U.S. Department of the Interior

U.S. Geological Survey

Scientific Investigations Report 2006-5198

Prepared in cooperation with the West Virginia Conservation Agency and

the Eastern Panhandle Conservation District

Hydrogeology, Aquifer Geochemistry, and Ground-Water

Quality in Morgan County, West Virginia

Hydrogeology, Aquifer Geochemistry, and Ground-Water 

Quality in Morgan County, West Virginia

By Carol J. Boughton and Kurt J. McCoy

Prepared in cooperation with the West Virginia Conservation Agency and 

the Eastern Panhandle Conservation District 

Scientific Investigations Report 2006–5198

U.S. Department of the Interior

U.S. Geological Survey
U.S. Department of the Interior

DIRK KEMPTHORNE, Secretary

U.S. Geological Survey

P. Patrick Leahy, Acting Director

U.S. Geological Survey, Reston, Virginia: 2006

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reproduce any copyrighted materials contained within this report.

Suggested citation:

Boughton, C.J., and McCoy, K.J., 2006, Hydrogeology, aquifer geochemistry, and ground-water quality in Morgan 

County, West Virginia: U.S. Geological Survey Scientific Investigations Report 2006–5198, 56 p.
iii

Contents 

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

Introduction.....................................................................................................................................................1

Purpose and Scope ..............................................................................................................................1

Description of Study Area ...................................................................................................................1

Methods of Investigation..............................................................................................................................3

Previous Studies ............................................................................................................................................5

Hydrogeology..................................................................................................................................................6

Geology...................................................................................................................................................6

Hydrology ...............................................................................................................................................9

Relation of Geology to Ground-Water Flow.............................................................................9

Aquifer Properties .....................................................................................................................10

Water Levels...............................................................................................................................15

Aquifer Geochemistry and Ground-Water Quality .................................................................................17

Geochemical Properties...................................................................................................................17

Water-Quality Characteristics..........................................................................................................17

pH..................................................................................................................................................17

Specific Conductance...............................................................................................................17

Temperature................................................................................................................................20

Alkalinity......................................................................................................................................21

Water Hardness .........................................................................................................................22

Dissolved Oxygen.......................................................................................................................22

Turbidity .......................................................................................................................................22

Inorganic Constituents.......................................................................................................................22

Major Ions...................................................................................................................................23

Bromide and Fluoride................................................................................................................23

Iron and Manganese.................................................................................................................27

Trace Elements...........................................................................................................................29

Nutrients...............................................................................................................................................29

Nitrate and Nitrite......................................................................................................................29

Ammonia Species......................................................................................................................30

Phosphorous and Orthophosphate.........................................................................................30

Radon-222.............................................................................................................................................31

Bacteria................................................................................................................................................32

Summary and Conclusions.........................................................................................................................33

Acknowledgments.......................................................................................................................................34

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

Appendix 1. Well-construction and aquifer properties for selected wells, Morgan County, 

West Virginia...................................................................................................................................38

Appendix 2a-d. Water-quality data values for wells, Morgan County, West Virginia...................41

Appendix 3a-c. Water-quality data values for springs, Morgan County, West Virginia...............54
iv

Figures

1.-3. Maps showing:

1. Location and physical features of study area ..............................................................................2

2. Location of wells and springs sampled in Morgan County, West Virginia ..............................4

3. Geology of Morgan County, West Virginia, including major structural features and 

lines of section .............................................................................................................7

4. Generalized geologic section of the Great Cacapon and Paw Paw quadrangles, 

Morgan County, West Virginia....................................................................................................8

5. Generalized geologic section of Stotlers Crossroads quadrangle, Morgan County, 

West Virginia .................................................................................................................................8

6. Conceptual model of ground-water flow through a faulted and fractured anticlinal ridge 

bordered by a synclinal ridge ...................................................................................................11

7. Block diagram showing possible circulation of flow to a warm spring located near the 

crest of an anticline at the intersection of two faults...........................................................11

8. Map showing locations and magnitudes of transmissivities, Morgan County, 

West Virginia ...............................................................................................................................14

9. Map showing ground-water-level altitudes and depth to static water levels in 

Morgan County, West Virginia..................................................................................................16

10.-15. Boxplots showing:

10. Distribution of pH values in ground-water samples from hydrogeologic units 

located in Morgan County, West Virginia ..........................................................18

11. Relation between concentration of pH and alkalinity in ground-water samples 

from Morgan County, West Virginia....................................................................18

12. Relation between concentration of pH and dissolved silica in ground-water 

samples from Morgan County, West Virginia....................................................19

13. Distribution of specific conductance in ground-water samples from hydrogeologic 

units located in Morgan County, West Virginia.................................................19

14. Distribution of temperature in ground-water samples from springs and wells 

located in Morgan County, West Virginia ..........................................................20

15. Distribution of temperature in ground-water samples from hydrogeologic units 

located in Morgan County, West Virginia ..........................................................21

16. Diagrams showing relative geochemical composition of ground water from springs 

and wells, by hydrogeologic unit, Morgan County, West Virginia......................................24

17.-22. Boxplots showing:

17. Distribution of concentrations of iron in ground-water samples from hydrogeologic 

units located in Morgan County, West Virginia.................................................27

18. Distribution of concentrations of manganese in ground-water samples from 

hydrogeologic units located in Morgan County, West Virginia......................28

19. Relation between concentrations of iron and manganese in ground-water samples 

from Morgan County, West Virginia....................................................................28

20. Relation between concentrations of zinc and aluminum in ground-water samples 

from Morgan County, West Virginia....................................................................30

21. Distribution of concentration of radon-222 in ground-water samples from 

hydrogeologic units located in Morgan County, West Virginia......................31

22. Relation between the ratio of casing length to well depth and the occurrence of 

bacteria in wells located in Morgan County, West Virginia............................33
Table 

1. Comparison of historical transmissivity and specific-capacity data (Kozar and Mathes, 2001) 

with results from this study for geologic units occurring in Morgan County, 

West Virginia ...............................................................................................................................12

Conversion Factors, Datum, and Abbreviations

Multiply By To obtain

Length

inch (in.) 25.4 millimeter (mm)

foot (ft) 0.3048 meter (m)

mile (mi) 1.609 kilometer (km)

Area

square mile (mi2) 2.590 square kilometer (km2) 

Flow rate

gallon per minute (gal/min) 0.06309 liter per second (L/s)

inch per year (in/yr) 25.4 millimeter per year (mm/yr)

Radioactivity

picocurie per liter (pCi/L) 0.037 becquerel per liter (Bq/L) 

Specific capacity

gallon per minute per foot 

[(gal/min)/ft)]

0.2070 liter per second per meter [(L/s)/m]

Transmissivity

foot squared per day (ft2/d) 0.09290 meter squared per day (m2/d) 

Temperature in degrees Celsius (°C) may be converted to degrees Fahrenheit (°F) as follows:

°F=(1.8×°C)+32

Vertical coordinate information is referenced to the National Geodetic Vertical Datum of 1929 (NGVD 29).

Horizontal coordinate information is referenced to the North American Datum of 1983 (NAD 83).

Altitude, as used in this report, refers to distance above the vertical datum.

Transmissivity: The standard unit for transmissivity is cubic foot per day per square foot times foot of aquifer thickness 

[(ft3/d)/ft2]ft. In this report, the mathematically reduced form, foot squared per day (ft2/d), is used for convenience.

Specific conductance is given in microsiemens per centimeter at 25 degrees Celsius (μS/cm at 25°C).

Concentrations of chemical constituents in water are given either in milligrams per liter (mg/L) or micrograms per liter (μg/L).
vi

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Abstract

Private and public wells throughout Morgan County, 

W. Va., were tested to determine aquifer hydraulic, geochemical, and water-quality characteristics. The entire study area 

is located in the Valley and Ridge Physiographic Province, a 

region of complex geologic structure and lithology. Aquifers 

in the study area are characterized by thin to thick bedded 

formations with interbedding among the various limestones, 

shales, sandstones, and siltstones that are folded into a series 

of steeply dipping north-south trending anticlines and synclines. Zones of ground-water production typically consist 

of one to two fracture sets, with little to no production from 

unfractured bedrock matrix. Measurements of transmissivity 

range from 2 to 1,490 feet squared per day, with the larger 

transmissivities occurring near bedding contacts and in zones 

with cross-faulting or jointing. Ground water flows from 

recharge areas in the uplands to local drainages and to deeper 

flow systems that appear to be controlled by regional geologic 

structure. The overall flow direction is from south to north 

within the study area.

Ground water within the study area is predominantly a 

calcium-bicarbonate type water reflecting contact with carbonate rocks. Sodium-bicarbonate and calcium-magnesium-sulfate end-members also exist, with many samples exhibiting 

mixing, which may be the result of flow between the differing 

rock types or within units containing both carbonate rocks and 

shales. Values of water-quality characteristics that were greater 

than U.S. Environmental Protection Agency drinking-water 

standards included radon-222, pH, turbidity, iron, manganese, 

aluminum, and total- and fecal-coliform and Escherichia coli 

(E. coli) bacteria. Concentrations of radon-222 were detected 

in all samples from all units, with the largest concentrations 

(1,330 and 2,170 picocuries per liter) from the Clinton 

Formation.

Introduction

Economic expansion and population growth from the 

Baltimore, Md., and Washington, D.C., metropolitan corridor 

to Morgan County has led to increased construction of homes 

and businesses with commensurate demands on available 

ground-water supplies. Additional sources of good-quality 

water are needed to allow for continued population and economic growth and to provide alternative supplies in the event 

of a drought such as that during 2001–02. The U.S. Geological Survey (USGS), in cooperation with the West Virginia 

Conservation Agency and the Eastern Panhandle Conservation 

District, conducted a study to assess ground-water conditions 

to provide technical data that could be used as a basis for 

management of Morgan County water resources and future 

planning. Additionally, USGS assessed water-quality and geochemical characteristics of springs in cooperation with West 

Virginia University.

Purpose and Scope

This report describes hydrogeologic, geochemical, and 

water-quality characteristics of aquifers and geochemical 

and water-quality characteristics of select springs located in 

Morgan County, W. Va. The aquifer characteristics include the 

hydrogeologic, physical, and geochemical setting that may 

affect the observed quality. Geochemical, water-quality, and 

hydraulic data were collected over a 1-year period beginning 

in the spring of 2004 through the spring of 2005.

Description of Study Area

Morgan County occupies approximately 231 mi2 in 

the eastern panhandle of West Virginia (fig. 1). The county

was formed in 1820 from parts of Hampshire and Berkeley 

Counties and was named in honor of General Daniel Morgan, a prominent soldier of the Revolution (Holmes, 1995). 

The Potomac River forms the county’s western and northern 

boundaries. Hampshire County, W. Va., and Frederick County, 

Va., form the southwestern and southeastern boundaries, 

respectively. Berkeley County, W. Va., bounds Morgan County 

to the east.

Morgan County lies in the Valley and Ridge Physiographic Province as defined by Fenneman (1946) and is 

characterized by a series of north-northeast trending anticlines 

and synclines, which form prominent valleys and ridges. The 

major physiographic features of much of Morgan County are 

steep-sloped mountains alternating with narrow valleys. 

Hydrogeology, Aquifer Geochemistry, and Ground-Water 

Quality in Morgan County, West Virginia

By Carol J. Boughton and Kurt J. McCoy
 Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia

Figure 1. Location and physical features of study area.
The exception is the eastern part of the county, which is characterized by rolling terrain transitioning to the Great Valley 

along the Route 9 corridor. 

The climate of Morgan County is affected both by 

prevailing continental storm tracks from the west and maritime effects from the Atlantic Ocean (Doll and others, 1963). 

Precipitation in Morgan County falls as winter snow and as 

spring, summer, and fall rains. Weakened hurricanes can produce considerable rain during the late summer and early fall as 

the storm tracks flow northeastward along the Allegheny front. 

The mean annual precipitation as measured at Cacapon State 

Park is approximately 39 in/yr (National Oceanic and Atmospheric Administration, 2002) and ranges from approximately 

36 in/yr in the valleys to 44 in/yr along the Sleepy Creek 

Mountain divide (Hobba and others, 1972).

In addition to the Potomac River, the Cacapon River and 

Sleepy Creek are two relatively large perennial streams within 

the county. Both streams flow in a northerly direction and 

drain into the Potomac River. The Sleepy Creek watershed is 

entirely within the county. 

Smaller streams include Warm Springs Run, Breakneck Run, and Dry Run. The Potomac River bounds Morgan 

County on the west and north. All other streams tend to flow 

in a northerly direction parallel to major geologic structural 

controls and discharge into the Potomac River. Tributaries tend 

to follow trellis geomorphic patterns within structurally controlled basins. Sir Johns Run and Rock Gap Run are among 

exceptions that flow through interbasin water gaps controlled 

by lineaments (Lessing and others, 1991). 

Historically, land use in Morgan County has been that 

of the rural landscape. Grimsley (1916) reported that Morgan 

County was one of the important peach and apple orchard 

sections of the state, exporting large quantities of those fruits. 

Additionally, the county had up to 25 canneries, mostly for 

tomatoes, another significant agricultural product (Grimsley, 

1916). Two incorporated towns existed in 1910, Berkeley 

Springs (Bath) and Paw Paw, having populations of 864 and 

725, respectively (Grimsley, 1916). The leading industry was 

sand and glass, derived from the relatively pure, silica-rich 

Oriskany Sandstone that occurs in the county (Ice, 1933).

As reported in 1980, approximately 81 percent of land 

use in Morgan County was forest, 17 percent was agricultural 

land, and 1 percent was urban or built-up land (McColloch and 

Lessing, 1980). However, landscape and demographics within 

the county have changed appreciably during the past 20 years. 

In 1980, the Morgan County population was 10,606 

(U.S. Department of Commerce, 1991). According to the 

2000 census, the population had increased to 14,943, an 

approximate 40 percent increase in 20 years. During 1990–

2000, the population increased by 23.2 percent 

(U.S. Department of Commerce, 2005). Former agricultural 

and forested land is being urbanized to accommodate the 

increasing population. 

Methods of Investigation

Well sampling sites were selected on the basis of (1) spatial distribution throughout the county and within representative geologic formations; (2) well age, in that wells that were 

recently completed were preferred, whenever possible; and 

(3) landowner’s willingness to provide permission for access 

to existing wells. 

Well-completion reports from the West Virginia Bureau 

for Public Health for 565 wells completed in Morgan County 

during 1997–2002 were reviewed for potential sampling-site 

suitability. The well-completion reports were evaluated for 

completeness and lithologic accuracy based upon knowledge 

of the geology within the county. Recently completed wells 

were preferred to ensure that the wells were properly grouted 

and sealed, thereby minimizing the potential for surface contamination along an open well bore (West Virginia Bureau for 

Public Health, 1984). After initial screening, less than one-half 

of the reports were considered to represent potentially appropriate well sites. Wells were excluded on the basis of incorrect 

lithologic descriptions and inadequate detail.

Potential wells were evaluated to provide spatial distribution throughout the county and among geologic formations. 

Most of the wells that were sampled were domestic wells used 

daily by the homeowners. Others were used seasonally or only 

for watering yards or for watering livestock, and some were 

public-supply wells. 

Hydrogeologic units were sampled in an east-west cross 

section through the county with most aquifers having representative sites to the northern and the southern limits of 

the county to maximize areal distribution of sampling sites. 

Researchers at West Virginia University selected the spring 

sites for sampling. The USGS sampled these in cooperation 

with the university researchers who did a detailed assessment 

of springs in the study area. The resulting ground-water sampling network of 91 wells and 8 springs provides information 

about the variability of hydrogeologic characteristics, groundwater quality, and aquifer geochemistry within and among the 

water-bearing units (fig. 2). 

Ground water was sampled using the techniques 

described in Wilde and others (1999) by purging each well 

with its existing pump. Springs were sampled with a pump as 

close to the point of emergence as possible. Measurements of 

pH, specific conductance (SC), dissolved oxygen (DO), water 

temperature, and turbidity in water from the pumping well or 

spring were recorded until stability criteria were met. 

Methods of Investigation 
Figure 2. Location of wells and springs sampled in Morgan County, West Virginia.

 Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia
Then samples were collected and preserved in the field. 

Samples were shipped to the USGS National Water Quality 

Laboratory (NWQL) in Lakewood, Colo., where they were 

analyzed for concentrations of calcium, magnesium, sodium, 

potassium, chloride, sulfate, fluoride, iron, manganese, silica, 

total dissolved solids, hardness, and nutrients (nitrogen and 

phosphorous species) (American Public Health Association, 

1998; Fishman, 1993; Fishman and Friedman, 1989; Patton 

and Truitt, 1992). Subsets of ground-water samples were analyzed for the trace elements bromide, barium, arsenic, aluminum, zinc, strontium, cadmium, lead, antimony, and nickel 

(Faires, 1993; Fishman and Friedman, 1989; Garbarino, 1999; 

Garbarino and Struzeski, 1998) and for the naturally occurring radioactive gas radon-222 (American National Standards 

Institute, 2004). 

Carbonate alkalinity, bicarbonate alkalinity, and total 

alkalinity were measured in the field using the techniques 

described in Wilde and Radtke (1998). Total-coliform, fecalcoliform, and Escherichia coli (E. coli) bacteria were plated 

on site, incubated, and counted using techniques described in 

Myers and Wilde (2003). 

Previous Studies

A detailed, systematic assessment of ground-water conditions throughout Morgan County has not been published previously. Grimsley (1916) provided an account of the historical 

and industrial development, the physiography, and the geology 

of the eastern panhandle counties, including Morgan County. 

The warm springs now known as Berkeley Springs in the town 

of Bath, W. Va., were prized by native Americans before the 

arrival of white settlers and George Washington noted them in 

his journal as early as 1747. According to Grimsley’s account 

(1916), the springs were known for their uniform water 

temperature from 21 to 23oC throughout the year. Erskine 

(1948) documented seasonal temperatures and discharge from 

Berkeley Spring, Ziler Spring, and Breakneck Run Springs in 

his discussion of the principal springs in West Virginia. 

Hoffman (1962) anticipated that the water needs of individual states, including West Virginia, might parallel the future 

national trend. He further suggested that West Virginia needed 

a close appraisal of its water resources and water problems 

due, in part, to its proximity to the eastern seaboard. According to Doll and others (1963), inadequate hydrologic data for 

planning purposes and increasing competition for water were 

among the water problems facing West Virginia.

Morgan County has been included in several regional 

studies. Doll and others (1963) described the water resources 

of the Potomac River Basin in West Virginia. Three wells in 

Morgan County, one from the Oriskany Sandstone and two 

from the Chemung Group, were identified as yielding 

50 gal/min or more. They noted that artesian conditions occur 

in the deep-lying sandstone beds, reducing the amount of lift 

required but not necessarily producing large well yields. The 

largest reported concentration of total iron from shale aquifers 

was 10.0 mg/L and from limestone aquifers was 5.0 mg/L. 

Water from shale aquifers tended to be more acidic than that 

from limestone aquifers. Within the Potomac River Basin, 

water from shallow, karstic limestone aquifers tended to have 

larger concentrations of nitrate and chloride at some locations. 

The one sample from Morgan County had much smaller concentrations of nitrate and chloride than other sites discussed 

(Doll and others, 1963). 

Hobba and others (1972) published a compendium of 

water-resources information for the Potomac River Basin. 

Sandstone and carbonate-rock aquifers within the basin were 

characterized as having the largest supplies available, owing 

to fractures and solution cavities. Throughout the Potomac 

River Basin, carbonate aquifer yields are highly variable, 

from 5 to over 500 gal/min, and depend upon the well depth 

and local geologic structure. The Oriskany Sandstone yields 

were variable depending upon whether the unit is well jointed, 

cemented, or friable. Low water tables may occur beneath 

ridges underlain by permeable zones of the Oriskany Sandstone as ground-water drains from the unit. In Morgan County, 

only one well, near Paw Paw, W. Va., was identified as producing from alluvium. Ground-water quality throughout the 

Potomac River Basin was found to be variable because of the 

complexity of the lithology and structure (Hobba and others, 

1972).

Schwietering (1981) expanded on the work of Hobba 

and others (1972), describing ground-water conditions and 

aquifers on a statewide scale for West Virginia. Geohydrologic 

units were described in detail; however, few data were published specific to Morgan County except for a further discussion of Berkeley Springs. 

 Hobba (1985) describes ground-water quantity and quality in Hardy, Hampshire, and western Morgan Counties. These 

limited published data illustrate wide ranges in hydrogeologic 

and water-quality characteristics for sites in Morgan County. 

Ferrell (1987) and Mathes and others (1998) provide 

summaries of available ground-water quality data, and Kozar 

and Mathes (2001) provide a compendium of aquifer characteristics throughout West Virginia. However, few data were 

available for Morgan County in these studies. 

Cooper and Hanna (1988) compiled instantaneous 

discharge and temperature data for surface-water stations 

throughout West Virginia for 1945–75. Cacapon River near 

Great Cacapon, W. Va., was the only site located in Morgan 

County for which data were available. 

Hobba and others (1979) discussed the geology, hydrology, and geochemistry of the Berkeley Springs area in their 

study of thermal springs in the Appalachians. McColloch 

(1986) produced a compendium of springs of West Virginia 

that summarizes available data for 14 springs in Morgan 

County, including Hancock Station Spring, Michael Farm 

Spring, Berkeley Springs, Robert Milborn Spring, Fahren 

Spring, Mitchum Farm Spring, Coolfont Spring, Whisner 

Farm Spring, Neely Farm Spring, Ziler Spring, Cacapon State 

Previous Studies 
Park Spring, Ridge Hatchery Spring, O.B. Overmale Springs, 

and an unnamed spring. 

Hydrogeology

Ground water is stored in intergranular spaces, in bedrock 

fracture features, and in solutionally enhanced fractures within 

Morgan County. The intergranular space within the bedrock 

matrix is referred to as primary porosity. Ground water does 

not flow readily through the intergranular spaces in bedrock 

because of a lack of connectivity and of cementation of voids. 

Ground water flows more readily through bedrock with 

secondary porosity. Secondary porosity occurs in fracture 

features, including faults, joints, and partings at contact zones 

and in solutionally enhanced features, which have much larger 

effective porosity. The structural and depositional geology 

controls the directional orientation and size of the fractures.

Geology

The rocks of Morgan County (fig. 3) are of Ordovician (Oswego and Juniata Formations), Silurian (Tuscarora 

Sandstone, Clinton Group, McKenzie Formation, Williamsport 

Sandstone, Wills Creek Formation, Tonoloway Formation), 

Devonian (Helderberg Group, Oriskany Sandstone, Onesquethaw Group, Marcellus Formation, Mahantango Formation, Harrell Shale, Brallier Formation, Chemung Group, and 

Hampshire Formation), and Mississipian (Pocono Group), 

ages (Cardwell and others, 1968). The rocks were folded and 

faulted extensively during the formation of the Appalachian 

Mountains, resulting in a series of northeast-southwest trending anticlines and synclines with beds of varying width (figs. 4 

and 5). The beds plunge slightly to the north. Underlying resistant rocks such as sandstones form the ridges and less resistant 

rocks such as shales typically form the valleys (Hobba and 

others, 1972). 

Lithologic descriptions in well-completion reports and 

other available mapping are approximate on a site-specific 

basis; therefore, throughout this report, undifferentiated references to the Brallier Formation will include the Brallier Formation and the Harrell Shale and references to the Tonoloway 

Formation will include the Tonoloway Formation, Wills Creek 

Formation, and Williamsport Sandstone. The Needmore Shale 

and Huntersville Chert are mapped as the Onesquethaw Group 

(Cardwell and others, 1968), but the section is so narrow in the 

study area that it is not mappable at the 1:250,000 scale. 

Deposits of unconsolidated alluvial material typically 

occur near major streams and consist primarily of clay and silt, 

with some discontinuous lenses of sand and gravel. Alluvial 

deposits occasionally occur on terraces, but are typically 

unsaturated. Significant saturated thicknesses are generally 

found only near major streams (Hobba and others, 1972). No 

wells were identified as producing from the alluvium in this 

study; therefore, the alluvial aquifer system is not discussed 

further in this report. 

The Pocono Group is gray, hard, massive sandstone with 

some shale beds. The thickness of the Pocono Group is as 

much as 1,030 ft (Cardwell and others, 1968). It is underlain 

by the Hampshire Formation, a maroon to reddish-brown siltstone and shale in the upper 300 to 400 ft of the formation and 

fine-grained, well-cemented, hard, massive red sandstone with 

some shale in the lower part. The thickness of the Hampshire 

Formation is as much as 3,350 ft (Cardwell and others, 1968). 

The Chemung Group is typically a rusty-yellowish brown. The 

upper formation is thin-bedded, hard, blocky sandstone underlain principally by thin-bedded siltstone and shale. The thickness of the Chemung Group is as much as 2,115 ft (Cardwell 

and others, 1968). A massive sandstone member occurs at its 

base in the easternmost areas (Hobba and others, 1972). The 

Pocono Group, Hampshire Formation, and Chemung Group 

occur extensively in both the western and eastern parts of the 

county.

The Brallier Formation is a greenish-gray shale with siltstone and sandstone that constitutes approximately 35 percent 

of the formation. The thickness of the Brallier Formation is 

as much as 1,300 ft (Cardwell and others, 1968). The Harrell Shale is black shale that occurs in the lower 50 to 400 ft 

of this formation. The thickness of the Harrell Shale is zero 

to 50 ft (Cardwell and others, 1968). Lying below the Harrell 

Shale, the Mahantango Formation consists of brown sandy 

shales with occasional sandstone beds and concretions found 

near the contact with the underlying Marcellus Formation. 

The thickness of the Mahantango Formation is as much as 

1,200 ft (Cardwell and others, 1968). The Marcellus Formation is black carbonaceous, clayey, thinly laminated, fissile 

shale containing pyrite and minor amounts of siltstone (Reger, 

1924). The thickness of the Marcellus Formation is as much 

as 200 ft (Cardwell and others, 1968). Thinly bedded and 20 

to 40 ft thick, the Purcell Member of Pennsylvanian limestone 

(Cardwell and others, 1968) occurs approximately 50 to 150 ft 

from the base (Reger, 1924), and large limestone concretions 

are known to occur near the base of the Marcellus Formation 

(Hobba and others, 1972). 

The Onesquethaw Group, consisting of the Needmore 

Shale and Huntersville Chert, occurs below the Marcellus Formation. The Needmore Shale is a predominately dark gray or 

green, calcitic, mostly nonfissile, gamma-ray-emitting shale. 

It includes the Black Beaver Dam Shale member and grades 

westward into the Huntersville Chert. The Tioga bentonite 

occurs near the top of the Needmore Shale. The thickness of 

the Needmore Shale ranges from 75 ft to 140 ft (Cardwell and 

others, 1968).

 Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia
Figure 3. Geology of Morgan County, West Virginia, including major structural features and lines of section. Geology modified from 

Lessing and others (1997), Lessing and others (1991), and Cardwell (1968).

Hydrogeology 
Figure 4. Generalized geologic section of the Great Cacapon and Paw Paw quadrangles, Morgan County, West Virginia. Modified from 

Lessing and others (1997). (Line section of A-A’ as shown on figure 3.)

Figure 5. Generalized geologic section of Stotlers Crossroads quadrangle, Morgan County, West Virginia. Modified from Kulander and 

others (1995). (Line of section B-B’ as shown on figure 3.)

 Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia

0 5,000 10,000 Feet

Sea Level

4,000

8,000

Sea Level

4,000

8,000

Stotlers Crossroads

Quadrangle

Great Cacapon

Quadrangle

Stotlers Crossroads

Quadrangle

Big Pool

Quadrangle

EXPLANATION

Fault

Cacapon Mountain 

 Anticlinorium

Pious Ridge Synclinorium

Sleepy Creek Anticlinorium

Meadow Branch 

B Synclinorium

Woods Fault

B’

0 5,000 10,000 Feet

Sea Level

Great Cacapon

Quadrangle

EXPLANATION

Fault

A Town Hill Syncline

A’

4,000

8,000

Sea Level

4,000

8,000

Paw Paw

Quadrangle

Potomac River

Whip Cove Anticline

Sideling Hill Synclinorium

Cacapon River Fault

Boundary Fault

Cacapon Mountain Anticlinorium

Pine Ridge Anticlinorium

Pious Ridge Syncline

Great Cacapon

Quadrangle

Glengary

Quadrangle

MD WV
The other member of the Onesquethaw Group is the 

Huntersville Chert, which grades from a nearly pure, slightly 

calcitic or dolomitic chert (interbedded with the Needmore 

Shale), to a limestone westward. That limestone, commonly 

referred to as the Onondaga, includes the glauconitic [(K,Na)(

Fe3+,Al,Mg)2(Si,Al)4O10(OH)2] Bobs Ridge Sandstone member (Cardwell and others, 1968). Although the Onesquethaw 

(Onondaga) Group is narrow and may not constitute a potentially significant aquifer, its mineralogy may affect groundwater quality where it does occur. The gamma-ray emissions 

may be associated with radon in drinking water. Glauconite is 

used as a water softener, so its occurrence could account for 

zones of naturally occurring soft water.

The Oriskany Sandstone is a medium- to thick-bedded 

brown to white sandstone lying between two layers of soft calcareous chert. The thickness of the Oriskany Sandstone ranges 

from 12 ft to 275 ft (Cardwell and others, 1968). Cementation 

of these rocks varies from very hard silica cement to softer 

carbonate cement to friable and devoid of cement depending 

upon the location. The upper chert layer ranges in thickness 

from 0 to 100 ft. In Morgan County, the lower Shriver Chert is 

very thin or absent (Hobba and others, 1972).

The Helderberg Group varies from thin-bedded, light-colored, cherty limestone in the upper part to thin-bedded shale 

in the middle part to massive-bedded relatively pure limestone 

in the lower part. The thickness of the Helderberg Group is 

as much as 170 ft (Cardwell and others, 1968). The underlying Tonoloway Formation consists of gray, flaggy, thin beds 

containing some silica and dolomite and grading downward 

into flaggy limestone and calcareous shales of the Wills Creek 

Shale. Red or green sandy shales and one hard sandstone bed 

occur at the base (Hobba and others, 1972). The thickness of 

the Tonoloway Formation is as much as 590 ft and the thickness of the Wills Creek Shale is as much as 400 ft (Cardwell 

and others, 1968).

The McKenzie Formation is a bluish-gray, wavy-bedded, 

flaggy limestone and limy shale, whereas the underlying Clinton Group consists of red shale with thin beds of sandstone 

and occasional limestone layers. The thickness of the 

McKenzie Formation is as much as 240 ft (Cardwell and 

others, 1968). The Tuscarora Sandstone is thick-bedded, 

extremely hard, resistant, and is colored gray to pink. By way 

of contrast, the “red beds” of the Juniata Formation are thinbedded block sandstone and shale. In places, this formation 

is underlain by thick-bedded gray Oswego Sandstone (Hobba 

and others, 1972). The thickness of the Tuscarora Sandstone 

is as much as 100 ft; of the Juniata Formation is as much as 

320 ft; and of the Oswego Sandstone is as much as 300 ft 

(Cardwell and others, 1968).

Hydrology

The study area is predominantly underlain by folded, 

faulted, and fractured sedimentary shale, carbonate, and sandstone rocks that form the aquifer systems. Recharge occurs 

throughout the study area, particularly in the upland areas. 

Discharge occurs locally to streams and springs, then regionally to the Potomac River. Ground-water discharge, including 

spring discharge, provides base flow to the streams.

Relation of Geology to Ground-Water Flow

The flow of ground water in the study area is complicated 

because of the structural and lithologic complexity of the Valley and Ridge Physiographic Province. The bedrock generally 

has small primary permeability in the rock matrix and much 

larger secondary permeability in fractures, along bedrock contacts, and in solutionally enhanced zones of preferential flow. 

Similar to the hydrogeology of the Appalachian Plateaus Physiographic Province (Wyrick and Borchers, 1981), wells that do 

not penetrate fractures or solution channels will not produce 

usable amounts of water. Flow paths in Morgan County are 

complicated by the complex system of steeply dipping, northsouth trending anticlines and synclines that form the topography typical of the Valley and Ridge Physiographic Province. 

Well yields in primarily limestone rock along the axes 

of anticlines are found to be appreciably larger than those 

along axes of synclines (Clark and others, 1976). Siddiqui and 

Parizek (1972) found that variation in structural control is not 

a statistically significant factor in the productivity of wells 

not located on fracture traces. Ground-water flow in Morgan 

County may occur through fracture sets that parallel anticlinal 

axes. Where deep vertical faults or horizontal thrust faults 

intersect these fractures, they provide conduits for potentially 

large well yield. 

McCoy and others (2005a, 2005b) found in Berkeley 

and Jefferson Counties that discrete fracture zones within 

the bedrock yield water to the majority of wells tested. Over 

500 recent (1997–2004) well-completion reports for Morgan 

County were examined during the course of this study. Not 

all completion reports clearly indicated the water-production 

zones encountered. The completion reports that indicate location of production zones show a clear pattern of production 

from one to two discrete zones, sometimes described as being 

at contacts between units and sometimes as apparent fracture 

zones within a given bedrock unit. There was no indication of 

usable, continuous production along the well bore from either 

fractures or bedrock matrix. Although many fractures intersect 

a borehole, only a few may yield usable quantities of ground 

water. Aquifer yields are dependent upon water produced from 

fractures, faults, or along contact zones. 

Ground water flows from areas with higher hydraulic 

head toward areas of lower hydraulic head. The preferential 

flow path followed will be that which has the largest transmissivity or ability to transmit water. Toth (1963) describes 

an idealized model for flow systems in most field areas with 

negligible local topographic relief; however, in areas with pronounced local relief, such as the Valley and Ridge Province, it 

is possible that only local systems develop (Freeze and Cherry, 

1979).

Hydrogeology 
Within the study area, the ground water flows from 

recharge areas in the uplifted geologic features such as 

Cacapon Mountain and Sleepy Creek Mountain toward the 

valleys and then discharges to the north toward the Potomac 

River. Locally, ground water flows to springs, streams, or 

nearby pumping wells that intercept the flow and cause minor, 

localized perturbations in the flow path.

Transmissivity, typically, is the largest downdip along 

bedding planes or fractures parallel to bedding planes, 

although intersecting faults or fracture zones may act as drains 

and route flow across structural features. The folded and 

uplifted bedrock of the Appalachian Mountains may serve as 

a barrier to flow between major tributary basins such as the 

Cacapon and Warm Springs Run watersheds except where 

flow occurs along bedding planes or through other fractured 

and faulted features (fig. 6). 

Cross-faulting occurs near the town of Bath, where the 

Berkeley Springs arise (Hobba and others, 1979). Ground 

water contributing to the Berkeley Springs is thought to be 

derived from recharge to and deep flow through the Oriskany 

Sandstone. Water budget, temperature, and geochemical data 

tend to support this conceptual model (Hobba and others, 

1979). Water is recharged rapidly into and through the friable 

Oriskany Sandstone and the cross-faulting serves as a drain, 

routing water to the Berkeley Springs (fig. 7).

Other structural offsets occur in addition to the fault 

trace depicted above. Structural offsets also occur at Rock 

Gap Run, North Fork Run, and Breakneck Run, which dissect 

Warm Springs Ridge and at Constant Run (Ziler Ford), which 

dissects Tonoloway Ridge at its southern edge. Cardwell and 

others (1968) mapped joints (approximately perpendicular to 

faults) coincident with the Constant Run, Rock Gap Run, and 

North Fork Run drainages. In addition to the Berkeley Springs, 

other regional springs occur in the study area. 

Lessing and others (1991) report the relations between 

eight warm springs and the geology of eastern West Virginia 

by use of side-looking airborne-radar (SLAR). All of the 

springs discharge from Oriskany Sandstone or adjacent limestones of the Helderberg Group, although deep ground-water 

circulation to the Helderberg Group may be through the Oriskany Sandstone. They hypothesize that precipitation recharges 

the Oriskany Sandstone at ridgetop outcrops, then percolates 

deeply through the friable Oriskany Sandstone along fault 

zones where the ground water is geothermally heated. The 

ground water then flows through the highly permeable lineament, surfacing at the spring sites rapidly enough that the heat 

is not dissipated.

Ridge Hatchery Spring (site 93) surfaces in Breakneck 

Run, and Cacapon Spring (site 94) occurs in North Fork Run. 

Bedrock in lower Breakneck Run is highly fractured and 

occurs as blocky rubble along the mountainside and onto the 

valley floor. Zones of blocky fractured bedrock and bedrock 

rubble are very transmissive to water. Shallow subsurface flow 

can be heard beneath the rubblized deposits along the valley floor in the Breakneck Run drainage. Recharge areas for 

the Ridge Hatchery Springs include Cacapon Mountain and 

potentially some local component of flow from Warm Springs 

Ridge. Ridge Hatchery Springs does not appear to have come 

from a deep flow system, as evidenced by water temperature 

and specific conductance. 

Aquifer Properties

The specific capacity of a well is the rate of discharge of 

a well divided by the drawdown of the water level in the well 

and depends both upon the hydraulic properties of the aquifer 

and upon the construction and other features of the well. Specific-capacity estimates may be used to evaluate regional differences in transmissivity, which is the capability of an aquifer 

to transmit water through a unit width of aquifer under a unit 

hydraulic gradient (Heath, 1983). Short-term, single-well aquifer tests are used as the basis for estimating transmissivity of 

aquifer units in Morgan County. Transmissivity estimates are 

useful for developing a conceptual model of the aquifer and 

as input for modeling a ground-water flow system; however, 

transmissivity can be highly variable from one geographic 

location to another, both within a given geologic unit and 

among units. Additionally, an aquifer with a large transmissivity may be vulnerable to rapid contaminant transport, and 

aquifers with large transmissivities may be locally depleted if 

stressed beyond their sustainable yield.

Kozar and Mathes (2001) compiled aquifer characteristics from existing sources for the entire State of West Virginia. 

Two key characteristics discussed in that publication are specific capacity, defined as the rate of discharge of a well divided 

by the drawdown of the water level in the well; and transmissivity, defined as the rate at which water of a prevailing viscosity is transmitted through a unit width of aquifer under a unit 

hydraulic gradient (Kozar and Mathes, 2001). Although few of 

the data originated from wells in Morgan County, the values 

provide insight as to the range of values for hydraulic properties that occur throughout the extent of the hydrogeologic 

units. Specific-capacity and tranmissivity data from throughout West Virginia (Kozar and Mathes, 2001) are summarized 

in table 1 for hydrogeologic units that occur in the study area. 

Except where otherwise noted, no data from the Kozar and 

Mathes (2001) report are available for the study area. 

The largest specific capacity (600 (gal/min)/ft) and transmissivity (60,000 ft2

/d) are in the Helderberg Group, Tonoloway Formation, and Wills Creek Shale. The Pocono Group 

and related MacCrady Formation, Hampshire Formation, and 

Chemung Group have the potential for moderate yields with 

maximum specific capacities of 8.67 (gal/min)/ft, 

12.5 (gal/min)/ft, and 30.7 (gal/min)/ft, respectively, and 

maximum transmissivities of 2,300 ft2/d, 2,900 ft2/d, and 

8,300 ft2/d, respectively. One site located in the study area 

has a specific capacity of 0.89 (gal/min)/ft and an estimated 

transmissivity of 240 ft2/d from the Hampshire Formation 

(Kozar and Mathes, 2001). 

10 Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia
Figure . Conceptual model of ground-water flow through a faulted and fractured 

anticlinal ridge bordered by a synclinal ridge. Water infiltrates through faults and 

fractures along the anticlinal ridge, then flows parallel to the bedding plane to 

recharge a confined aquifer underlying the nearby syncline (modified from Hobba 

and others, 1979).

Figure 7. Block diagram showing possible circulation of flow to a warm spring 

located near the crest of an anticline at the intersection of two faults (modified from 

Hobba and others, 1979).

Hydrogeology 11
Table 1. Comparison of historical transmissivity and specific-capacity data (Kozar and Mathes, 2001) with results from this study for geologic units occurring in 

Morgan County, West Virginia. [ft2/d, foot squared per day; [(gal/min)/ft], gallons per minute per foot of drawdown]

Historical transmissivity data

(ft2/d)

Transmissivity data from this study

(ft2/d)

Historical specific-capacity data

[(gal/min)/ft]

Specific-capacity data from this 

study

[(gal/min)/ft]

Geologic unit Minimum Median Maximum Minimum Median Maximum Minimum Median Maximum Minimum Median Maximum

Pocono Group 33 210 2,300 1

5 1

5 1

5 0.17 0.83 8.67 10.13 10.13 10.13

Hampshire 

Formation

3 74 2,900 2 21 577 .01 .31 12.5 .06 .23 .86

Chemung Group 32 270 8,300 2 22.5 1,490 .12 1.35 30.7 .09 .46 3.75Brallier Formation 

and Harrell Shale

3 72 390 2 4.5 96 .01 .28 1.60 .06 .27 1.00

Mahantango 

Formation

3 92 840 2 19 944 .01 .38 3.75 .08 .53 4.61

Marcellus 

Formation and Needmore Shale

16 170 1,300 54 128 327 .07 .86 7.00 .05 .40 .99

Oriskany 

Sandstone

19 82 1,500 (2) (2) (2) .10 .35 8.00 (2) (2) (2)

Helderberg Group, 

Tonoloway Formation, and Wills Creek Shale

17 200 60,000 3 29.5 138 .07 .82 600 .06 .59 1.42

McKenzie 

Formation, Clinton Group, and Tuscarora Sandstone

6 23 1,100 2 124.5 266 .02 .11 6.50 .38 1.05 3.75

1 One sample available.2 No samples taken.

12  Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia
The Mahantango Formation; Marcellus Formation and Needmore Shale; Oriskany Sandstone; and McKenzie Formation, 

Clinton Group, and Tuscarora Sandstone generally have much 

smaller maximum specific capacities of 3.75 (gal/min)/ft, 

7.00 (gal/min)/ft, 8.00 (gal/min)/ft, and 6.50 (gal/min)/ft, 

respectively, and transmissivities of 840 ft2/d, 1,300 ft2/d, 

1,500 ft2/d, and 1,100 ft2/d, respectively. The Brallier Formation and Harrell Shale have the smallest maximum specific 

capacity (1.60 (gal/min)/ft) and maximum transmissivity 

(390 ft2/d) (Kozar and Mathes, 2001) (table 1). 

Single-well aquifer tests were done on private and publicsupply wells to estimate transmissivity of aquifers in Morgan 

County (Appendix 1). Short-term aquifer tests, consisting of a 

drawdown phase and recovery phase, were done at most sites. 

In some instances, well production was so small and drawdown was so rapid that aquifer tests were discontinued prior 

to completion of the tests to avoid effects to the homeowner’s 

well. In other instances, water levels were at a depth greater 

than 300 ft and could not be measured with available equipment. Some wells contained spacers or other equipment that 

precluded downhole placement of the pressure transducer 

necessary to conduct the test. Pump-cycling (the pump turning 

on and off) occurred at many of the sites.

During the drawdown test, the wells were pumped for 

approximately 30 minutes at a flow rate ranging from 0.80 to 

60.0 gal/min. The analytical technique of Theis (1935) could 

not be used for tests in which interference occurred because of 

pump cycling. Transmissivity was computed only from recovery data at those sites. 

When the pumping is terminated, water from within 

the aquifer flows toward the well bore and, over time, the 

water level recovers to static conditions. During this aquifer 

recovery period, water-level data typically were recorded for 

approximately 60 minutes, with some recorded for as long 

as 131 minutes. Recovery data were analyzed by using the 

techniques of Theis (1935), which are based upon certain 

simplifying assumptions of aquifer properties: a homogeneous 

(identical properties throughout), isotropic (same properties 

with the same values when measured along axes in all directions), confined aquifer that is uniform in thickness and infinite in extent. The well is assumed to be infinitesimally small 

in diameter and to fully penetrate a confined aquifer. These 

are considered ideal aquifer conditions. Conditions in Morgan 

County are nonideal conditions; however, the technique was 

applied to generate a range of values for the aquifer properties 

of hydrogeologic units in the study area. 

With the exception of the highly friable zones of the Oriskany Sandstone, aquifers in Morgan County are very heterogeneous and anisotropic. Typically, well-completion reports 

for the county indicate the presence of only one to two isolated 

zones of production along the length of the wellbore. Parameter estimates in poorly transmissive zones of the aquifer are 

subject to error because of unaccounted-for wellbore storage 

effects. 

Tiedeman and Hsieh (2001) tested fractured crystallinerock aquifers and concluded that the borehole connects highly 

permeable zones separated by impermeable rock. Hsieh and 

Shapiro (1996) further state that single-well tests show the 

effects of only the few highly transmissive fractures and are 

not representative of the overall bulk-rock properties. Schad 

and Teutsch (1994) suggest that the Theis solution can be 

used for comparison of values within a single dataset rather 

than representing the values as valid for a rock type. For the 

purposes of this report, the transmissivity values are used to 

evaluate the variability within aquifers and among rock types 

in Morgan County and should not be used for direct comparison with data from other areas, although they may provide a 

basis for design of more complex aquifer tests. 

Parameter estimates from drawdown and recovery tests 

agreed to within 174 percent of each other. Parameter estimates from recovery tests exceeded those from drawdown 

tests at 74 percent of the sites. Reported values reflect the 

average transmissivity derived from both the pumping and 

recovery tests. The median transmissivity for the entire dataset 

(91 wells with 21 pumping and 70 recovery tests) was 

23.0 ft2/d, with a minimum of 2.0 ft2/d and a maximum of 

1,490 ft2/d (Appendix 1).

Linear regression analysis of Morgan County well sites 

shows no significant correlation (r2 = 0.00) between well 

depth and transmissivity. The median transmissivity for wells 

with depths less than or equal to 150 ft below land surface is 

27.2 ft2/d. The median transmissivity for wells greater than 

150 ft below land surface is 21.4 ft2/d. This transmissivity distribution indicates that discrete flow zones, although smaller 

at depth, are not restricted to the upper portion of the aquifers. 

The data also are consistent with data from nearby Berkeley 

County, W. Va., that indicate a slight reduction in aquifer yield 

below a depth of approximately 150 ft below land surface 

(Shultz and others, 1995). Transmissivities range over more 

than two orders of magnitude. The largest calculated transmissivities were at site 77, which lies approximately at the 

contact between the Chemung Group and the Brallier Formation with a transmissivity of 1,420 ft2

/d, and at site 85, which 

lies approximately at the contact between the Mahantango and 

Brallier Formations, with a transmissivity of 944 ft2/d (fig. 8). 

In the study area, larger aquifer transmissivity typically occurs 

at or near geologic contacts and in zones of cross-faulting or 

thrust-faulting. 

Transmissivity data for geologic units located in the study 

area from previous studies are compared with those from 

this study (table 1). In general, the transmissivities from this 

study were smaller than those previously documented for the 

Hampshire Formation, Chemung Group, and Brallier, Mahantango, Marcellus, Tonoloway, and Clinton Formations (Kozar 

and Mathes, 2001). Only one site was sampled in the Pocono 

Group, and that transmissivity was nearly an order of magnitude smaller than those reported by Kozar and Mathes (2001). 

Hydrogeology 13
Figure 8. Locations and magnitudes of transmissivities, Morgan County, West Virginia. Geology after Cardwell (1968).

14  Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia
Values for previous transmissivity data within the study area 

for the Marcellus and Hampshire Formations (Kozar and 

Mathes, 2001) are within the range of values obtained during 

this study. Site-specific hydrogeologic details are difficult to 

assess from the literature; however, depths for the sites with 

the largest transmissivities reported by Kozar and Mathes 

(2001) tend to be shallower than the typical well depth in 

Morgan County. Well yields decrease appreciably at depths 

below approximately 150 ft below land surface because of a 

decrease in fracturing (Shultz and others, 1995). Lithostatic 

pressure from the mass of overlying rock tends to compress 

fracture partings. Tranmissivity of the Oriskany Sandstone was 

not sampled during this study because it has narrow outcrops 

along Warm Springs Ridge where few dwellings exist, thus 

limiting availability of sampling sites.

Site-specific geographic location cannot be used to 

predict transmissivity. Wells in close geographic proximity 

within the study area have transmissivities that vary by more 

than two orders of magnitude. The exception is that aquifers 

tested along ridgetops tend to have smaller transmissivities 

than those in valley settings, and zones of production tend to 

be deep, in excess of 400 ft below land surface. 

Water Levels

Ground-water flow paths are a reflection of the complex 

geologic setting in the study area. Static water-level data were 

obtained at 84 sites throughout Morgan County (fig. 9). 

Data density is not adequate to predict local or site-specific flow systems with any certainty or to develop countywide 

static water-level contours. These data are used to develop a 

conceptual model of the generalized ground-water-flow patterns, which will be addressed progressively from west to east 

in the study area.

The Sideling Hill Syncline is a recharge area with 

recharge draining to depth through the fractured Hampshire 

Formation. Wells range from 380 to 460 ft deep and have low 

yields from fracture sets at depth. Static water levels range 

from approximately 100 ft to greater than 220 ft below land 

surface. Bare Ridge, Road Ridge, and Tonoloway Ridge may 

form structural barriers to the east. Ground-water flow appears 

to be northward within the Willett Run drainage, as the static 

water level is several hundred feet lower at the north end of 

that drainage than at its southern reaches. 

Water levels at locations near the Cacapon River range 

from 20 ft to approximately 60 ft below land surface. The 

ground-water gradient indicates that ground-water flow follows a path similar to the Cacapon River from the southern 

boundary of the study area, through a water gap at Constant 

Run that occurs at the south end of Tonoloway Ridge, and then 

northward. The Constant Run water gap is coincidental with 

cross-faulting that occurs in that gap between the south end of 

Tonoloway Ridge and the north end of Little Mountain (fig. 3). 

That fault trace appears to be present at the Potomac River 

to the west and is evident as far east as Cacapon Mountain. 

It appears to act as a subsurface drain to the north-northeast, 

along the Cacapon River Fault. There may be a ground-water 

divide north of the fault trace, but additional data are required 

to validate that hypothesis. 

Cacapon Mountain is a recharge area. The hinge line of 

the Cacapon Mountain Anticline may be a drainage divide 

with ground water flowing to the west and the east; however, the Boundary Fault underlies Cacapon Mountain. This 

slip-fault extends as deep as the Martinsburg Decollement, 

several thousand feet below land surface and may serve as a 

bounding fault to the west or the fault zone may serve as a 

conduit for deep flow to the ground-water system east of the 

anticline. Grimsley (1916) characterizes this area has having a 

series of crumpled, fluted folds mapped at the surface, which 

tends to support the potential for flow through fractures or 

joints. Alternatively, ground water could flow toward the west 

and may leave the system through the Cacapon River Fault 

zone (fig. 4). Deep flow to the east from the crest of Cacapon 

Mountain could account for head needed to produce the artesian conditions (water levels within 10 feet or less from land 

surface) that occur in Sir Johns Run and east of Warm Springs 

Ridge (sites 33, 34, 61, 70, 73, and 74) (fig. 2).

Hydrogeologic data are not available along the crest 

of Cacapon Mountain (the anticline hinge-line), but one 

site (59) near the top of the mountain has a static water level 

of approximately 1,080 ft above sea level, considerably higher 

than others in the Sir Johns Run drainage. Sir Johns Run 

drainage is described by Grimsley (1916) as a Silurian valley 

lying between the resistant sandstone ridge that caps Cacapon 

Mountain and Warm Springs Ridge also formed by another 

resistant sandstone unit, the Oriskany Sandstone. The drainage 

between was formed by erosion of intervening, less resistant 

shales. Ground-water level altitudes in Sir Johns Run drainage tend to be lower toward the north, from approximately 

890 ft to 710 ft at the north end of the drainage, indicating 

that ground water flows northward. There is an anomaly in the 

water levels in Warm Springs Run drainage north of the town 

of Bath. This localized perturbation of the flow path may be 

the result of dewatering operations at a mine in Warm Springs 

Ridge.

The Third Hill Mountain complex lies along the hinge 

line of the Meadow Branch Synclinorium. Localized recharge 

occurs along this ridge, which also acts as a ground-water 

divide with flow to the northeast and northwest following the 

north-south structural trends with the units plunging slightly 

to the north. Water levels confirm this conceptual model. Six 

wells were hydraulically tested in the area east of Third Hill 

Mountain; the transmissivity measured at four of those wells 

was more than 100 ft2/d, whereas the transmissivity at two of 

the sites was appreciably less than 20 ft2/d. This variability 

may be complicated by the occurrence of the Woods thrust 

fault in that area that offsets already complex geology. Grimsley (1916) reported the presence of striated and polished rock 

surfaces, known as slickensides, on the faults near Third Hill 

Mountain. Slickenside rocks may act as barriers to flow rather 

than as conduits typical of extensively fractured rock.

Hydrogeology 15
Figure 9. Ground-water-level altitudes and depth to static water levels in Morgan County, West Virginia.

16  Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia
Aquifer Geochemistry and GroundWater Quality 

Ninety-one wells and eight springs in the study area were 

evaluated for aquifer geochemistry and ground-water-quality 

characteristics (Appendixes 2 and 3). Geochemical properties 

and ground-water quality are largely affected by composition 

of the rocks in the aquifer. Additionally, contaminants may be 

introduced by human activities or other environmental factors. 

USEPA has established regulatory water-quality standards for 

specified constituents for the point of delivery from public 

water supply systems. The standards are based upon potential 

human-health or esthetic effects (U.S. Environmental Protection Agency, 2005a, b, c).

Geochemical Properties 

Geochemical properties of aquifer systems are naturally 

variable and dependent upon the mineralogic composition of 

the rocks encountered along the ground-water flow path. The 

three major sedimentary rock types (carbonates, sandstones, 

shales) all occur in Morgan County. Limestone and dolomite 

rocks have a predominant calcium-bicarbonate or calciummagnesium-bicarbonate geochemical signature, respectively. 

Pure sandstone is quartzite that may be cemented by silica 

or by calcium carbonate or may contain little cementation. 

In Morgan County, cementation of the Oriskany Sandstone 

varies depending upon location. Sandstone cemented by silica 

may have up to 99 percent pure silica content, which will be 

reflected in the geochemical signature. Shales primarily consist of various clay minerals and quartz. Shales formed under 

anaerobic conditions may retain organic matter and may have 

a large sulfur content. Other shales may be enriched in metals 

such as arsenic, barium, boron, chromium, copper, fluoride, 

gallium, lithium, mercury, selenium, titanium, uranium, 

yttrium, vanadium, and zinc (Brownlow, 1979). Ground water 

may reflect a mixture of the geochemical characteristics as it 

flows progressively through one rock unit and then through 

another. Complex geochemical interactions may result in 

dissolution of certain constituents and precipitation of other 

constituents over time. Geochemical properties and concentrations of water-quality constituents for wells and springs 

sampled during this study are presented in Appendixes 2 and 

3, respectively. 

Water-Quality Characteristics

Where appropriate, concentrations or other water-quality values are compared with U.S. Environmental Protection 

Agency (USEPA) Maximum Contaminant Levels (MCLs) and 

Secondary Maximum Contaminant Levels (SMCLs) drinkingwater standards established for water at the point of delivery 

from public drinking-water supply systems. The MCLs are 

health-based drinking-water standards, whereas SMCLs are 

established on the basis of cosmetic effects such as skin or 

tooth discoloration, esthetic effects such as taste, odor, or 

color, and potential damage to plumbing systems such as corrosiveness (U.S. Environmental Protection Agency, 2005b and 

d). No water-quality standards are established for water from 

private wells or springs.

pH

The USEPA SMCL states that pH should range from 

6.5 to 8.5 (U.S. Environmental Protection Agency, 2005d). A 

pH of 7.0 indicates a neutral aqueous solution. A pH higher 

than 7.0 is indicative of alkaline water, and a pH lower than 

7.0 is indicative of acidic water. The corrosiveness of water to 

pipes and plumbing increases as the pH decreases. Excessive 

alkalinity in water also can attack metals. The pH of water at 

32 sites was lower than 6.5 pH units. No samples had pH in 

excess of 8.5 pH units (fig. 10). The maximum pH measured 

at any of the sites was 7.7 pH units. The median pH of samples 

from the Clinton Formation was 5.55 and from the Marcellus Formation was 5.75. The pH in all other units combined 

was 6.75. The pH of the Marcellus and Clinton Formations is 

appreciably more acidic than the other units, which tend to be 

more neutral.

Geochemically, pH is a significant control on the dissolution of certain naturally occurring metals. Alternatively, pH is 

controlled by the aquifer material. For instance, in oxidizing 

conditions, pH may be low because of dissolution of ferrous-containing minerals, whereas pH may rise because of 

hydrolysis of silicates resulting in a geochemical environment 

that is both alkaline and reducing (Garrels and Christ, 1965). 

In the study area, alkalinity increases at pH measurements 

greater than approximately 6 (fig. 11). Concentrations of 

silica increase appreciably at pH measurements greater than 6 

(fig. 12).

Specific Conductance

Specific conductance is a measure of the ability of a substance to conduct an electrical current and is reported in units 

of microsiemens per centimeter at 25 degrees Celsius (μS/cm). 

Specific conductance of water increases as the concentrations 

of dissolved ions increase. More mineralization produces a 

higher specific conductance. Specific-conductance values from 

the Tonoloway Formation had the largest variability among the 

hydrogeologic units sampled, ranging from 318 to 737 μS/cm, 

with a median value of 445 μS/cm and a standard deviation of 

118.7 μS/cm (fig. 13). Specific-conductance values from the 

Brallier Formation had the least variability, ranging from 202 

to 322 μS/cm, with a median value of 270 μS/cm and a standard deviation of 35.5 μS/cm. Samples from all other formations varied by up to an order of magnitude from the minimum 

to the maximum specific-conductance value.

Aquifer Geochemistry and Ground-Water Quality 17
Figure 10. Distribution of pH values in ground-water samples from hydrogeologic units located in 

Morgan County, West Virginia.

Figure 11. Relation between concentration of pH and alkalinity in ground-water samples from 

Morgan County, West Virginia.

18  Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia
Figure 12. Relation between concentration of pH and dissolved silica in ground-water samples from 

Morgan County, West Virginia.

Figure 13. Distribution of specific conductance in ground-water samples from hydrogeologic units 

located in Morgan County, West Virginia.

Aquifer Geochemistry and Ground-Water Quality 19
Temperature

Ground-water temperature responds to heat flow from the 

Earth’s interior and, near the Earth’s surface, seasonally variable heat from the sun (Heath, 1983). The near-surface, seasonally variable zone is approximately 30 to 80 ft thick, and 

ground-water temperatures in that zone may vary seasonally 

by as much as 5 to 10oC (Heath, 1983). Mean annual groundwater temperature of this shallow zone is estimated to be in the 

range of 10 to 13oC in the study area (Heath, 1983). At depths 

below 100 ft below land surface, ordinary geothermal temperature gradients range from approximately 0.6 to 0.7oC per 

100 ft (Driscoll, 1986). Elevated ground-water temperatures 

may indicate that the ground-water flow path is through a deep 

aquifer system in which geothermal heating has taken place. 

Meteoric water that is recharged at relatively high elevation 

on the crest or limb of an anticline may flow along bedding 

planes or fracture zones deep into an adjacent syncline where 

geothermal heating takes place. The flow then rises to or near 

the surface, where the same bed crops out in another anticline 

(Reeves, 1932) or through zones of weakness in the bedrock 

such as those caused by transverse or thrust faults. Perry and 

others (1979) evaluated geothermal heat flow in Bath County, 

Va., which lies in a physiographic setting similar to that found 

in Morgan County, W. Va. In that study, the Brallier Formation 

of Devonian age was found to have a geothermal gradient of 

approximately 0.4oC per 100 ft. 

The ground-water temperature was measured at all well 

and spring sites in the study area. The temperatures measured 

at the well sites ranged from 10.9 to 16.0oC with a median 

temperature of 13.0oC (fig. 14). These temperatures indicate 

that ground water in the study area is derived from flow systems potentially ranging from a near-surface system, less than 

200 ft below land surface, to a system as deep as 1,500 ft or 

more. However, depending upon the flow path, geothermally 

heated ground water may cool within the flow system before 

its interception by a well or its issuance at the surface.

20 Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia

Figure 14. Distribution of temperature in ground-water samples from springs and wells located in 

Morgan County, West Virginia.
Temperatures at the spring sites ranged from 9.9 to 

21.7oC. The median temperature of the springs was 10.9oC. 

Lessing and others (1991) reported temperatures from geothermally heated warm springs in Morgan County ranging 

from 15.3oC at Hancock Spring to 22.2oC at Berkeley Springs. 

Hancock Spring was not sampled during the current study. The 

Berkeley Springs discharge from five major orifices, one of 

which is the Ladies Spring. The Ladies Spring (site 100) sample was 21.7o

C and was the only spring sampled during this 

study that had a temperature indicative of a deep flow system. 

Water produced from the Marcellus Formation was generally 

warmer than the other formations, ranging from a minimum 

of 12.3oC to a maximum of 16.0oC and with a median of 

13.8oC (fig. 15). Water produced from the Brailler Formation 

had a similar temperature profile, ranging from a minimum of 

12.4oC to a maximum of 14.2oC and with a median of 13.9oC. 

Water samples produced from the Mahantango Formation 

had the smallest temperature range from 11.6 to 13.0oC and 

a median of 12.4oC. The results indicate that water sampled 

from the Marcellus and Brailler Formations may flow along 

deeper flow paths than those in the Mahantango Formation. 

Alkalinity

Alkalinity is defined as the capacity of a solution to 

neutralize acid at a designated end-point. Alkalinity may be 

produced by noncarbonate anions such as sulfate, phosphate, 

and nitrate. However, in most natural water, nearly all alkalinity is produced by dissolved carbonate and bicarbonate and is 

commonly expressed in terms of equivalent calcium carbonate 

or carbonate alkalinity (Hem, 1985). Precipitation contains 

atmospheric carbon dioxide and dissolves additional carbon 

dioxide as it infiltrates through the soil zone. Carbonate rocks, 

such as limestone and dolomite, are composed primarily of 

calcium carbonate (CaCO3). As ground water containing 

carbon dioxide comes in contact with carbonate rocks, the calcium carbonate in the rocks is dissolved, producing bicarbonate. The USEPA (2005b) has not established a water-quality 

standard for alkalinity. Concentrations of alkalinity in samples 

from the Tonoloway Formation were considerably larger than 

from any other aquifer. The median concentration of alkalinity for the Tonoloway Formation was 184 mg/L, the minimum 

was 69 mg/L, and the maximum was 305 mg/L.The median 

Aquifer Geochemistry and Ground-Water Quality   21

Figure 15. Distribution of temperature in ground-water samples from hydrogeologic units located in 

Morgan County, West Virginia.

Aquifer Geochemistry and Ground-Water Quality   21
concentration of alkalinity for all other ground-water samples 

was 94 mg/L, the minimum concentration was 8 mg/L, and the 

maximum was 238 mg/L. The concentration of alkalinity of all 

of the ground-water samples collected was produced primarily 

by bicarbonate. 

Water Hardness

Water hardness is caused primarily by calcium and 

magnesium ions in solution. In this report, the convention 

used for expressing hardness is “hardness as CaCO3” and is 

calculated as described by (Hem, 1985). The USEPA (2005b) 

has not established a standard for hardness, which is typically 

associated with effects observed in the use of soap or with the 

encrustations left by some types of water when they are heated 

(Hem, 1985). Hardness is commonly classified as follows: soft 

(0 to 60 mg/L); moderately hard (61 to 120 mg/L); hard (121 

to 180 mg/L); and very hard (greater than 180 mg/L) (Durfor 

and Becker, 1964). On the basis of those criteria, approximately 13 percent of the samples analyzed were soft water, 

56 percent were moderately hard water, 18 percent were hard 

water, and 13 percent were very hard water. Ground-water 

hardness as CaCO3 in the Tonoloway Formation ranged from 

80 to 400 mg/L with a median concentration of 220 mg/L, 

considerably larger than from other aquifers. Concentrations 

of hardness as CaCO3 from all other formations ranged from 

16 to 260 mg/L with a median concentration of 98 mg/L. 

Dissolved Oxygen

Oxygen is supplied to ground water through recharge and 

by movement of air through the unsaturated zone. Recharge 

water can be expected to contain concentrations of DO similar 

to surface water. The equilibrium concentration of DO in 

water is primarily a function of water temperature and atmospheric pressure. Traditional theory holds that water in deep 

ground-water systems is typically undersaturated with respect 

to oxygen. As ground water flows through an aquifer system, 

DO reacts with available, oxidizable, aquifer material such 

as pyrite (FeS2) and siderite (FeCO3) or naturally occurring 

organic material resulting in a decreased concentration of DO. 

In settings with shallow soil overlying permeable fractured 

rock, DO at detectable concentrations may persist throughout 

the flow system (Freeze and Cherry, 1979). Concentrations 

of DO from 2 to 8 mg/L have been measured in ground water 

from deep aquifers in the south-central Great Basin Physiographic Province (Fenneman, 1946). The residence time for 

ground water in these aquifers ranges from thousands to more 

than 10,000 years (Winograd and Robertson, 1982). Edmunds 

and others (1982) reported appreciable concentrations of DO 

in recently recharged water in a sandstone aquifer in England, 

whereas downdip concentrations of DO in the same aquifer 

were depleted to less than 0.1 mg/L. Hydrogeochemical calculations resulted in an estimate of an approximate 5,000-year 

residence time for the water in that aquifer to have evolved to 

those low concentrations.

For this study, concentrations of DO ranged from estimated values of less than 0.1 to 10.3 mg/L. The 10.3 mg/L 

concentration represents 100 percent saturation of DO at the 

measured temperature and barometric pressure. Water was 

observed to be cascading down the wellbore at sites 30, 39, 40, 

and 83, and air bubbles became entrained within the homeowner’s plumbing system at site 47; therefore, concentrations 

of DO at those locations are assumed to be elevated above that 

which would have occurred naturally within the aquifer. The 

concentration of DO at several other sites was elevated for 

no observed reason. It is possible that ground water flows so 

rapidly through the fracture systems that geochemical reduction of the concentration of DO is minimized. It also is possible that turbulent flow occurs within open fracture systems 

or solutionally enhanced conduits, thus entraining oxygen 

in place. Pumping with rapid drawdown in low-production 

domestic wells may induce mechanical entrainment of DO. 

Turbidity

Turbidity is a measure of the cloudiness of water 

(U.S. Environmental Protection Agency, 2005b). Turbidity 

occurs naturally in ground water, depending upon the aquifer 

medium. Wells may produce nonturbid water at low pumping rates, but at higher pumping rates, turbidity may increase 

dramatically. The increased turbidity could be from turbid 

recharging water being pulled into the stressed aquifer or from 

turbulent flow that picks up sediment in fractures or conduits 

within the aquifer and suspends it in the ground water (Hobba 

and others, 1972). The maximum turbidity measured during 

this study was 330 nephelometric turbidity units (NTU), the 

median turbidity was 3.9 NTU, and 22 samples had turbidity 

of less than 1 NTU. USEPA has established a maximum for 

turbidity in public supply systems as 5 NTU prior to treatment, 

with more stringent requirements for public-water-supply 

systems that filter (U.S. Environmental Protection Agency, 

2005b). USEPA requirements are established on the basis of 

turbidity caused by disease-causing organisms typically found 

in surface water, not ground water. Thirty-five of the wells 

sampled had turbidity measurements greater than 5 NTU at the 

pumping rates sustained over approximately a 30-minute time 

interval. Turbidity measurements typically did not stabilize, 

but increased throughout the pumping test, indicating that the 

aquifer could not sustain production at the indicated pumping 

rate without inducing turbidity. 

Inorganic Constituents

Inorganic constituents are those that do not contain carbon. Ninety-one wells and eight springs were sampled in the 

study area for a variety of inorganic constituents; results are 

summarized in Appendixes 2 and 3, respectively.

22  Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia
Major Ions

Major inorganic ions are calcium, magnesium, sodium, 

potassium, bicarbonate, chloride, and sulfate, which typically occur in natural water in concentrations of 1 mg/L or 

larger. These constituents exist in pairs of cations and anions, 

which are indicative of the mineralogy of the hydrogeologic 

setting through which the water has flowed. For instance, 

calcium-bicarbonate- dominant ground water is indicative of 

a limestone aquifer, calcium-magnesium-bicarbonate water 

may be indicative of a dolomite aquifer, and sodium-chloride 

dominant ground water is typical of a sedimentary setting rich 

in evaporite salts. Geochemical characterization becomes more 

complex where the aquifer system consists of a mixture of 

rock types or if the ground water has flowed through differing 

types of rock units.

Ground water within a study area may be classified by 

use of a trilinear diagram suggested by Piper (Hem, 1985). To 

use this diagram, the concentration of each major cation and 

anion is expressed as a percentage of the total milliequivalents 

per liter in each sample. The percentage of major cations and 

anions in each sample is then plotted as a single point on the 

lower left and lower right triangles of the diagram, respectively. These points are projected to a single point on the plotting field, which lies between the two triangles. For example, 

if the point falls near the left point of the plotting field, then 

the water may be classified as a calcium-bicarbonate-type 

water. If a point falls near the lower right tip of the plotting 

field, the water is classified as a sodium-potassium-bicarbonate-type water. The trilinear method describes the percentage 

of the major cations and anions. That is, the percentage of 

each constituent or group of constituents is represented by 

where a point lies in the plotting field; however, this graphical 

method does not indicate the concentration of the dissolved 

constituents. Geochemical signatures of ground-water and 

spring samples analyzed for this study are shown in figure 16. 

The predominant geochemical signature of ground water 

and spring water in Morgan County was calcium-bicarbonatetype water; however, there also were vastly differing groundwater samples with predominantly sodium-bicarbonate and 

predominantly calcium-magnesium-sulfate signatures. 

Most of the spring-water samples were of the calciumbicarbonate type (fig. 16). A distinct exception was that of 

spring site 94 at Cacapon State Park, which showed a calcium-sulfate-chloride signature similar to that of the Marcellus 

Formation. Spring site 93 has a geochemical signature that lies 

between the calcium-bicarbonate and calcium-sulfate-chloride signatures, indicating that the ground water has flowed 

through some combination of limestone and shale units and 

plots close to ground-water samples from the Hampshire Formation (fig. 16). 

The Pocono Group, Chemung Group, and Hampshire and 

Tonoloway Formations produce predominantly calcium-bicarbonate waters. Some samples had an elevated sulfate signature. Hobba and others (1972) attributed the possible source 

of an increased sulfate signature in the Tonoloway Formation 

as the presence of anhydrite (CaSO4) and salt (NaCl) deposits. 

Anhydrite and salt are known to occur at depth west of the 

study area but generally are thought to have been removed by 

ground-water circulation in the Potomac River Basin; however, residual deposits that have not been completely dissolved 

remain in rocks in the study area. The Hampshire Formation and Chemung Group also had some samples that had an 

increased sodium-bicarbonate signature. One sample (site 8) 

that is mapped at the surface in the Hampshire Formation had 

a nearly 100 percent sodium-bicarbonate composition, a very 

soft water. A narrow section of the Onesquethaw Group occurs 

at the surface near that well location. Deposits of glauconite, 

which is used as water softener, are known to occur in that 

group. Thicknesses of the Hampshire Formation and underlying units are not well known in that area, which is structurally 

complex. It is possible that the 300 ft well at that site is tapping water that originates from the Onesquethaw Group. Most 

samples from the Clinton Formation had a calcium-bicarbonate signature, with one exception: a calcium-sodium sulfate 

water that bore a signature similar to that from a warm spring 

in the Oriskany Sandstone (Hobba and others, 1972).

Bromide and Fluoride 

In addition to chloride, analyses were done for two other 

halides: bromide and fluoride. USEPA (2005b and d) has not 

established a drinking-water standard currently (2006) for 

bromide. The largest concentration of bromide detected was 

0.13 mg/L at one site. USEPA (2005b and d) has established 

standards for fluoride. An MCL of 4.0 mg/L is established on 

the basis of potential health effects, including bone disease 

or mottled teeth. The SMCL of 2.0 mg/L is established for 

naturally occurring fluoride that may cause tooth discoloration 

or pitting during the formative period prior to eruption of teeth 

in children (U.S. Environmental Protection Agency, 2005d). 

None of the spring or well samples had concentrations of 

fluoride greater than the MCL or the SMCL. Approximately 

42 percent of the samples had concentrations lower than the 

detection limit of 0.2 mg/L. The largest concentration was 

0.3 mg/L, at three sites.

Aquifer Geochemistry and Ground-Water Quality   23
Figure 16. Relative geochemical composition of ground water from springs and wells, 

by hydrogeologic unit, Morgan County, West Virginia.

24  Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia

(A)

(B)
Figure 16. Relative geochemical composition of ground water from springs and 

wells, by hydrogeologic unit, Morgan County, West Virginia.—Continued

Aquifer Geochemistry and Ground-Water Quality   25

(D)

(C)
Figure 16. Relative geochemical composition of ground water from springs and 

wells, by hydrogeologic unit, Morgan County, West Virginia.—Continued

26  Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia

(E)

(F)
Iron and Manganese

Trace concentrations of iron and manganese occur naturally in many rocks and soils as various mineral assemblages. 

Martens (1945) reported deposits of limonite (Fe2O3.H2O), an 

iron ore mineral occurring 6 mi west of Hedgesville, near the 

eastern boundary of Morgan County. The deposits are neither 

large nor of sufficiently high quality to be of contemporary 

commercial interest. Their occurrence does provide insight 

as to one potential source of large concentrations of iron in 

ground water. Concentrations of dissolved iron greater than 

the SMCL of 300 μg/L typically precipitate when exposed to 

air or to DO in water and may cause turbidity, staining, and 

objectionable taste and color, and may corrode pipes, pumps, 

or other equipment (U.S. Environmental Protection Agency, 

2005d). With the exception of the Tonoloway Formation and 

the one sample from the Pocono Group, ground water with 

concentrations of dissolved iron greater than 300 μg/L was 

found in all formations throughout the study area (fig. 17).

Ground water with a concentration of dissolved iron of 

at least 300 μg/L occurred in approximately 32 percent of the 

wells sampled (Appendix 2). The maximum concentration of 

dissolved iron in all ground-water samples was 24,100 μg/L 

and the median was 42 μg/L. The maximum concentration of 

dissolved iron in spring-water samples (site 93) was 

2,010 μg/L. The concentration of dissolved iron in all other 

spring-water samples was less than the detection limit of 

6 μg/L. 

Dissolved manganese in excess of the SMCL of 50 μg/L 

may result in black to brown color, black staining, and a bitter 

taste in the water (U.S. Environmental Protection Agency, 

2005d). The maximum concentration of dissolved manganese 

in all ground-water samples was 3,920 μg/L (fig. 18) and the 

median was 106.5 μg/L. The maximum concentration of dissolved manganese in spring-water samples was 212 μg/L. The 

median concentration of dissolved manganese from all springwater samples was 0.60 μg/L. Ground water with concentrations of dissolved manganese greater than 50 μg/L was found 

in all formations (fig. 18). Approximately 60 percent of the 

ground-water samples had concentrations of dissolved manganese greater than the SMCL (U.S. Environmental Protection 

Agency, 2005d).

The concentrations of iron and manganese are positively 

related (fig. 19). If the concentration of iron is small at a 

site, the concentration of manganese tends to be small. If the 

concentration of iron is large at a site, the concentration of 

manganese generally is large also. 

Figure 17. Distribution of concentrations of iron in ground-water samples from hydrogeologic units 

located in Morgan County, West Virginia.

Aquifer Geochemistry and Ground-Water Quality   27
Figure 18. Distribution of concentrations of manganese in ground-water samples from 

hydrogeologic units located in Morgan County, West Virginia.

28  Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia

Figure 19. Relation between concentrations of iron and manganese in ground-water samples from 

Morgan County, West Virginia.
Trace Elements

Trace elements occur in aquifer systems in which 

naturally occurring geochemical conditions are favorable for 

dissolving the elements from assemblages in the rock matrix. 

Trace elements sampled at a subset of sites were aluminum, 

arsenic, antimony, barium, cadmium, lead, nickel, strontium, 

and zinc.

The SMCL for aluminum (U.S. Environmental Protection 

Agency, 2005d) is a range from 50 to 200 μg/L. Aluminum 

may cause colored water, scaling, and sedimentation (U.S. Environmental Protection Agency, 2005d). The maximum concentration of aluminum sampled was 2,340 μg/L, with nine of 

the samples equal to or greater than the 50-μg/L SMCL. Those 

samples were from the Brallier Formation, Chemung Group, 

and Clinton and Hampshire Formations. Five samples had 

concentrations less than the detection limit of 2 μg/L. Those 

samples occurred in the same formations and in the Tonoloway Formation. The median concentration of aluminum was 

10 μg/L. 

The MCL for antimony is 6 μg/L (U.S. Environmental 

Protection Agency, 2005b). The potential health effects from 

exposure above that MCL are an increase in blood cholesterol 

and a potential for blood sugar to be decreased. Antimony was 

not detected in any sample at the minimum detection level of 

0.20 μg/L.

The USEPA MCL for arsenic is 10 μg/L (U.S. Environmental Protection Agency, 2005b). Concentrations of arsenic 

greater than the MCL may cause skin damage, problems with 

circulatory systems, or increased risk of cancer (U.S. Environmental Protection Agency, 2005b). The maximum concentration of arsenic sampled was 8 μg/L, with no sample concentrations greater than the 10 μg/L MCL. Eighteen samples had 

concentrations less than the detection limit of 2 μg/L. 

The MCL for barium is 200 μg/L (U.S. Environmental Protection Agency, 2005b). Barium in concentrations 

exceeding the MCL may cause an increase in blood pressure 

(U.S. Environmental Protection Agency, 2005b). The maximum concentration of barium sampled was 390 μg/L, with 

nine sample concentrations great than the 200-μg/L MCL. 

Those samples came from the Brallier Formation, Chemung 

Group, and Clinton, Hampshire, and Tonoloway Formations. 

The smallest concentration of barium detected was 16.9 μg/L 

and the median concentration was 76 μg/L. 

The MCL for cadmium is 5 μg/L (U.S. Environmental Protection Agency, 2005b). Concentrations of cadmium 

exceeding the MCL may cause kidney damage. The maximum 

concentration of cadmium sampled was 0.5 μg/L. None of 

the sample concentrations were greater than the 5-μg/L MCL. 

The smallest concentration of cadmium was 0.02 μg/L and the 

median concentration was 0.04 μg/L. 

The MCL for lead is an action level of 15 μg/L (U.S. Environmental Protection Agency, 2005b). For infants and 

children, lead may delay physical and mental development and 

cause slight deficits in attention span and learning abilities. 

For adults, concentrations of lead exceeding the MCL may 

cause kidney problems or high blood pressure. The maximum 

concentration of lead detected was 1.7 μg/L with 10 sample 

concentrations less than the detection limit of 0.05 μg/L. The 

median concentration of lead was 0.04 μg/L.

No MCL or SMCL currently (2006) exists for nickel 

(U.S. Environmental Protection Agency, 2005b and d). The 

maximum concentration of nickel detected was 30.6 μg/L, and 

the median concentration was 1.78 μg/L. Two samples had 

concentrations less than the detection limit. The three samples 

with the largest concentrations occurred in the Hampshire 

Formation.

No MCL or SMCL currently (2006) exists for elemental strontium (U.S. Environmental Protection Agency, 2005b 

and d). The maximum concentration of strontium detected 

was 5,520 μg/L. The smallest concentration of strontium was 

8.87 μg/L and the median concentration was 87.6 μg/L. The 

three samples with the largest concentrations were from the 

Hampshire Formation.

The SMCL for zinc is 500 μg/L (U.S. Environmental 

Protection Agency, 2005d). Concentrations of zinc exceeding 

the SMCL may give a metallic taste to the water. The maximum concentration of zinc sampled was 696 μg/L, the only 

concentration greater than the 500-μg/L SMCL; the sample 

was from the Marcellus Formation. The median concentration 

was 46.0 μg/L. Eleven samples had concentrations below the 

detection limit of 6-micrograms per liter. 

Zinc and aluminum occur contemporaneously in the study 

area (fig. 20). The concentration of zinc is generally small 

at sites with a small concentration of aluminum. With little 

exception, the concentration of aluminum is large at site with 

a large concentration of zinc. A less strong positive relation 

exists between concentrations of strontium and lead. 

Nutrients

All samples were analyzed for the following nutrients: 

ammonia, nitrate-plus-nitrite, nitrate, total phosphorus, and 

orthophosphate. The occurrence of nutrients in ground water at 

elevated concentrations frequently is caused by contamination 

from septic tank effluent, confined animal-feedlot operations, 

or fertilizer application. At elevated concentrations, certain 

nutrients may cause adverse effects on human health. 

Nitrate and Nitrite

Small concentrations of nitrogen species occur naturally 

in rocks. Soils and biological matter contain larger concentrations of nitrogen species. In ground water, nitrate is usually the 

only nitrogen form of significance, although nitrogen species 

may occur at all oxidation states from -3 to +5, depending 

upon conditions (Hem, 1985). 

Aquifer Geochemistry and Ground-Water Quality   29
USEPA has established MCLs for nitrate of 10 mg/L as N 

and for nitrite of 1.0 mg/L as N (U.S. Environmental Protection Agency, 2005a). Infants below the age of 6 months may 

suffer from an acute condition known as methemoglobinemia 

(blue-baby syndrome) from water containing concentrations 

that exceed the MCLs. Nitrates and nitrites also have the 

potential to cause diuresis, increased starchy deposits, and 

hemorrhaging of the spleen from long-term exposures at concentrations exceeding the MCLs (U.S. Environmental Protection Agency, 2005b). 

The largest concentration of nitrate-plus-nitrite as N was 

2.6 mg/L, and 69 percent of the samples had concentrations 

less than the detection limit of 0.06 mg/L. The maximum 

concentration of nitrite as N, 0.042 mg/L, was the only value 

larger than the minimum reporting level (MRL), 0.008 mg/L, 

although there are several estimated values below the MRL. 

Ammonia Species

The sources of ammonia species in natural water are 

assumed to be similar to those of other nitrogen species and 

typically are transformed to nitrate; however, ammonia is 

present in some natural waters (Hem, 1985). The largest 

concentration of ammonia as N detected during this study was 

0.20 mg/L, and approximately 70 percent of the samples had 

concentrations less than the detection limit of 0.04 mg/L. No 

MCL or SMCL currently (2006) exists for ammonia in drinking water (U.S. Environmental Protection Agency, 2005b).

Phosphorous and Orthophosphate

Phosphorous occurs in a wide range of oxidation states in 

natural water; the most probable species are phosphate anions, 

complexes with metal ions, and colloidal particulate material 

(Hem, 1985). Phosphorous, as an element essential for animal 

metabolism, is always present in animal metabolic waste 

(Hem, 1985). As such, its presence in large concentrations 

may indicate contamination from animal or human waste. No 

MCL or SMCL currently (2006) exists for phosphorous or 

orthophosphate in drinking water (U.S. Environmental Protection Agency, 2005b). 

The largest concentration of phosphorous detected during this study was 0.25 mg/L and more than 85 percent of 

the samples had concentrations less than the detection limit 

of 0.04 mg/L. The largest concentration of orthophosphate 

as P was 0.17 mg/L and more than 84 percent of the samples 

had concentrations less than the detection limit of 0.02 mg/L 

(U.S. Environmental Protection Agency, 2005b).

Figure 20. Relation between concentrations of zinc and aluminum in ground-water samples from 

Morgan County, West Virginia.

30 Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia
Radon-222

Radon-222 is a radioactive gas that occurs naturally as 

a decay product of uranium. Radon-222 gas is dissolved in 

ground water and degasses when the water is exposed to the 

open atmosphere. It can enter homes when water valves are 

opened, particularly during the use of showers. Rocks that 

are known to have a high uranium content include granitic 

rocks, some volcanic rocks, dark shales, sedimentary rocks 

that contain phosphate, and metamorphic rocks derived from 

these rocks (Otton and others, 1993). The accumulation and 

transport of radon in the subsurface depends upon the uranium 

content, grain size, permeability, and the extent of fracturing in 

the host rock. The rocks of Morgan County include dark shales 

and other sedimentary rocks that can contain uranium.

Radon-222 can destroy lung tissue and cause lung 

cancer (Otton and others, 1993) or can cause stomach cancer 

(U.S. Environmental Protection Agency, 2005c). In 1999, 

USEPA reinstated a proposed enforceable maximum contaminant level (PMCL) for radon in drinking water of 300 pCi/L, 

but with an alternate maximum contaminant level (AMCL) 

proposed at a concentration of 4,000 pCi/L. The drinkingwater standard that would apply for a community water system 

(CWS) would depend upon whether or not the State or CWS 

develops a radon Multimedia Mitigation (MMM) program. If a 

CWS serves 10,000 persons and either the State or the system 

has an approved MMM program, then the 4,000 pCi/L AMCL 

would apply; otherwise, the 300 pCi/L standard would apply. 

USEPA further proposes a nonenforceable Maximum Contaminant Level Goal (MCLG) of zero for radon-222 in drinking water (U.S. Environmental Protection Agency, 2005c). 

MCLGs are defined by USEPA as the level of a contaminant 

in drinking water below which there is no known or expected 

risk to health. MCLGs allow for a margin of safety and are 

nonenforceable public-health goals.

Radon-222 was detected in all wells sampled, ranging 

from 10 to 2,170 pCi/L, with a median value of 365 pCi/L. 

The two samples from the Clinton Formation had radon-222 

concentrations much larger than the other formations, 1,330 

and 2,170 pCi/L. Concentrations in 56 percent of the samples 

were greater than the PMCL of 300 pCi/L. Concentrations in 

none of the samples were greater than the proposed AMCL of 

4,000 pCi/L (fig. 21).

Figure 21. Distribution of concentration of radon-222 in ground-water samples from hydrogeologic 

units located in Morgan County, West Virginia.

Aquifer Geochemistry and Ground-Water Quality   31

Clinton

Tonoloway

Marcellus

Mahantango

Brallier

Chemung

10 1

10 2

10 3

9

2

3

4

5

6

7

9

2

3

4

5

6

7

9

2

3

RADON-222, IN PICOCURIES PER LITER

EXPLANATION

number of values

90th percentile

75th percentile

median

25th percentile

10th percentile

* outlier

6

2 4 3 1 6
Bacteria

Well and spring samples were tested for fecal coliform 

bacteria, total coliform bacteria, and Escherichia coli (E. coli).

These microorganisms occur in the feces of warmblooded 

animals, including humans. The presence of these microorganisms indicates the presence of fecal contamination and the 

possible presence of other harmful bacteria, viruses, or other 

pathogens into the ground-water system. Certain strains of 

E. coli are of particular concern because they can cause health 

problems such as fever, diarrhea, and, in certain instances, kidney failure (U.S. Centers for Disease Control and Prevention, 

2005). USEPA has established an MCLG for total coliforms 

(including fecal coliform and E. coli) of zero colonies per 

100 milliliters (col/100 mL) for public drinking water supply 

systems (U.S. Environmental Protection Agency, 2005a). 

Ninety-one wells in the study area were tested for 

coliform bacteria. Fecal coliform bacteria were detected in 

5 ground-water samples (5 percent), total coliform bacteria 

were detected in 42 ground-water samples (46 percent), and 

E. coli were detected in 2 ground-water samples (2 percent).

Approximately 69 percent of the wells sampled were constructed after 1983 and constructed with a grout surface seal 

(West Virginia Bureau for Public Health, 1984). West Virginia 

Bureau for Public Health (1984) requires installation of a concrete pad around the casing at the surface but does not require 

grouting the entire length of the casing. Proper surface seals 

and grouting of wells helps to reduce the potential for transport of fecal contaminants along the casing from the surface to 

the aquifer. The casings of most of the wells sampled appeared 

to be in good condition at the surface, although no downhole observations were possible. Additionally, most of the 

wells were located at a distance from potential fecal-material 

sources such as barnyard manure or pet waste. Proper siting 

of wells with respect to septic systems can reduce or eliminate 

the potential of microbial transport through the aquifer from 

that source.

The occurrence of total coliform bacteria was compared 

with geologic unit, age of well, depth of well, the ratio of 

well depth to casing length, and aquifer transmissivity as 

determined during the recovery phase of the aquifer test. No 

significant correlation was found among the occurrence of 

total coliform bacteria and any of these characteristics. Wellsite proximities to septic systems were not evaluated as part of 

this study.

Mathes (2000) studied the relation of bacteria to septic 

systems in Berkeley County, W. Va., and found no apparent 

relation among septic-system density and the concentration of bacterial colonies detected. This lack of correlation 

was attributed to the structural complexity of the limestone 

aquifers in the study area. The geology in Morgan County is 

equally complex. Soils are generally shallow, and all of the 

bedrock units have undergone faulting, folding, and fracturing. 

Septic systems sited on shallow soils may result in percolation 

through underlying fractures, where contamination may be 

transported rapidly into the aquifer. Mathes (2000) found little 

difference in the frequency of total coliform bacteria between 

shallow wells and deep wells. Similarly, no correlation was 

found during this study. Mathes (2000) also found that the 

greatest concentrations of E. coli and fecal coliform bacteria 

were in shallow wells. No such correlation was found during 

this study; however, evaluation of well-completion reports for 

Morgan County indicates that well production in the domestic wells frequently consists of two or more fracture zones. 

The uppermost fracture zone is frequently at a depth of less 

than 100 ft below land surface, and produces 1 to 2 gal/min, 

inadequate for a domestic supply well. Drilling is continued 

until another fracture zone is penetrated, providing a combined 

production adequate to supply domestic needs. The upper 

zones are rarely grouted; therefore, the potential exists for 

contamination from shallower zones even in deep wells. 

The ratio of well depth to casing length was developed 

and correlated with the occurrence of total coliform bacteria. 

No significant correlation exists; however, the sites with the 

largest total coliform bacteria concentration had a ratio of total 

well depth to casing length less than or equal to 0.35 (fig. 22). 

The most contaminated site with a ratio exceeding 0.35 was a 

newly constructed well, which may have had residual contamination from drilling. In highly folded, faulted, and fractured 

terrain, longer grouted casings may be needed to protect 

underlying aquifers. 

Eight springs were sampled for the presence of bacteria. 

No bacteria were detected in two of the eight springs. Total 

coliform bacteria were detected in six of the springs, and 

E. coli were detected at two spring sites.

Natural springs are open to the surrounding environment 

and are therefore susceptible to microbial contamination by 

feces from wildlife or domestic animals that frequent the area. 

Properly constructed spring houses can protect a water source 

from fecal contamination. The two springs that were free from 

coliform bacteria have enclosed spring structures. With the 

exception of one free-flowing, natural spring, all of the springs 

tested were protected by spring houses or spring boxes. The 

structures varied significantly from site to site. At one site, 

frogs were observed in a spring house that had an unscreened 

discharge pipe that could serve as an opening for other animals 

to enter. No inventory of potential sources of contamination 

was done during the course of this study.

32  Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia
Summary and Conclusions

With few exceptions, municipal and private users in the 

study area depend upon ground water for their water supplies. Aquifers in Morgan County are composed of carbonate, 

sandstone, and shale rocks of ages ranging from Late Ordovician to Early Mississippian. The rocks are characterized by 

thin to thick bedded formations. Interbedding occurs among 

the various limestones, shales, sandstones, and siltstones that 

includes calcareous shale and sandstone and cherty limestone 

and shale. The hydrogeology is complicated by the structural 

complexity typical of the Valley and Ridge Physiographic 

Province. That structural complexity consists of a series of 

steeply dipping north-south trending anticlines, synclines, and 

thrust faults that are intersected by cross-faulting in several 

locations throughout the study area.

Static ground-water altitudes decrease from recharge 

areas in the mountains to the valley floors. Along the valley 

floors, altitudes decrease from the southern part of the county 

to the Potomac River in the north. Thus, ground water ultimately flows in a northerly direction. Small drainages have 

developed where cross-faulting or jointing occurs and these 

drainages provide local recharge zones. Static water levels 

may vary among nearby or adjacent sites by as much as 200 ft 

in some localities because of the complexity of the geologic 

stratigraphy and structure. This variability also may indicate 

the presence of separate or otherwise isolated aquifers at different depths because of the local structural complexity. 

Transmissivities were determined for aquifers throughout 

the study area. Transmissivities ranged from 2 to 1,420 ft2/d. 

The largest transmissivities generally occurred at or near 

contacts between geologic units (at bedding planes) or in the 

presence of thrust-faults or cross-faults. Small transmissivities (less than or equal to 5 ft2

/d) occurred in all aquifer units 

except the Marcellus Formation, which had transmissivities 

ranging from 54 to 327 ft2/d and had the largest median transmissivity at 128 ft2

/d. The largest transmissivity recorded was 

1,490 ft2/d from the Chemung Group, but near a bedding contact with the Brallier Formation. Production from wells within 

the study area is typically from one or two fracture zones. 

Water quality and geochemistry are variable throughout the county and within aquifer units. Geochemically, the 

ground water ranges from nearly 100 percent sodium-bicarbonate water to nearly 100 percent calcium-magnesium-sulfate-chloride water as end-members. Most of the water tested 

is calcium-bicarbonate water, which is typical of water from a 

limestone aquifer. Geochemical mixing has occurred among or 

within aquifer units. 

Water-quality characteristics for which values were 

greater than U.S. Environmental Protection Agency Maximum 

Contaminant Levels or Secondary Maximum Contaminant 

Levels include radon-222, pH, turbidity, iron, manganese, 

aluminum, and total- and fecal-coliform and E. coli bacteria. 

Concentrations of radon-222 were greater than the 300 pCi/L 

Proposed Maximum Contaminant Level in more than half of 

the wells tested. Total coliform occurred in 42 wells, fecal 

coliform in 5 wells, and E. coli in 2 wells. More than 35 percent of the wells tested had turbidity greater than 5 NTU. The 

largest measurement was 330 NTU. Pumping stress on aquifers with low production tended to increase turbidity. Specific 

conductance (SC) ranged from 44 to 737 μS/cm. The median 

SC was 240 μS/cm. Hardness as CaCO3 ranged from 16 to 

400 mg/L. The median hardness was 98 mg/L. 

Figure 22. Relation between the ratio of casing length to well depth and the occurrence of 

bacteria in wells located in Morgan County, West Virginia.

Summary and Conclusions  33
Acknowledgments

The authors thank Danny Evans of the West Virginia 

Conservation Agency and the Eastern Panhandle Conservation 

District for their cooperation in this study. We also gratefully 

acknowledge the Morgan County Rural Water Committee and 

the Morgan County Planning Commission for their assistance 

and West Virginia University for their collaboration during the course of the study. We particularly thank the many 

individuals, establishments, and authorities in the county that 

permitted access to their wells for collection of hydraulic and 

water-quality data. 

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36  Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia
Appendixes 1 through 3

  37
Appendix 1. Well-construction and aquifer properties for selected wells, Morgan County, West Virginia. —Continued

[USGS, U.S. Geological Survey; ft bls, feet below land surface; ft, foot; in., inch; Hydrogeologic unit codes: 354CLNN, Clinton Group; 351TNLY, Tonoloway Formation; 344MRCL, Marcellus Formation; 344MNNG, Mahantango Formation; 341BRLR, Brallier Formation; 341CMNG, Chemung Group; 341HMPR, Hampshire Formation; 337POCN, Pocono Group; gal/min, gallons per minute; (gal/min)/ft, gallons per minute per foot of drawdown; ft2/d, foot squared per day; --, not determined. See figure 9 for well locations]

Site 

number

1USGS 

station 

name

Well 

depth 

(ft bls)

Length of 

casing 

(ft)

Casing 

diameter 

(in.)

Landsurface 

altitude 

(ft)

Static 

water 

level 

(ft bls)

Date 

water 

level 

measured

Hydrogeologic 

unit

Discharge 

(gal/min)

Specific 

capacity 

((gal/min)/ft)

Transmissivity 

average 

(ft2/d)

1 Mrg-0090 142 11 6 560 63.41 7-6-2004 344MNNG -- 0.10 62 Mrg-0178 225 59.4 6 801 103.02 5-10-2005 341CMNG 3.6 .10 33 Mrg-0146 120 40 6 745 34.61 11-3-2004 341BRLR 5.7 .45 1134 Mrg-0114 320 118 6 500 106.05 8-11-2004 341CMNG -- .13 6.55 Mrg-0124 320 -- 6 730 50.6 8-26-2004 341CMNG -- 3.75 3176 Mrg-0104 140 39 6 780 48.85 8-2-2004 341BRLR -- 1.00 967 Mrg-0122 145 -- 6 680 78.9 8-25-2004 341CMNG -- -- --8 Mrg-0144 300 105 6 590 8.77 11-2-2004 341HMPR 3.2 .12 69 Mrg-0130 220 60 6 864 154.92 9-2-2004 354CLNN 7.8 1.05 206

10 Mrg-0095 140 -- 6 710 26.59 7-12-2004 341CMNG 5.3 .91 2911 Mrg-0139 160 83 6 744 35.02 10-19-2004 341CMNG 3.1 3.16 211.512 Mrg-0136 163 -- 6 743 50.1 9-22-2004 341CMNG 4 -- --13 Mrg-0142 160 42 6 797 43.17 10-21-2004 341CMNG 8.2 .90 92.514 Mrg-0145 180 100 6 751 23.78 10-19-2004 341CMNG 7.5 .33 2115 Mrg-0135 177 40 6 870 90.75 9-22-2004 341CMNG 5.2 .49 5516 Mrg-0156 160 39 6 589 45.43 4-13-2005 344MNNG 4.8 .53 3217 Mrg-0094 200 20 6 480 24.93 7-12-2004 341CMNG 10.2 1.10 12218 Mrg-0161 365 78.65 6 484 16.98 4-19-2005 351TNLY 10.8 1.42 13819 Mrg-0137 269 40 6 847 37.91 9-23-2004 341CMNG 1.5 .17 520 Mrg-0143 200 40 6 561 51.08 11-2-2004 344MNNG 4.8 .08 221 Mrg-0140 560 49 6 908 103.02 10-20-2004 341CMNG 5.7 .09 322 Mrg-0092 405 40 6 840 67.73 7-7-2004 341CMNG 9 .50 39.523 Mrg-0149 100 60 6 567 37.31 11-4-2004 344MNNG 2.6 1.43 13124 Mrg-0147 225 40 6 532 62.9 11-3-2004 344MNNG 3.7 .36 10825 Mrg-0112 120 59 6 680 20 8-10-2004 341CMNG -- 1.05 16826 Mrg-0138 120 100 6 552 48.04 9-23-2004 344MNNG 6.1 4.61 57727 Mrg-0141 150 30 6 586 34 10-20-2004 344MNNG 1.4 .12 628 Mrg-0176 265 59.0 6 731 79.71 5-6-2005 341HMPR 9 .86 7429 Mrg-0159 350 -- 6 768 -- 4-15-2005 354CLNN 3 -- --30 Mrg-0091 205 80 6 680 77.95 7-7-2004 341CMNG 5.2 .15 831 Mrg-0179 122 19.1 6 722 14.85 5-11-2005 344MRCL 5.6 .40 54

38  Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia
Appendix 1. Well-construction and aquifer properties for selected wells, Morgan County, West Virginia. —Continued

[USGS, U.S. Geological Survey; ft bls, feet below land surface; ft, foot; in., inch; Hydrogeologic unit codes: 354CLNN, Clinton Group; 351TNLY, Tonoloway Formation; 344MRCL, Marcellus Formation; 344MNNG, Mahantango Formation; 341BRLR, Brallier Formation; 341CMNG, Chemung Group; 341HMPR, Hampshire Formation; 337POCN, Pocono Group; gal/min, gallons per minute; (gal/min)/ft, gallons per minute per foot of drawdown; ft2/d, foot squared per day; --, not determined. See figure 9 for well locations]

Site 

number

1USGS 

station 

name

Well 

depth 

(ft bls)

Length of 

casing 

(ft)

Casing 

diameter 

(in.)

Landsurface 

altitude 

(ft)

Static 

water 

level 

(ft bls)

Date 

water 

level 

measured

Hydrogeologic 

unit

Discharge 

(gal/min)

Specific 

capacity 

((gal/min)/ft)

Transmissivity 

average 

(ft2/d)

32 Mrg-0148 140 45 6 635 44.09 11-4-2004 341CMNG 4.1 .64 5433 Mrg-0120 160 25 6 840 4.27 8-25-2004 351TNLY 6.1 .55 4534 Mrg-0116 195 -- 6 -- 2.36 8-12-2004 341CMNG -- -- --35 Mrg-0155 240 18.85 6 778 98.38 4-13-2005 341CMNG 5.4 .63 2036 Mrg-0106 380 98 6 1,100 104.35 8-3-2004 341HMPR -- .23 737 Mrg-0170 320 61.5 6 1,013 92.17 4-28-2005 341HMPR 3.2 .26 1638 Mrg-0100 -- -- 6 940 227.25 7-15-2004 341HMPR -- -- --39 Mrg-0085 219 -- 6 830 -- 5-19-2004 351TNLY -- -- --40 Mrg-0121 200 -- 6 890 -- 8-25-2004 354CLNN -- -- --41 Mrg-0160 150 38.45 6 1,129 60.01 4-19-2005 337POCN 5 0.13 542 Mrg-0123 205 -- 6 920 34.3 8-26-2004 351TNLY -- -- --43 Mrg-0113 130 46 6 910 16.5 8-10-2004 354CLNN -- 3.72 26644 Mrg-0088 560 -- 6 980 -- 7-1-2004 341HMPR -- -- --45 Mrg-0118 208 -- 6 860 8.6 8-24-2004 341MRCL -- .99 12846 Mrg-0110 143 -- 6 910 17.61 8-5-2004 351TNLY -- .07 347 Mrg-0167 260 58 6 642 104.81 4-25-2005 351TNLY 4.3 1.02 3448 Mrg-0097 300 60 6 920 31.95 7-13-2004 351TNLY -- .06 249 Mrg-0117 260 135 6 880 95.75 6-29-2004 351TNLY 10.6 .63 2150 Mrg-0133 240 60 6 910 27.75 9-9-2004 341CMNG 10.5 .47 5551 Mrg-0171 205 38.75 6 913 84.33 5-2-2005 341CMNG 10 .25 9.552 Mrg-0172 160 18.0 6 869 34.52 5-2-2005 341CMNG 3.5 .15 453 Mrg-0173 62 8.0 6 787 8.47 5-3-2005 351TNLY 4.6 .51 2554 Mrg-0103 123 25 6 930 25.5 7-28-2004 341CMNG 5.2 .28 11.555 Mrg-0102 305 60 6 930 22.15 7-28-2004 341CMNG 14.2 .44 4856 Mrg-0101 310 62 6 820 7.97 7-27-2004 341BRLR 5.6 .27 2157 Mrg-0105 320 -- 6 890 154.73 8-3-2004 341CMNG -- -- --58 Mrg-0093 150 33 6 680 27.88 7-8-2004 341CMNG 5.4 .09 1159 Mrg-0107 180 159 6 1,140 61.93 8-4-2004 354CLNN -- .38 4360 Mrg-0131 150 70 6 831 93.83 9-8-2004 341CMNG 3.1 .75 2661 Mrg-0132 130 30 6 848 1 9-8-2004 351TNLY 1 .71 362 Mrg-0128 300 20 6 845 160.02 9-1-2004 341CMNG 4.7 .14 8

Appendixes  39
Appendix 1. Well-construction and aquifer properties for selected wells, Morgan County, West Virginia. —Continued

[USGS, U.S. Geological Survey; ft bls, feet below land surface; ft, foot; in., inch; Hydrogeologic unit codes: 354CLNN, Clinton Group; 351TNLY, Tonoloway Formation; 344MRCL, Marcellus Formation; 344MNNG, Mahantango Formation; 341BRLR, Brallier Formation; 341CMNG, Chemung Group; 341HMPR, Hampshire Formation; 337POCN, Pocono Group; gal/min, gallons per minute; (gal/min)/ft, gallons per minute per foot of drawdown; ft2/d, foot squared per day; --, not determined. See figure 9 for well locations]

Site 

number

1USGS 

station 

name

Well 

depth 

(ft bls)

Length of 

casing 

(ft)

Casing 

diameter 

(in.)

Landsurface 

altitude 

(ft)

Static 

water 

level 

(ft bls)

Date 

water 

level 

measured

Hydrogeologic 

unit

Discharge 

(gal/min)

Specific 

capacity 

((gal/min)/ft)

Transmissivity 

average 

(ft2/d)

63 Mrg-0125 420 79 6 723 63.2 8-31-2004 341BRLR 7.3 0.11 4.564 Mrg-0126 400 40 6 701 25.23 8-31-2004 341BRLR 6.2 .06 265 Mrg-0127 720 60 6 835 87.22 9-1-2004 341CMNG 4.3 .10 366 Mrg-0096 225 40 6 640 53.77 7-13-2004 341BRLR 6.5 .82 2467 Mrg-0108 260 58 6 800 112.51 8-4-2004 341BRLR -- .34 1368 Mrg-0129 340 80 6 925 56.95 9-2-2004 341MRCL 4.5 .05 269 Mrg-0109 -- -- 6 780 185.81 8-4-2004 341BRLR -- -- --70 Mrg-0119 300 -- 6 700 3.55 8-24-2004 341BRLR -- -- --71 Mrg-0099 460 -- 6 1,200 -- 7-14-2004 341HMPR 7.1 -- --72 Mrg-0098 405 -- 6 1,230 146.77 7-14-2004 341HMPR 7.6 -- --73 Mrg-0168 80 39.2 6 818 3 4-26-2005 344MNNG 4.3 2.40 32774 Mrg-0111 400 19 6 740 4.65 8-9-2004 341BRLR -- -- --75 Mrg-0169 320 39 6 888 50.7 4-26-2005 341BRLR 3.2 .12 476 Mrg-0158 51 27.1 6 561 15.75 4-14-2005 341HMPR .8 .15 4077 Mrg-0089 180 40 6 900 36.85 7-1-2004 341CMNG -- 3.26 1,49078 Mrg-0087 425 -- 6 880 56.85 6-30-2004 341CMNG 10.7 1.06 76.579 Mrg-0166 480 -- 6 800 268.45 4-22-2005 344MRCL 5.6 -- --80 Mrg-0175 185 58.6 6 915 53.4 5-5-2005 341CMNG 7 .28 1581 Mrg-0086 186 -- 6 1,010 -- 5-19-2004 341CMNG -- -- --82 Mrg-0154 121 21.8 6 848 32.9 4-12-2005 341HMPR 4.2 .52 3883 Mrg-0164 300 38.9 6 866 64.63 4-21-2005 344MNNG 60 .89 19584 Mrg-0174 440 -- 6 1,003 281.33 5-3-2005 344MRCL 6 -- --85 Mrg-0163 300 40.5 6 913 137.86 4-20-2005 344MNNG 7.2 6.32 94486 Mrg-0165 400 -- 6 853 226.77 4-21-2005 344MRCL 2.5 -- --87 Mrg-0134 250 80 6 1,025 35.23 9-10-2004 341CMNG 7.9 .41 1488 Mrg-0115 220 99 6 1,110 38.6 8-11-2004 341HMPR -- .41 2289 Mrg-0153 220 58.85 6 1,125 69.6 4-12-2005 341HMPR 4.8 .16 590 Mrg-0162 187 47.3 6 1,128 45.8 4-20-2005 341HMPR 2.8 .06 291 Mrg-0150 135 -- 6 1,025 50.21 3-17-2005 341HMPR 3.2 -- --92 Mrg-0157 103 -- 6 656 19.70 4-14-2005 341BRLR 4.5 0.08 2

1USGS station name designates the chronological order in which sampling sites were established in a given county; for example, Mrg-0090 is the 90th well site established in Morgan County, West Virginia.

40 Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia
Appendix 2a. Water-quality data values for wells, Morgan County, West Virginia. —Continued

[USGS, U.S. Geological Survey. Units of measure: deg C, degrees Celsius; μS/cm, microsiemens per centimeter at 25oC; mg/L, milligrams per liter; NTU, nephelometric turbidity units. Symbols: --, not determined; <, less than; E, estimated]

Site 

number

1USGS

station 

name Date

Temperature, 

(deg C)

Specific 

conductance 

(μS/cm)

pH 

(units)

Oxygen, 

dissolved 

(mg/L)

Turbidity 

(NTU)

Alkalinity,

(mg/L as 

CaCO3)

Bicarbonate, 

dissolved, 

field 

(mg/L as 

HCO3)

Carbonate, 

dissolved,

field 

(mg/L as 

CO3)

Water 

hardness 

(mg/L as 

CaCO3)

Calcium, 

dissolved 

(mg/L)

1 Mrg-0090 7-6-2004 13.5 160 5.7 5.6 <50 -- -- -- -- --2 Mrg-0178 5-10-2005 12.8 164 6.8 2.6 55 67 82 <1 89 28.63 Mrg-0146 11-3-2004 12.8 230 6.4 E.4 19 72 88 <1 92 16.44 Mrg-0114 8-11-2004 12.6 220 6.8 E.3 10 106 129 <1 99 17.15 Mrg-0124 8-26-2004 13.4 226 6.7 -- <2.0 105 128 <1 100 226 Mrg-0104 8-2-2004 14.2 321 6.9 -- 4.8 125 152 <1 150 31.77 Mrg-0122 8-25-2004 12.3 284 6.5 -- 2.4 85 104 <1 130 19.98 Mrg-0144 11-2-2004 12.9 254 7.1 E.2 -- 121 148 <1 -- E.019 Mrg-0130 9-2-2004 13.4 80 4.8 5.7 <1.0 8 10 <1 18 1.81

9 Mrg-0130 9-9-2004 13.6 77 4.7 4.8 <1.0 -- -- -- -- --

10 Mrg-0095 7-12-2004 13.2 209 6.4 E.6 <1.0 105 128 <1 82 15.611 Mrg-0139 10-19-2004 13.5 169 6.6 -- -- 113 138 <1 66 13.912 Mrg-0136 9-22-2004 13.8 266 6.2 E.5 7 80 98 <1 100 17.513 Mrg-0142 10-21-2004 12.6 228 6.4 E.7 -- 83 101 <1 91 18.114 Mrg-0145 10-19-2004 12.2 296 6.8 E.2 -- 173 211 <1 130 38.915 Mrg-0135 9-22-2004 13.2 403 6.8 2.3 <1.0 131 160 <1 160 39.316 Mrg-0156 4-13-2005 12.1 157 6.5 2.0 <1.0 66 80 <1 63 17.717 Mrg-0094 7-12-2004 12.6 273 7.3 E.2 2.7 110 134 <1 62 15.318 Mrg-0161 4-19-2005 14.3 440 7.2 E.3 <1.0 184 224 <1 220 69.219 Mrg-0137 9-23-2004 14.0 201 6.8 E.4 100 76 93 <1 77 14.720 Mrg-0143 11-2-2004 12.9 178 6.4 1.7 <1.0 71 87 <1 69 15.721 Mrg-0140 10-20-2004 12.2 309 7.6 E.3 -- 164 200 <1 140 4022 Mrg-0092 7-7-2004 13.8 225 7.3 E.4 <3.0 106 129 <1 97 25.323 Mrg-0149 11-4-2004 11.6 207 6.8 E.2 <1.0 69 84 <1 78 18.324 Mrg-0147 11-3-2004 12.1 198 6.1 E.9 29 49 60 <1 90 18.425 Mrg-0112 8-10-2004 13.8 202 6.2 E.9 <1.0 77 94 <1 61 10.126 Mrg-0138 9-23-2004 13.0 227 6.6 E.3 1.7 65 79 <1 98 2527 Mrg-0141 10-20-2004 12.9 283 6.3 E.4 -- 69 84 <1 100 21.428 Mrg-0176 5-6-2005 12.5 213 6.9 E.8 4.7 93 113 <1 91 18.229 Mrg-0159 4-15-2005 12.4 458 5.0 E.8 5 10 12 <1 160 20.5

Appendixes  41
Appendix 2a. Water-quality data values for wells, Morgan County, West Virginia. —Continued

[USGS, U.S. Geological Survey. Units of measure: deg C, degrees Celsius; μS/cm, microsiemens per centimeter at 25oC; mg/L, milligrams per liter; NTU, nephelometric turbidity units. Symbols: --, not determined; <, less than; E, estimated]

Site 

number

1USGS

station 

name Date

Temperature, 

(deg C)

Specific 

conductance 

(μS/cm)

pH 

(units)

Oxygen, 

dissolved 

(mg/L)

Turbidity 

(NTU)

Alkalinity,

(mg/L as 

CaCO3

)

Bicarbonate, 

dissolved, 

field 

(mg/L as 

HCO3

)

Carbonate, 

dissolved,

field 

(mg/L as 

CO3

)

Water 

hardness 

(mg/L as 

CaCO3

)

Calcium, 

dissolved 

(mg/L)

30 Mrg-0091 7-7-2004 13.0 137 6.6 31.4 2 64 78 <1 57 11.731 Mrg-0179 5-11-2005 14.1 298 6.7 E.3 20 99 121 <1 110 32.132 Mrg-0148 11-4-2004 12.2 88 5.9 5.3 <1.0 24 29 <1 32 6.1433 Mrg-0120 8-25-2004 12.4 318 7.3 -- <1.0 163 199 <1 180 6234 Mrg-0116 8-12-2004 12.9 368 6.9 E.4 4 185 226 <1 190 60.435 Mrg-0155 4-13-2005 12.5 322 7.2 E.3 2.4 138 168 <1 140 33.836 Mrg-0106 8-3-2004 13.5 125 6.0 -- <10 64 78 <1 51 1437 Mrg-0170 4-28-2005 12.5 256 7.0 E.9 <1.0 17 130 <1 110 23.438 Mrg-0100 7-15-2004 12.6 293 7.7 E.2 <1.0 127 155 <1 94 23.139 Mrg-0085 5-19-2004 13.8 502 7.3 313 <1.0 176 214 <1 -- --40 Mrg-0121 8-25-2004 12.4 158 6.7 -- <1.0 69 84 <1 80 27.641 Mrg-0160 4-19-2005 12.2 140 6.2 1.1 3.8 67 82 <1 58 10.242 Mrg-0123 8-26-2004 12.8 737 6.8 2.6 <15 305 372 <1 400 12743 Mrg-0113 8-10-2004 11.8 160 6.1 8.7 25 75 91 <1 76 23.244 Mrg-0088 7-1-2004 12.4 245 7.3 E.4 <1.0 129 157 <1 100 20.745 Mrg-0118 8-24-2004 15.1 214 6.1 E.3 5 71 87 <1 87 25.946 Mrg-0110 8-5-2004 13.0 456 7.1 2.3 91 210 256 <1 270 73.847 Mrg-0167 4-25-2005 11.7 323 7.4 45.9 24 141 172 <1 160 45.848 Mrg-0097 7-13-2004 14.2 393 7.0 4.3 <2.0 202 246 <1 210 56.249 Mrg-0117 6-29-2004 12.3 500 6.7 5.9 <5.0 209 255 <1 240 75.150 Mrg-0133 9-9-2004 13.8 478 7.0 E.3 22 238 290 <1 190 3951 Mrg-0171 5-2-2005 12.2 272 7.3 E.4 2.7 119 145 <1 110 31.752 Mrg-0172 5-2-2005 11.8 227 6.5 E.4 100 94 115 <1 110 36.153 Mrg-0173 5-3-2005 11.2 402 7.2 E.3 17 189 230 <1 220 76.354 Mrg-0103 7-28-2004 14.7 279 6.3 -- 9.1 159 194 <1 130 23.255 Mrg-0102 7-28-2004 13.1 242 6.3 E.7 <1.0 114 139 <1 90 13.156 Mrg-0101 7-27-2004 13.2 202 6.7 E.6 <1.0 110 134 <1 95 20.857 Mrg-0105 8-3-2004 14.1 158 6.0 -- 310 30 37 <1 71 10.858 Mrg-0093 7-8-2004 13.9 180 6.4 -- -- 80 98 <1 78 20.859 Mrg-0107 8-4-2004 13.1 198 6.3 6 <20 70 85 <1 110 39.8

42  Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia
Appendix 2a. Water-quality data values for wells, Morgan County, West Virginia. —Continued

[USGS, U.S. Geological Survey. Units of measure: deg C, degrees Celsius; μS/cm, microsiemens per centimeter at 25oC; mg/L, milligrams per liter; NTU, nephelometric turbidity units. Symbols: --, not determined; <, less than; E, estimated]

Site 

number

1USGS

station 

name Date

Temperature, 

(deg C)

Specific 

conductance 

(μS/cm)

pH 

(units)

Oxygen, 

dissolved 

(mg/L)

Turbidity 

(NTU)

Alkalinity,

(mg/L as 

CaCO3)

Bicarbonate, 

dissolved, 

field 

(mg/L as 

HCO3)

Carbonate, 

dissolved,

field 

(mg/L as 

CO3)

Water 

hardness 

(mg/L as 

CaCO3)

Calcium, 

dissolved 

(mg/L)

60 Mrg-0131 9-8-2004 13.4 182 6.5 4.7 1.3 129 157 <1 82 13.761 Mrg-0132 9-8-2004 16.0 451 7.3 1.4 8 231 282 <1 260 53.762 Mrg-0128 9-1-2004 13.4 305 7.4 2.1 25 171 208 <1 82 20.263 Mrg-0125 8-31-2004 13.2 294 7.4 E.5 4 133 162 <1 130 29.964 Mrg-0126 8-31-2004 14.1 269 7.6 E.6 23 107 130 <1 89 25.165 Mrg-0127 9-1-2004 13.5 167 6.3 1 <1.0 84 102 <1 70 10.266 Mrg-0096 7-13-2004 13.2 249 6.6 E.8 4.8 94 115 <1 110 33.967 Mrg-0108 8-4-2004 12.4 275 7.6 -- 1.2 130 158 <1 130 33.368 Mrg-0129 9-2-2004 13.7 313 6.7 E.3 59 140 171 <1 150 51.569 Mrg-0109 8-4-2004 14.2 271 7.2 -- 1.5 107 130 <1 120 28.870 Mrg-0119 8-24-2004 13.1 270 7.4 -- <20 96 117 <1 120 33.871 Mrg-0099 7-14-2004 13.5 252 7.6 1.9 <1.0 115 140 <1 110 23.872 Mrg-0098 7-14-2004 13.3 263 7.1 2.9 15 117 143 <1 130 25.373 Mrg-0168 4-26-2005 12.3 435 6.6 E.6 5.7 83 101 <1 160 34.874 Mrg-0111 8-9-2004 13.9 270 7.2 <.2 <10 127 155 <1 120 28.575 Mrg-0169 4-26-2005 12.7 322 6.7 E.5 1.2 111 135 <1 140 3776 Mrg-0158 4-14-2005 12.4 222 6.9 E.3 11 94 115 <1 87 22.377 Mrg-0089 7-1-2004 12.5 224 7.6 E.3 <2.0 108 132 <1 98 27.278 Mrg-0087 6-30-2004 13.4 235 7.3 E.1 <2.0 113 138 <1 100 25.579 Mrg-0166 4-22-2005 13.8 75 5.0 8.9 <1.0 8 10 <1 27 7.7580 Mrg-0175 5-5-2005 13.2 195 6.6 E.4 4.3 83 101 <1 86 14.281 Mrg-0086 5-19-2004 13.8 252 6.3 E.8 2.4 98 119 <1 -- 21282 Mrg-0154 4-12-2005 11.9 44 5.3 5.1 2 17 21 <1 16 2.1583 Mrg-0164 4-21-2005 12.4 239 6.6 32.4 1.1 94 115 <1 98 19.784 Mrg-0174 5-3-2005 12.6 82 5.1 10.3 330 11 13 <1 30 8.8285 Mrg-0163 4-20-2005 13 227 6.9 E.5 <1.0 84 102 <1 98 28.986 Mrg-0165 4-21-2005 13.5 103 5.4 5.4 10 22 27 <1 38 10.487 Mrg-0134 9-10-2004 12.6 241 6.4 E.6 17 110 134 <1 100 17.188 Mrg-0115 8-11-2004 12.8 263 7.4 <.2 <4.0 137 167 <1 130 25.589 Mrg-0153 4-12-2005 12 124 6.4 2.5 1.8 47 57 <1 50 8.77

Appendixes  43
Appendix 2a. Water-quality data values for wells, Morgan County, West Virginia. —Continued

[USGS, U.S. Geological Survey. Units of measure: deg C, degrees Celsius; μS/cm, microsiemens per centimeter at 25oC; mg/L, milligrams per liter; NTU, nephelometric turbidity units. Symbols: --, not determined; <, less than; E, estimated]

Site 

number

1USGS

station 

name Date

Temperature, 

(deg C)

Specific 

conductance 

(μS/cm)

pH 

(units)

Oxygen, 

dissolved 

(mg/L)

Turbidity 

(NTU)

Alkalinity,

(mg/L as 

CaCO3

)

Bicarbonate, 

dissolved, 

field 

(mg/L as 

HCO3

)

Carbonate, 

dissolved,

field 

(mg/L as 

CO3

)

Water 

hardness 

(mg/L as 

CaCO3

)

Calcium, 

dissolved 

(mg/L)

90 Mrg-0162 4-20-2005 12 131 6.8 2 3.8 57 69 <1 58 12.791 Mrg-0150 3-17-2005 10.9 163 7.0 0.7 51 79 96 <1 63 13

1USGS station name designates the chronological order in which sampling sites were established in a given county; for example, Mrg-0090 is the 90th well site established in Morgan County, West Virginia.2 Sample concentration reported as “Total.”3 Water cascading down well bore during test.4Air entrained in plumbing system.

44  Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia
Appendix 2b. Water-quality data values for wells, Morgan County, West Virginia. —Continued

[USGS, U.S. Geological Survey. Units of measure: mg/L, milligrams per liter. Symbols: --, not determined; <, less than; E, estimated]

Site 

number

1USGS 

station 

name Date

Magnesium, 

dissolved 

(mg/L)

Potassium, 

dissolved 

(mg/L)

Sodium, 

dissolved 

(mg/L)

Bromide, 

dissolved 

(mg/L)

Chloride, 

dissolved 

(mg/L)

Fluoride, 

dissolved 

(mg/L)

Silica, 

dissolved 

(mg/L)

Sulfate, 

dissolved 

(mg/L)

Solids, 

residue at 

180 deg C 

dissolved 

(mg/L)

Ammonia, 

dissolved 

(mg/L as 

NH4)

Ammonia,

dissolved 

(mg/L) 

as N)

1 Mrg-0090 7-6-2004 -- -- -- -- -- -- -- -- -- -- --2 Mrg-0178 5-10-2005 4.16 0.83 0.72 -- 3.23 0.2 8.3 23.5 115 -- <0.043 Mrg-0146 11-3-2004 12.5 .67 7.69 -- 21.9 .2 21.2 3.8 131 -- <.044 Mrg-0114 8-11-2004 13.7 .71 9.78 -- 4.03 .2 22.8 3.5 136 -- E.025 Mrg-0124 8-26-2004 11.8 .59 11.9 -- 1.17 <.2 24.7 3.1 141 0.08 .066 Mrg-0104 8-2-2004 16.7 .59 8.38 -- 24.7 .2 20.3 5.1 183 .05 .047 Mrg-0122 8-25-2004 18.7 .63 9.14 -- 5.04 .2 22.1 52.6 185 -- E.028 Mrg-0144 11-2-2004 <.008 <.16 59 -- .92 .1 13.1 2.8 -- -- <.049 Mrg-0130 9-2-2004 3.31 .44 5.28 0.12 14.3 <.2 8 3.1 43 -- <.049 Mrg-0130 9-9-2004 -- -- -- -- -- -- -- -- -- -- --

10 Mrg-0095 7-12-2004 10.4 .71 9.68 -- 2.08 .2 22.2 2.8 130 -- <.0411 Mrg-0139 10-19-2004 7.53 .64 8.05 -- 1.16 .2 23 2.6 126 -- <.0412 Mrg-0136 9-22-2004 14.9 .79 8.82 -- 27.4 .2 28.5 2.9 151 .06 .0513 Mrg-0142 10-21-2004 11.1 .7 9.76 -- 13.8 .2 29.8 2.6 140 -- E.0314 Mrg-0145 10-19-2004 8.68 .48 10.6 .02 5.16 .2 35.1 3.6 209 -- E.03

15 Mrg-0135 9-22-2004 13.8 .58 18.3 -- 28.5 <.2 15.2 10.7 206 -- <.04

16 Mrg-0156 4-13-2005 4.5 .57 7.16 -- 1.09 .1 19 9.3 99 -- <.04

17 Mrg-0094 7-12-2004 5.68 .39 33.1 -- 6.56 .2 14.7 8.7 151 .06 .05

18 Mrg-0161 4-19-2005 12.5 1.82 3.63 -- 5.92 .1 8.1 34.3 246 .22 .1719 Mrg-0137 9-23-2004 9.75 .82 9.95 -- 7.22 .2 17.4 5.7 112 -- <.04

20 Mrg-0143 11-2-2004 7.26 .71 9.03 -- 1.4 .1 21.7 12.4 111 -- <.04

21 Mrg-0140 10-20-2004 8.75 .37 11.8 -- 2.24 .1 19 8.8 190 -- <.04

22 Mrg-0092 7-7-2004 8.25 .34 8.16 .02 2.17 .2 17.7 7.5 134 -- <.04

23 Mrg-0149 11-4-2004 7.78 .71 8.87 -- 10.3 .2 20.6 9 118 -- <.04

24 Mrg-0147 11-3-2004 10.7 .92 5.14 -- .86 E.1 27.1 36.6 130 -- <.04

25 Mrg-0112 8-10-2004 8.6 .72 10.1 -- 17.2 <.2 27.5 1.3 129 .15 .1226 Mrg-0138 9-23-2004 8.68 .67 5.83 -- 2.35 <.2 28.1 30.5 143 -- E.02

27 Mrg-0141 10-20-2004 11.4 1.04 13.1 -- 36.2 .1 26.9 6.7 160 .07 .05

28 Mrg-0176 5-6-2005 11.1 .7 9.38 -- 1.36 .3 22.7 8 128 -- E.0329 Mrg-0159 4-15-2005 25.9 2.09 1.16 -- .76 <.1 11.6 172 268 .07 .06

30 Mrg-0091 7-7-2004 6.69 .71 5.41 -- .88 <.2 18.1 5.2 88 -- <.0431 Mrg-0179 5-11-2005 6.43 .74 .78 -- .78 .3 21.1 6.1 128 -- <.04

Appendixes  45
Appendix 2b. Water-quality data values for wells, Morgan County, West Virginia. —Continued

[USGS, U.S. Geological Survey. Units of measure: mg/L, milligrams per liter. Symbols: --, not determined; <, less than; E, estimated]

Site 

number

1USGS 

station 

name Date

Magnesium, 

dissolved 

(mg/L)

Potassium, 

dissolved 

(mg/L)

Sodium, 

dissolved 

(mg/L)

Bromide, 

dissolved 

(mg/L)

Chloride, 

dissolved 

(mg/L)

Fluoride, 

dissolved 

(mg/L)

Silica, 

dissolved 

(mg/L)

Sulfate, 

dissolved 

(mg/L)

Solids, 

residue at 

180 deg C 

dissolved 

(mg/L)

Ammonia, 

dissolved 

(mg/L as 

NH4)

Ammonia,

dissolved 

(mg/L) 

as N)

32 Mrg-0148 11-4-2004 4.01 0.61 4.04 -- 2.52 E0.1 14.9 4.2 57 -- <0.0433 Mrg-0120 8-25-2004 6.25 .7 2.24 -- 1.51 <.2 8.1 11 190 0.06 .0534 Mrg-0116 8-12-2004 8.59 .58 7.85 0.05 5.15 <.2 21.4 8.9 226 .06 .0535 Mrg-0155 4-13-2005 13.5 .46 9.59 -- 7.32 .2 22.4 4.3 175 .1 .0836 Mrg-0106 8-3-2004 3.93 .78 6.36 -- .89 <.2 23.2 5.7 94 -- <.0437 Mrg-0170 4-28-2005 13.2 1.31 9.19 -- 3.4 .2 19 6.7 141 -- <.0438 Mrg-0100 7-15-2004 8.8 1.23 26.4 -- 2.92 <.2 14.1 12.1 165 -- <.0439 Mrg-0085 5-19-2004 223 8 25.7 <.05 17 2<.1 -- 27 -- 2.03 2.0240 Mrg-0121 8-25-2004 2.77 .5 1.27 -- .96 <.2 7.2 4 86 -- <.0441 Mrg-0160 4-19-2005 7.8 .93 7.99 -- .9 .2 22.8 2.5 94 -- <.0442 Mrg-0123 8-26-2004 19.8 .89 13.9 .13 8.8 .2 8.6 71.3 444 -- <.0443 Mrg-0113 8-10-2004 4.41 .74 2.07 .03 2.95 <.2 7.2 3.9 91 -- <.0444 Mrg-0088 7-1-2004 11.9 1.22 14.5 -- 1.32 <.2 15.6 4.8 147 -- <.0445 Mrg-0118 8-24-2004 5.32 .72 3.49 .02 1.17 <.2 21.9 30.4 139 -- E.0446 Mrg-0110 8-5-2004 21.5 .53 .85 -- 2.13 <.2 6.7 5.9 238 -- <.0447 Mrg-0167 4-25-2005 12.2 .83 .79 -- .96 .1 6.9 7.7 160 -- <.0448 Mrg-0097 7-13-2004 16.5 1.1 .83 -- 1.72 <.2 7.1 4 208 -- <.0449 Mrg-0117 6-29-2004 12.1 .73 15 -- 32.5 <.2 7.7 3.5 275 -- <.0450 Mrg-0133 9-9-2004 22.7 .42 29.7 -- 24.7 .2 21.4 7.7 290 .07 .0551 Mrg-0171 5-2-2005 8.07 .4 14.1 -- 2.29 .2 17.2 8.1 153 -- <.0452 Mrg-0172 5-2-2005 4.2 .37 3.53 -- 1.53 E.1 17.2 7.8 127 -- <.0453 Mrg-0173 5-3-2005 7.66 .39 2.13 -- 1.96 .1 8.5 8.5 219 -- <.0454 Mrg-0103 7-28-2004 16.6 .65 11.4 -- 8.66 <.2 27.2 7.2 192 -- E.0255 Mrg-0102 7-28-2004 14 .7 11.1 -- 4.5 <.2 26 4 148 -- E.0256 Mrg-0101 7-27-2004 10.5 .85 9.13 -- .67 .2 20.2 7 135 -- E.0357 Mrg-0105 8-3-2004 10.7 .66 8.34 -- 1.18 <.2 21.2 2.9 74 -- <.0458 Mrg-0093 7-8-2004 6.33 .41 6.97 .04 6.12 <.2 20.4 7 118 -- <.0459 Mrg-0107 8-4-2004 1.74 .47 .49 -- .55 <.2 7.8 6.6 99 -- <.0460 Mrg-0131 9-8-2004 11.6 .53 9.34 .03 .81 .2 24.2 1.1 139 -- <.0461 Mrg-0132 9-8-2004 29.4 .73 2.82 .04 3.23 <.2 11.8 15.2 269 -- <.0462 Mrg-0128 9-1-2004 7.71 .36 38.6 -- .99 <.2 16.8 10.7 198 .08 .0663 Mrg-0125 8-31-2004 12.6 .31 15.3 -- 1.08 .2 17 12.2 168 .15 .12

46  Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia
Appendix 2b. Water-quality data values for wells, Morgan County, West Virginia. —Continued

[USGS, U.S. Geological Survey. Units of measure: mg/L, milligrams per liter. Symbols: --, not determined; <, less than; E, estimated]

Site 

number

1USGS 

station 

name Date

Magnesium, 

dissolved 

(mg/L)

Potassium, 

dissolved 

(mg/L)

Sodium, 

dissolved 

(mg/L)

Bromide, 

dissolved 

(mg/L)

Chloride, 

dissolved 

(mg/L)

Fluoride, 

dissolved 

(mg/L)

Silica, 

dissolved 

(mg/L)

Sulfate, 

dissolved 

(mg/L)

Solids, 

residue at 

180 deg C 

dissolved 

(mg/L)

Ammonia, 

dissolved 

(mg/L as 

NH4)

Ammonia,

dissolved 

(mg/L) 

as N)

64 Mrg-0126 8-31-2004 6.5 0.43 22.7 -- 2.29 0.2 16.1 21 159 0.2 0.1565 Mrg-0127 9-1-2004 10.8 .63 8.68 -- .87 <.2 24.2 2.4 110 -- E.0366 Mrg-0096 7-13-2004 5.24 .7 7.26 -- 1.86 <.2 19.5 9.1 134 -- <.0467 Mrg-0108 8-4-2004 11.4 .39 10.2 -- 1.37 <.2 15.9 12.9 163 .07 .0568 Mrg-0129 9-2-2004 4.73 .64 5.05 -- 11 <.2 9.7 17.2 184 -- <.0469 Mrg-0109 8-4-2004 11.8 .34 12.8 -- 1.85 .2 16.5 22.6 159 -- <.0470 Mrg-0119 8-24-2004 7.16 .63 15.6 0.02 1.89 .2 15.8 18.9 153 .22 .1771 Mrg-0099 7-14-2004 11.9 1.18 11.7 -- 1.54 <.2 14.8 5.8 140 -- <.0472 Mrg-0098 7-14-2004 15.6 1.57 6.78 -- 1.47 <.2 14.2 8.9 151 -- <.0473 Mrg-0168 4-26-2005 18.8 .41 15.3 -- 60.7 .1 27.8 21 232 .26 .274 Mrg-0111 8-9-2004 11.9 .37 13.3 .03 1.66 .2 15.7 17.8 166 -- <.04

75 Mrg-0169 4-26-2005 11.2 .77 10.8 -- 3.77 0.3 29.6 29.8 192 -- E.0376 Mrg-0158 4-14-2005 7.57 .5 9.12 -- 1.84 .2 19.9 8.8 129 .09 .0777 Mrg-0089 7-1-2004 7.21 .33 8.53 -- 1.2 <.2 15.2 7.9 133 -- E.0478 Mrg-0087 6-30-2004 9.27 .47 9.41 -- 3.66 .2 16 5.6 138 -- <.0479 Mrg-0166 4-22-2005 1.87 1.19 .69 -- 1.45 <.1 6.9 13.4 46 -- <.0480 Mrg-0175 5-5-2005 12.2 .79 7.81 -- 6.06 .2 22.9 2.1 117 -- <.0481 Mrg-0086 5-19-2004 215 2.7 212 .12 6.6 2.2 -- 1.4 -- 2<.01 2<.0282 Mrg-0154 4-12-2005 2.64 .46 3.4 -- .68 <.1 15.2 1.8 37 -- <.0483 Mrg-0164 4-21-2005 11.7 .66 11.7 -- .65 .2 22.8 17.9 143 .08 .0684 Mrg-0174 5-3-2005 1.82 1.7 .79 -- 1.75 <.1 6.6 11.8 40 -- <.0485 Mrg-0163 4-20-2005 6.32 .72 7.77 -- .97 .2 19.7 17.3 132 -- <.0486 Mrg-0165 4-21-2005 2.89 .83 3.51 -- 6.43 <.1 8.1 12.4 58 -- <.0487 Mrg-0134 9-10-2004 15.1 .49 10.8 -- 5.52 <.2 29.1 3 148 -- E.0488 Mrg-0115 8-11-2004 14.9 1.42 9.79 -- 1.83 <.2 16.7 4.3 157 -- <.0489 Mrg-0153 4-12-2005 6.74 .74 5.11 -- .75 .1 20.1 4.7 76 -- <.0490 Mrg-0162 4-20-2005 6.33 .7 4.25 -- .67 .1 16.3 5.2 81 -- <.0491 Mrg-0150 3-17-2005 7.47 .48 9.02 -- .96 .1 19.4 4.7 103 -- <.04

1USGS station name designates the chronological order in which sampling sites were established in a given county; for example, Mrg-0090 is the 90th well site established in Morgan County, West Virginia.

2Sample concentration reported as “Total.” 

Appendixes  47
Appendix 2c. Water-quality data values for wells, Morgan County, West Virginia. —Continued

[USGS, U.S. Geological Survey.Units of measure: mg/L, milligrams per liter; col/100 ml, colonies per 100 milliliters; μg/L, micrograms per liter. Symbols:--, not determined; <, less than; E, estimated]

Site 

number

1USGS 

station 

name Date

Nitrate+

nitrite, 

dissolved

(mg/L 

as N)

Nitrite, 

dissolved

(mg/L 

as N)

Orthophosphate, 

dissolved

(mg/L )

Orthophosphate, 

dissolved 

(mg/L 

as P)

Phosphorus, 

dissolved

(mg/L)

E. coli, 

(col/100 

ml)

Coliform, 

fecal 

(col/100 

ml)

Coliform, 

total 

(col/100 

ml)

Aluminum, 

total

(μg/L)

Antimony, 

dissolved

(μg/L)

1 Mrg-0090 7-6-2004 -- -- -- -- -- -- -- -- -- --2 Mrg-0178 5-10-2005 1.11 <0.008 -- <0.02 <0.04 <1 -- <1 -- --3 Mrg-0146 11-3-2004 <.06 <.008 -- <.02 <.04 <1 <1 E4 -- --

4 Mrg-0114 8-11-2004 <.06 <.008 -- E.01 E.03 <1 <1 <1 -- --

5 Mrg-0124 8-26-2004 <.06 <.008 -- <.02 E.04 <1 <1 <1 -- --

6 Mrg-0104 8-2-2004 <.06 <.008 -- E.01 <.04 <1 <1 E12 -- --

7 Mrg-0122 8-25-2004 <.06 <.008 -- <.02 <.04 <1 <1 <1 -- --

8 Mrg-0144 11-2-2004 <.06 <.008 0.092 .03 .04 <1 <1 <1 -- --

9 Mrg-0130 9-2-2004 .34 <.008 -- <.02 <.04 -- -- -- 70 <0.209 Mrg-0130 9-9-2004 -- -- -- -- -- <1 <1 E17 -- --

10 Mrg-0095 7-12-2004 <.06 <.008 -- <.02 <.04 -- <1 -- -- --

11 Mrg-0139 10-19-2004 <.06 <.008 -- <.02 E.03 <1 <1 E2 -- --12 Mrg-0136 9-22-2004 <.06 <.008 -- <.02 <.04 <1 <1 E7 -- --

13 Mrg-0142 10-21-2004 <.06 <.008 -- <.02 .09 <1 <1 E380 -- --

14 Mrg-0145 10-19-2004 <.06 <.008 -- <.02 E.02 <1 <1 <1 13 --

15 Mrg-0135 9-22-2004 .18 <.008 -- <.02 <.04 <1 <1 <1 -- --

16 Mrg-0156 4-13-2005 .08 <.008 -- <.02 <.04 <1 <1 <1 -- --

17 Mrg-0094 7-12-2004 <.06 <.008 .095 .03 E.04 -- <1 -- -- --

18 Mrg-0161 4-19-2005 <.06 <.008 -- <.02 <.04 <1 <1 <1 <2 --

19 Mrg-0137 9-23-2004 <.06 <.008 -- E.01 E.03 <1 E38 22 -- --20 Mrg-0143 11-2-2004 <.06 <.008 -- <.02 <.04 <1 <1 120 -- --21 Mrg-0140 10-20-2004 E.04 <.008 -- <.02 <.04 <1 <1 E5 -- --

22 Mrg-0092 7-7-2004 E.04 .042 -- <.02 <.04 <1 <1 70 50 --23 Mrg-0149 11-4-2004 <.06 <.008 -- <.02 <.04 <1 <1 E12 -- --

24 Mrg-0147 11-3-2004 <.06 <.008 -- E.02 <.04 <1 <1 E5 -- --

25 Mrg-0112 8-10-2004 <.06 <.008 -- <.02 <.04 <1 <1 <1 17 <.20

26 Mrg-0138 9-23-2004 <.06 <.008 -- <.02 <.04 <1 350 100 -- --27 Mrg-0141 10-20-2004 <.06 <.008 -- <.02 <.04 <1 <1 E4 -- --

28 Mrg-0176 5-6-2005 <.06 <.008 -- E.01 <.04 <1 <1 49 7 E.1329 Mrg-0159 4-15-2005 <.06 <.008 -- <.02 <.04 <1 <1 E5 -- --

30 Mrg-0091 7-7-2004 .09 <.008 .175 .06 .07 <1 <1 E13 -- --

31 Mrg-0179 5-11-2005 <.06 <.008 -- E.01 <.04 <1 -- <1 -- --

48  Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia
Appendix 2c. Water-quality data values for wells, Morgan County, West Virginia. —Continued

[USGS, U.S. Geological Survey.Units of measure: mg/L, milligrams per liter; col/100 ml, colonies per 100 milliliters; μg/L, micrograms per liter. Symbols:--, not determined; <, less than; E, estimated]

Site 

number

1USGS 

station 

name Date

Nitrate+

nitrite, 

dissolved

(mg/L 

as N)

Nitrite, 

dissolved

(mg/L 

as N)

Orthophosphate, 

dissolved

(mg/L )

Orthophosphate, 

dissolved 

(mg/L 

as P)

Phosphorus, 

dissolved

(mg/L)

E. coli, 

(col/100 

ml)

Coliform, 

fecal 

(col/100 

ml)

Coliform, 

total 

(col/100 

ml)

Aluminum, 

total

(μg/L)

Antimony, 

dissolved

(μg/L)

32 Mrg-0148 11-4-2004 1.51 <0.008 -- E0.02 E0.03 <1 <1 E4 -- --33 Mrg-0120 8-25-2004 <.06 <.008 -- <.02 <.04 <1 <1 <1 -- --

34 Mrg-0116 8-12-2004 <.06 <.008 -- <.02 <.04 E2 <1 33 <2 <0.20

35 Mrg-0155 4-13-2005 <.06 <.008 0.067 .02 E.02 <1 <1 <1 5 <.20

36 Mrg-0106 8-3-2004 E.04 <.008 .509 .17 .18 <1 <1 <1 -- --

37 Mrg-0170 4-28-2005 .12 <.008 .233 .08 .09 <1 <1 <1 -- --

38 Mrg-0100 7-15-2004 <.06 <.008 .107 .04 E.03 <1 <1 E3 -- --

39 Mrg-0085 5-19-2004 -- 2<.01 -- -- -- -- -- -- <3 2<140 Mrg-0121 8-25-2004 .13 <.008 -- <.02 <.04 <1 <1 <1 -- --

41 Mrg-0160 4-19-2005 E.05 <.008 .31 .1 .1 <1 <1 <1 3 --

42 Mrg-0123 8-26-2004 2.06 <.008 -- <.02 <.04 <1 <1 <1 90 <.20

43 Mrg-0113 8-10-2004 .24 <.008 -- <.02 <.04 E3 <1 E13 110 <.20

44 Mrg-0088 7-1-2004 <.06 <.008 .209 .07 .07 <1 <1 24 -- --45 Mrg-0118 8-24-2004 <.06 E.005 -- E.01 .11 <1 <1 <1 18 <.20

46 Mrg-0110 8-5-2004 .07 <.008 -- <.02 <.04 <1 E2 E4 -- --

47 Mrg-0167 4-25-2005 E.06 <.008 -- <.02 <.04 <1 <1 <1 2 --

48 Mrg-0097 7-13-2004 E.04 <.008 -- <.02 <.04 <1 <1 E1 -- --

49 Mrg-0117 6-29-2004 .62 <.008 -- <.02 <.04 <1 <1 E2 -- --

50 Mrg-0133 9-9-2004 <.06 <.008 -- <.02 <.04 <1 <1 <1 -- --

51 Mrg-0171 5-2-2005 <.06 <.008 -- <.02 <.04 <1 <1 52 -- --52 Mrg-0172 5-2-2005 <.06 <.008 -- <.02 <.04 <1 <1 <1 -- --

53 Mrg-0173 5-3-2005 <.06 <.008 -- <.02 <.04 <1 <1 <1 13 <.20

54 Mrg-0103 7-28-2004 E.06 <.008 -- <.02 <.04 <1 <1 120 -- --55 Mrg-0102 7-28-2004 <.06 E.004 -- <.02 E.02 <1 <1 480 -- --56 Mrg-0101 7-27-2004 <.06 <.008 -- E.01 <.04 <1 <1 E3 -- --57 Mrg-0105 8-3-2004 <.06 <.008 -- <.02 .25 <1 E2 <1 -- --

58 Mrg-0093 7-8-2004 .24 E.006 -- <.02 <.04 <1 <1 E1 E1 --

59 Mrg-0107 8-4-2004 <.06 <.008 -- <.02 <.04 <1 <1 <1 -- --

60 Mrg-0131 9-8-2004 <.06 <.008 .08 .03 E.04 <1 <1 <1 10 <.20

61 Mrg-0132 9-8-2004 1.83 <.008 -- <.02 <.04 <1 <1 E6 5 <.20

62 Mrg-0128 9-1-2004 <.06 <.008 -- <.02 <.04 <1 <1 E15 -- --

63 Mrg-0125 8-31-2004 <.06 <.008 -- E.01 <.04 <1 <1 E4 -- --

Appendixes  49
Appendix 2c. Water-quality data values for wells, Morgan County, West Virginia. —Continued

[USGS, U.S. Geological Survey.Units of measure: mg/L, milligrams per liter; col/100 ml, colonies per 100 milliliters; μg/L, micrograms per liter. Symbols:--, not determined; <, less than; E, estimated]

Site 

number

1USGS 

station 

name Date

Nitrate+

nitrite, 

dissolved

(mg/L 

as N)

Nitrite, 

dissolved

(mg/L 

as N)

Orthophosphate, 

dissolved

(mg/L )

Orthophosphate, 

dissolved 

(mg/L 

as P)

Phosphorus, 

dissolved

(mg/L)

E. coli, 

(col/100 

ml)

Coliform, 

fecal 

(col/100 

ml)

Coliform, 

total 

(col/100 

ml)

Aluminum, 

total

(μg/L)

Antimony, 

dissolved

(μg/L)

64 Mrg-0126 8-31-2004 <0.06 <0.008 -- <0.02 <0.04 <1 <1 <1 -- --65 Mrg-0127 9-1-2004 <.06 <.008 -- <.02 <.04 <1 <1 <1 -- --

66 Mrg-0096 7-13-2004 <.06 <.008 -- E.01 E.03 <1 E1 110 -- --

67 Mrg-0108 8-4-2004 <.06 <.008 -- <.02 <.04 <1 <1 <1 -- --

68 Mrg-0129 9-2-2004 .07 <.008 -- <.02 <.04 <1 <1 25 -- --69 Mrg-0109 8-4-2004 .08 <.008 -- <.02 <.04 <1 <1 <1 -- --

70 Mrg-0119 8-24-2004 <.06 <.008 -- <.02 <.04 <1 <1 <1 890 <0.20

71 Mrg-0099 7-14-2004 .08 <.008 0.11 .04 E.03 <1 <1 <1 -- --72 Mrg-0098 7-14-2004 1.42 <.008 .169 .06 .06 <1 <1 E13 -- --

73 Mrg-0168 4-26-2005 <.06 <.008 .071 .02 .07 <1 <1 <1 3 --

74 Mrg-0111 8-9-2004 <.06 <.008 -- <.02 .15 <1 <1 E12 -- --

75 Mrg-0169 4-26-2005 <.06 <.008 .071 .02 E.04 <1 <1 <1 7 --

76 Mrg-0158 4-14-2005 <.06 <.008 -- <.02 <.04 <1 <1 <1 -- --

77 Mrg-0089 7-1-2004 <.06 <.008 -- <.02 <.04 <1 <1 740 -- --

78 Mrg-0087 6-30-2004 <.06 <.008 -- <.02 <.04 <1 <1 30 -- --79 Mrg-0166 4-22-2005 1.7 <.008 .092 .03 .05 <1 <1 <1 12 --

80 Mrg-0175 5-5-2005 <.06 <.008 -- <.02 <.04 <1 <1 E8 8 <.20

81 Mrg-0086 5-19-2004 -- 2<.01 -- -- 2.06 <1 <1 <1 <3 2<1

82 Mrg-0154 4-12-2005 <.06 <.008 -- E.01 <.04 <1 <1 <1 50 <.20

83 Mrg-0164 4-21-2005 <.06 <.008 -- <.02 <.04 <1 <1 E2 -- --

84 Mrg-0174 5-3-2005 2.6 <.008 .095 .03 E.03 <1 <1 <1 2,340 <.20

85 Mrg-0163 4-20-2005 <.06 <.008 -- E.01 <.04 <1 <1 <1 2 --86 Mrg-0165 4-21-2005 .15 <.008 -- E.01 E.02 <1 <1 <1 290 --

87 Mrg-0134 9-10-2004 <.06 <.008 -- E.01 .09 <1 <1 650 -- --

88 Mrg-0115 8-11-2004 <.06 <.008 -- E.02 E.02 <1 <1 <1 -- --

89 Mrg-0153 4-12-2005 .16 <.008 .279 .09 .09 <1 <1 <1 -- --

90 Mrg-0162 4-20-2005 .13 <.008 .058 .02 E.03 <1 <1 <1 60 --

91 Mrg-0150 3-17-2005 E.05 <.008 -- <.02 <.04 -- <1 -- -- --

1USGS station name designates the chronological order in which sampling sites were established in a given county; for example, Mrg-0090 is the 90th well site established in Morgan County, West Virginia.2 Sample concentration reported as “Total.” 

50 Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia
Appendix 2d. Water-quality data values for wells, Morgan County, West Virginia. —Continued

[USGS, U.S. Geological Survey. Units of measure: μg/L, micrograms per liter, pCi/L, picocuries per liter. Symbols: --, not determined; <, less than; E, estimated]

Site 

number

1USGS

station 

name Date

Arsenic, 

total 

(μg/L)

Barium, 

total 

(μg/L)

Cadmium, 

dissolved 

(μg/L)

Iron, 

dissolved 

(μg/L)

Lead, 

dissolved 

(μg/L)

Manganese, 

dissolved 

(μg/L)

Nickel, 

dissolved 

(μg/L)

Strontium, 

dissolved 

(μg/L)

Zinc, 

total 

(μg/L)

Radon-222, 

total 

(pCi/L)

1 Mrg-0090 7-6-2004 -- -- -- -- -- -- -- -- -- --2 Mrg-0178 5-10-2005 -- -- -- <6 -- <0.6 -- -- -- --3 Mrg-0146 11-3-2004 -- -- -- 2,870 -- 1,020 -- -- -- --4 Mrg-0114 8-11-2004 -- -- -- 375 -- 394 -- -- -- --5 Mrg-0124 8-26-2004 -- -- -- 1,970 -- 369 -- -- -- --6 Mrg-0104 8-2-2004 -- -- -- 298 -- 449 -- -- -- --7 Mrg-0122 8-25-2004 -- -- -- 4,400 -- 977 -- -- -- --8 Mrg-0144 11-2-2004 -- -- -- 7 -- <.6 -- -- -- --9 Mrg-0130 9-2-2004 <2 52.4 E0.04 <6 1.7 38.2 12.5 8.87 18 2,1709 Mrg-0130 9-9-2004 -- -- -- -- -- -- -- -- -- --

10 Mrg-0095 7-12-2004 -- -- -- 2,440 -- 482 -- -- -- --11 Mrg-0139 10-19-2004 -- -- -- 944 -- 298 -- -- -- --12 Mrg-0136 9-22-2004 -- -- -- 769 -- 705 -- -- -- --13 Mrg-0142 10-21-2004 -- -- -- 2,950 -- 965 -- -- -- --14 Mrg-0145 10-19-2004 <2 344 -- 2,150 -- 698 -- -- E5 12015 Mrg-0135 9-22-2004 -- -- -- E4 -- 14 -- -- -- --

16 Mrg-0156 4-13-2005 -- -- -- <6 -- 7.1 -- -- -- --17 Mrg-0094 7-12-2004 -- -- -- E5 -- 73.8 -- -- -- --

18 Mrg-0161 4-19-2005 <2 60.4 -- 223 -- 57.9 -- -- 238 --

19 Mrg-0137 9-23-2004 -- -- -- 9 -- 526 -- -- -- --20 Mrg-0143 11-2-2004 -- -- -- 27 -- 53.1 -- -- -- --

21 Mrg-0140 10-20-2004 -- -- -- 13 -- 102 -- -- -- --22 Mrg-0092 7-7-2004 7 309 -- 45 -- 288 -- -- 9 --

23 Mrg-0149 11-4-2004 -- -- -- 534 -- 322 -- -- -- --

24 Mrg-0147 11-3-2004 -- -- -- 216 -- 55.8 -- -- -- --25 Mrg-0112 8-10-2004 2 340 <.04 6,070 <.08 1,510 .51 29.5 E3 450

26 Mrg-0138 9-23-2004 -- -- -- 2,490 -- 124 -- -- -- --27 Mrg-0141 10-20-2004 -- -- -- 610 -- 925 -- -- -- --

28 Mrg-0176 5-6-2005 3 223 <.04 462 <.08 230 1.76 132 10 --29 Mrg-0159 4-15-2005 -- -- -- 24,100 -- 3,920 -- -- -- --

30 Mrg-0091 7-7-2004 -- -- -- <6 -- 32.9 -- -- -- --

31 Mrg-0179 5-11-2005 -- -- -- <6 -- <.6 -- -- -- --32 Mrg-0148 11-4-2004 -- -- -- <6 -- 22.2 -- -- -- --

Appendixes  51
Appendix 2d. Water-quality data values for wells, Morgan County, West Virginia. —Continued

[USGS, U.S. Geological Survey. Units of measure: μg/L, micrograms per liter, pCi/L, picocuries per liter. Symbols: --, not determined; <, less than; E, estimated]

Site 

number

1USGS

station 

name Date

Arsenic, 

total 

(μg/L)

Barium, 

total 

(μg/L)

Cadmium, 

dissolved 

(μg/L)

Iron, 

dissolved 

(μg/L)

Lead, 

dissolved 

(μg/L)

Manganese, 

dissolved 

(μg/L)

Nickel, 

dissolved 

(μg/L)

Strontium, 

dissolved 

(μg/L)

Zinc, 

total 

(μg/L)

Radon-222, 

total 

(pCi/L)

33 Mrg-0120 8-25-2004 -- -- -- 131 -- 98.6 -- -- -- --

34 Mrg-0116 8-12-2004 3 220 <.04 1,080 <.08 556 1.34 137 <4 41035 Mrg-0155 4-13-2005 3 291 <.04 393 <.08 287 1.01 79.8 <6 8036 Mrg-0106 8-3-2004 -- -- -- <6 -- 4.2 -- -- -- --37 Mrg-0170 4-28-2005 -- -- -- <6 -- E.5 -- -- -- --38 Mrg-0100 7-15-2004 -- -- -- <6 -- 9 -- -- -- --39 Mrg-0085 5-19-2004 <4 76 2<.5 2152 2<2 2<17 2<1 -- -- 340

40 Mrg-0121 8-25-2004 -- -- -- 14 -- 10 -- -- -- --41 Mrg-0160 4-19-2005 <2 137 -- 12 -- 210 -- -- <6 --42 Mrg-0123 8-26-2004 E2 53.5 E.02 <6 .26 E.7 3.4 1,140 8 --43 Mrg-0113 8-10-2004 <2 37.5 <.04 62 .11 19.3 1.8 219 6 1,33044 Mrg-0088 7-1-2004 -- -- -- <6 -- <.8 -- -- -- --45 Mrg-0118 8-24-2004 2 52.9 <.04 7,050 <.08 118 30.6 51.3 191 1046 Mrg-0110 8-5-2004 -- -- -- 37 -- 8.7 -- -- -- 35047 Mrg-0167 4-25-2005 <2 48.8 -- E5 -- 0.6 -- -- <6 --48 Mrg-0097 7-13-2004 -- -- -- <6 -- <.8 -- -- -- --49 Mrg-0117 6-29-2004 -- -- -- 44 -- 2.4 -- -- -- --50 Mrg-0133 9-9-2004 -- -- -- 831 -- 274 -- -- -- --51 Mrg-0171 5-2-2005 -- -- -- <6 -- 2.1 -- -- -- --52 Mrg-0172 5-2-2005 -- -- -- 18 -- 103 -- -- -- --53 Mrg-0173 5-3-2005 <2 16.9 <.04 129 0.15 118 3.21 588 <6 10054 Mrg-0103 7-28-2004 -- -- -- 263 -- 1,300 -- -- -- --55 Mrg-0102 7-28-2004 -- -- -- 4,900 -- 1,060 -- -- -- --56 Mrg-0101 7-27-2004 -- -- -- 10 -- 240 -- -- -- --57 Mrg-0105 8-3-2004 -- -- -- 19 -- 289 -- -- -- --58 Mrg-0093 7-8-2004 3 227 -- 517 -- 636 -- -- 5 --59 Mrg-0107 8-4-2004 -- -- -- 89 -- 6.7 -- -- -- --60 Mrg-0131 9-8-2004 E1 128 <.04 <6 .29 12.2 1.31 92.9 E4 17061 Mrg-0132 9-8-2004 -- 74.7 <.04 <6 E.05 1 1.67 5,520 E3 49062 Mrg-0128 9-1-2004 -- -- -- 10 -- 16.1 -- -- -- --63 Mrg-0125 8-31-2004 -- -- -- 28 -- 60.9 -- -- -- --64 Mrg-0126 8-31-2004 -- -- -- 68 -- 102 -- -- -- --65 Mrg-0127 9-1-2004 -- -- -- 1,590 -- 346 -- -- -- --

52  Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia
Appendix 2d. Water-quality data values for wells, Morgan County, West Virginia. —Continued

[USGS, U.S. Geological Survey. Units of measure: μg/L, micrograms per liter, pCi/L, picocuries per liter. Symbols: --, not determined; <, less than; E, estimated]

Site 

number

1USGS

station 

name Date

Arsenic, 

total 

(μg/L)

Barium, 

total 

(μg/L)

Cadmium, 

dissolved 

(μg/L)

Iron, 

dissolved 

(μg/L)

Lead, 

dissolved 

(μg/L)

Manganese, 

dissolved 

(μg/L)

Nickel, 

dissolved 

(μg/L)

Strontium, 

dissolved 

(μg/L)

Zinc, 

total 

(μg/L)

Radon-222, 

total 

(pCi/L)

66 Mrg-0096 7-13-2004 -- -- -- <6 -- 13.9 -- -- -- --67 Mrg-0108 8-4-2004 -- -- -- 13 -- 129 -- -- -- --68 Mrg-0129 9-2-2004 -- -- -- 42 -- 125 -- -- -- 56069 Mrg-0109 8-4-2004 -- -- -- E5 -- 10.2 -- -- -- --70 Mrg-0119 8-24-2004 4 328 <.04 126 <.08 123 .8 1,290 10 38071 Mrg-0099 7-14-2004 -- -- -- <6 -- 1.1 -- -- -- --72 Mrg-0098 7-14-2004 -- -- -- <6 -- <.8 -- -- -- --73 Mrg-0168 4-26-2005 <2 98.8 -- 2,760 -- 110 -- -- E6 --74 Mrg-0111 8-9-2004 -- -- -- 77 -- 120 -- -- -- --75 Mrg-0169 4-26-2005 2 49.1 -- 1,120 -- 1,050 -- -- 23 --76 Mrg-0158 4-14-2005 -- -- -- 1,380 -- 534 -- -- -- --77 Mrg-0089 7-1-2004 -- -- -- 42 -- 135 -- -- -- --78 Mrg-0087 6-30-2004 -- -- -- <6 -- 179 -- -- -- --79 Mrg-0166 4-22-2005 E1 21.2 -- E5 -- 8.6 -- -- 13 --80 Mrg-0175 5-5-2005 8 390 <.04 1,140 <.08 382 1.96 36.1 12 --81 Mrg-0086 5-19-2004 8 150 2<.5 23,370 -- 21,190 2<1 -- 3 25082 Mrg-0154 4-12-2005 <2 25.9 <.04 <6 .95 E.5 2.14 9.69 8 --83 Mrg-0164 4-21-2005 -- -- -- 404 -- 358 -- -- -- --84 Mrg-0174 5-3-2005 <2 101 .11 8 E.05 14 3.32 28.5 696 64085 Mrg-0163 4-20-2005 <2 47.8 -- 8 -- 85.1 -- -- 8 7086 Mrg-0165 4-21-2005 E1 26.3 -- E3 -- 4.7 -- -- 31 --87 Mrg-0134 9-10-2004 -- -- -- 855 -- 213 -- -- -- --88 Mrg-0115 8-11-2004 -- -- -- 60 -- 239 -- -- -- --89 Mrg-0153 4-12-2005 -- -- -- E6 -- 11.1 -- -- -- --90 Mrg-0162 4-20-2005 <2 38 -- <6 -- 2.7 -- -- E3 --91 Mrg-0150 3-17-2005 -- -- -- 89 -- 220 -- -- -- --

1USGS station name designates the chronological order in which sampling sites were established in a given county; for example, Mrg-0090 is the 90th well site established in Morgan County, West Virginia.2 Sample concentration reported as “Total.” 

Appendixes  53
Appendix 3a. Water-quality data values for springs, Morgan County, West Virginia.

[USGS, U.S. Geological Survey. Units of measure: mg/L, milligrams per liter; μg/L, micrograms per liter, col/100 ml, colonies per 100 milliliters. Symbols: --, not determined; <, less than; E, estimated]

Site 

number

1USGS 

station 

name Date

Nitrate+ 

nitrite, 

dissolved 

(mg/L 

as N)

Nitrite, 

dissolved

(mg/L 

as N)

Orthophosphate, 

dissolved

(mg/L )

Orthophosphate, 

dissolved

(mg/L 

as P)

Phosphorus, 

dissolved

(mg/L)

E. coli, 

(col/

100 ml)

Coliform, 

fecal 

(col/100 

ml)

Coliform, 

total 

(col/100 

ml)

Iron, 

dissolved 

(μg/L)

Manganese, 

dissolved

(μg/L)

93 Mrg-0058 5/10/2005 <0.06 <0.008 -- <0.02 <0.04 <1 -- E3 2,010 212

94 Mrg-0012S 3/15/2005 .11 <.008 -- <.02 <.04 <1 <1 <1 <6 <.6

95 Mrg-0060S 5/9/2005 .31 <.008 -- <.02 <.04 E4 -- 67 <6 112

96 Mrg-0177S 5/10/2005 .39 <.008 -- <.02 <.04 <1 -- 21 <6 E.6

97 Mrg-0151S 3/16/2005 .21 <.008 -- <.02 <.04 -- <1 -- <6 <.6

97 Mrg-0151S 5/9/2005 -- -- -- -- -- <1 -- E9 -- --98 Mrg-0017S 3/16/2005 .4 <.008 -- <.02 <.04 -- E1 -- <6 <.6

98 Mrg-0017S 5/9/2005 -- -- -- -- -- E2 -- E11 -- --

99 Mrg-0075S 3/15/2005 .66 <.008 -- <.02 <.04 <1 <1 E8 E4 5.6

100 Mrg-0042 3/15/2005 .26 <.008 0.077 .03 E.04 <1 <1 <1 <6 <.6

1USGS station name designates the chronological order in which sampling sites were established in a given county; for example, Mrg-0012S is the 12th spring site established in Morgan County, West Virginia. 

54  Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia
Appendix 3b. Water-quality data values for springs, Morgan County, West Virginia.

[USGS, U.S. Geological Survey. Units of measure: mg/L, milligrams per liter. Symbols: --, not determined; <, less than; E, estimated] 

Site 

number

1USGS 

station 

name Date

Magnesium, 

dissolved 

(mg/L)

Potassium, 

dissolved 

(mg/L)

Sodium, 

dissolved

(mg/L)

Chloride, 

dissolved

(mg/L)

Fluoride, 

dissolved 

(mg/L)

Silica, 

dissolved 

(mg/L)

Sulfate,

dissolved 

(mg/L)

Solids,

residue at 

180 deg C 

dissolved 

(mg/L)

Ammonia, 

dissolved 

(mg/L 

as NH4)

Ammonia, 

dissolved 

(mg/L) 

as N)

93 Mrg-0058 5/10/2005 7.21 0.62 6.53 3.84 0.1 21.1 33.8 165 0.09 0.0794 Mrg-0012S 3/15/2005 7.15 .67 1.49 1.05 .1 9.3 5.8 189 -- <.0495 Mrg-0060S 5/9/2005 9.1 .65 8 1.02 E.1 5.4 11.4 89 -- <.0496 Mrg-0177S 5/10/2005 20.4 .67 3.06 .99 <.1 6.4 8.1 358 -- <.0497 Mrg-0151S 3/16/2005 9.3 .57 2.62 6.03 .1 7.8 3.5 197 -- <.0497 Mrg-0151S 5/9/2005 -- -- -- -- -- -- -- -- -- --98 Mrg-0017S 3/16/2005 6.71 .96 2.3 4.43 E.1 6.7 6.7 137 -- <.0498 Mrg-0017S 5/9/2005 -- -- -- -- -- -- -- -- -- --99 Mrg-0075S 3/15/2005 2.38 .9 .83 1.36 <.1 5.7 11.2 31 -- <.04

100 Mrg-0042 3/15/2005 4.67 .95 4.64 2.37 E.1 9.9 14.6 161 -- <.04

1USGS station same designates the chronological order in which sampling sites were established in a given county; for example, Mrg-0012S is the 12th spring site established in Morgan County, West Virginia. 

Appendixes  55
Appendix 3c. Water-quality data values for springs, Morgan County, West Virginia.

[USGS, U.S. Geological Survey. Units of measure: mg/L, milligrams per liter; Deg C, degrees Celsius; mv, millivolts; μS/cm, microsiemens per centimeter at 25oC ; NTU, nephelometric turbidity units. Symbols: --, not determined; <, less than; E, estimated]

Site 

number

1USGS

station 

name Date

Landsurface 

altitude 

(feet above 

mean sea 

level)

Redox 

potential 

(mv)

Turbidity 

(NTU)

Oxygen, 

dissolved 

(mg/L)

pH 

(units)

Specific 

conductance 

(μS/cm)

Temperature, 

(Deg C)

Water 

hardness 

(mg/L 

as CaCO3

)

Calcium, 

dissolved 

(mg/L)

93 Mrg-0058 5/10/2005 925 196 <1.0 7.8 6.9 258 9.9 130 40.894 Mrg-0012S 3/15/2005 900 140 <1.0 3.2 7.2 416 11.2 190 63

95 Mrg-0060S 5/9/2005 560 260 3.6 10.1 7.3 218 10 64 10.596 Mrg-0177S 5/10/2005 872 217 <1.0 4.3 6.7 814 10.8 390 12497 Mrg-0151S 3/16/2005 820 148 <1.0 3.1 7.6 441 11.8 200 62.997 Mrg-0151S 5/9/2005 820 221 1.1 2.9 7 450 11.9 -- --98 Mrg-0017S 3/16/2005 820 152 <1.0 6 7.4 323 9.9 130 39.798 Mrg-0017S 5/9/2005 820 232 <1.0 5.9 6.8 332 11 -- --99 Mrg-0075S 3/15/2005 1,000 184 <1.0 6 5.4 59 10.5 18 3.33

100 Mrg-0042 3/15/2005 620 125 <1.0 4.3 7.1 366 21.7 140 48.8

1USGS station name designates the chronological order in which sampling sites were established in a given county; for example, Mrg-0012S is the 12th spring site established in Morgan County, West Virginia. 

56  Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia

Carol J. Boughton and Kurt J. McCoy—Hydrogeology, Aquifer Geochemistry, and Ground-Water Quality in Morgan County, West Virginia—

Scientific Investigations Report 2006-5198

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