Hydraulic Conductivity of the St. Francois Confining Unit in the … · 2011. 8. 25. · hydraulic conductivity for the St. Francois confin ing unit in the study area was calculated

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Depositional Environment, Stratigraphy, and Vertical Hydraulic Conductivity of the St. Francois Confining Unit in the Fristoe Unit of the Mark Twain National Forest, Missouri

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Water-Resources Investigations Report 00-4037

Prepared in cooperation with theU.S. Department of Agriculture, Forest Service,U.S. Department of the Interior, Bureau of Land Management,U.S. Environmental Protection Agency, andMissouri 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


By Michael J. Kleeschulte 1 and Cheryl M. Seeger2

Water-Resources Investigations Report 00-4037

In cooperation with theU.S. Department of Agriculture, Forest Service,U.S. Department of the Interior, Bureau of Land Management,U.S. Environmental Protection Agency, andMissouri 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 purchasedfrom:

District ChiefU.S. Geological Survey U.S. Geological Survey1400 Independence Road Branch of Information ServicesMail Stop 100 Box 25286Rolla, 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


By Michael J. Kleeschulte 1 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 envi ronment 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 Precam- brian 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 transi-

U.S. Geological Survey ^Missouri Department of Natural Resources

tion from shaley deposits with a limited stromato lite zone to carbonate with more frequent stromatolites suggest a general shallowing of the sequence as the Bonneterre Formation was depos ited.

The Bonneterre Formation-Davis Forma tion contact denotes abrupt intrashelf basin devel opment 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 Derby- Doerun Dolomite was formed during a pair of car bonate 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 northwest- southeast. 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 Sand stone, 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 dolostoneât the top and base of the forma- . tion. The shales restricted the flow of dolomitizing fluids from reaching most Davis Formation lime stones. 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 sim ilar 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. Fran cois 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 con ductivity of samples collected from the Derby- Doerun Dolomite and Davis Formation in the Fris toe 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.

In the Viburnum Trend, there is a statisti cally significant difference (p-value = 0.006) between the ranked vertical hydraulic conductivity of the Derby-Doerun Dolomite and Davis Forma tion. Although the vertical hydraulic conductivity of both formations is small, the median vertical hydraulic conductivity of the Derby-Doerun Dolo mite 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 con ductivity than shales.

The net shale thickness is not the single con trolling 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 carbonate- shale thickness is important in determining the effectiveness of the confining unit.

The estimated range of effective vertical hydraulic conductivity for the St. Francois confin ing unit in the study area was calculated to be a maximum of 1 x 10" 12 foot per second and a min imum 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 devel oped 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 ongo ing 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. Depart ment of Agriculture, Forest Service and U.S. Depart ment 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 well- developed karst terrain with an extensive network of solution-enlarged fractures ranging from small chan nels to large conduits. The two largest springs in Mis souri 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

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an annual mean discharge of 346 ft /s (Hauck and oth ers, 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 con cerns 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 (Jeffer son City Dolomite to the base of the Lamotte Sandstone) overlie the igneous granites and rhyolites of the Precam- brian basement rock in the study area (fig. 2). The forma tions from the Jefferson City Dolomite to the Eminence Dolomite are predominant at land surface; these rocks, together with the Potosi Dolomite, form the Ozark aqui fer, 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 Derby- Doerun Dolomite and the Davis Formation. This confin ing 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 Depart ment 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 con fining 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 cur rently (2000) active, the geology and depositional envi ronment in these two areas during Late Cambrian time when these formations were deposited may be similar.

Introduction

91°30' 90°30'

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Base from U.S. Geological Survey digital data, 1:100,000, 1994 Universal Transverse Mercator projection, Zone 15

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EXPLANATION

H ST. FRANCOIS MOUNTAINSm PRECAMBRIAN-ROCK OUTCROP

[3D PROSPECTING AREA

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, . BOREHOLE AND IDENTIFICATIONVR ,NUMBER (table 1)

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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'

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

Introduction 5

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Extensive studies performed in the Viburnum Trend by Palmer (1991) and Thacker and Anderson (1979) indi cate the environment that existed when the St. Francois confining unit was deposited affects the mud content of deposited sediments, which in turn affects the confin ing ability of the formations.

In 1990, the first of several consecutive geohydrologic studies was started in and adjacent to the Fris- toe 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 ground- water trough between Hurricane Creek, which is adja cent to the prospecting area, and Big Spring. This indi cates 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 tran sitional contact with the overlying Davis Formation of the St. Francois confining unit. By including a descrip tion of the formations of the St. Francois aquifer, the entire interval from the Precambrian basement rock to the Davis Formation was considered. A better under standing 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 hydrau

lic conductivity of the confining unit, the excessive depth of the confining unit, and the resulting installa tion 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 restric tions associated with the results of the laboratory hydraulic conductivity analysis, such as the inability to account for the effects of secondary permeability fea tures (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 inter preted 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 dis cussion was expanded to include the St. Francois aqui fer.

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 forma tion thickness. After the stratigraphic data were com piled, structure maps were prepared depicting the altitude of the top of formations in the St. Francois aquifer and confining unit. Other maps show the thick ness of the St. Francois confining unit and the areal dis tribution 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 .sam ples from the St. Francois confining unit in the study area. This was achieved by performing laboratory ver tical permeability analyses on rock cores from explora tion holes. Ground water obtained from the Bonneterre Formation was used as the transmitting fluid during the analysis, allowing the vertical permeability to be con verted to vertical hydraulic conductivity.

Purpose and Scope

Study Area

Data for this report were collected from a four- county area of southeastern Missouri. However, the area of intense data collection (study area) for the core log and laboratory vertical hydraulic conductivity anal ysis 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 Com pany. 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 oper ates 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 compa nies 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 Dolo mite into the Lamotte Sandstone or Precambrian base ment, 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 bore holes 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 sec tion, quarter-quarter section, and quarter-quarter-quar ter section. The quarter sections are represented by letters A, B, C, and D, in counterclockwise order, start ing in the northeastern quadrant. Two or more explora tion 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 car bonate 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 environ ments 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 car bonate rock. These classes include:

Mudstone Mud-supported carbonate rocks pri marily 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 per cent, 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 sup port generally is a property of rocks deposited in an agi tated-water or high-energy environment. Rocks exhibiting properties of both high- and low-energy depositional environments are peculiar. The unusual


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properties may simply be a result of compaction of wackestone (especially where interstices are com pletely filled with mud), may indicate the introduction of mud-rich sediments into an area occupied by previ ously 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 pro duced 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 skele tal matter (corals), lamination contrary to gravity (lami nations 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 low- energy 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 Sand stone) of southern Missouri.

DEPOSITIONAL TEXTURE RECOGNIZABLE

Original components not bound together during deposition

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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 Base ment confining unit which is dominantly granite and rhyolite. Imes (1989) states that this confining unit is virtually impermeable. In areas where extensive fault ing and fracturing has occurred Imes reports the base ment 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 Bon- neterre Formation and the Lamotte Sandstone. In areas of southeastern Missouri near the St. Francois Moun tains 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 base ment rocks.

The Derby-Doerun Dolomite and the Davis For mation 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 second ary porosity and permeability have not developed regionally in the St. Francois confining unit. The fine grained 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 con fining unit are the thickness and the shale content (usu ally a minimally permeable material) of the unit. Whereas these normally are good measures of the con fining 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 per meability 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 perme ability features in the units could not be assessed.

Although the characterization of the Ozark aqui fer is not within the scope of this report, a general description of the unit is provided to show the signifi cance 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 predomi nantly 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 correla tion that exists between the ore deposits and stratigraphic traps, structural highs, and "reef structures was discovered (Wharton, 1975). This relation pro vided 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 forma tions. 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 under standing of these factors gives insight as to the hydrologic characteristics of subsurface structural fea tures and facies, which influence the confining ability of geohydrologic units.


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 Bon neterre Formation are typically described by no more than a few lines per formation. Also, various carbonate- rock 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. Re- logging 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 deposi tion of Upper Cambrian alluvial and marine sediments. This erosion gave the more resistant Precambrian igne ous knobs an irregular shape. They typically have steep sides, but are separated by broad flat valleys and where these Precambrian knobs are present, overlying forma tions 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 sedi ments 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 forma tions (in ascending order): Lamotte Sandstone, Bon neterre Formation (including the Sullivan Siltstone and Whetstone Creek Members), Davis Formation, Derby- Doerun 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 Paleo zoic Erathem (Palmer and Seeger, 1998).

The St. Francois Mountains (located about 45 miles to the northeast of the study area; fig. 1) and Pre cambrian knobs affected mineralization in the Vibur num 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 deposi tional environment in the area and affected the forma tion of island complexes. These island complexes were conducive for the development of algal reefs which were covered by sediments that later formed the Bon neterre 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 clas tic material led to the accumulation of sediments that formed the Lamotte Sandstone. The Lamotte Sand stone basal conglomerate is associated with fan depos its (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 con glomerates) and mudflows (clay matrix conglomer ates). Both types of fan deposits are described in the borehole logs. Coarseness of the alluvial deposits gen erally decreases with distance from the Precambrian highland area. Palmer (199la) interpreted arkosic sec tions as gravel-based channel deposits, sandbars, lami nated sheet-flood deposits, and overbank deposits (from bottom to top through each fining-upward

Depositional Enviroment 11

WEST EAST

Derby-Doerun Dolomite

Davis Formation

ShaleandMudstone

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 Pre cambrian 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-bed ding 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 grad ual 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; Yes- berger, 1982). Differences between sandstone- and car bonate-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 period ically suppressed algal stromatolite growth. Stroma- tolitic 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 crypt- algal "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.


Arkosic zones (up to 4 feet thick) may be inter preted 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 whiterock, 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 suffi cient detail to determine which depositional environ ment 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 hema- titic (iron oxide) patches remain in many whiterock sequences and grade outward to pale olive-green clay- rich coarse-crystalline dolostone, suggesting that red dened limestones were the precursor to whiterock dolo stone (Palmer, 199la). Dissolution of the precursor limestones suggests that these areas were subaerially exposed. The Sullivan Siltstone Member is a transgres- sive 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 con glomerate beds are interpreted as possible storm-gener ated debris flow deposits that moved down slopes of only a few degrees (Palmer, 199la). One core descrip tion 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 dolos tone in short distances. Retention of limestone in the basal part suggests that the southern and extreme north western 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 For mation, unlike that of the basal Bonneterre Formation basin which had a narrow, discontinuous rim and car bonate-dominant facies. Horizontal burrows in the Davis Formation are suggestive of slow periodic depo sition in a marine subtidal setting, where the shelf underwent gradual drowning during a slow transgres sion. 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 lay ers 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 up- slope to sequences with thinner mudstone beds and thicker grainstone or packstone beds. Intraclast con glomerate beds (storm-generated debris flow deposits) presumably moved down slopes of only a few degrees. Abundant intraclast beds in individual cores may sug gest 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 high lands remained exposed during the Upper Cambrian carbonate deposition. Continued exposure of the Pre cambrian highlands may have been caused by the orig inal 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 AREABOREHOLE 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.


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 deter mined 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 deter mine the net shale thickness of the Derby-Doerun Dolomite and the Davis Formation. These logs typi cally 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 con glomeratic 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 sys tem 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 sys tems 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 base ment 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 Forma tion and Gasconade Dolomite, a structural dome was identified during geologic mapping of the area con ducted in 1996 by the USGS (R.W. Harrison, U.S. Geo logical 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 indi cated so far up in the geologic section is that younger horizontal sediment layers originally buried the Pre cambrian basement rocks in southeastern Missouri. Over time, loading on the buried sediments caused compaction and subsidence. Thick sediments depos ited away from and on the flanks of the buried knobs subsided more than the much thinner sediments depos ited 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 sec tion was drilled.


The Lamotte Sandstone is a white to light tan or gray, well-sorted, well-indurated mature quartzose sandstone. It generally varies from fine- to medium- grained, 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 sec ondary calcite fracture fill and calcite- and dolomite- lined 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 sand stone; clast size is up to 1 foot in diameter. The thickest conglomerate section is 33 feet; the thickest arkose sec tion is 31 feet. Some clasts are scattered in thin beds throughout the sandstone, suggesting continual shed ding 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 Pre cambrian knobs that protrude above the top of the sur rounding 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 dolos tone 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 Mem ber). 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 Forma tion 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 bound-

stratigraphy 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 boreholecompleted in the Precambrian basement

o Amax Exploration, Inc. A St. Joe Lead Company V Asarco/Amselcon Cominco American, Inc./Phelps Dodge Mining

Company

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


stones and vary in color from gray to gray-tan, and tan. Argillaceous zones are pale green. Bleached zones sug gest that parts of the section are whiterock. The dolostones are fine to medium crystalline, fine- to medium- grained, 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) stroma tolites 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 bed ding, and, in one log, a 100-foot vertical slump struc ture. 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 frag ments (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 Forma tion 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 dolo stones 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 fea tures; reef zones reach thicknesses of 100 feet. Burrow ing is also common in the unit. Clastic material includes occasional shale partings, and quartzose, arko sic, and porphyry conglomeratic layers. Solution struc tures 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 cal cite and/or dolomite.

The whiterock is comprised of fine- to coarse grained 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 over grown 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 lam inated, well indurated, fine- to medium-grained quart zose siltstone to sandstone. The unit thickens to the west and south. Siltstone is interbedded with thin dolo stone lithoclast conglomerates, grainstone beds (prima rily 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 dolo- mitic 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 deforma tion. Vugs have calcite, and contain trace sulfide min eralization which is most common in brecciated zones. Cores suggest that an incipient facies change to dolo stone 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 abun dant pelletal glauconite. Digitate stromatolites and crypt-algal laminates are noted; digitate stromatolites are more common to the north and laminate stromato lites 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 inade quate 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 occa sional 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 (bore hole 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 For mation, as opposed to the presence of structural fea tures.

Davis Formation

The Davis Formation is composed of interbedded shales and carbonates, with both shale- and carbon ate-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. Individ ual 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. Limestone- filled burrows comprise the only carbonate in some shale layers. Carbonate layers in shale-dominant hori zons 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 inter- beds in carbonate-dominant zones vary from partings to several feet thick.

Davis Formation carbonates primarily are lime stone, 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 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 crystal line. The limestones contain pellets, fossil fragments (type not specified), oolites, glauconite (some are pel letal), relict crypt-algal laminates and infrequent digi tate stromatolites. Mudstones are sometimes bioturbated; burrows are horizontal and may be selec tively dolomitized. Some layers are composed of car bonate intraclast conglomerate. Scattered vertical fracturing is present, but is less common than in forma tions above and below. Solution features include hori zontal and vertical stylolites, and local solution and slump breccias. Scattered arkosic or porphyry con glomeratic 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 dolo-


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

EXPLANATIONBOREHOLE 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/AmselcoD 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 lime stone; vugs are partially occluded by calcite and dolo mite. 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 for mation 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 Bon- neterre Formation with the presence of the two struc tural 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 spec ified), oolites, and carbonate lithic clasts. Digitate stro matolites 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 dolo stones 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 Dolo mite structure map is similar to that of the Davis For mation 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 Dolo mite 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 con tact 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 con fining unit also was mapped (table 1, fig. 12). The thickness ranged from less than 50 feet in the northeast ern part of the study area to more than 150 feet in the southwest. This is consistent with the current under standing of the environment at the time these forma tions 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 Pre- cambrian 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 Pre- cambrian knobs identified by Fletcher (1974) in the Viburnum Trend. The decrease in thickness and clastic/ carbonate composition of the Davis Formation can


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 CompanyV Asarco/AmselcoD 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 boreholecompleted 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/AmselcoQ Cominco American, Inc./Phelps Dodge Mining

Company

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


91°25' 91°20'

37°00'

36°55'

36°50'

nEXPLANATION

PROSPECTING AREA BOREHOLE Gray symbol with contour represents borehole with data dissimilar to that in surrounding boreholes 400 LINE OF EQUAL THICKNESS Shows thickness

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/Amselcod 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

BOREHOLEo Amax Exploration, Inc. A St. Joe Lead Company V Asarco/Amselcon Cominco American, Inc./Phelps Dodge Mining

Company

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


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 carbon ate rocks (Freeze and Cherry, 1979). By determining the thickness of the confining unit, the net shale thick ness 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 confin ing 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 con ductivity 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 vis cosity 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 hydrau lic 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 conduc tivity 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 sam ples 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 num ber 35, table 2) was logged as the Derby-Doerun Dolo mite, but after further inspection, the core was determined to probably be from the lower Potosi Dolo mite; 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 deter mined in the laboratory for the rock core samples using methods described by the American Petroleum Insti tute (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 Vibur num 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 labora tory-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 pre cipitated salt, then oven dried for 24 hours at a temper ature 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 mea suring 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 cal culated net confining stress was applied. The differen tial 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 persecond

k = effective permeability, in darcies p = mass density of the fluid, in grams per

cubic centimeters g = acceleration of gravity, in centimeters per

second squaredILI = fluid viscosity, in centipoise After substitution, the conversion of vertical per

meability 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 corre lation 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 hydrau lic 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 hydrau lic 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 Wilcoxon- Mann-Whitney rank sum test (two-tailed) was used when comparing two data sets and an analysis of vari ance 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 signif icance (a-value) of 0.05 was used to test the null hypothesis which states, the vertical hydraulic conduc tivity 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 conductiv ity of samples collected from the Derby-Doerun Dolo mite 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 simi larity of the median values of the two data sets. How ever, the interquartile range (the range between the upper and lower quartiles) of vertical hydraulic con ductivity shown for the Derby-Doerun Dolomite sam ples has more than an order of magnitude greater span than the interquartile range shown for the Davis Forma-


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(18)

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Potosi Derby- Davis BonneterreDolomite Doerun Formation Formation

DolomiteFORMATION

Derby- Doerun

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; rrLnoP 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 PERCENTILEDATA 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

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Figure 13. Boxplots showing the vertical hydraulic conductivities of formations and rock types in the Fristoe Unit and Viburnum Trend Continued.


tion samples. The samples collected from the Potosi Dolomite and the Bonneterre Formation are shown for comparison purposes, although they are of no impor tance 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 Derby- Doerun 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 signif icant (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 sim ilar.

In the Viburnum Trend, there is no statistically significant (p-value = 0.412) vertical hydraulic conduc tivity difference in ranked samples containing carbon ate 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 prima rily carbonate rocks and the Davis Formation contains primarily shale, this relation is also observed in the Viburnum Trend formation vertical hydraulic conduc tivity 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 con ductivity for individual formations and rock types in the Fristoe Unit was compared with those in the Vibur num 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 carbon ate 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 conduc tivity of rock samples from the Fristoe Unit are similar to those from the Viburnum Trend.

One conclusion that can be drawn from the ver tical 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 confin ing unit. Because the vertical hydraulic conductivity of the carbonate rocks and shale in the confining unit are similar, the entire carbonate-shale thickness is impor tant in determining the effectiveness of the confining unit.

Using the results of this study, the range of esti mated 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 mini mum 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 conduc tivities 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 unitK|, 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 con fining unit in the study area was estimated to be a max imum 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 second ary permeability has developed along faults and frac tures.

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 stratigra phy of the St. Francois confining unit, and quantifying the vertical hydraulic conductivity of rock core sam ples from the confining unit using laboratory tech niques. 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 bot tom 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 characteris tic of intrashelf basin areas. These sediments were deposited during repeated cycles of marine transgres sions 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; ero sion gave the Precambrian igneous knobs an irregular shape. This erosion and a marine transgression with continued deposition of clastic material led to the accu mulation of sediments that formed the Lamotte Sand stone, 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 carbonate- dominant 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 Forma tion was deposited. Several rock sequences in the Bon neterre 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 shal lowing. The intrashelf basin likely had a wide, contin uous 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 Dolo mite was formed during a pair of carbonate deposi tional cycles. The basal shaley sequence represents a transition with the Davis Formation.

Arkosic and porphyry conglomeratic material throughout the section indicates Precambrian high lands remained exposed during Upper Cambrian car bonate deposition. Continued exposure of the Precambrian highlands may have been caused by the original height of the highlands, or be the result of con tinued uplift on fault-related structures.

Thirty-three exploration holes penetrated Pre cambrian knobs. These boreholes appear to intercept two linear structures or ridges that trend northwest- southeast. 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 base ment 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 iden tified 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 struc tures present in the basal part are digitate stromatolites as much as 1 foot high, occasional crypt-algal lami-


nates, and minor hummocky algal forms. Grains are oolites and fossil fragments (type not specified). The upper part of the lower Bonneterre Formation is com posed 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 well- defined digitate stromatolites with infrequent hum mocky algal features; reef zones reach thicknesses of 100 feet. Dark green shale partings are present through out the Whetstone Creek Member of the upper Bon neterre 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 Bon neterre Formation indicates problems associated with using core logs from various sources to map formation tops. The fingering effect of the contours in the south ern part of the prospecting area may be caused by dif ferent 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 interbed ded shales and carbonates, with both shale- and carbon ate-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 prima rily 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 Bon neterre Formation, with the presence of the two linear highs in the study area and the general dip of the forma tion 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 con tact 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 Derby- Doerun 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 Derby- Doerun 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 conductiv ity. 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 sam ples. 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 conduc tivity 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 Derby- Doerun 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 signif icant (p-value = 0.790) vertical hydraulic conductivity difference in ranked samples containing carbonate or shale or both rock types. This is also true when compar ing 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 control ling factor that determines the effectiveness of the con fining 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 con fining unit.

The range of estimated effective vertical hydrau lic 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

19lower and upper net shale thickness ranges; 1 x 10 to 3 x 10" 14 foot per second as the upper and lower ver tical 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 quar tiles) of the shale. Resulting estimates of effective ver tical hydraulic conductivity were calculated to be a

1 0maximum 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 Sympo sium, 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 Mis- souri-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 MO- 96-1, 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 Sys tem, in Koenig, J.W., ed., revised 1995, Thomp son, 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, Deposi tional history of the Lamotte Sandstone of south eastern 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 Sur vey 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 Hydro- logic Investigations Atlas HA-711-B, 1 sheet.


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 adja cent to the Ozark Plateaus province, Missouri, Arkansas, Kansas, and Oklahoma St. Francois confining unit: U.S. Geological Survey Hydro- logic 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 Mis souri, 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. Geologi cal Survey Water-Resources Investigations Report 95-4096, 1 sheet.

Iman, R.L., and Conover, W.J., 1983, A modernapproach 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 nomencla ture 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 Investiga tions 58, p. 15-19.

1977, Sedimentology of the Bonneterre Forma tion, southeast Missouri: Economic Geology, v. 72, p. 408-419.

Lohman, S.W., and others, 1972, Definitions of selected ground-water terms-Revisions and con ceptual 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 Geol ogy, 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, Vin cent E., eds., Field guide to the Upper Cambrian of southeastern Missouri: stratigraphy, sedimentology, and economic geology: Department of Geol ogy and Geophysics, University of Missouri at Rolla, p. 1-24.

Palmer, J.R., 199la, Distribution of lithofacies and inferred depositional environments in the Cam brian 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 characteris tics, uppermost Lamotte Sandstone, Bonneterre Formation, and basal Davis Formation, in two closely spaced drillcores; Greer 7.5 minute quad rangle, 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 ofRun Exploratory Drilling Project, Bureau of Land Geology and Land Survey, Report of Investiga-Management permits ES 19219 and ES 19220: tions 58, p. 3-14.Rolla, Missouri, U.S. Department of Agriculture, Yesberger, W.L., 1982, Paleoenvironments and deposi-70 p. with appendices. tional history of the Upper Cambrian Lamotte

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


TABLES

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Core log analysis data 39

Tabl

e 1.

Cor

e lo

g an

alys

is d

ata

Contin

ued

[YY

YY

MM

DD

, yea

r, m

onth

, day

; DD

MM

SS, d

egre

es, m

inut

es, s

econ

ds; a

ll un

its f

or d

epth

, alti

tude

, and

thic

knes

s ar

e in

fee

t; de

pth

and

altit

ude

refe

r to

the

form

atio

n to

p]

positional En 3 (D 3 J* U (5*

Q> TJ 0) 3 a (D 1 T "a i o° o o a. c s f 1 m 5- i1 0) 5' 1 § 2L n

o (0 2 55'

(0 o

Site

nu

mbe

r(fi

g. 6

)

1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23

Der

by-D

oeru

n

Dep

th

1,42

5

1,17

1

1,44

5

1,28

4

1,37

5

1,34

5

1,33

5

1,40

5

1,39

7

1,38

2

1,47

8

1,23

0

1,40

5

1,35

4

1,23

5

1,52

5

1,33

5

1,37

0

1,34

6

1,38

4

1,34

8

Alti

tud

e

-403

-271

-439

-398

-413

-525

-500

-625

-382

-487

-493

-335

-445

-449

-600

-620

-555

-420

-426

-409

-368

Dol

omite

Thi

ckne

ss

70 59 50 61 81 85 49 76 66 43 24 61 58 66 59 62 57 85 58 97

Thi

ckne

ss o

f S

t. D

avis

For

mat

ion

Fra

ncoi

s co

nfin

ing

uni

t B

onne

terr

e F

orm

atio

n

Dep

th

1,49

5

1,23

0

1,49

5

1,34

5

1,45

6

1,43

0

1,38

4

1,48

1

1,46

3

1,42

5

1,50

2

1,29

1

1,46

3

1,42

0

1,29

8

1,29

4

1,58

7

1,17

1

1,42

7

1,43

1

1,44

2

1,44

5

Alti

tud

e

-473

-330

-489

-459

-494

-610

-549

-701

-448

-530

-517

-396

-503

-515

-468

-659

-682

-581

-477

-511

-467

-465

Thi

ckne

ss

212

196

241

218

290

192

260

219

304

210

266

191

261

256

210

238

225

250

255

194

246

260

Tot

al

282

255

291

279

371

277

309

295

370

253

290

252

319

322

297

287

183

312

279

304

357

Net

sha

le

Dep

th

1,70

7

1,42

6

71

1,73

6

1,56

3

1,74

6

1,62

2

1,64

4

1,70

0

1,76

7

82

1,63

5

84

1,76

8

1,48

2

1,72

4

1,67

6

1,50

8

1,53

2

125

1,81

2

1,42

1

1,51

8

1,68

2

1,62

5

1,68

8

33

1,70

5

Alti

tud

e

-685

-526

-730

-677

-784

-802

-809

-920

-752

-740

-783

-587

-764

-771

-678

-897

-907

-831

-738

-732

-705

-713

-725

Thi

ckne

ss

405

395

404

325

427

375

408

345

374

299

363

392

399

431

427

445

422

381

397

399

Lam

otte

San

dsto

ne

Dep

th

2,11

2

2,13

1

1,96

7

2,07

1

2,04

9

2,01

9

2,10

8

2,11

2

2,00

9

2,06

7

2,08

7

2,06

8

1,90

7

1,96

3

2,23

9

1,86

6

1,94

0

2,06

3

2,08

5

2,10

4

Alti

tude

Thi

ckne

ss

-1,0

90

-1,1

25

-1,0

81

-1,1

09

-1,2

29

-1,1

84

-1,3

28

-1,0

97

-1,1

14

-1,0

82

-1,1

27

-1,1

63

-1,0

77

-1,3

28

-1,3

34

-1,2

76

-1,1

60

-1,1

13

-1,1

10

20

-1,1

24

Pre

cam

bria

n ro

ck

Dep

th

Alti

tude

1,55

0 -6

50

2,02

1 -1

,101

2,10

5 -1

,130

Tabl

e 1.

Cor

e lo

g an

alys

is d

ata

Contin

ued

[YY

YY

MM

DD

, ye

ar,

mon

th, d

ay;

DD

MM

SS,

degr

ees,

min

utes

, sec

onds

; al

l un

its f

or d

epth

, al

titud

e, a

nd t

hick

ness

are

in f

eet;

dept

h an

d al

titud

e re

fer

to th

e fo

rmat

ion

top]

o 0 3 6" (Q a> 2L V) v> a. 0) sr A

Site

nu

mbe

r(fi

g. 6)

24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46

Dat

e dr

illed

(Y

YY

YM

MD

D)

1979

1008

1979

1020

1979

0728

1979

1207

1979

0927

1979

0921

1979

0830

1979

1002

1979

1011

1980

0206

1979

1026

1979

1113

1979

1112

1979

1210

1979

1031

1979

1106

1979

1127

1980

0123

1979

1213

1979

1218

1980

0215

1980

0111

1979

1228

Lat

itude

(D

DM

MSS

)

3658

20

3655

43

3652

14

3655

43

3655

41

3654

42

3654

24

3653

01

3655

36

3656

19

3655

00

3654

49

3654

43

3654

37

3655

26

3655

18

3654

10

3655

10

3656

46

3654

06

3654

30

3655

45

3655

43

Lon

gitu

de

(DD

MM

SS)

9111

43

9118

25

9113

02

9121

59

9120

38

9119

15

9119

49 ^

9121

14

9118

25

9119

15

9117

39

9119

07

9117

46

9117

53

9118

31

9118

41

9116

39

9117

29

9123

38

9118

02

9117

58

9120

57

9121

15

Min

ing

com

pany

bo

reho

le

iden

tific

atio

n

AM

AX

80

1-02

4

AM

AX

80

1-02

5

AM

AX

80

1-02

6

AM

AX

80

1-02

7

AM

AX

80

1-02

8

AM

AX

80

1-02

9

AM

AX

80

1-03

0

AM

AX

80

1-03

1

AM

AX

80

1-03

2

AM

AX

80

1-03

3

AM

AX

80

1-03

4

AM

AX

80

1-03

5

AM

AX

80

1-03

6

AM

AX

80

1-03

7

AM

AX

80

1-03

8

AM

AX

801

-03

9

AM

AX

80

1-04

0

AM

AX

801

-04

1

AM

AX

80

1-04

2

AM

AX

801

-04

3

AM

AX

801

-044

AM

AX

801

-045

AM

AX

801

-04

6

Loc

al w

ell

num

ber

T27

NR

02W

29C

DA

1

T26

NR

03W

17B

AB

1

T26

NR

02W

31C

DC

3

T26

NR

04W

14B

BA

1

T26

NR

04W

13B

AA

1

T26

NR

03W

19A

BC

1

T26

NR

03W

19C

BB

1

T26

NR

04W

35A

AC

1

T26

NR

03W

17B

AC

2

T26

NR

03W

07A

CB

1

T26

NR

03W

16C

CB

1

T26

NR

03W

19A

BA

1

T26

NR

03W

20A

AD

1

T26

NR

03W

20A

DB

1

T26

NR

03W

17B

CA

1

T26

NR

03W

17C

BB

1

T26

NR

03W

21D

DA

1

T26

NR

03W

16C

BD

1

T26

NR

04W

04D

CC

1

T26

NR

03W

20D

CD

1

T26

NR

03W

20A

DC

1

T26

N R

04W

1 3

BB

B 1

T26

NR

04W

14A

AB

1

Alti

tude

of

land

sur

face

730

940

975

990

985

920

880

920

920

880

930

880

970

1,03

5

920

830

980

960

980

905

970

940

830

Bor

ehol

e de

pth

1,86

7

2,04

8

1,92

4

2,13

6

2,05

5

2,10

2

2,09

5

2,19

0

2,03

3

1,97

7

2,11

6

2,02

0

1,98

3

2,09

0

2,09

7

1,83

2

1,94

5

2,12

0

2,14

7

2,10

6

1,73

8

2,00

7

1,95

7

6 </> itional

Environmen

»* s B> <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 S 55' 8

Tab

le I

.Co

rel

[YY

YY

MM

DD

,og a

naly

sis

data

C

ontin

ued

year

, mon

th, d

ay;

DD

MM

SS, d

egre

es, m

inut

es, s

econ

ds;,

all

units

for

dep

th, a

ltitu

de, a

nd th

ickn

ess

are

in f

eet;

dept

h an

d al

titud

e re

fer t

o th

e fo

rmat

ion

top]

Thi

ckne

ss o

f St

.Si

te

num

ber

(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

Der

by-D

oeru

n D

olom

ite

Dep

th

1,27

0

1,35

1

1,40

5

1,39

6

1,43

0

1,42

7

1,36

6

1,46

5

1,37

1

1,28

7

1,37

3

1,33

6

1,37

2

1,41

4

1,34

9

1,19

2

1,30

7

1,41

8

1,50

6

1,36

8

1,29

7

1,35

8

1,28

4

Alti

tude

-540

-411

-430

-406

-445

-507

-486

-545

-451

-407

-443

-456

-402

-379

-429

-362

-327

-458

-526

-463

-327

-418

-454

Thi

ckne

ss

63 64

120 62 67

88 77 34 78 38 47 25 66 74 63 58 54 79

97 63 69 71

Dav

is F

orm

atio

n Fr

anco

is c

onfi

ning

uni

t B

onne

terr

e Fo

rmat

ion

Dep

th

1,41

4

1,46

9

1,51

6

1,49

2

1,49

4

1,45

4

1,54

2

1,40

5

1,36

5

1,411

1,38

3

1,39

7

1,48

0

1,42

3

1,25

5

1,36

5

1,47

2

1,58

5

1,46

5

1,36

0

1,42

7

1,35

5

Alti

tude

-474

-494

-526

-507

-574

-574

-622

-485

-485

-481

-503

-427

-445

-503

-425

-385

-512

-605

-560

-390

-487

-525

Thi

ckne

ss

212

233

202

207

204

208

222

214

205

220

213

214

205

217

206

260

213

228

202

188

224

212

Tota

l

189

275

297

322

269

271

296

299

248

283

258

260

239

271

291

269

318

267

307

299

251

293

283

Net

sha

le

Dep

th

1,45

9

1,62

6

30

1,70

2

1,71

8

1,69

9

1,69

8

1,66

2

80

1,76

4

1,61

9

94

1,57

0

61

1,63

1

1,59

6

1,61

1

1,68

5

1,64

0

1,46

1

1,62

5

1,68

5

71

1,81

3

.46

1,66

7

1,54

8

1,65

1

49

1,56

7

Alti

tude

-729

-686

-727

-728

-714

-778

-782

-844

-699

-690

-701

-716

-641

-650

-720

-631

-645

-725

-833

-762

-578

-711

-737

Thi

ckne

ss

397

420

388

348

375

426

416

412

369

481

413

370

437

360

413

315

419

348

358

Lam

otte

San

dsto

ne

Dep

th

1,85

6

2,04

6

2,10

6

2,04

7

2,07

3

2,08

8

2,18

0

2,03

1

1,93

9

2,11

2

2,00

9

2,05

5

2,07

7

1,82

1

2,09

8

2,12

8

2,08

6

1,99

9

1,92

5

Alti

tude

T

hick

ness

-1,1

26

-1,1

06

-1,1

16

-1;0

62

-1,1

53

-1,2

08

-1,2

60

-1,1

11

-1,0

59

-1,1

82

-1,1

29

-1,0

20

30

-1,1

57

-991

-1,1

38

-1,1

48

-1,1

81

-1,0

59

-1,0

95

Prec

ambr

ian

rock

Dep

th

Alti

tude

1,91

4 -9

39

1,98

1 -1

,011

2,08

5 -1

,050

1,91

4 -9

34

1,67

2 -7

02

Tabl

e 1.

Cor

e lo

g an

alys

is d

ata

Contin

ued

[YY

YY

MM

DD

, yea

r, m

onth

, day

; D

DM

MSS

, deg

rees

, m

inut

es, s

econ

ds;

all

units

for

dep

th,

altit

ude,

and

thi

ckne

ss a

re in

fee

t; de

pth

and

altit

ude

refe

r to

the

form

atio

n to

p]

o o 3 6" CO a> SL (A w 0.

0) 8 .&

Site

nu

mbe

r (fi

g. 6

)

47 48 49 50 51 52 53 54 55 56 57 58 59 60 61 62 63 64 65 66 67 68 69

Dat

e dr

illed

(Y

YY

YM

MD

D)

1980

0418

1980

0606

1980

0229

1980

0503

1980

0328

1980

0328

1980

0314

1980

0319

1980

0416

1980

0326

1980

0409

1980

0716

' 19

8002

28

1980

0207

1980

0125

1980

0408

1980

0220

1980

0628

1980

0425

1980

0503

1980

0813

1980

0905

1980

0512

Lat

itude

(D

DM

MSS

)

3651

04

3656

54

3658

18

3654

10

3651

47

3653

10

3652

22

3651

29

3652

49

3650

41

3652

06

3653

07

3656

42

3655

55

3655

49

3651

21

3655

40

3656

18

3651

52

3655

11

3655

13

3655

43

3654

24

Lon

gitu

de

(DD

MM

SS)

9118

54

9123

15

9118

08

9116

49

9118

13

9113

01

9113

06

9118

37

9114

13

9121

02

9121

50

9121

06

9121

47

9118

53

9118

55

9114

36

9120

00

9126

20

9115

15

9120

57

9120

55

9122

21

9119

58

Min

ing

com

pany

bo

reho

le

iden

tific

atio

n

AM

AX

80

1-04

7

AM

AX

801-

048

AM

AX

801

-049

AM

AX

80

1-05

0

AM

AX

80

1-05

1

AM

AX

80

1-05

2

. A

M A

X 8

0 1-

053

AM

AX

80

1-05

4

AM

AX

80

1-05

5

AM

AX

801-

056

AM

AX

80

1-05

7

AM

AX

80

1-05

8

AM

AX

80

1-05

9

AM

AX

80

1-06

0

AM

AX

801

-061

AM

AX

80

1-06

2

AM

AX

801-

063

AM

AX

80

1-06

4

AM

AX

801-

065

AM

AX

80

1-06

6

AM

AX

801-

067

AM

AX

80

1-06

8

AM

AX

801-

069

Loc

al w

ell

num

ber

T25

N R

03W

08B

CB

1

T26

NR

04W

04D

AD

1

T27

NR

03W

32B

AA

1

T26

NR

03W

21D

DB

1

T25

NR

03W

05A

CD

1

T26

N R

02W

30C

DB

1

T26

NR

02W

31C

DB

1

T25

NR

03W

05C

DB

1

T26

NR

03W

36B

CA

1

T25

NR

04W

12C

CB

1

T25

NR

04W

02B

AC

1

T26

NR

04W

35A

AA

1

T26

NR

04W

02C

DD

1

T26

NR

03W

07D

DA

1

T26

NR

03W

07D

DC

1

T25

NR

03W

02D

DD

1

T26

NR

04W

13A

AA

1

T26

NR

04W

07B

CA

1

T25

NR

03W

02B

DC

1

T26

NR

04W

13C

BC

1

T26

NR

04W

13C

BD

1

T26

NR

04W

15A

AB

1

T26

NR

03W

19C

BB

1

Alti

tude

of

land

sur

face

895

890

1,03

0

960

840

990

985

920

795

920

980

920

.985 86

5

855

1,01

0

980

980

950

915

945

900

885

Bor

ehol

e de

pth

2,24

7

2,03

8

2,13

7

2,07

2

2,18

5

2,20

0

2,16

9

2,26

7

1,94

7

2,24

7

2,23

4

2,19

5

1,96

8

1,97

2

1,97

7

2,32

5

1,97

2

2,09

9

2,55

7

2,13

7

2,14

8

2,06

2

2,11

7

Tabl

e 1.

Cor

e lo

g an

alys

is d

ata

Contin

ued

[YY

YY

MM

DD

, yea

r, m

onth

, day

; D

DM

MSS

, deg

rees

, min

utes

, sec

onds

; al

l un

its f

or d

epth

, al

titud

e, a

nd th

ickn

ess

are

in f

eet;

dept

h an

d al

titud

e re

fer t

o th

e fo

rmat

ion

top]

positional Em ^ 1 3 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> ~ 2 55'

(0 o

Site

nu

mbe

r (f

ig. 6

)

47 48 49 50 51 52 53 54 55 56 57 58 59 60 61 62 63 64 65 66 67 68 69

Der

by-D

oeru

n D

olom

ite

Dep

th

1,45

5

1,33

7

1,45

5

1,35

5

1,43

0

1,45

9

1,45

2

1,47

0

1,23

5

1,45

1

1,48

7

1,48

8

1,31

7

1,29

7

1,28

4

1,56

7

1,34

8

1,36

6

1,49

7

1,43

0

1,41

7

1,37

5

1,38

2

Alti

tude

-560

-447

-425

-395

-590

-469

-467

-550

-440

-531

-507

-568

-332

-432

-429

-557

-368

-386

-547

-515

-472

-475

-497

Thi

ckne

ss

71 131 55 65 62 66 50 64 72 63 64 82 73 63 72 70 67 99 65 71 112 77 88

Thi

ckne

ss o

f St

. D

avis

For

mat

ion

Fran

cois

con

fini

ng u

nit

Dep

th

1,52

6

1,46

8

1,51

0

1,42

0

1,49

2

1,52

5

1,50

2

1,53

4

1,30

7

1,51

4

1,55

1

1,57

0

1,39

0

1,36

0

1,35

6

1,63

7

1,41

5

1,46

5

1,56

2

1,50

1

1,52

9

1,45

2

1,47

0

Alti

tude

-631

-578

-480

-460

-652

-535

-517

-614

-512

-594

-571

-650

-405

-495

-501

-627

-435

-485

-612

-586

-584

-552

-585

Thi

ckne

ss

278

194

202

203

254

195

255

286

180

283

293

202

237

190

193

238

217

240

237

220

199

187

205

Tota

l

349

325

257

268

316

261

305

350

252

346

357

284

310

253

265

308

284

339

302

291

311

264

293

Net

sha

le

106 96 57 77 100 58 72 88 51 162 80 71 59 79

Bon

nete

rre

Form

atio

n

Dep

th

1,80

4

1,66

2

1,71

2

1,62

3

1,74

6

1,72

0

1,75

7

1,82

0

1,48

7

1,79

7

1,84

4

1,77

2

1,62

7

1,55

0

1,54

9

1,87

5

1,63

2

1,70

5

1,79

9

1,72

1

1,72

8

1,63

9

1,67

5

Alti

tude

-909

-772

-682

-663

-906

-730

-112

-900

-692

-877

-864

-852

-642

-685

-694

-865

-652

-725

-849

-806

-783

-739

-790

Thi

ckne

ss

424

350

387

427

432

468

390

428

444

436

383

416

330

402

422

441

360

441

399

308

.394

420

Lam

otte

San

dsto

ne

Prec

ambr

ian

rock

Dep

th

2,22

8

2,01

2

2,09

9

2,05

0

2,17

8

2,18

8

2,14

7

2,24

8

1,93

1

2,23

3

2,22

7

2,18

8

1,95

7

1,95

2

1,97

1

2,31

6

2,06

5

2,24

0

2,12

0

2,03

6

2,03

3

2,09

5

Alti

tude

T

hick

ness

D

epth

A

ltitu

de

-1,3

33

-1,1

22

-1,0

69

-1,0

90

-1,3

38

-1,1

98

-1,1

62

-1,3

28

-1,1

36

-1,3

13

-1,2

47

-1,2

68

-972

-1,0

87

-1,1

16

-1,3

06

1,93

1 -9

51

-1,0

85

-1,2

90

-1,2

05

-1,0

91

-1,1

33

-1,2

10

Tab

le 1

. Cor

e lo

g an

alys

is d

ata

Co

ntin

ue

d

[YY

YY

MM

DD

, ye

ar,

mon

th, d

ay;

DD

MM

SS, d

egre

es,

min

utes

, se

cond

s; a

ll un

its f

or d

epth

, al

titud

e, a

nd t

hick

ness

are

in f

eet;

dept

h an

d al

titud

e re

fer

to th

e fo

rmat

ion

top]

o

o <3 6" (Q Q> 3 2L (0 55'

Q.

Q) sr

Site

nu

mbe

r(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

Dat

e dr

illed

(Y

YY

YM

MD

D)

1980

0523

1980

0520

1980

0530

1980

0614

1980

0618

1980

0723

1980

0718

1980

0826

1980

0819

1980

0725

1980

0623

1980

0628

1980

0703

1980

0714

1980

0718

1980

0806

1980

0801

1980

0812

1980

0903

1980

1025

1980

1103

1980

1107

1980

1124

Lat

itude

(D

DM

MSS

)

3650

04

3655

31

3655

36

3651

15

3654

30

3654

33

3659

06

3655

33

3655

21

3655

43

3655

36

3655

39

3655

42

3655

44

3655

38

3652

01

3649

34

3649

50

3656

01

3653

02

3652

43

3652

54

3652

31

Lon

gitu

de

(DD

MM

SS)

9116

33

9118

31

9118

27

9113

29

9119

41

9119

29

9122

10

9120

53

9120

58

9120

14

9120

44

9120

32

9120

45

9120

55

9120

26

9115

16

9117

22

9120

44

9118

41

9112

56

9112

54

9113

02

91 1

302

Min

ing

com

pany

bo

reho

le

iden

tific

atio

n

AM

AX

80

1-07

0

AM

AX

80

1-07

1

AM

AX

80

1-07

2

AM

AX

80

1-07

3

AM

AX

80

1-07

4

AM

AX

80

1-07

5

AM

AX

80

1-07

6

AM

AX

80

1-07

7

AM

AX

801-

078

AM

AX

80

1-07

9

AM

AX

80

1-08

0

AM

AX

80

1-08

1

AM

AX

80

1-08

2

AM

AX

801-

083

AM

AX

801-

084

AM

AX

801-

085

AM

AX

80

1-08

6

AM

AX

801

-087

AM

AX

801-

088

AM

AX

801-

089

AM

AX

80

1-09

0

AM

AX

801-

091

AM

AX

80

1-09

2

Loc

al w

ell

num

ber

T25

NR

03W

15B

DC

1

T26

N R

03W

1 7

BC

A2

T26

NR

03W

17B

AC

1

T25

NR

03W

12A

AA

1

T26

NR

03W

19B

CD

1

T26

NR

03W

19B

DC

1

T27

NR

04W

27A

AD

1

T26

NR

04W

13B

CA

1

T26

NR

04W

13B

CC

1

T26

N R

04W

1 3

AA

B 1

T26

NR

04W

13B

AC

1

T26

NR

04W

13B

AD

1

T26

N R

04W

1 3

BA

B 1

T26

NR

04W

13B

BA

1

T26

NR

04W

13A

BC

1

T25

NR

03W

02B

AC

1

T25

NR

03W

21B

AA

1

T25

NR

04W

13C

DB

1

T26

NR

03W

08C

BC

1

T26

NR

02W

30C

DD

1

T26

NR

02W

31B

DA

1

T26

NR

02W

31B

AC

1

T26

NR

02W

31C

AB

1

Alti

tude

of

land

sur

face

640

930

930

990

900

830

1,09

0

985

940

950

975

960

955

920

920

920

690

890

870

1,00

0

970

980

990

Bor

ehol

e de

pth

1,92

6

2,10

0

2,06

8

2,34

5

2,10

8

2,01

8

2,05

2

2,08

8

2,13

5

2,03

6

2,07

8

2,08

4

2,05

8

1,98

9

2,05

3

2,28

5

2,14

8

2,24

8

1,97

4

2,16

5

2,21

8

2,17

3

2,22

3

*;

Tabl

e 1.

Cor

e lo

g an

alys

is d

ata

Contin

ued

[YY

YY

MM

DD

, yea

r, m

onth

, day

; D

DM

MSS

, deg

rees

, m

inut

es,

seco

nds;

all

units

for

dep

th,

altit

ude,

and

thi

ckne

ss a

re in

fee

t; de

pth

and

altit

ude

refe

r to

the

form

atio

n to

p]

positional Em ^ I (D 3 CO Q> (5* o Q> 3 a. s o' 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

nu

mbe

r (f

ig. 6

)

70 71 72 73 74 75 76 77 78 79 80 81 82 83 84 85 86 87 88 89 90 91 92

Der

by-D

oeru

n

Dep

th

1,15

9

1,35

4

1,35

8

1,56

2

1,39

3

1,29

9

1,53

8

1,45

3

1,44

2

1,34

0

1,45

0-

1,39

3

1,37

4

1,34

5

1,35

1

1,56

2

1,41

3

1,49

6

1,28

8

1,47

1

1,47

7

1,45

4

1,50

2

Alti

tude

-519

-424

-428

-572

-493

-469

-448

-468

-502

-390

-475

-433

-419

-425

-431

-642

-723

-606

-418

-471

-507

-474

-512

Dol

omite

Thi

ckne

ss

66 73 72 71 87 80 109 66 63 61 65 74 78 64 74 59 75 57 63 68 70 71 86

Thi

ckne

ss o

f St

. D

avis

For

mat

ion

Fra

ncoi

s co

nfin

ing

unit

Dep

th

1,22

5

1,42

7

1,43

0

1,63

3

1,48

0

1,37

9

1,64

7

1,51

9

1,50

5

1,40

1

1,51

5

1,46

7

1,45

2

1,40

9

1,42

5

1,62

1

1,48

8

1,55

3

1,35

1

1,53

9

1,54

7

1,52

5

1,58

8

Alti

tude

-585

-497

-500

-643

-580

-549

-557

-534

-565

-451

-540

-507

-497

-489

-505

-701

-798

-663

-481

-539

-577

-545

-598

Thi

ckne

ss

237

206

198

213

202

208

158

204

213

204

198

202

203

207

208

204

210

269

186

226

236

231

248

Tot

al

303

279

270

284

289

288

267

270

276

265

263

276

281

271

282

263

285

326

249

294

306

302

334

Net

sha

le

71 54 43 74 72 62 50 62 62 98 63 143 87 44 47

Bon

nete

rre

Form

atio

n

Dep

th

1,46

2

1,63

3

1,62

8

1,84

6

1,68

2

1,58

7

1,80

5

1,72

3

1,71

8

1,60

5

1,71

3

1,66

9

1,65

5

1,61

6

1,63

3

1,82

5

1,69

8

1,82

2

1,53

7

1,76

5

1,78

3

1,75

6

1,83

6

Alti

tude

-822

-703

-698

-856

-782

-757

-715

-738

-778

-655

-738

-709

-700

-696

-713

-905

-100

8

-932

-667

-765

-813

-776

-846

Thi

ckne

ss

439

465

425

496

416

414

337

342

407

396

354

398

387

352

402

437

445

408

410

342

400

399

383

Lam

otte

San

dsto

ne

Pre

cam

bria

n ro

ck

Dep

th

1,90

1

2,09

8

2,05

3

2,34

2

2,09

8

2,00

1

2,14

2

2,06

5

2,12

5

2,00

1

2,06

7

2,06

7

2,04

2

1,96

8

2,03

5

2,26

2

2,14

3

2,23

0

1,94

7

2,10

7

2,18

3

2,15

5

,221

9

Alti

tude

T

hick

ness

D

epth

A

ltitu

de

-1,2

61

-1,1

68

-1,1

23

-1,3

52

-1,1

98

-1,1

71

-1,0

52

-1,0

80

-1,1

85

-1,0

51

-1,0

92

-1,1

07

-1,0

87

-1,0

48

-1,1

15

-1,3

42

-1,4

53

-1,3

40

-1,0

77

-1,1

07

46

2,15

3 -1

,153

-1,2

13

-1,1

75

14

2,16

9 -1

,189

-1,2

29

Tabl

e 1.

Cor

e lo

g an

alys

is d

ata

Co

ntin

ue

d

[YY

YY

MM

DD

, ye

ar,

mon

th, d

ay;

DD

MM

SS, d

egre

es,

min

utes

, sec

onds

; al

l un

its f

or d

epth

, al

titud

e, a

nd t

hick

ness

are

in f

eet;

dept

h an

d al

titud

e re

fer

to th

e fo

rmat

ion

top]

o

o (D 0

(O £tt SL CO 55'

Q. 3 ^

Site

nu

mbe

r (f

ig. 6

)

93 94 95 96 97 98 99 100

101

102

103

104

105

106

107

108

109

110

111

112

113

114

115

Dat

e dr

illed

(Y

YY

YM

MD

D)

1980

0823

1980

1003

1980

0919

1980

0910

1980

0927

1980

0919

1980

0912

1980

0920

1980

0927

1980

1011

1980

1018

1980

1002

1980

1211

1980

1209

1980

1122

1980

1018

1980

0000

1980

1108

1980

1111

1980

1112

1980

1217

1980

1230

1980

1230

Lat

itude

(D

DM

MSS

)

3649

02

3651

50

3650

51

3654

17

3654

06

3653

58

3655

12

3655

19

3655

28

3654

44

3655

24

3655

32

3652

03

3651

56

3655

43

3655

10

3655

02

3654

56

3656

04

3655

59

3648

50

3655

46

3655

42

Lon

gitu

de

(DD

MM

SS)

9120

47

9117

16

. 911

701

9120

28

9120

31

9120

42

9120

46

9120

41

9120

40

9119

14

9118

36

9120

26

9113

04

9122

31

9121

32

9118

43

9118

49

9118

58

9119

45

9119

42

9119

07

9121

39

9121

25

Min

ing

com

pany

bo

reho

le

iden

tific

atio

n

AM

AX

80

1-09

3

AM

AX

80

1-09

4

AM

AX

80

1-09

5

AM

AX

80

1-09

6

AM

AX

80

1-09

7

AM

AX

80

1-09

8

AM

AX

80

1-09

9

AM

AX

80

1-10

0

AM

AX

801

-101

AM

AX

801

-102

AM

AX

801

-103

AM

AX

801

-10

4

AM

AX

801

-105

AM

AX

801

-10

6

AM

AX

801

-10

7

AM

AX

801

-108

AM

AX

801

-109

AM

AX

801

-110

AM

AX

801

-111

AM

AX

801

-112

AM

AX

801

-1 1

4

AM

AX

801

-1 1

5

AM

AX

801

-1 1

6

Loc

al w

ell

num

ber

T25

NR

04W

24C

AC

1

T25

NR

03W

04A

CC

1

T25

NR

03W

09D

AB

1

T26

N R

04W

24D

BC

1

T26

NR

04W

24D

CC

1

T26

N R

04W

25B

AB

1

T26

NR

04W

13C

AC

1

T26

N R

04W

1 3

CA

B 1

T26

N R

04W

1 3

BD

B 1

T26

NR

03W

19A

BC

2

T26

NR

03W

17B

CD

1

T26

N R

04W

1 3

AC

B 1

T25

NR

02W

06B

AB

1

T25

NR

04W

03A

CD

1

T26

NR

04W

14A

BB

1

T26

NR

03W

17C

BC

1

T26

NR

03W

18D

DA

3

T26

NR

03W

18D

DC

1

T26

NR

03W

07C

BC

1

T26

NR

03W

07C

1

T25

NR

03W

19D

DC

1

T26

NR

04W

14B

AA

1

T26

NR

04W

14A

BA

Alti

tude

of

land

sur

face

580

640

830

910

890

840

900

900

960

910

940

900

970

986

950

840

910

900

880

930

925

960

945

Bor

ehol

e de

pth

1,96

2

2,00

2

2,22

1

2,12

8

2,11

1

2,09

6

2,08

5 \

2,07

3

2,12

4

2,08

8

1,85

4

2,05

8

2,20

4

2,27

8

2,13

8

1,88

2

1,83

2

1,94

4

1,98

7

1,88

4

2,32

8

2,09

9

2,10

0

g

Tabl

e 1.

Cor

e lo

g an

alys

is d

ata

Contin

ued

[YY

YY

MM

DD

, yea

r, m

onth

, day

; D

DM

MSS

, deg

rees

, m

inut

es,

seco

nds;

all

units

for

dep

th,

altit

ude,

and

thi

ckne

ss a

re in

fee

t; de

pth

and

altit

ude

refe

r to

the

form

atio

n to

p]

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 </> 2 55'

(0 o C

Site

nu

mbe

r (f

ig. 6

)

93 94 95 96 97 98 99 100

101

102

103

104

105

106

107

108

109

110

111

112

113

114

115

Der

by-D

oeru

n D

olom

ite

Dep

th

1,19

3

1,27

9

1,50

5

1,42

9

1,39

9

1,38

5

1,38

7

1,38

1

1,41

3

1,39

0

1,29

1

1,33

4

1,46

7

1,53

3

1,41

2

1,22

1

1,23

7

1,29

6

1,30

1

1,30

8

1,56

4

1,41

2

1,39

3

Alti

tude

-613

-639

-675

-519

-509

-545

-487

-481

-453

-480

-351

-434

-497

-547

-462

-381

-327

-396

-421

-378

-639

-452

-448

Thi

ckne

ss

97 67 78 63 87 72 59 67 75 70 65 68 70 99 85 60 75 63 61 56 44 83 83

Thi

ckne

ss o

f St

. D

avis

For

mat

ion

Fran

cois

con

fini

ng u

nit

Bon

nete

rre

Form

atio

n

Dep

th

1,29

0

1,34

6

1,58

3

1,49

2

1,48

6

1,45

7

1,44

6

1,44

8

1,48

8

1,46

0

1,35

6

1,40

2

1,53

7

1,63

2

1,49

7

1,28

1

1,31

2

1,35

9

1,36

2

1364

1,60

8

1,49

5

1,47

6

Alti

tude

-710

-706

-753

-582

-596

-617

-546

-548

-528

-550

-416

-502

-567

-646

-547

-441

-402

-459

-482

-434

-683

-535

-531

Thi

ckne

ss

221

213

196

203

200

213

206

197

212

189

185

206

217

209

197

192

180

191

152

195

266

197

198

Tota

l

318

280

274

266

287

285

265

264

287

259

250

274

287

308

282

252

255

254

213

251

310

280

281

Net

sha

le

Dep

th

1,51

1

102

1,55

9

1,77

9

74

1,69

5

77

.1,6

86

89

1,67

0

73

1,65

2

73

1,64

5

1,70

0

1,64

9

1,54

1

41

1,60

8

1,75

4

104

1,84

1

1,69

4

57

1,47

3

1,49

2

1,55

0

1,51

4

1,55

9

114

1,87

4

1,69

2

1,67

4

Alti

tude

-931

-919

-949

-785

-796

-830

-752

-745

-740

-739

-601

-708

-784

-855

-744

-633

-582

-650

-634

-629

-949

-732

-729

Thi

ckne

ss

437

427

438

424

418

413

418

407

405

417

413

406

422

412

398

239

382

426

430

407

398

Lam

otte

San

dsto

ne

Dep

th

1,94

8

1,98

6

2,21

7

2,11

9

2,10

4

2,08

3

2,07

0

2,05

2

2,10

5

2,06

6

2,02

1

2,16

0

2,26

3

2,10

6

1,87

1

1,73

1

1,93

2

1,94

0

2,30

4

2,09

9

2072

Alti

tude

T

hick

ness

-1,3

68

-1,3

46

-1,3

87

-1,2

09

-1,2

14

-1,2

43

-1,1

70

-1,1

52

-1,1

45

-1,1

56

-1,1

21

-1,1

90

33

-1,2

77

-115

6

-1,0

31

8

-821

13

-1,0

32

10

-1,0

60

-1,3

79

-1,1

39

-1,1

27

Prec

ambr

ian

rock

Dep

th

Alti

tude

1,84

5 -9

05

2,19

3 -1

,223

1,87

9 -1

,039

1,74

4 -8

34

1,94

2 -1

,042

1,87

8 -9

48

Tabl

e 1.

Cor

e lo

g an

alys

is d

ata

Contin

ued

[YY

YY

MM

DD

, ye

ar, m

onth

, day

; D

DM

MSS

, deg

rees

, m

inut

es, s

econ

ds;

all

units

for

dep

th,

altit

ude,

and

thi

ckne

ss a

re in

fee

t; de

pth

and

altit

ude

refe

r to

the

form

atio

n to

p]

o

o (D 6" (O 0) SL (0 55'

Q.

0) sr ^

Site

nu

mbe

r (f

ig. 6

)

116

117

118

119

120

121

122

123

124

125

126

127

128

129

130

131

132

133

134

135

136

137

138

Dat

e dr

illed

(Y

YY

YM

MD

D)

1980

1229

1981

0116

1981

0110

1981

0122

1981

0130

1981

0207

1981

0226

1 98

1 030

5

1981

0307

1981

0311

1981

0313

1981

0321

1981

0321

1981

0330

1981

0416

1981

0406

1981

0416

1981

0417

1981

0425

1981

0504

1981

0727

1981

0606

1981

0613

Lat

itude

(D

DM

MSS

)

3652

07

3651

55

3652

05

3650

41

3652

33

3651

36

3652

10

3652

50

3658

09

3655

43

3655

43

3651

11

3651

31

3651

14

3656

02

3656

01

3656

12

3655

05

3652

35

3652

55

3656

42

3650

31

3656

40

Lon

gitu

de

(DD

MM

SS)

9122

03

9122

15

9121

03

9120

15

9120

44

9121

33

9119

20

9119

15

9122

14

9121

07

9121

46

9120

35

9122

06

9121

28

9119

33

9119

50

9119

28

9121

14

9119

30

9120

30

9122

04

9123

20

9119

10

Min

ing

com

pany

bo

reho

le

iden

tific

atio

n

AM

AX

AM

AX

AM

AX

AM

AX

801-

801-

801-

801-

AM

AX

801

-

AM

AX

AM

AX

AM

AX

801-

801-

801-

AM

AX

801

-

AM

AX

AM

AX

AM

AX

AM

AX

AM

AX

AM

AX

AM

AX

AM

AX

AM

AX

AM

AX

AM

AX

AM

AX

AM

AX

AM

AX

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

Loc

al w

ell

num

ber

T25

N

T25

N

T25

N

T25

N

R04

W02

BB

C1

R04

W03

AD

D1

R04

W01

BB

C1

R04

W 1

2DD

B1

T26

NR

04W

36C

AC

1

T25

NR

04W

02D

CB

1

T25

NR

03W

06A

B1

T26

N

T27

N

T26

N

T26

N

T25

N

T25

N

T25

N

T26

N

T26

N

T26

N

T26

N

T26

N

T26

N

T26

N

T25

N

T26

N

R03

W31

AC

B1

R04

W34

AD

A1

R04

W 1

4AA

A1

R04

W 1

4BA

B1

R04

W 1

2BD

A1

R04

W02

CC

C1

R04

W 1

1AB

D1

R03

W07

C 2

rR

03W

07C

BC

1

R03

W 0

7DB

B 1

R04

W 1

4DD

B1

R03

W31

CA

D1

R04

W36

AC

B1

R04

W02

CC

CI

R04

W 1

6AA

A1

R03

W06

DC

C1

Alti

tude

of

land

sur

face

979

960

960

920

940

930

935

900

1,02

0

945

990

940

855

890

870

885

950

960

880

905

925

680

950

Bor

ehol

e de

pth

2,25

8

2,25

8

2,25

8

2,26

8

2,25

1

2,25

4

2,26

3

2,42

8

2,17

8

2,07

8

2,12

3

2,27

8

2,14

8

2,24

8

1,99

0

2,00

8

2,06

8

2,16

0

2,25

8

2,20

8

2,04

1

1,96

8

2,07

4

g

Tabl

e 1.

Cor

e lo

g an

alys

is d

ata

Contin

ued

[YY

YY

MM

DD

, yea

r, m

onth

, day

; D

DM

MSS

, deg

rees

, min

utes

, sec

onds

; al

l uni

ts f

or d

epth

, alti

tude

, and

thic

knes

s ar

e in

fee

t; de

pth

and

altit

ude

refe

r to

the

form

atio

n to

p]

positional Em ^ 3 3 (D 3 5 £ <5' S o 3-

0) 3 Q. o' SL I "o. i o'

O O Q.

C ft f i D) i 5' z o> o' 3 SL

n o 3 (A 2 55'

(0 o c 2.

Site

nu

mbe

r(fi

g. 6)

116

117

118

119

120

121

122

123

124

125

126

127

128

129

130

131

132

133

134

135

136

137

138

Der

by-D

oeru

n

Dep

th

1,53

2

1,52

1

1,54

6

1,52

8

1,51

8

1,52

3

1,51

9

1,48

5

1,48

1

1,39

6

1,43

4

1,54

4

1,40

4

1,48

1

1,28

3

1,30

3

1,37

4

1,45

6

1,52

4

1,49

8

1,34

0

1,24

6

1,39

0

Alti

tude

-553

-561

-586

-608

-578

-593

-584

-585

-461

-451

-444

-604

-549

-591

-413

-418

-424

-496

-644

-593

-415

-566

-440

Dol

omite

Thi

ckne

ss

94 112 67 70 97 110 98 70 74 68 88 81 98 74 72 49 68 74 73 70 89 67 66

Thi

ckne

ss o

f St.

Dav

is F

orm

atio

n Fr

anco

is c

onfi

ning

uni

t B

onne

terr

e Fo

rmat

ion

Dep

th

1,62

6

1,63

3

1,61.3

1,59

8

1,61

5

1,63

3

1,61

7

1,55

5

1,55

5

1,46

4

1,52

2

1,62

5

1,50

2

1,55

5

1,35

5

1,35

2

1,44

2

1,53

0

1,59

7

1,56

8

1,42

9

1,31

3

1,45

6

Alti

tude

-647

-673

-653

-678

-675

-703

-682

-655

-535

-519

-532

-685

-647

-665

-485

-467

-492

-570

-717

-663

-504

-633

-506

Thi

ckne

ss

214

198

224

223

199

192

207

216

203

201

197

214

201

219

201

201

200

198

203

201

204

222

196

Tota

l

308

310

291

293

296

_

302

305

286

277

269

285

295

299

293

273

250

268

272

276

271

293

289

262

Net

sha

le

Dep

th

1,84

0

1,83

1

1,83

7

1,82

1

63

1,81

4

75

1,82

5

79

1,82

4

76

1,77

1

60

1,75

8

66

1,66

5

1,71

9

1,83

9

1,70

3

1,77

4

1,55

6

1,55

3

1,64

2

64

1,72

8

1,80

0

82

1,76

9

1,63

3

1,53

5

1,65

2

Alti

tude

-861

-871

-877

-901

-874

-895

-889

-871

-738

-720

-729

-899

-848

-884

-686

-668

-692

-768

-920

-864

-708

-855

-702

Thi

ckne

ss

400

415

409

428

425

417

425

378

400

400

427

424

426

376

361

390

412

428

417

388

405

395

Lam

otte

San

dsto

ne

Prec

ambr

ian

rock

Dep

th

2,24

0

2,24

6

2,24

6

2,24

9

2,23

9

2,24

2

2,24

9

2,13

6

2,06

5

2,11

9

2,26

6

2,12

7

2,20

0

1,93

2

1,91

4

2,03

2

2,14

0

2,22

8

2,18

6

2,02

1

1,94

0

2,04

7

Alti

tude

T

hick

ness

D

epth

A

ltitu

de

-1,2

61

-1,2

86

-1,2

86

-1,3

29

-1,2

99

-1,3

12

-1,3

14

-1,1

16

-1,1

20

-1,1

29

-1,3

26

-1,2

72

-1,3

10

-1,0

62

-1,0

29

-1,0

82

-1,1

80

-1,3

48

-1,2

81

-1,0

96

-1,2

60

-1,0

97

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Core log analysis data 51

en

Tabl

e 1.

Cor

e lo

g an

alys

is d

ata

Contin

ued

[YY

YY

MM

DD

, yea

r, m

onth

, day

; D

DM

MSS

, deg

rees

, m

inut

es,

seco

nds;

all

units

for

dep

th,

altit

ude,

and

thi

ckne

ss a

re in

fee

t; de

pth

and

altit

ude

refe

r to

the

form

atio

n to

p]

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 "J (D 2 0> 5- I 3

Z Q)

5'

3 SL

n o (D w j* S 55'

(0 o c

Site

nu

mbe

r (f

ig-

6)

139

140

141

142

143

144

145

146

147

148

149

150

151

152

153

154

155

156

157

158

159

160

161

Der

by-D

oeru

n

Dep

th

1,38

8

1,26

9

1,35

8

1,28

6

1,50

6

1,52

8

1,48

8

1,39

0

1,32

2

1,56

3

1,40

4

1,42

0

1,42

1

1,50

7

1,54

2

1,30

6

1,50

7

1,49

8

1,39

0

1,54

0

Alti

tude

-408

-416

-438

-486

-551

-608

-578

-415

-457

-579

-529

-510

-576

-472

-615

-371

-577

-568

-450

-580

Dol

omite

Thi

ckne

ss

73 69 66 68 87 88 86 69 79 74 79 80 90 93 68 144 57 69 80 63

Thi

ckne

ss o

f S

t. D

avis

For

mat

ion

Fra

ncoi

s co

nfin

ing

uni

t B

onne

terr

e F

orm

atio

n

Dep

th

1,46

1

1,33

8

1,42

4

1,35

4

1,59

3

1,61

6

1,57

4

1,45

9

1,40

1

1,63

7

1,48

3

1,50

0

1,51

1

1,60

0

1,61

0

1,45

0

1,56

4

1,56

7

1,47

0

1,60

3

Alti

tude

-481

-485

-504

-554

-638

-696

-664

-484

-536

-653

-608

-590

-666

-565

-683

-515

-634

-637

-530

-643

Thi

ckne

ss

197

194

198

195

214

203

200

203

199

208

195

202

213

192

206

206

141

170

194

152

Tot

al

270

263

264

263

301

291

286

272

278

282

274

282

303

285

274

350

198

239

274

215

Net

sha

le

Dep

th

1,65

8

1,53

2

1,62

2

1,54

9

85

1,80

7

1,81

9

1,77

4

1,66

2

1,60

0

1,84

5

125

1,67

8

99

1,70

2

74

1,72

4

90

1,79

2

104

1,81

6

1,65

6

1,70

5

1,73

7

1,66

4

1,75

5

1,71

3

1,55

5

1,71

4

Alti

tude

-678

-679

-702

-749

-852

-899

-864

-687

-735

.

-861

-803

-792

-879

-757

-889

-721

-775

-807

-724

-795

-693

-445

-689

Thi

ckne

ss

412

416

418

401

402

419

420

397

365

341

403

422

404

430

363

374

391

392

Lam

otte

San

dsto

ne

Pre

cam

bria

n ro

ck

Dep

th

2,07

0

1,94

8

2,04

0

1,95

0

2,20

9

2,23

8

2,19

4

1,99

7

2,21

0

2,01

9

2,10

5

2,14

6

2,19

6

2,24

6

2,01

9

2,03

8

2,10

4

2,10

6

Alti

tude

Thi

ckne

ss

Dep

th

Alti

tude

-1,0

90

-1,0

95

-1,1

20

-1,1

50

-1,2

54

-1,3

18

-1,2

84

1,86

0 -8

85

-1,1

32

-1,2

26

-1,1

44

-1,1

95

-1,3

01

-1,1

61

-1,3

19

-1,0

84

-1,0

98

-1,0

84

-1,0

81

Tabl

e 1.

Cor

e lo

g an

alys

is d

ata

Contin

ued

[YY

YY

MM

DD

, yea

r, m

onth

, day

; D

DM

MSS

, deg

rees

, m

inut

es, s

econ

ds;

all

units

for

dep

th,

altit

ude,

and

thi

ckne

ss a

re in

fee

t; de

pth

and

altit

ude

refe

r to

the

form

atio

n to

p]

o

o Jo 6" (O Q> 3 9L w w'

Q.

Q> ST en

Site

nu

mbe

r (f

ig. 6

)

162

163

164

165

166

167

168

169

170

171

172

173

174

175

176

177

178

179

180

181

182

183

184

Dat

e dr

illed

(Y

YY

YM

MD

D)

1980

0508

1980

0829

1980

1024

1980

1104

1981

0303

1981

0319

1981

0523

1981

0415

1981

0506

1981

0604

1984

0709

1984

0730

1984

0816

1984

1200

1981

0916

1982

0513

1981

0512

1979

1129

1980

0106

1980

0125

1963

1007

1963

1119

1963

1231

Lat

itude

(D

DM

MSS

)

3656

18

3656

02

3656

03

3656

38

3657

01

3657

41

3701

48

3657

53

3655

57

3701

40

3656

22

3658

25

3658

38

3655

52

3700

07

3656

30

3657

42

3701

45

3701

50

3701

27

3701

21

3701

01

3700

37

Lon

gitu

de

(DD

MM

SS)

9116

55

9120

00

9120

34

9121

44

9114

02

9121

31

9121

17

9120

54

9113

19

9119

26

9120

12

9120

55

9120

54

9120

35

9116

56

9112

32

9115

39

9119

02

9118

32

9118

21

9118

03

9117

31

9118

01

Min

ing

com

pany

bo

reho

le

iden

tific

atio

n

ASA

RC

OPK

-14

ASA

RC

O P

K- 1

5

ASA

RC

OPK

-17

ASA

RC

O P

K- 1

8

ASA

RC

O P

K-2

6

ASA

RC

O P

K-2

7

ASA

RC

O P

K-2

8

ASA

RC

O P

K-3

0

ASA

RC

O P

K-3

2

ASA

RC

O P

K-3

5

AM

SEL

CO

PK

-42

AM

SEL

CO

PK

-43

AM

SEL

CO

PK

-44

ASA

RC

O P

K-4

6

CO

MIN

CO

SF-

25

CO

MIN

CO

SF-

28

CO

MIN

CO

SF-

6

CO

MIN

CO

WN

-21

CO

MIN

CO

WN

-22

CO

MIN

CO

WN

-23

PH D

DG

068

689

PH D

DG

068

689

PH D

DG

068

691

Loc

al w

ell

num

ber

T26

NR

03W

09A

CA

1

T26

NR

04W

12D

AD

1

T26

NR

04W

12C

AD

1

T26

NR

04W

11B

AB

1

T26

NR

03W

01B

DC

1

T27

NR

04W

35D

CB

1

T27

NR

04W

11A

BA

1

T27

N R

04W

36C

BB

1

T26

N R

02W

07D

BB

1

T27

NR

03W

07B

CA

1

T26

NR

04W

12A

DB

1

T27

N R

04W

25C

CC

2

T27

NR

04W

25C

BC

1

T26

NR

04W

12C

DD

1

T27

NR

03W

16D

CC

1

T26

NR

02W

06D

CD

1

T27

NR

03W

34D

AC

1

T27

NR

03W

07A

BC

1

T27

N R

03W

08B

BB

1

T27

NR

03W

08B

CD

1

T27

NR

03W

08C

1

T27

NR

03W

08D

1

T27

NR

03W

17A

1

Alti

tude

of

land

sur

face

1,00

5

950

990

980

970

1,00

0

1,05

0

1,06

5

875

995

915

1,02

5

1,01

0

1,00

0

950

730

985

1,08

0

1,06

0

1,06

5

1,05

5

918

921

Bor

ehol

e de

pth

2,16

4

2,14

0

1,91

4

1,63

1

2,12

8

2,10

9

2,01

7

2,16

1

2,11

4

1,95

5

2,00

4

2,13

3

2,13

5

2,03

5

2,00

4

1,93

2

2,16

1

1,56

3

1,90

3

1,87

0

1,47

8

1,56

3

1,91

7

Tabl

e 1.

Cor

e lo

g an

alys

is d

ata

Contin

ued

[YY

YY

MM

DD

, yea

r, m

onth

, day

; D

DM

MSS

, deg

rees

, m

inut

es, s

econ

ds;

all

units

for

dep

th,

altit

ude,

and

thi

ckne

ss a

re in

fee

t; de

pth

and

altit

ude

refe

r to

the

form

atio

n to

p]

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 (5 w 3 (0* (0

O C

Site

D

erby

-Doe

run

Dol

omite

nu

mbe

r

(fig

. 6)

D

epth

A

ltitu

de

Thi

ckne

ss

162

1,20

0 -1

95

319

163

164

165

166

1,33

7 -3

67

204

167

1,31

8 -3

18

257

168

169

170

1,35

2 -4

77

162

171

172

173

1,40

0 -3

75

142

174

175

176

1,10

0 -1

50

177

1,19

0 -4

60

197

178

1,41

3 -4

28

149

179

180

181

1,15

6 -9

1

182

1,10

5 -5

0 30

5

183

970

-52

348

184

1,11

6 -1

95

209

Thi

ckne

ss o

f S

t. D

avis

For

mat

ion

Fra

ncoi

s co

nfin

ing

uni

t B

onne

terr

e F

orm

atio

n

Dep

th

1,51

9

1,38

6

1,54

1

1,57

5

1,60

0

1,51

4

1,41

2

1,54

2

1,51

3

1,42

2

1,38

7

1,56

2

1,41

0

1,31

8

1,32

5

Alti

tude

-514

-396

-571

-575

-535

-639

-497

-517

-503

-422

-657

-577

-355

-400

-404

Thi

ckne

ss

201

200

102

135

142

195

165

192

191 95 153 80 87

Tot

al

520

306

392

357

334

456

292

302

357

428

296

Net

sha

le

Dep

th

1,72

0

1,64

7

1,58

6

1,48

5

1,64

3

1,71

0

1,60

7

1,74

2

1,70

9

1,46

4

1,57

7

1,73

4

1,70

4

1,55

6

1,48

2

1,71

5

1,35

8

1,49

9

1,51

3

1,39

8

1,41

2

Alti

tude

-715

-697

-596

-505

-673

-710

-557

-677

-834

-469

-662

-709

-694

-606

-752

-730

-278

-439

-448

-480

-491

Thi

ckne

ss

439

400

477

385

393

406

400

446

405

416

417

402

415

448

Lam

otte

San

dsto

ne

Dep

th

2,15

9

2,04

7

2,12

0

2,09

5

2,00

0

2,14

8

2,10

9

1,91

0

1,98

2

2,12

0

1,97

3

1,88

4

2,13

0

1,86

0

Alti

tude

Thi

ckne

ss

-1,1

54

-1,0

97

-1,1

50

-1,0

95

-950

-1,0

83

-1,2

34

-915

-1,0

67

-1,1

10

-1,0

23

-1,1

54

-1,1

45

-939

50

Pre

cam

bria

n ro

ck

Dep

th

1,91

0

1,62

7

2,01

8

1,54

7

1,83

7

1,84

7

1,43

7

1,55

7

1,91

0

Alti

tude

-920

-647

-1,0

18

-467

-111

-782

-382

-639

-989

Tabl

e 1.

Cor

e lo

g an

alys

is d

ata

Co

ntin

ue

d

[YY

YY

MM

DD

, ye

ar,

mon

th, d

ay;

DD

MM

SS, d

egre

es, m

inut

es,

seco

nds;

all

units

for

dep

th,

altit

ude,

and

thi

ckne

ss a

re i

n fe

et;

dept

h an

d al

titud

e re

fer

to th

e fo

rmat

ion

top]

o

o <3 6" (0 Q> 3 5L w 55° Q.

Q) ET en

Site

nu

mbe

r(fi

g. 6)

185

186

187

188

189

190

191

192

193

194

195

196

197

198

199

200

201

202

203

204

205

206

207

Dat

e dr

illed

(Y

YY

YM

MD

D)

1963

1017

1968

0626

1976

0401

1976

1216

1977

0223

1977

0405

1977

0510

1977

0517

1977

0609

1977

0623

1977

0825

1979

0222

1979

0614

1979

0626

1979

0802

1981

0511

1981

1209

1981

1230

1982

0126

1982

0324

1982

0401

1982

0429

Lat

itude

(D

DM

MSS

)

3700

04

3702

20

3702

54

3656

12

3659

36

3657

54

3701

12

3659

18

3659

18

3700

27

3702

47

3659

43

3658

02

3652

47

3700

23

3701

25

3702

48

3652

07

3652

05

3653

59

3653

58

3654

04

3654

30

Lon

gitu

de

(DD

MM

SS)

9114

17

9120

19

9126

27

9108

10

9116

10

9111

30

9119

15

9114

43

9110

48

9121

58

9120

44

9117

27

9116

28

9115

30

9124

23

9122

42

9120

00

9119

58

9123

10

9118

15

9114

59

9116

32

9116

32

Min

ing

com

pany

bo

reho

le

iden

tific

atio

n

PH D

DG

068

692

PH

DD

G27

N4W

1-1

ST J

OE

68W

44

ST J

OE

76W

05

ST

JOE

76W

20

ST

JOE

77W

02

ST

JOE

77W

03

ST

JOE

77W

05

ST

JOE

77W

06

ST J

OE

77W

07

,

ST

JOE

77W

08

ST

JOE

77W

11

ST J

OE

79W

03

ST J

OE

79W

05

ST

JOE

79W

06

ST J

OE

79W

08

ST

JOE

81W

09

ST J

OE

82W

03

ST

JOE

82W

07

ST

JOE

82W

11

ST

JOE

82W

19

ST

JOE

82W

21

ST

JOE

82W

25

Loc

al w

ell

num

ber

T27

NR

03W

14D

1

T27

NR

04W

01C

AA

1

T28

N R

05W

36D

DB

1

T26

NR

02W

11A

B 1

T27

N R

03W

22C

A 1

T27

N R

02W

32A

C 1

T27

N R

03W

07C

C 1

T27

N R

03W

23D

C 1

T27

NR

02W

21C

A 1

T27

NR

04W

14C

B 1

T28

N R

04W

36C

C 1

T27

NR

03W

21B

C 1

T27

N R

03W

34B

C 1

T26

N R

03W

35B

C 1

T27

NR

04W

17D

A 1

T27

NR

04W

10C

A 1

T28

N R

04W

36D

D 1

T25

NR

03W

06B

B1

T25

NR

04W

03B

B1

T26

NR

03W

29A

BB

1

T26

NR

03W

23C

DD

1

T26

NR

03W

22C

CC

1

T26

NR

03W

22B

CC

1

Alti

tude

of

land

sur

face

914

1,03

0

917

631

951

761

1,02

3

808

731

1,03

3

1,10

9

901

871

706

1,08

1

1,10

6

1,11

5

960

745

920

790

970

965

Bor

ehol

e de

pth

1,97

6

1,87

6

1,94

8

1,94

0

1,80

6

1,89

5

1,91

2

1,88

6

1,99

9

1,77

8

1,98

7

2,06

5

2,04

5

2,15

6

2,15

8

1,79

4

2,29

0

2,02

2

2,17

9

2,24

8

1,52

8

2,17

1

«;

Tabl

e 1.

Cor

e lo

g an

alys

is d

ata

Contin

ued

[YY

YY

MM

DD

, yea

r, m

onth

, day

; D

DM

MSS

, deg

rees

, m

inut

es, s

econ

ds;

all

units

for

dep

th, a

ltitu

de, a

nd th

ickn

ess

are

in f

eet;

dept

h an

d al

titud

e re

fer

to th

e fo

rmat

ion

top]

positional Environme

ni

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

nu

mbe

r (f

ig-

6)

185

186

187

188

189

190

191

192

193

194

195

196

197

198

199

200

201

202

203

204

205

206

207,

Der

by-D

oeru

n

Dep

th

1,14

9

1,18

3

1,22

7

1,14

0

1,25

5

1,38

7

1,28

8

1,25

2

1,13

0

1,36

0

1,21

6

1,34

3

1,36

5

1,27

2

1,40

3

1,44

8

1,23

1

1,52

8

1,26

6

Alti

tude

-235

-153

-310

-509

-304

-626

-265

-444

-399

-327

-107

-442

-494

-566

-322

-342

-116

-568

-521

Dol

omite

Thi

ckne

ss

289

284

119

156

189

124

149

257

222

105

174

103 51 58 158

164

140 91

87

Thi

ckne

ss o

f S

t. D

avis

For

mat

ion

Fra

ncoi

s co

nfin

ing

uni

t B

onne

terr

e F

orm

atio

n

Dep

th

1,43

8

1,46

7

1,34

6

1,29

6

1,44

4

1,51

1

1,43

7

1,50

9

1,35

2

1,46

5

1,39

0

1,44

6

1,41

6

1,33

0

1,56

1

1,61

2

1,37

1

1,61

9

1,35

3

1,51

7

1,37

0

1,54

0

Alti

tud

e

-524

-437

-429

-665

-493

-750

-414

-701

-621

-432

-281

-545

-545

-624

-480

-506

-256

-659

-608

-597

-580

-575

Thi

ckne

ss

86 75 232

217

143 49 187 41 147

256

133

218

314

323

271

233

166

232

265

202

176

203

Tot

al

375

359

351

373

332

173

336

298

369

361

307

321

365

381

429

397

306

323

352

Net

sha

le

Dep

th

1,52

4

1,54

2

1,57

8

1,51

3

1,58

7

1,56

0

1,62

4

1,55

0

1,49

9

1,72

1

1,52

3

1,66

4

1,73

0

1,65

3

1,83

2

1,84

5

24

1,53

7

139

1,85

1

1,61

8

1,71

9

83

1,54

6

1,45

7

1,74

3

Alti

tud

e

-610

-512

-661

-882

-636

-799

-601

-742

-768

-688

-414

-763

-859

-947

-751

-739

-422

-891

-873

-799

-756

-487

-778

Thi

ckne

ss

406

466

286

298

320

229

328

367

256

234

303

328

377

310

294

421

385

389

419

399

Lam

otte

San

dsto

ne

Dep

th

1,93

0

2,00

8

1,86

4

1,81

1

1,90

7

1,85

3

1,87

8

1,86

6

1,97

7

1,75

7

1,96

7

2,05

8

2,03

0

2,14

2

2,13

9

2,27

2

2,00

3

2,10

8

1,96

5

2,14

2

Alti

tud

e

Thi

ckne

ss

-1,0

16

27

-978

-947

-1,1

80

-956

-830

-1,0

70

-1,1

35

-944

-648

10

-1,0

66

-1,1

87

-1,3

24

-1,0

61

-1,0

33

-1,3

12

-1,2

58

-1,1

88

-1,1

75

-1,1

77

Pre

cam

bria

n ro

ck

Dep

th

Alti

tud

e

1957

-1

043

1,76

7 -6

58

1,52

1 -5

51

Tabl

e 1.

Cor

e lo

g an

alys

is d

ata

Contin

ued

[YY

YY

MM

DD

, ye

ar,

mon

th, d

ay;

DD

MM

SS, d

egre

es,

min

utes

, sec

onds

; al

l un

its f

or d

epth

, al

titud

e, a

nd t

hick

ness

are

in

feet

; de

pth

and

altit

ude

refe

r to

the

form

atio

n to

p]

o

o <3 6" CO &> 3 SL CO co" 0, lu ST CJ1

Site

nu

mbe

r (f

ig. 6

)

208

209

210

211

212

213

214

215

216

217

218

219

220

22

1

222

223

224

225

226

227

228

229

230

Dat

e dr

illed

(Y

YY

YM

MD

D)

1982

0609

1982

0826

1982

1012

1982

0112

1983

0209

1983

0330

1983

0415

1983

0516

1983

0531

1983

0725

1983

0810

1983

0825

1983

0907

1983

1017

1984

0703

1985

0122

1985

0130

1985

0827

1985

1014

1985

1011

1985

1205

1988

0629

1988

0727

Lat

itude

(D

DM

MSS

)

3653

39

3647

53

3647

24

3700

54

3704

05

3651

28

3654

19

3653

59

3650

36

3646

45

3652

09

3652

54

3651

35

3704

04

3646

58

3650

02

3650

21

3650

04

3656

55

3658

38

3650

01

3646

22

3648

59

Lon

gitu

de

(DD

MM

SS)

9118

23

9116

19

9113

24

9118

19

9122

02

9122

48

9116

32

9116

12

9122

20

9115

23

9124

17

9123

50

9123

10

9122

25

9115

36

9121

38

9121

37

9121

09

9121

56

9121

00

9121

31

9114

34

9120

07

Min

ing

com

pany

bo

reho

le

iden

tific

atio

n

ST J

OE

82W

27

ST

JOE

82W

31

ST J

OE

82W

34

ST

JOE

83W

06

ST J

OE

83W

09

ST

JOE

83W

12

ST

JOE

83W

14

ST

JOE

83W

15

ST

JOE

83W

17

ST

JOE

83W

25

ST

JOE

83W

30

ST

JOE

83W

34

ST

JOE

83W

35

ST J

OE

83W

44

ST

JOE

84W

44

ST

JOE

85W

09

ST

JOE

85W

11

ST

JOE

85W

31

ST

JOE

85W

35

ST

JOE

85W

37

ST

JOE

86W

02

ST

JOE

88W

03

ST

JOE

88W

04

Loc

al w

ell

num

ber

T26

NR

03W

29B

DD

1

T25

NR

03W

27C

DD

1

T25

NR

02W

31B

CC

1

T27

NR

03W

17B

BA

1

T28

NR

04W

27A

DC

1

T25

NR

04W

03C

D1

T26

N R

03W

22C

BB

1

T26

NR

03W

22C

DD

1

T25

NR

04W

10D

DD

1

T24

NR

03W

02A

BC

1

T25

NR

04W

04B

CC

1

T26

NR

04W

33B

DA

1

T25

N R

04W

03C

CB

1

T28

NR

04W

27B

DD

1

T24

N R

03W

02B

AA

1

T25

NR

04W

14D

B 2

T25

NR

04W

14A

B1

T25

NR

04W

14D

A1

T26

NR

04W

02C

BD

1

T27

NR

04W

26D

AD

1

T25

NR

04W

14D

B1

T24

NR

03W

01B

DC

1

T25

NR

04W

24D

D1

Alti

tude

of

land

sur

face

870

540

855

985

1,05

0

925

985

785

918

860

930

960

725

1,04

0

805

912

919

644

890

997

874

810

920

Bor

ehol

e de

pth

2,15

5

1,94

5

2,43

5

1,98

2

1,59

8

2,22

5

1,54

9

1,96

0

2,24

2

2,40

6

2,19

6

2,20

6

1,98

7

1,78

6

2,33

7

2,26

5

2,23

6

1,95

7

1,94

6i

2,08

0

2,18

3

2,40

0

2,32

1

g

Tabl

e 1.

Cor

e lo

g an

alys

is d

ata

Contin

ued

[YY

YY

MM

DD

, yea

r, m

onth

, day

; D

DM

MSS

, deg

rees

, min

utes

, sec

onds

; all

units

for

dep

th, a

ltitu

de, a

nd th

ickn

ess

are

in f

eet;

dept

h an

d al

titud

e re

fer t

o th

e fo

rmat

ion

top]

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

nu

mbe

r (f

ig.

6)

208

209

210

211

212

213

214

215

216

217

218

219

220

221

222

223

224

225

226

227

228

229

230

Der

by-D

oeru

n D

olom

ite

Dep

th

1,15

0

1,31

2

1,05

6

1,28

2

1,17

4

1,42

0

1,54

4

1,25

9

1,17

7

1,02

2

1,26

6

1,40

5

1,44

7

1,59

8

1,53

7

Alti

tude

-610

-327 -6

-297

-389

-502

-684

-329

-217 18

-376

-408

-573

-788

-617

Thi

ckne

ss

65 120

194 60 99 128

139

242

386

233 58 49 88 90 112

Thi

ckne

ss o

f S

t. D

avis

For

mat

ion

Fra

ncoi

s co

nfin

ing

un

it B

onne

terr

e F

orm

atio

n

Dep

th

1,49

5

1,21

5

1,43

2

1,25

0

1,54

6

1,34

2

1,27

3

1,54

8

1,68

3

1,50

1

1,56

3

1,35

3

1,25

5

1,60

1

1,55

2

1,54

0

1,27

1

1,32

4

1,45

4

1,53

5

1,68

8

1,64

9

Alti

tud

e

-625

,

-675

-447

-200

-621

-357

-488

-630

-823

-571

-603

-628

-215

-796

-640

-621

-627

-434

-457

-661

-878

-729

Thi

ckne

ss

200

240

171

150

278

140

180

282

254

337

.

270

248

242

252

274

315

305

314

289

267

254

312

Tot

al

305

291

344

200

279

410

393

579

656

475

372

338

355

344

424

Net

sha

le

Dep

th

100

1,69

5

145

1,45

5

89 27

1,60

3

1,40

0

1,82

4

75

1,48

2

1,45

3

117

1,83

0

148

1,93

7

156

1,83

8

129

1,83

3

1,60

1

1,49

7

1,85

3

1,82

6

1,85

5

1,57

6

96

1,63

8

58

1,74

3

1,80

2

1,94

2

159

1,96

1

Alti

tude

-825

-915

-618

-350

-899

-497

-668

-912

-1,0

77

-908

-873

-876

-457

-1,0

48

-914

-936

-932

-748

-746

-928

-1,1

32,

-1,0

41

Thi

ckne

ss

410

454

286

152

375

346

460

349

296

384

211

464

421

366

370

282

281

442

347

Lam

otte

San

dsto

ne

Dep

th

2,10

5

1,90

9

1,88

9

1,55

2

2,19

9

2,17

6

2,39

7

2,18

7

2,12

9

1,98

5

1,70

8

2,31

7

2,24

7

2,22

1

1,94

6

1,92

0

2,02

4

2,38

4

2,30

8

Alti

tude

Thi

ckne

ss

-1,2

35

-1,3

69

-904

63

-502

39

-1,2

74

-1,2

58

-1,5

37

-1,2

57

-1,1

69

-1,2

60

-668

46

-1,5

12

-1,3

35

-1,3

02

-1,3

02

-1,0

30

-1,0

27

-1,5

74

-1,3

88

Pre

cam

bria

n ro

ck

Dep

th

Alti

tude

1,95

2 -9

67

1,59

1 -5

41

1,54

8 -5

63

1,93

7 -1

,152

1,75

4 -7

14

Tabl

e 1.

Cor

e lo

g an

alys

is d

ata

Contin

ued

[YY

YY

MM

DD

, yea

r, m

onth

, day

; DD

MM

SS, d

egre

es, m

inut

es, s

econ

ds; a

ll un

its f

or d

epth

, alti

tude

, and

thic

knes

s ar

e in

fee

t; de

pth

and

altit

ude

refe

r to

the

form

atio

n to

p]

o to o> 3

0)

Site

nu

mbe

r(fi

g. 6)

231

232

233

234

235

236

237

238

Bor

ehol

es in

VB

1

VB

2

VB

3

VB

4

VB

5

Dat

e dr

illed

(Y

YY

YM

MD

D)

1988

0808

1988

0817

1988

0912

1989

0405

1989

1206

1990

0321

1992

1130

1993

0203

Lat

itude

(D

DM

MSS

)

3648

49

3650

13

3648

16

3648

53

3646

28

3646

21

3651

16

3651

20

Lon

gitu

de

(DD

MM

SS)

9120

20

9121

40

9119

46

9121

03

9113

56

9113

15

9121

53

9122

04

Min

ing

com

pany

bo

reho

le

iden

tific

atio

n

ST

JOE

88W

05

ST J

OE

88W

06

ST J

OE

88W

09

ST

JOE

89W

01

ST J

OE

89W

22

ST J

OE

90W

03

ST

JOE

93W

08

ST

JOE

93W

18

Loca

l wel

l num

ber

T25

N R

04W

24D

D 2

T25

N R

04W

14A

C1

T25

NR

03W

30C

AB

1

T25

NR

04W

24C

CC

1

T24

NR

03W

01A

DD

1

T24

NR

02W

06B

DD

1

T25

NR

04W

11B

AC

1

T25

NR

04W

11B

BB

1

Min

imum

Max

imum

Alti

tude

of

land

sur

face

870

910

890

551

830

850

965

930

540

1,11

5

Bor

ehol

e de

pth

2,24

5

2,22

1

2,31

5

1,93

5

2,59

0

2,50

5

2,28

5

2,26

2

1,47

8

2,59

0

Vib

urnu

m T

rend

fro

m w

hich

cor

e sa

mpl

es w

ere

colle

cted

and

sen

t fo

r la

bora

tory

per

mea

bilit

y an

alys

is

3723

51

3722

09

3722

35

3720

27

3717

57

9107

17

9110

58

9109

20

9109

24

9108

46

ASA

RC

O A

C 3

7

ASA

RC

O A

C 4

5

ASA

RC

O A

C 8

4

ASA

RC

O L

C 5

03

AS

AR

CO

LC

810

T31

NR

02W

11A

AA

C1

T31

NR

02W

17D

BB

1

T31

NR

02W

15C

BB

D1

T31

NR

02W

34B

BB

1

T30

NR

02W

10D

CD

1

1,16

0

1,27

0

1,10

0

1,00

0

1,10

0

gTa

ble

1. C

ore

log

anal

ysis

data

Contin

ued

[YY

YY

MM

DD

, yea

r, m

onth

, day

; D

DM

MSS

, deg

rees

, m

inut

es,

seco

nds;

all

units

for

dep

th,

altit

ude,

and

thi

ckne

ss a

re in

fee

t; de

pth

and

altit

ude

refe

r to

the

form

atio

n to

p]

u

O

CO itional

Environment

w 3 5 D

3" a> Q. s o' 9L I 'a. § o'

O

0 a c

o

Site

nu

mbe

r (f

ig.

6)

231

232

233

234

235

236

237

238

Der

by-D

oeru

n D

olom

ite

Dep

th

1,50

0

1,51

6

1,59

2

1,50

1

1,49

8

970

1,59

8

Alti

tude

Thi

ckne

ss

-590

18

-626

99

-742

10

0

-536

10

8

-568

86

-788

18

18

386

Thi

ckne

ss o

f S

t.D

avis

For

mat

ion

Fra

ncoi

s co

nfin

ing

uni

t B

onne

terr

e F

orm

atio

n La

mot

te S

ands

tone

P

reca

mbr

ian

rock

Dep

th

1,52

1

1,51

8

1,61

5

1,25

0

1,69

2

1,60

9

1,58

4

1,17

1

1,69

2

"^

Bor

ehol

es in

Vib

urnu

m T

rend

fro

m w

hich

cor

e

(D Q> 0) 5' 1 i SL

n o (A 2 55'

w

O c

VB

1

VB

2

VB

3

VB

4

VB

5

780

800

728

758

965

380

470

372

242

135

897

900

844

871

1,06

5

Alti

tude

Thi

ckne

ss

Tot

al

Net

sha

le

Dep

th

Alti

tude

Thi

ckne

ss

Dep

th

Alti

tude

Thi

ckne

ss

Dep

th

Alti

tude

-651

31

3 1,

834

-964

39

7 2,

231

-1,3

61

-608

31

9 33

7 1,

837

-927

38

6 2,

223

-1,3

13

-725

29

6 39

5 1,

911

-1,0

21

390

2,30

1 -1

,411

-699

28

0 13

1 1,

530

-979

38

6 1,

916

-1,3

65

124

-842

31

0 41

0 10

0 2,

002

-1,1

52

448

2,45

0 -1

,600

-644

28

3 39

1 1,

892

-927

37

3 2,

265

-1,3

00

-654

27

0 35

6 1,

854

-924

39

0 2,

244

-1,3

14

-878

41

17

3 24

1,

358

-1,1

52

152

1,55

2 -1

,600

8

1,43

7 -1

,223

-200

33

7 65

6 16

2 2,

002

-278

49

6 2,

450

-502

63

, 2,

193

-382

sam

ples

wer

e co

llect

ed a

nd s

ent

for

labo

rato

ry p

erm

eabi

lity

anal

ysis

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Porosity, Vertical Permeability, and Vertical Hydraulic Conductivity Data 61

Tabl

e 2.

Por

osity

, ve

rtic

al p

erm

eabi

lity,

and

ver

tical

hyd

raul

ic c

ondu

ctiv

ity d

ata

[DD

R,

Der

by-D

oeru

n D

olom

ite;

DV

S, D

avis

For

mat

ion;

BN

T, B

onne

terr

e Fo

rmat

ion,

PO

T, P

otos

i D

olom

ite;

C, c

arbo

nate

roc

k; S

, sha

le; B

, bot

h ca

rbon

ate

rock

and

sha

le; <

, les

so

m o o 2. 6" 2L

m 3 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 S- 0) 5"

z Si o' 3 Si ? 3 (A 55'

(0 O

than

; %

, per

cent

]

Sam

ple

num

ber

Min

ing

com

pany

bo

reho

leid

entif

ica

tion

Form

atio

n

Sam

ple

dept

h,in

fee

t

Con

fini

ng

pres

sure

, in

po

unds

per

squa

re in

ch(g

auge

d)1

Poro

sity

,in

perc

ent

Den

sity

, in

gra

ms

per

cubi

cce

ntim

eter

Ver

tical

pe

rmea

bilit

y,in

mill

idar

cies

Ver

tical

hy

drau

lic

cond

uctiv

ity,

in f

eet

per

seco

ndL

ithol

ogy

Des

crip

tion

St. J

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ead

Com

pany

C

onti

nued

19 20 21 22 23 24 25 26 27 28 29 30.

31 32 33 34

83W

34

83W

34

83W

34

83W

34

83W

34

82W

03

82W

03

82W

03

82W

03

82W

03

82W

03

82W

27

82W

27

82W

27

82W

27

82W

27

DV

S

DV

S

DV

S

DV

S

DV

S

DD

R

DD

R

DV

S

DV

S

DV

S

BN

T

DD

R

DD

R

DV

S

DV

S

DV

S

1,57

3

1,68

5

1,72

5

1,78

5

1,79

1

1,56

4

1,58

1

1,62

4

1,69

2

1,84

1

1,89

4

1,44

5

1 ,47

9

1,52

2

1,59

7

1,67

9

1,19

0

1,28

0

1,31

0

1,35

0

1,36

0

1,19

0

1,20

0 i1,

230

1,28

0

1,40

0

1,44

0

1,10

0

1,12

0

1,15

0

1,21

0

1,28

0

1.93

5.32

5.61

3.28

5.99 .6

1

.80

2.37

3.49

.4.9

3

3.18

1.08

1.16

5.00

3.23

6.7

2.75

4

2.68

9

2.71

9

2.80

1

2.75

4

2.82

5

2.82

0

2.82

0

2.67

6

2.75

0

2.80

4

2.83

2

2.81

4

2.67

5

2.72

1

2.78

2

<0.0

0000

1

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054

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0001

<.00

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17X

1Q-

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1.71

X 1

0'12

1.62

X 1

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17X

10'

14

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17X

10'

14

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17X

10'

14

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17X

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1.11

X J

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2

<3.

17X

10'

14

3.11

X 1

0'12

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7X 1

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7X 1

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7X 1

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6.15

X 1

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<3.

17X

10'

14

1.14

X 1

0-'2

C S S C B C C C S S C C C S B S

Dol

omiti

c pa

ckes

tone

with

sha

le s

eam

s

Shal

e

Shal

e

Dig

itate

lim

ey m

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with

wac

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Shal

e w

ith d

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one

Den

se d

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Den

se d

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par

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Shal

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Dol

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Shal

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Am

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Com

pany

35 36 37

801-

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801-

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POT

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1,42

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1,47

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1,50

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2.07

3.54

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2.84

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0.00

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C C C

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Por

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than

; %

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cent

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, 38 39 40 41 42 43 44 45 46 47 48 49 50 51 52 53 54 55 56 57

801-

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801-

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801-

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801-

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1,52

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1,54

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1,57

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1,43

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1,45

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1,48

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1,51

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1,53

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1,49

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1,51

2

1,53

6

1,56

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1,58

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1,60

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1,52

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1,56

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1,60

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1,63

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1,64

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1,15

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1,17

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1,07

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1,09

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1,10

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1,12

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1,15

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1,16

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1,13

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1,15

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1,16

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1,19

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1,20

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1,22

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1,16

0

1,18

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1,21

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1,24

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1,25

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4.02 .8

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4.57

2.31

2.59

2.61

4.49

2.15

2.69

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2.65

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3.13

2.39

2.51

2.71

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2.68

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2.74

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2.85

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2.64

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2.69

6

2.66

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2.70

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2.84

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2.85

0

2.69

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2.69

9

2.66

6

2.71

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2.84

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2.79

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2.71

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2.65

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< o Q)

Tab

le 2

. P

oros

ity,

vert

ical

per

mea

bilit

y, a

nd v

ertic

al h

ydra

ulic

con

duct

ivity

dat

a

[DD

R, D

erby

-Doe

run

Dol

omite

; DV

S, D

avis

For

mat

ion;

BN

T, B

onne

terr

e Fo

rmat

ion,

PO

T, P

otos

i D

olom

ite; C

, car

bona

te ro

ck; S

, sha

le; B

, bot

h ca

rbon

ate

rock

and

sha

le; <

, les

s th

an;

%, p

erce

nt]

Sam

ple

. nu

mbe

r

Min

ing

com

pany

bo

reho

le

iden

tific

a

tion

Form

atio

n

Sam

ple

dept

h,

in f

eet

Con

finin

g pr

essu

re,

in

poun

ds p

er

squa

re in

ch

(gau

ged)

1

Poro

sity

, in

pe

rcen

t

Den

sity

, in

gra

ms

per

cubi

c ce

ntim

eter

Ver

tical

pe

rmea

bilit

y,

in

mill

idar

cies

Ver

tical

hy

drau

lic

cond

uctiv

ity,

in f

eet p

er

seco

ndLi

thol

ogy

Des

crip

tion

Asa

rco C

onti

nued

77 78 79 80 81 82 83 84 85 86 87 88

AC

84

AC

84

AC

84

LC

503

LC

503

LC

503

LC

503

LC

810

LC

810

LC

810

LC

810

LC

810

DV

S

DV

S

DV

S

DD

R

DV

S

DV

S

DV

S

DD

R

DD

R

DV

S

DV

S

DV

S

878

946

1,00

3

806

910

976

1,00

6

1,02

3

1,06

0

1,09

6

1,15

9

1,20

4

670

720

760

610

690

740

760

780

810

830

880

920

10.7 .3

6

8.18 1.69

5.75

9.05

2.14

3.24

3.99

7.25

2.19

1.59

2.71

8

2.71

5

2.79

9

2.81

8

2.76

0

2.68

9

2.70

1

2.79

4

2.81

3

2.71

1

2.71

1

2.69

9

0.00

0030

.000

012

.000

134

.000

106

<.00

0001

<.00

0001

<.00

0001

.000

062

.000

009

<.00

0001

<.00

0001

<.00

0001

9.41

X 1

0'13

3.81

X 1

0'13

4.25

X 1

0'12

3.35

X 1

0'12

<3.1

7X 1

0'14

<3.1

7X 1

0'14

<3.1

7X 1

0'14

1.96

X 1

0'12

2.86

X 1

Q-'3

<3.1

7X 1

0'14

<3.1

7X 1

0"14

<3.1

7X 1

Q-'4

S C B C S s B B B S C B

Shal

e

Lim

ey w

acke

ston

e

Shal

e w

ith d

olom

itic

wac

kest

one

Dol

omiti

c w

acke

ston

e

Shal

e (9

0%)

with

lim

ey w

acke

ston

e

Shal

e

Lim

ey w

acke

ston

e (7

0%)

with

sha

le

Dol

omiti

c m

udst

one

with

sha

le (

10%

)

Dol

omiti

c m

udst

one

with

sha

le (

10%

)

Shal

e

Lim

ey m

udst

one

Lim

ey m

udst

one

50%

with

sha

le 5

0%

'The

app

lied

conf

inin

g pr

essu

re i

s ap

prox

imat

ely

equa

l to

the

pres

sure

cal

cula

ted

usin

g a

grad

ient

of 0

.758

pou

nds

per s

quar

e in

ch p

er f

oot o

f dep

th.

U.S

. G

OV

ER

NM

EN

T P

RIN

TIN

G O

FF

ICE

: 20

00-5

55-1

81/4

0045

KLE

ES

CH

ULTE

AN

D S

EE

GE

R D

epositional Environm

ent, Stratigraphy, and V

ertical Hydraulic C

onductivity U

SG

S W

RIR

00-4037 of the St. Francois C

onfining Unit in the Fristoe U

nit of the Mark Tw

ain National Forest, M

issouri

Documents

Hydraulic Conductivity of the St. Francois Confining Unit in the … · 2011. 8. 25. · hydraulic conductivity for the St. Francois confin ing unit in the study area was calculated