NR03W34DAC1

T27NR03W07ABC1

T27N R03W 08BBB 1

T27NR03W08BCD1

T27NR03W08C1

T27NR03W08D1

T27NR03W 17A1

Al

lan
Table 1. Core log analysis data Continued

[YYYYMMDD, year, month, day; DDMMSS, degrees, minutes, seconds; all units for depth, altitude, and thickness are in feet; depth and altitude 

Depositional Em

 ^

3

3

(D

3

W

Q>

u o

0)

3

Q.

(D

o'

SL

I

Q.

Q)

o' 

O

O

Q.

C

s

1

(0

S

1

3 

Z

fi)

6'

3

SJ. 

 n

o

(5w

3(0*

(0 

O

C

Site Derby-Doerun Dolomite 

number 

(fig. 6) Depth Altitude Thickness

162 1,200 -195 319

163

164

165

166 1,337 -367 204

167 1,318 -318 257

168

169

170 1,352 -477 162

171

172

173 1,400 -375 142

174

175

176 1,100 -150

177 1,190 -460 197

178 1,413 -428 149

179

180

181 1,156 -91

182 1,105 -50 305

183 970 -52 348

184 1,116 -195 209

Thickness of St. 

Davis Formation Francois confining unit Bonneterre Formation

Depth

1,519

1,386

1,541

1,575

1,600

1,514

1,412

1,542

1,513

1,422

1,387

1,562

1,410

1,318

1,325

Altitude

-514

-396

-571

-575

-535

-639

-497

-517

-503

-422

-657

-577

-355

-400

-404

Thickness

201

200

102

135

142

195

165

192

191

95

153

80

87

Total

520

306

392

357

334

456

292

302

357

428

296

Net shale Depth

1,720

1,647

1,586

1,485

1,643

1,710

1,607

1,742

1,709

1,464

1,577

1,734

1,704

1,556

1,482

1,715

1,358

1,499

1,513

1,398

1,412

Altitude

-715

-697

-596

-505

-673

-710

-557

-677

-834

-469

-662

-709

-694

-606

-752

-730

-278

-439

-448

-480

-491

Thickness

439

400

477

385

393

406

400

446

405

416

417

402

415

448

Lamotte 

Depth

2,159

2,047

2,120

2,095

2,000

2,148

2,109

1,910

1,982

2,120

1,973

1,884

2,130

1,860

Altitu

-1,154

-1,097

-1,150

-1,095

-950

-1,083

-1,234

-915

-1,067

-1,110

-1,023

-1,154

-1,145

-939 
Table 1 . Core log analysis data Continued

[YYYYMMDD, year, month, day; DDMMSS, degrees, minutes, seconds; all units for depth, altitude, and thickness are in feet; depth and a

o 

o

<3

6"

(0

Q>

3

5L

w55°

Q. 

Q)

ET

en

Site 

number

(fig. 6)

185

186

187

188

189

190

191

192

193

194

195

196

197

198

199

200

201

202

203

204

205

206

207

Date drilled 

(YYYYMMDD)

19631017

19680626

19760401

19761216

19770223

19770405

19770510

19770517

19770609

19770623

19770825

19790222

19790614

19790626

19790802

19810511

19811209

19811230

19820126

19820324

19820401

19820429

Latitude 

(DDMMSS)

370004

370220

370254

365612

365936

365754

370112

365918

365918

370027

370247

365943

365802

365247

370023

370125

370248

365207

365205

365359

365358

365404

365430

Longitude 

(DDMMSS)

911417

912019

912627

910810

911610

911130

911915

911443

911048

912158

912044

911727

911628

911530

912423

912242

912000

911958

912310

911815

911459

911632

911632

Mining company 

borehole 

identification

PH DDG 068692

PHDDG27N4W1-1

ST JOE 68W44

ST JOE 76W05

STJOE76W20

STJOE77W02

STJOE77W03

STJOE77W05

STJOE77W06

ST JOE 77W07 ,

STJOE77W08

STJOE77W11

ST JOE 79W03

ST JOE 79W05

STJOE79W06

ST JOE 79W08

STJOE81W09

ST JOE 82W03

STJOE82W07

STJOE82W11

STJOE82W19

STJOE82W21

STJOE82W25

Local well number

T27NR03W 14D1

T27NR04W01CAA1

T28N R05W 36DDB 1

T26NR02W 11AB 1

T27N R03W 22CA 1

T27N R02W 32AC 1

T27N R03W 07CC 1

T27N R03W 23DC 1

T27NR02W21CA 1

T27NR04W 14CB 1

T28N R04W 36CC 1

T27NR03W21BC 1

T27N R03W 34BC 1

T26N R03W 35BC 1

T27NR04W 17DA 1

T27NR04W 10CA 1

T28N R04W 36DD 1

T25NR03W06BB1

T25NR04W03BB1

T26NR03W29ABB1

T26NR03W23CDD1

T26NR03W22CCC1

T26NR03W22BCC1

A

lan
«; Table 1. Core log analysis data Continued

[YYYYMMDD, year, month, day; DDMMSS, degrees, minutes, seconds; all units for depth, altitude, and thickness are in feet; depth and altitude r

positional Environmeni

w

3 

(5*

0> o

Q>

3

a

o'

2L

X*a. 

§

o'

O 

O

a

|

f

1

D)

Q)

in National F

o

(A

"2

55'

(0

O

c

Site 

number 

(fig- 6)

185

186

187

188

189

190

191

192

193

194 

195

196

197

198

199

200

201 

202 

203

204

205

206

207,

Derby-Doerun

Depth

1,149

1,183

1,227

1,140

1,255

1,387

1,288

1,252

1,130

1,360 

1,216

1,343

1,365

1,272

1,403

1,448

1,231 

1,528 

1,266

Altitude

-235

-153

-310

-509

-304

-626

-265

-444

-399

-327 

-107

-442

-494

-566

-322

-342

-116 

-568 

-521

Dolomite

Thickness

289

284

119

156

189

124

149

257

222

105 

174

103

51

58

158

164

140 

91 

87

Thickness of St. 

Davis Formation Francois confining unit Bonneterre Formation

Depth

1,438

1,467

1,346

1,296

1,444

1,511

1,437

1,509

1,352

1,465 

1,390

1,446

1,416

1,330

1,561

1,612

1,371 

1,619 

1,353

1,517

1,370

1,540

Altitude

-524

-437

-429

-665

-493

-750

-414

-701

-621

-432 

-281

-545

-545

-624

-480

-506

-256 

-659 

-608

-597

-580

-575

Thickness

86

75

232

217

143

49

187

41

147

256 

133

218

314

323

271

233

166

232 

265

202

176

203

Total

375

359

351

373

332

173

336

298

369

361 

307

321

365

381

429

397

306

323 

352

Net shale Depth

1,524

1,542

1,578

1,513

1,587

1,560

1,624

1,550

1,499

1,721 

1,523

1,664

1,730

1,653

1,832

1,845

24 1,537 

139 1,851 

1,618

1,719

83 1,546

1,457

1,743

Altitude

-610

-512

-661

-882

-636

-799

-601

-742

-768

-688 

-414

-763

-859

-947

-751

-739

-422 

-891 

-873

-799

-756

-487

-778

Thickness

406

466

286

298

320

229

328

367

256 

234

303

328

377

310

294

421 

385

389

419

399

Lamotte S

Depth

1,930

2,008

1,864

1,811

1,907

1,853

1,878

1,866

1,977 

1,757

1,967

2,058

2,030

2,142

2,139

2,272 

2,003

2,108

1,965

2,142

Altitu

-1,016 

-978

-947

-1,180

-956

-830

-1,070

-1,135

-944 

-648 

-1,066

-1,187

-1,324

-1,061

-1,033

-1,312 

-1,258

-1,188

-1,175

-1,177
Table 1 . Core log analysis data Continued

[YYYYMMDD, year, month, day; DDMMSS, degrees, minutes, seconds; all units for depth, altitude, and thickness are in feet; depth and alti

o 

o

<3

6"

CO

&>

3

SL

COco"

0,

lu

ST

CJ1

Site 

number 

(fig. 6)

208

209

210

211

212

213

214

215

216

217

218

219

220

 221

222

223

224

225

226

227

228

229

230

Date drilled 

(YYYYMMDD)

19820609

19820826

19821012

19820112

19830209

19830330

19830415

19830516

19830531

19830725

19830810

19830825

19830907

19831017

19840703

19850122

19850130

19850827

19851014

19851011

19851205

19880629

19880727

Latitude 

(DDMMSS)

365339

364753

364724

370054

370405

365128

365419

365359

365036

364645

365209

365254

365135

370404

364658

365002

365021

365004

365655

365838

365001

364622

364859

Longitude 

(DDMMSS)

911823

911619

911324

911819

912202

912248

911632

911612

912220

911523

912417

912350

912310

912225

911536

912138

912137

912109

912156

912100

912131

911434

912007

Mining company 

borehole 

identification

ST JOE 82W27

STJOE82W31

ST JOE 82W34

STJOE83W06

ST JOE 83W09

STJOE83W12

STJOE83W14

STJOE83W15

STJOE83W17

STJOE83W25

STJOE83W30

STJOE83W34

STJOE83W35

ST JOE 83W44

STJOE84W44

STJOE85W09

STJOE85W11

STJOE85W31

STJOE85W35

STJOE85W37

STJOE86W02

STJOE88W03

STJOE88W04

Local well number

T26NR03W29BDD1

T25NR03W27CDD1

T25NR02W31BCC1

T27NR03W 17BBA1

T28NR04W27ADC1

T25NR04W03CD1

T26N R03W 22CBB 1

T26NR03W22CDD1

T25NR04W 10DDD1

T24NR03W02ABC1

T25NR04W04BCC1

T26NR04W33BDA1

T25N R04W 03CCB 1

T28NR04W27BDD1

T24N R03W 02BAA 1

T25NR04W 14DB 2

T25NR04W 14AB1

T25NR04W 14DA1

T26NR04W02CBD1

T27NR04W26DAD1

T25NR04W 14DB1

T24NR03W01BDC1

T25NR04W24DD1

Alt

land 
g Table 1. Core log analysis data Continued

[YYYYMMDD, year, month, day; DDMMSS, degrees, minutes, seconds; all units for depth, altitude, and thickness are in feet; depth and altitude r

positional Environment

I(5*

3

3-

0)

3 

Q.

3. o'

u.

X

^. 

3

lie Conductivi

f

(D

0)

Q)

in Nationi

_ 

 n

o

3

(0

2 . 55° 

u> O

c

Site 

number 

(fig. 6)

208

209 

210

211

212 

213

214

215

216

217 

218 

219

220

221

222

223

224 

225

226

227

228

229

230

Derby-Doerun Dolomite

Depth

1,150

1,312

1,056

1,282

1,174

1,420

1,544 

1,259 

1,177

1,022

1,266

1,405

1,447

1,598

1,537

Altitude

-610

-327

-6

-297

-389

-502

-684 

-329 

-217

18

-376

-408

-573

-788

-617

Thickness

65

120

194

60

99

128

139 

242 

386

233

58

49

88

90

112

Thickness of St. 

Davis Formation Francois confining unit Bonneterre Formation

Depth

1,495

1,215

1,432

1,250 

1,546

1,342

1,273

1,548

1,683 

1,501 

1,563

1,353

1,255

1,601

1,552

1,540 

1,271

1,324

1,454

1,535

1,688

1,649

Altitude

-625 ,

-675

-447

-200 

-621

-357

-488

-630

-823 

-571 

-603

-628

-215

-796

-640

-621 

-627

-434

-457

-661

-878

-729

Thickness

200

240

171

150

278

140

180

282

254 

337 . 

270

248

242

252

274

315 

305

314

289

267

254

312

Total

305

291

344

200

279

410

393 

579 

656

475

372

338

355

344

424

Net shale Depth

100 1,695

145 1,455 

89

27 1,603

1,400 

1,824

75 1,482

1,453

117 1,830

148 1,937 

156 1,838 

129 1,833

1,601

1,497

1,853

1,826

1,855 

1,576

96 1,638

58 1,743

1,802

1,942

159 1,961

Altitude

-825

-915

-618

-350 

-899

-497

-668

-912

-1,077 

-908 

-873

-876

-457

-1,048

-914

-936 

-932

-748

-746

-928

-1,132,

-1,041

Thickness

410

454

286

152 

375

346

460 

349 

296

384

211

464

421

366 

370

282

281

442

347

Lamotte 

Depth

2,105

1,909

1,889

1,552 

2,199

2,176

2,397 

2,187 

2,129

1,985

1,708

2,317

2,247

2,221 

1,946

1,920

2,024

2,384

2,308

Altitu

-1,235

-1,369

-904 

-502 

-1,274

-1,258

-1,537 

-1,257 

-1,169

-1,260

-668 

-1,512

-1,335

-1,302 

-1,302

-1,030

-1,027

-1,574

-1,388
Table 1 . Core log analysis data Continued

[YYYYMMDD, year, month, day; DDMMSS, degrees, minutes, seconds; all units for depth, altitude, and thickness are in feet; depth and a

o 

to 

o>

3 

0)

Site 

number

(fig. 6)

231

232

233

234

235

236

237

238

Boreholes in

VB1

VB2

VB3

VB4

VB5

Date drilled 

(YYYYMMDD)

19880808

19880817

19880912

19890405

19891206

19900321

19921130

19930203

Latitude 

(DDMMSS)

364849

365013

364816

364853

364628

364621

365116

365120

Longitude 

(DDMMSS)

912020

912140

911946

912103

911356

911315

912153

912204

Mining company 

borehole 

identification

STJOE88W05

ST JOE 88W06

ST JOE 88W09

STJOE89W01

ST JOE 89W22

ST JOE 90W03

STJOE93W08

STJOE93W18

Local well number

T25N R04W 24DD 2

T25N R04W 14AC1

T25NR03W30CAB1

T25NR04W24CCC1

T24NR03W01ADD1

T24NR02W06BDD1

T25NR04W 11BAC1

T25NR04W 11BBB1

Minimum

Maximum

A

lan

Viburnum Trend from which core samples were collected and sent for laboratory permeability analysis

372351

372209

372235

372027

371757

910717

911058

910920

910924

910846

ASARCO AC 37

ASARCO AC 45

ASARCO AC 84

ASARCO LC 503

ASARCOLC810

T31NR02W 11AAAC1

T31NR02W 17DBB1

T31NR02W 15CBBD1

T31NR02W34BBB1

T30NR02W 10DCD1
g

Table 1. Core log analysis data Continued

[YYYYMMDD, year, month, day; DDMMSS, degrees, minutes, seconds; all units for depth, altitude, and thickness are in feet; depth and altitude r

u 

O 

CO

itional Environment

w

3

5 D 

3"

a>

Q.

so'

9L

I

'a.

§

o'

O 

0

a

c 

o

Site 

number 

(fig. 6)

231

232

233

234

235 

236

237

238

Derby-Doerun Dolomite

Depth

1,500

1,516

1,592

1,501

1,498

970 

1,598

Altitude Thickness

-590 18

-626 99

-742 100

-536 108

-568 86

-788 18 

18 386

Thickness of St.

Davis Formation Francois confining unit Bonneterre Formation Lamotte 

Depth

1,521

1,518

1,615

1,250

1,692

1,609

1,584

1,171 

1,692

"^ Boreholes in Viburnum Trend from which core

(D

Q>

0) 5'

1

i

SL 

 n

o

(A

255' 

w 

O

c

VB1

VB2

VB3

VB4 

VB5

780

800

728

758 

965

380

470

372

242 

135

897

900

844

871 

1,065

Altitude Thickness Total Net shale Depth Altitude Thickness Depth Altitu

-651 313 1,834 -964 397 2,231 -1,361

-608 319 337 1,837 -927 386 2,223 -1,313

-725 296 395 1,911 -1,021 390 2,301 -1,411

-699 280 131 1,530 -979 386 1,916 -1,365

124 

-842 310 410 100 2,002 -1,152 448 2,450 -1,600

-644 283 391 1,892 -927 373 2,265 -1,300

-654 270 356 1,854 -924 390 2,244 -1,314

-878 41 173 24 1,358 -1,152 152 1,552 -1,600 

-200 337 656 162 2,002 -278 496 2,450 -502 

samples were collected and sent for laboratory permeability analysis

263

370

256

129

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Porosity, Vertical Permeability, and Vertical Hydraulic Conductivity Data 61
Table 2. Porosity, vertical permeability, and vertical hydraulic conductivity data

[DDR, Derby-Doerun Dolomite; DVS, Davis Formation; BNT, Bonneterre Formation, POT, Potosi Dolomite; C, carbonate rock; S, shale; B, both 

o m o 

o 

2.

6"

2L 

m3

I

(D

i

Q>

 n

D)

 o

3"

Q)

3

Q.

(D

3. o'

SL

Z

a.

c_

o' 

0

O

a

£ _

f

i

03

S0)5" 

z

Si o'

3

Si

?

3

(A

55'

(0

O

than; %, percent] 

Sample

number

Mining 

company 

borehole

identification Formation

Sample

depth,

in feet

Confining 

pressure, in 

pounds per

square inch

(gauged)1

Porosity,

in

percent

Density, 

in grams

per cubic

centimeter

Vertical 

permeability,

in

millidarcies

Vertical 

hydraulic 

conductivity,

in feet per

second Lithology 

St. Joe Lead Company Continued

19

20

21

22

23

24

25

26

27

28

29

30.

31

32

33

34

83W34

83W34

83W34

83W34

83W34

82W03

82W03

82W03

82W03

82W03

82W03

82W27

82W27

82W27

82W27

82W27

DVS

DVS

DVS

DVS

DVS

DDR

DDR

DVS

DVS

DVS

BNT

DDR

DDR

DVS

DVS

DVS

1,573

1,685

1,725

1,785

1,791

1,564

1,581

1,624

1,692

1,841

1,894

1,445

1 ,479

1,522

1,597

1,679

1,190

1,280

1,310

1,350

1,360

1,190

1,200

i

1,230

1,280

1,400

1,440

1,100

1,120

1,150

1,210

1,280

1.93

5.32

5.61

3.28

5.99

.61

.80

2.37

3.49

.4.93

3.18

1.08

1.16

5.00

3.23

6.7

2.754

2.689

2.719

2.801

2.754

2.825

2.820

2.820

2.676

2.750

2.804

2.832

2.814

2.675

2.721

2.782

<0.000001

.000054

.000051

<.000001

<.000001

<.000001

<.000001

.000035

<.000001

.000098

<.000001

<.000001

<.000001

.000019

<.000001

.000036

<3.17X 1Q-' 4

1.71 X 10' 12

1.62 X 10' 12

<3.17X 10' 14

<3.17X 10' 14

<3.17X 10' 14

<3.17X lO' 14

1.11 X JO' 12

<3.17X 10' 14

3.11 X 10' 12

<3.17X 1Q-' 4

<3.17X 10' 14

<3.17X 10' 14

6.15 X 10' 13

<3.17X 10' 14

1.14X 10-' 2

C

S

S

C

B

C

C

C

S

S

C

C

C

S

B

S

Dolomitic 

Shale

Shale

Digitate lim

Shale with 

Dense dolo

Dense dolo

Dolomitic 

Shale

Shale

Dolomitic 

Dolomitic 

Dolomitic 

Shale with 

Shale 60% 

Shale 90% 

Amax Lead Company

35

36

37

801-002

801-002

801-002

POT

DDR

DVS

1,425

1,479

1,508

1,080

1,120

. 1,140

2.07

3.54

1.73

2.824

2.843

2.756

0.000047

.000004

<.000001

1.49X KT 12

1.27X10' 13

<3.17X 10' 14

C

C

C

Dolomitic 

Dolomitic 

Dolomitic 
Table 2. Porosity, vertical permeability, and vertical hydraulic conductivity data

[DDR, Derby-Doerun Dolomite; DVS, Davis Formation; BNT, Bonneterre Formation, POT, Potosi Dolomite; C, carbonate rock; S, shale; B, b

than; %, percent]

Sample 

number

Mining 

company 

borehole 

identification Formation

Sample 

depth, 

in feet

Confining 

pressure, in 

pounds per 

square inch 

(gauged)1

Porosity, 

in 

percent

Density, 

in grams 

per cubic 

centimeter

Vertical 

permeability, 

in 

millidarcies

Vertical 

hydraulic 

conductivity, 

in feet per 

second Lithology 

Amax Lead Company Continued

TJ 

O

5w

»

o'

SL

 o

(D 

0)

2!

1

D>

3

Q.

(D

3. o'

X

a

1 o' 

0

O

a

0

<

D

0)

of

, 38

39

40

41

42

43

44

45

46

47

48

49

50

51

52

53

54

55

56

57

801-002

801-002

801-002

801-009

801-009

801-009

801-009

801-009

801-009

t

801-010

801-010

801-010

801-010

801-010

801-010

801-016

801-016

801-016

801-016

801-016

DVS

DVS

DVS

DDR

DVS

DVS

DVS

DVS

DVS

DDR

DVS

DVS

DVS

DVS

DVS

DDR

DDR

DVS

DVS

DVS

1,521

1,544

1,578

1,409

1,435

1,457

1,485

1,512

1,535

1,492

1,512

1,536

1,564

1,585

1,608

1,528

1,560

1,602

1,630

1,649

1,150

1,170

1,200

1,070

1,090

1,100

1,125

1,150

1,160

1,130

1,150

1,160

1,190

1,200

1,220

1,160

1,180

1,210

1,240

1,250

.73

4.02

.88

4.57

2.31

2.59

2.61

4.49

2.15

2.69

5.14

7.38

2.65

4.52

.82

1.23

.71

3.13

2.39

2.51

2.714

2.680

2.746

2.851

2.835

2.641

2.696

2.662

2.701

2.843

2.850

2.695

2.699

2.666

2.719

2.840

2.796

2.719

2.659

2.687

0.000010

.000022

<.000001

.0118

.000025

.000021

.000043

<.000001

.000019

.000015

.00231

.000080

.000016

<.000001

.000016

! .000016

.000005

<.000001

<.00000l

<.000001

3.17 X 10' 13

6.97 X 10' 13

<3.17X 10' 14

3.74 X 10' 10

7.83 X 10' 13

6.56 X 10' 13

1.37 X 10' 12

<3.17X 10' 14

5.86 X 10' 13

4.82 X 10' 13

7.31 X lO' 11

2.52 X 10' 12

5.10X ID' 13

<3.17X 10' 14

5.17X 10' 13

4.91 X 10" 13

1.65X JO' 13

<3.17X 10' 14

<3.17X 10' 14

<3.17X 10' 14

C

B

C

C

C

S

C

S

B

C

C

C

B

S

B

C

S

B

S

B

Limy mu

Shale wit

Limy wa

Dolomiti

Dolomiti

Shale

Limey m

Shale

Limey m

Dolomiti

Dolomiti

Dolomiti

Limey m

Shale

Limey pa

Dolomiti

Shale

Shale wit

Shale

Limey w
C/3 

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64 Depositional Environment, Stratigraphy, and Vertical Hydraulic Conductivity of the Mark Twain National Forest, Missouri
 <

o

Q)

Table 2. Porosity, vertical permeability, and vertical hydraulic conductivity data

[DDR, Derby-Doerun Dolomite; DVS, Davis Formation; BNT, Bonneterre Formation, POT, Potosi Dolomite; C, carbonate rock; S, shale; B, bo

than; %, percent]

Sample . 

number

Mining 

company 

borehole 

identification Formation

Sample 

depth, 

in feet

Confining 

pressure, in 

pounds per 

square inch 

(gauged)1

Porosity, 

in 

percent

Density, 

in grams 

per cubic 

centimeter

Vertical 

permeability, 

in 

millidarcies

Vertical 

hydraulic 

conductivity, 

in feet per 

second Lithology 

Asarco Continued

77

78

79

80

81

82

83

84

85

86

87

88

AC 84

AC 84

AC 84

LC503

LC503

LC503

LC503

LC810

LC810

LC810

LC810

LC810

DVS

DVS

DVS

DDR

DVS

DVS

DVS

DDR

DDR

DVS

DVS

DVS

878

946

1,003

806

910

976

1,006

1,023

1,060

1,096

1,159

1,204

670

720

760

610

690

740

760

780

810

830

880

920

10.7

.36

8.18

1.69

5.75

9.05

2.14

3.24

3.99

7.25

2.19

1.59

2.718

2.715

2.799

2.818

2.760

2.689

2.701

2.794

2.813

2.711

2.711

2.699

0.000030

.000012

.000134

.000106

<.000001

<.000001

<.000001

.000062

.000009

<.000001

<.000001

<.000001

9.41 X 10' 13

3.81 X 10' 13

4.25 X 10' 12

3.35 X 10' 12

<3.17X 10' 14

<3.17X 10' 14

<3.17X 10' 14

1.96 X 10' 12

2.86 X 1Q-' 3

<3.17X 10' 14

<3.17X 10" 14

<3.17X 1Q-' 4

S

C

B

C

S

s

B

B

B

S

C

B

Shale

Limey wa

Shale wit

Dolomitic 

Shale (90

Shale

Limey wa

Dolomitic 

Dolomitic 

Shale

Limey mu

Limey mu

'The applied confining pressure is approximately equal to the pressure calculated using a gradient of 0.758 pounds per square inch per foot of depth.

U.S. GOVERNMENT PRINTING OFFICE: 2000-555-181/40045
KLEESCHULTE AND SEEGER Depositional Environment, Stratigraphy, and Vertical Hydraulic Conductivity USGS 

of the St. Francois Confining Unit in the Fristoe Unit of the Mark Twain National Forest, Missouri