U.S. Department of the Interior

U.S. Geological Survey

Ground-Water Availability in Part of the

Borough of Carroll Valley, Adams County,

Pennsylvania, and the Establishment of a

Drought-Monitor Well

Water-Resources Investigations Report 02-4273

In cooperation with the

BOROUGH OF CARROLL VALLEY

Water-Resources Investigations Report 02-4273
U.S. Department of the Interior

U.S. Geological Survey

Ground-Water Availability

in Part of the Borough of Carroll Valley,

Adams County, Pennsylvania, and the

Establishment of a Drought-Monitor Well

by Dennis J. Low and Randall W. Conger

Water-Resources Investigations Report 02-4273

In cooperation with the

BOROUGH OF CARROLL VALLEY

New Cumberland, Pennsylvania

2002
ii

U.S. DEPARTMENT OF THE INTERIOR

GALE A. NORTON, Secretary

U.S. GEOLOGICAL SURVEY

Charles G. Groat, Director

For additional information Copies of this report may be

write to: purchased from:

District Chief U.S. Geological Survey

U.S. Geological Survey Branch of Information Services

215 Limekiln Road Box 25286

New Cumberland, Pennsylvania 17070-2424 Denver, Colorado 80225-0286

Email: dc_pa@usgs.gov Telephone: 1-888-ASK-USGS

Internet address: http://pa.water.usgs.gov
iii

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

Introduction . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 2

Purpose and scope . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 2

Acknowledgments . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 2

Previous work . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 5

Description of study area. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 5

Methods of investigation. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 7

Ground-water availability . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 8

Characteristics of a bedrock well . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 9

Casing length . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 11

Well depth . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 11

Water-producing zones . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 13

Discharge . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 18

Yield. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 18

Specific capacity . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 20

Ground-water flow and recharge. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 20

Water levels . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 24

Bedrock water-budget . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 31

Sources of possible anthropogenic recharge . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 32

Establishment of a drought-monitor well. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 36

Pennsylvania drought monitor network. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 36

Borough of Carroll Valley observation-well network and drought-monitor well . . . . . . . . . . . . . . . 37

Summary and conclusions . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 39

Selected references . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 40

Appendix A—Hydraulic conductivity and transmissivity . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 64

Appendix B—Borehole geophysical logs . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 66

Appendix C—Source and significance of selected indicators of ground-water quality . . . . . . . . . . . . . . . . 74

Appendix D—Results of analyses for wastewater compounds, endocrine-disrupting

potential, and possible compound uses . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 75

CONTENTS

Page
iv

Figures 1-2. Maps showing:

1. Location of study area, surrounding counties, physiographic provinces and

sections, selected population centers, major streams, and county

observation wells. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 3

2. Locations of inventoried wells and springs and bedrock geology, Borough

of Carroll Valley, Adams County, Pa. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 4

3. Diagram showing topographic, hydrologic, and geologic features, Borough of

Carroll Valley, Adams County, Pa. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 8

4. Sketch showing the cross-section of a bedrock well . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 10

5. Map showing depth to bedrock, Borough of Carroll Valley, Adams County, Pa. . . . . . . . 12

6-9. Graphs showing:

6. Number and density of water-producing zones per 50 feet of well depth in

the Loudoun Formation, Borough of Carroll Valley, Adams County, Pa.. . . . . . . . 14

7. Number and density of water-producing zones per 50 feet of well depth in

the metabasalt, Borough of Carroll Valley, Adams County, Pa. . . . . . . . . . . . . . . . . 15

8. Number and density of water-producing zones per 50 feet of well depth in

the metarhyolite, Borough of Carroll Valley, Adams County, Pa. . . . . . . . . . . . . . . 16

9. Number and density of water-producing zones per 50 feet of well depth in

the greenstone schist, Borough of Carroll Valley, Adams County, Pa. . . . . . . . . . . 17

10-11. Maps showing:

10. Spatial distribution of driller reported yields in gallons per minute,

Borough of Carroll Valley, Adams County, Pa. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 19

11. Spatial distribution of specific capacities in gallons per minute per foot of

drawdown, Borough of Carroll Valley, Adams County, Pa. . . . . . . . . . . . . . . . . . . . 21

12-13. Diagrams showing:

12. Annual hydrologic cycle for Pennsylvania . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 22

13. Classification of subsurface water. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 23

14. Hydrogeologic cross-section from Jack’s Mountain east to Pennsylvania Route

116,

Borough of Carroll Valley, Adams County, Pa. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 24

15. Graphs showing well-bore flow in wells AD-836 and AD-774 under

nonpumping and pumping conditions, Borough of Carroll Valley, Adams

County, Pa. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 25

ILLUSTRATIONS

Page
v

Figures 16-18. Graphs showing precipitation and water levels in wells:

16. AD-831, AD-832, and AD-846 . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 26

17. AD-837 and AD-839 . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 27

18. AD-788. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 27

19-20. Maps showing:

19. Potentiometric surface for November 14, 2000, Borough of Carroll Valley,

Adams County, Pa. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 29

20. Potentiometric surface for August 15, 2001, Borough of Carroll Valley,

Adams County, Pa. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 30

21-25. Graphs showing:

21. Binary mixing curves for chloride to bromide (Cl:Br) ratios, Borough of

Carroll Valley, Adams County, Pa. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 35

22. Normal monthly precipitation for South Mountain (1960-90) and monthly

precipitation for Borough of Carroll Valley, Adams County, Pa. (2001) . . . . . . . . . 36

23. Daily water levels in well AD-808, Borough of Carroll Valley, Adams

County, Pa. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 36

24. Relation between water levels in Borough of Carroll Valley, Adams County,

Pa.,

well AD-808 and Cumberland County, Pa., observation well CU-2 . . . . . . . . . . . . 38

25. Drought-warning levels for well AD-808, Borough of Carroll Valley, Adams

County, Pa. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 38

B1-B2. Graphs showing lithology and borehole geophysical logs and direction of

nonpumping flow within boreholes, Borough of Carroll Valley, Adams

County, Pa.:

B1. AD-774 collected on January 16, 2002, Section B . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 69

B2. AD-808 collected on January 29, 2002, Section P . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 71

B3. Graph showing lithology and borehole geophysical logs and direction of

nonpumping and pumping flow within borehole AD-836 collected on

January 10, 2002, Section WA, Borough of Carroll Valley, Adams County, Pa. . . . . . . . 73

ILLLUSTRATIONS—Continued

Page
vi

Table 1. Geohydrologic-stratigraphic column, Borough of Carroll Valley, Adams

County, Pa. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 6

2. Change, over time, in well depth, yield, and specific capacity, Borough of

Carroll Valley, Adams County, Pa. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 33

3. Results of analyses for nitrate, coliform, chloride, and bromide in ground water

of selected wells, Borough of Carroll Valley, Adams County, Pa. . . . . . . . . . . . . . . . . . . 33

4. Records of selected wells and springs, Borough of Carroll Valley, Adams

County, Pa. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 45

A1. Summary of driller drawdown tests (utilizing a storativity of 0.00001) in

determining transmissivity and hydraulic conductivity, Borough of Carroll

Valley, Adams County, Pa.. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 65

A2. Summary of U.S. Geological Survey slug tests and driller drawdown tests in

determining transmissivity of the metabasalt, Borough of Carroll Valley,

Adams County, Pa. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 65

B1. Wells logged at Borough of Carroll Valley, Adams County, Pa. . . . . . . . . . . . . . . . . . . . . . . 67

B2. Summary of heatpulse-flowmeter measurements within borehole AD-774

collected January 16, 2002, Section B, Borough of Carroll Valley, Adams

County, Pa. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 68

B3. Summary of heatpulse-flowmeter measurements within borehole AD-808

collected January 29, 2002, Section P, Borough of Carroll Valley, Adams

County, Pa. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 70

B4. Summary of heatpulse-flowmeter measurements within borehole AD-836

collected January 10, 2002, Section WA, Borough of Carroll Valley, Adams

County, Pa. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 72

D1. Wastewater compounds in selected wells, Borough of Carroll Valley, Adams

County, Pa. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 75

D2. Wastewater compound endocrine-disrupting potential and possible compound

uses . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 77

TABLES

Page
vii

Multiply By To obtain

Length

inch (in.) 25.4 millimeter

foot (ft) 0.3048 meter

Area

acre 4,047 square meter

square mile (mi2) 2.590 square kilometer

Flow rate

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

gallon per day (gal/d) 3.785 liter per day

gallon per day per acre [(gal/d)/acre] 0.0009353 liter per day per square

meter

Mass

ton, short 0.9072 megagram

Temperature

Temperature conversions for degrees Fahrenheit (°F) and degrees Celsius (°C) are given in the following

equations:

°C=5/9 (°F-32)

°F=1.8 °C+32

Transmissivity

square feet per day (ft2/d) 0.0929 square meters per day

Specific capacity

gallon per minute per foot 0.2070 liter per second per meter

[(gal/min)/ft)]

Hydraulic conductivity

foot per day (ft/d) 0.3048 meter per day

Volume

gallon per foot (gal/ft) 12.42 liter per meter

Other Abbreviations

Abbreviated water-quality units used in this report:

micrograms per liter (μg/L)

microsiemens per centimeter (μS/cm)

milligrams per liter (mg/L)

milliliters (mL)

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

North American Datum of 1927 (NAD 27). Vertical coordinate information is referenced to the National

Geodetic Vertical Datum of 1929 (NGVD 29).

CONVERSION FACTORS, DATUMS, AND ABBREVIATED WATER-QUALITY UNITS

1

GROUND-WATER AVAILABILITY IN PART OF THE BOROUGH OF

CARROLL VALLEY, ADAMS COUNTY, PENNSYLVANIA, AND THE

ESTABLISHMENT OF A DROUGHT-MONITOR WELL

by Dennis J. Low and Randall W. Conger

ABSTRACT

Continued population growth in the Borough of

Carroll Valley (Borough) coupled with the drought of

2001 have increased the demand for ground water in

the Borough. This demand has led Borough officials to

undertake an effort to evaluate the capability of the

crystalline-bedrock aquifers to meet future, projected

growth and to establish a drought-monitor well within

and for the use of the Borough. As part of this effort,

this report summarizes ground-water data available

from selected sections within the Borough and provides geohydrologic information needed to evaluate

ground-water availability and recharge sources within

part of the Borough.

The availability of ground water in the Borough

is limited by the physical characteristics of the underlying bedrock, and its upland topographic setting. The

crystalline rocks (metabasalt, metarhyolite, greenstone

schist) that underlie most of the study area are among

the lowest yielding aquifers in the Commonwealth.

More than 25 percent of the wells drilled in the metabasalt, the largest bedrock aquifer in the study area, have

driller reported yields less than 1.25 gallons per

minute. Driller reports indicate also that water-producing zones are shallow and few in number. In general,

50 percent of the water-producing zones reported by

drillers are penetrated at depths of 200 feet or less and

90 percent at depths of 370 feet or less. Borehole geophysical data indicate that most of the water-producing zones are at lithologic contacts, but such contacts

are penetrated infrequently and commonly do not

intersect areas of ground-water recharge. Single-well

aquifer tests and slug tests indicate that the bedrock

aquifers also do not readily transmit large amounts of

water. The median hydraulic conductivity and transmissivity of the bedrock aquifers are 0.01 foot per day

and 2.75 feet squared per day, respectively.

The crystalline and siliciclastic (Weverton and

Loudoun Formations) bedrock aquifers are moderately

to highly resistant to weathering, resulting in topographic highs coupled with steep, narrow valleys. This

rugged topography results in extensive surface runoff,

which limits infiltration and hence recharge to the shallow and deep ground-water systems. Streams that flow

through the study area generally are small and ephemeral. Where perennial, the streams represent areas of

ground-water discharge.

Thickness of the overlying mantle (regolith or

depth to bedrock) varies from 0 to more than 65 feet

over short distances. In general, a thick regolith will

store and transmit large quantities of water to the

underlying bedrock aquifers. In the study area, however, there is no correlation between thick regolith and

greater reported yields. Thus, it appears that the

hydraulic connection between water-bearing fractures

at depth and ground water stored in the regolith is

poor, which further limits ground-water availability.

Recharge to the bedrock aquifers from the

approximately 46 inches of annual precipitation averages about 13 inches per year, or 975 gallons per day

per acre. During drought years, however, this recharge

rate may average only 9 inches per year [675 gallons

per day per acre]. Decreased recharge to the bedrock

aquifers results in declining water levels and possibly

dry wells, as well as reduced flows to streams and

other surface-water bodies. Although the consumptive

use of ground water by homeowners is minor (about

14 percent), the pumping of a well will change the natural flow paths of ground water and reduce the

amount of water stored (at least temporarily) in the

bedrock aquifers.
2

Potentiometric-surface maps constructed for

November 2000 and August 2001 indicate that hydraulic gradients (and by inference ground-water flow

paths) do not exhibit large seasonal changes. In general, ground-water flow paths are dominated by Jack’s

Mountain, a topographic high. This area of high

hydraulic head drives ground water in a southeasterly

direction to the topographically lower study area. A

ridge that bisects the study area serves as a groundwater divide, directing water to Miney Branch and

Toms Creek that border the study area. Ground-water

levels tend to be nearer the land surface in valleys than

on hilltops or slopes.

Chemical and water-quality indicators, including chloride and nitrate (as N), and the presence of

coliform bacteria and wastewater compounds, suggest

that ground-water recharge can be affected by anthropogenic sources such as fertilizer, road salt, and sewage. Chloride concentrations ranged from 1.3 to

35.9 milligrams per liter. Concentrations of nitrate

greater than 2.0 milligrams per liter were found in

water from 12 of 35 wells sampled. Total coliform bacteria was found in water from 6 of 35 wells sampled

and fecal coliform bacteria in 2 of 35 wells sampled.

Chloride to bromide ratios in the water from 18 wells

ranged from 88 (dilute ground water) to 1,200 [ground

water probably effected by anthropogenic source(s)]. A

total of 6 of 67 wastewater compounds analyzed were

detected in the water from the six sampled wells. Concentrations of the wastewater compounds ranged from

less than 0.02 to 1.2 micrograms per liter. The most

common wastewater compounds (5 of 6 wells) were

DEET, Bisphenol A, triphenyl phosphate, and Phenol.

A drought-monitor well, AD-808, was established in the Borough. Well AD-808 was selected from

an original network of five other wells on the basis of

location, availability, and hydrologic factors. Continuous water-level data from well AD-808 exhibit typical

seasonal fluctuations (declining water levels in summer, increasing water levels in winter). The water level

in well AD-808 also responds rapidly to precipitation

events as well as changes in evapotranspiration. The

water level in well AD-808 is not influenced by nearby

pumping. Water-level duration curves for the purpose

of establishing well AD-808 as a drought-monitor well

in the Borough were constructed by utilizing the

47 years of record for Cumberland County observation

well CU-2.

INTRODUCTION

Continued population growth has increased the

demand for ground water in the Borough of Carroll

Valley (hereafter referred to as “Borough”) (fig. 1). In

1998, more than 20 wells in the Borough went dry, forcing home owners to either deepen existing wells, drill

new wells, or have water transported to their homes.

To address the capacity of ground water to meet the

increased demand, the U.S. Geological Survey (USGS)

and the Borough began a cooperative investigation of

ground water in sections B, E, H, I, IW, P, W, and WA in

2000 (fig. 2). The geohydrology, ground-water availability, ground-water flow, and the effect of drought

were evaluated through the use of databases maintained by the USGS, the Pennsylvania Department of

Conservation and Natural Resources Bureau of Topographic and Geologic Survey (PaGS), the Borough, and

water-well driller Randy Alexander; previous studies;

and field investigations. The desired outcomes of this

evaluation are (1) to provide Borough officials with a

better understanding of the geohydrology of the Borough and (2) to establish a drought-monitor well

within the Borough.

Purpose and Scope

This report provides geologic and hydrologic

information regarding the availability of ground water

in selected parts of the Borough and the effect of the

2001 drought on ground-water levels. This report

describes the geohydrologic (or ground-water) system

and the water-bearing and water-transmitting properties of the bedrock aquifers on the basis of data from

369 wells. Potentiometric-surface maps on the basis of

data from approximately 75 wells are presented. Possible anthropogenic sources of ground-water recharge

are evaluated through selected (nitrate, bacteria, chloride, bromide, and wastewater compounds) groundwater chemistry data. The report also summarizes relevant geologic literature through 2001 and the establishment of a drought-monitor well within the Borough.

Acknowledgments

The authors acknowledge the cooperation of citizens and personnel from the Borough, especially John

Washburn, Dick Deyo, and zoning officers Carl Bower

and Howard Rodriguez, for their assistance with field

work and with the planning and review of this report.

The authors acknowledge the cooperation of the well

owners for permitting access to their wells. The

authors thank water-well driller Randy Alexander for

use of his extensive database and his willingness to

answer questions regarding techniques of well con-
3

Figure 1. Location of study area, surrounding counties, physiographic provinces and sections, selected population centers,major streams, and county observation wells.
4

Figure 2. Locations of inventoried wells and springs and bedrock geology, Borough of Carroll Valley, Adams

County, Pennsylvania.
5

struction and drawdown tests. The authors also thank

the members of the report-preparation team (Kevin

Breen, Douglas Chichester, Denise Dumouchelle, Dennis Risser, Kim Otto); Scott Hoffman, Naomi Weisbeker, and James Bubb for their expertise and

assistance in the preparation of the map and figure

illustrations; and Terriann Preston and Kim Shank for

their support with page layout and word processing.

Previous Work

Stose (1906, 1907, 1909, 1932), Hall (1934), and

Jonas and Stose (1939) are some of the earliest authors

to work at or near South Mountain. These early workers emphasized the geology, structure, and mineral

resources on a county-wide scale. More recent authors

such as Fauth (1968, 1978), Freedman (1967), and Root

(1968, 1978) have studied South Mountain on a quadrangle-size scale. Work by Rankin and others (1969),

Rankin (1976), Simpson and Sundberg (1987), Key

(1991), and Root and Smith (1991) have re-examined

the tectonic history of South Mountain.

Meyer and Beall (1958) and Slaughter and Darling (1962) conducted studies on aquifer properties of

metarhyolites and metabasalts at South Mountain in

Maryland. The transmissivities and storage coefficients

derived for the metarhyolite and the metabasalt were

determined from single and multiple-well aquifer

tests. Trainer and Watkins (1975) working in the Upper

Potomac River Basin used streamflow discharges and

aquifer tests to determine the transmissivities and storage coefficients of fractured rock overlain by thin or

thick regolith. The work by Taylor and Royer (1981),

Low and Dugas (1999), and Low and others (2002),

which summarizes the ground water of Adams County

by formation and includes information on well yields

and water quality, are the most extensive studies of the

ground water at South Mountain currently available

for Pennsylvania.

Description of Study Area

The Borough was founded in 1974 and is in

south-central Pennsylvania, near the Maryland-Pennsylvania state line, occupying about 5.4 mi2 of Adams

County (fig. 1). The eastern half of the Borough lies

within the Gettysburg-Newark Lowland Section of the

Piedmont Physiographic Province and is underlain by

reddish-brown shale, siltstone, sandstone, and an erosion resistant diabase. The western half of the Borough,

which encompasses the study area (specifically sections B, E, H, I, IW, P, W, and WA), lies within the South

Mountain Section, the northernmost extension of the

Blue Ridge Physiographic Province (Fenneman, 1938).

The rocks that underlie the study area consist of sandstone and quartzite (Weverton Formation), phyllite

(Loudoun Formation), and volcanic extrusives (Catoctin Formation) (table 1; fig. 2). The topography is a

series of linear, sub-parallel, ridges and valleys with a

moderate to rugged expression, rising within the Borough from about 500 ft above NGVD 29 to a maximum

altitude of 1,020 ft. The Weverton Formation, metabasalt, and metarhyolite form steep but stable slopes and

ridges that are cut by deep, lateral valleys.

No through-going stream bisects the study area.

Small streams that originate in South Mountain and

border the study area include Miney Branch and Toms

Creek (fig. 2). The latter are small tributaries to the

Monocacy River, which lies within the Potomac River

Basin.

The climate of the Borough is humid continental;

precipitation is approximately 46 in. per year (Howard

Rodriguez, Borough of Carroll Valley, written commun., 2002). Summer and winter mean temperatures

are 25 and -1°C, respectively. Winds are predominantly

from the west (Pennsylvania Department of Environmental Resources, 1979). Weather systems that affect

the area generally originate in either Canada or central

United States and move eastward. Most precipitation

is derived from another flow pattern that originates in

the Gulf of Mexico.

Over the past decade (1990-2000), the Borough

was one of the fastest growing communities in the

Commonwealth, with a population growth of almost

126 percent or 1,457 to 3,291 (Adams County Office of

Planning and Development, written commun., 2001).

In the next 10 years, the population of the Borough is

expected to increase by 3 percent per year. A large segment of this growth is expected in the sections west of

Toms Creek, where domestic wells are common and

tap into the low yielding, crystalline-rock aquifers.

Land use in the Borough is dominated by single

family homes generally on 0.5 acre wooded or cleared

lots. Some agricultural land use, principally orchards,

remains as well as heavily wooded or brush covered

lots that are too steep to build on, have not received

septic permits, or have conservation easements.

Local population centers in the vicinity of the

study area include Carlisle, Chambersburg, Gettysburg, and York (fig. 1). However, it is the larger, proximal cities that have the greatest influence on the

Borough. Approximately 30 percent of the Borough’s

population commutes to Washington, D.C., Frederick,

Md., or the greater Washington area. Another 25 per-
6

Table 1. Geohydrologic-stratigraphic column, Borough of Carroll Valley, Adams County, Pennsylvania

[ft, feet; >, greater than; gal/min, gallons per minute; (gal/min)/ft, gallons per minute per foot of drawdown;

μS/cm, microsiemens per centimeter; pH, pH in standard units; ave., average; <, less than]

Age Geologic Formation Geologic description Well-construction

characteristics Water-yielding properties Quality of water

Cambrian

Weverton Formation Highly resistant;

sequence of gray to

pink, quartz-rich

rocks; major ridge

former; 800-1,000 ft

thick.

Well depths are 200

and 400 ft.

Yields are 3 gal/min.

Specific capacities are <0.01

and 0.02 (gal/min)/ft.

No field-water quality available. Water should be soft,

with low mineral content1.

Loudoun Formation Moderately resistant;

dark-gray, blue, to

purple phyllite (bottom) to quartz conglomerate (top); 100-

150 ft thick.

Well depths range

from 120-470;

ave. 274 ft.

Casing lengths range

from 21-90;

ave. 55 ft.

Yields range from 1-30; ave.

9.9 gal/min.

Specific capacities range from

<0.01-0.86;

ave. 0.26 (gal/min)/ft.

No field-water quality available. Water should be soft,

with low mineral content1.

Precambrian

Catoctin Formation

metabasalt Highly resistant; green

to gray, massive,

fine- to mediumgrained; contains

veins and masses of

epidote and quartz;

ridge former;

>1,000 ft thick.

Well depths range

from 80-780;

ave. 352 ft.

Casing lengths range

from 12-155;

ave. 42 ft.

Yields range from 0-150;

ave. 6.6 gal/min.

Specific capacities range from

<0.01-7.5,

ave. 0.14 (gal/min)/ft.

Specific conductance ranges

from 54-363;

ave. 218 μS/cm.

pH ranges from 5.1-6.3;

ave. 5.7.

Considerable range in mineral content and hardness;

objectionable quantities of

iron locally1.

metarhyolite Highly resistant; light

brown;

weathers orange,

gray, green; may

contain quartz

grains; ridge former;

300-400 ft thick.

Well depths range

from 100-600;

ave. 301 ft.

Casing lengths range

from 21-89;

ave. 49 ft.

Yields range from 0-40;

ave. 8.2 gal/min.

Specific capacities range from

<0.01-0.67;

ave. 0.08 (gal/min)/ft.

Specific conductance ranges

from 33-376;

ave. 163 μS/cm.

pH ranges from 6.8-7.2;

ave. 6.9.

Water should be soft, with

low mineral content1, 2.

greenstone schist Moderately hard; green

to gray phyllite or

schist; forms valleys

and slopes;

100-150 ft thick.

Well depths range

from 145-623;

ave. 363 ft.

Casing lengths range

from 20-80;

ave. 40 ft.

Yields range from 0.1-25;

ave. 5.1 gal/min.

Specific capacities range from

<0.01-0.40;

ave. 0.05 (gal/min)/ft.

Specific conductance

317 μS/cm, pH 5.5.

Water should be soft, with

low mineral content1,2.

1 Fauth (1978).

2 Low and others (2002).
7

cent are retirees who have moved to the Borough but

formerly worked in the greater Washington area (Carl

Bower, Borough of Carroll Valley, oral commun., 2002).

Methods of Investigation

Characterization of the bedrock aquifers is based

on data available from the USGS Ground-Water Site

Inventory (GWSI) and PaGS Water Well Inventory

(WWI) databases, the Borough, and driller Randy

Alexander. The 372 inventoried wells and springs

(fig. 2, table 4 (at the back of the report)) provided

information on (1) well depths, (2) casing lengths,

(3) regolith thickness, (4) depths to water-producing

zones, (5) well yields, (6) specific capacities, (7) hydraulic conductivities, and (8) transmissivities

(appendix A).

Wells were located in the field based on information and maps supplied by the Borough. Latitudes and

longitudes were obtained using either a Global Positioning System (GPS) that utilized the North American

Datum of 1983 (NAD 83) or by transferring the fieldlocated wells onto existing USGS 7.5-minute topographic quadrangle maps that conform to the North

American Datum of 1927 (NAD 27) or NAD 83.

The data presented in table 4 were supplemented

by 14 slug tests conducted by the USGS (appendix A)

and borehole geophysical logging. The slug tests consisted of rapidly dropping or removing a weighted

tube of known volume and recording the displacement

of water by means of an increase or decrease in water

level at 10-second intervals. Borehole geophysical logging consisted of running the caliper, temperature,

resistivity, natural gamma, and acoustic logs

(appendix B). Heatpulse-flowmeter surveys also were

conducted on the three wells logged (table B1). The caliper, temperature, resistivity, and acoustic logs were

used to identify fractures as well as potential waterproducing or water-thieving zones. The heatpulse

flowmeter was used to determine the direction of vertical flow in nonpumping and pumping wells and to

confirm the presence of water-producing or waterthieving zones. Natural-gamma logs were useful in

determining subsurface geology (figs. B1-B3).

Water levels were collected from 76 wells on

November 14, 2000, and 74 wells on August 15, 2001, to

aid in determining ground-water flow paths. Water

levels were measured by the use of electric tapes and

corrected to land surface by subtracting the height of

casing. For a number of lots, however, final grading of

the yard was not complete, which would affect future

land-surface corrections.

Water-quality samples were collected by the Borough in 1990 and 2001 for analysis of nitrate (as N) and

fecal and total coliform bacteria by the Pennsylvania

Department of Environmental Protection laboratory in

Harrisburg, Pa. In conjunction with the 2001 sampling,

the Borough also collected 54 additional water samples

for further water-quality analysis by the USGS. The

water samples collected for the USGS did not pass

through holding tanks, water softeners, or other types

of water holding or treatment. Specific conductance

and well records for the 54 samples were measured

and reviewed. Of the original 54 water samples, 35

were selected for analysis of chloride (Cl) at the USGS

National Water Quality Laboratory (NWQL), Denver,

Co. Based on the concentrations of nitrate and chloride,

and the presence or absence of coliform bacteria, 18

water samples then were analyzed by NWQL for bromide (Br). A Cl:Br ratio then was determined using

methods described by Jagucki and Darner (2001). On

the basis of the Cl:Br ratio and the presence or absence

of nitrate and coliform bacteria, six wells were revisited

and sampled. The waters from these six wells then

were analyzed for wastewater compounds as

described by Zaugg and others (2002).
8

GROUND-WATER AVAILABILITY

From a hydrologic viewpoint, the availability of

ground water in the Borough can be considered a

house divided. East of Toms Creek in the Triassic-age

rocks, ample supplies of ground water capable of meeting most domestic, commercial, and business needs are

available, with the exception of areas underlain by diabase (fig. 2). West of Toms Creek, ground-water supplies may not be sufficient to meet most domestic,

commercial, or business requirements, especially during drought.

The three major bedrock or crystalline-rock aquifers underlying the study area—metabasalt, metarhyolite, and greenstone schist—represent some of the

lowest yielding rocks in the Commonwealth (Low and

others, 2002). As a result of the low storage and transmissive properties characteristic of the crystalline-rock

aquifers, many of the drilled wells in the study area are

essentially a subsurface “stand pipe.” These “stand

pipes” usually contain sufficient amounts of stored

water to meet periods of peak domestic demand. When

the well is not used, the water level will rise as ground

water slowly infiltrates back into the well borehole,

refilling the “stand pipe.”

The water table represents a subdued reflection

of the land surface (fig. 3). The water table can be

depressed by excessive pumping or reach the surface

at springs and streams. Ground-water systems also can

be characterized as being either shallow or deep,

although most wells are open to both systems. The

paths and depths of the two flow systems vary but are

affected strongly by topography (ground water tends

to flow from areas of higher altitude such as ridge or

mountain tops to areas of lower altitude such as slopes

or valleys).

The shallow system supplies ground water to the

numerous small springs, streams, underlying regolith,

and shallow bedrock throughout the study area and

the Borough. The duration and intensity of precipitation has an almost immediate effect on the shallow system by raising static water levels and increasing

Figure 3. Topographic, hydrologic, and geologic features, Borough of Carroll Valley, Adams County, Pennsylvania.
9

ground-water discharge to springs and other surfacewater bodies. The shallow system is connected to the

deeper system through the regolith and bedrock by

way of secondary openings such as fractures, joints,

and cleavage planes.

The deeper system is characterized by longer,

more irregular flow paths and greater residence times.

Faults, such as the one that follows Jack’s Mountain

Road, may act as ground-water barriers, redirecting

ground-water flow and causing substantial differences

in water levels. The deeper system supplies the water

(base flow) that sustains such surface-water bodies as

Toms Creek, Miney Branch, and other streams between

precipitation events and during drought.

Ground-water availability is related to human

activities (casing length and well depth, onlot septic

systems, impermeable surfaces), geohydrologic properties of the underlying aquifers, proximity to recharge

boundaries, and precipitation. In the Borough, pumping a well and recycling this water back through the

onlot septic system change the natural ground-water

flow paths, but results in very little consumptive use.

Watering of vegetation, however, results in a much

larger consumptive use of ground water, mainly

through evapotranspiration (U.S. Geological Survey,

1999b). The increase of nonpermeable surfaces such as

houses, driveways, and streets increases surface runoff

while decreasing infiltration into the underlying aquifers.

The rugged topography and highly resistant

nature of the crystalline-rock aquifers result in large

amounts of surface runoff and reduced infiltration.

Ground-water recharge and availability are further

limited by the clays that form as a result of bedrock

weathering and the small number of secondary openings or water-bearing zones penetrated during the well

drilling process.

The major source of ground-water recharge is

precipitation. Over the past 9 years, the Borough has

received about 46 in. of precipitation per year. In 2001,

however, the Borough received about 31 in., a deficit of

15 in. or 33 percent. This significant reduction in precipitation has decreased the availability of ground

water throughout the Borough for domestic usage as

well as recharge to streams or base flow. The reduction

in precipitation also placed additional stresses on the

bedrock aquifers, resulting in a decrease in groundwater storage.

Characteristics of a Bedrock Well

Characteristics of a bedrock well (fig. 4) are most

strongly affected by rock type. Rock type affects the

amount of casing and well depth used in the construction of a well. Rock type also affects well yield. The

rocks underlying the study area are moderately to

highly resistant to weathering. This results in topographic highs such as ridges and mountain tops and

narrow, but steep valleys. In general, wells in valleys

require more casing but tend to have higher yields than

those on slopes and hilltops. Valleys and upland draws

form where the bedrock is most susceptible to physical

or chemical weathering, due largely to the existence of

fractures. This increased weathering results in a greater

depth to bedrock. Valleys and upland draws are also

low points through which upslope water (ground and

surface water) must pass through or drain and, therefore, have the capability for transmitting greater

amounts of water per unit volume of rock than topographically higher positions.

The depth and yield of a well is affected directly

by the size and distribution of water-producing zones

open to the well. In the study area, water-producing

zones can occur at the contact between different rock

types or other fractures. Faults, however, do not appear

to be particularly transmissive (permeable). Because of

the highly resistant, massive, and competent nature of

the bedrock, water-producing zones in the study area

do not appear to be abundant, productive, or interconnected. As a result, many wells are deep, subsurface

stand or storage pipes. Secondary development, such

as hydrofracturing, may increase the yield to the well

by enlarging (shattering) a water-producing zone or by

cleaning out clay, silt, and other debris that hinders

flow to the well.

Well-construction regulations also can be an

important factor that determines casing length, well

depth, and well yield (fig. 4). The Borough has established regulations that must be met in order to maintain minimum standards for quality of water and yield

(Howard Rodriguez, Borough of Carroll Valley, oral

commun., 2002). The Borough requires (1) the source of

supply shall be at a minimum of 100 ft distant from

potential sources of pollution (such as a septic tank or

leach field), (2) the use of watertight casing, (3) the

annular space must be filled completely with an

approved grouting material (such as concrete grout or

bentonite), and (4) a minimum reported yield of

4 gal/min. If the yield is less than 4 gal/min, the driller

must further evaluate the yielding and storage capability of the well by placing within the well a pump and

measuring the volume discharged plus the amount
10

BACK-FLOW PREVENTION

STATIC WATER TABLE (OR POTENTIOMETRIC SURFACE IF CONFINED)

BEDROCK

WATER-PRODUCING PUMP

DRIVE SHOE

CASING

BEDROCK

ZONE

GROUT

WELL CAP

PITLESS ADAPTOR

REGOLITH (SOIL AND WEATHERED BEDROCK)

LAND SURFACE

OPEN HOLE

FRACTURES

Figure 4. Cross-section of a bedrock well.

PUMPING WATER LEVEL (DRAWDOWN)
11

and rate of decline in the water level. If the well fails to

meet the Borough requirements, a second well must be

drilled, or the existing well can undergo secondary

development to increase the yield. If the second well

fails to meet the minimum discharge requirement of

the Borough or the combined yields of both wells fail

to meet the minimum requirement, the property is considered unsuitable for development and remains

empty.

Casing Length

Casing lengths generally are related to the resistance to weathering of the geologic formation, the

thickness of surficial deposits (regolith), regulatory

requirements, and driller preference. Casing length can

also serve as a surrogate for driller reported depth to

rock (Low, 1992). Casing (fig. 4) is installed through the

soil and weathered bedrock and must extend to a

depth of at least 20 ft, with an additional 10 ft of casing

extending into bedrock (Carl Bower, Borough of Carroll Valley, oral commun., 2002). Casing lengths for

wells in the study area are presented in the following

table. Casing lengths are slightly greater in the Loudoun Formation and metarhyolite than in the other rock

types. This also holds true if topographic expression,

such as slope, is considered. Casing length also may

affect well yield by sealing out not only surface water

infiltration but also shallow, productive water-producing zones.

Depth to bedrock or regolith thickness is highly

varied, ranging from 0 to 115 ft (median is 28 ft). In

many geologic terranes, thickness and composition of

the regolith play an important role in providing water

to a well. Regolith commonly absorbs and stores precipitation, then, over time, this stored water is slowly

released to the underlying bedrock aquifer(s) and

eventually to the well. A thick regolith, therefore, is

capable of storing and transmitting greater quantities

of water than a thin regolith. There does not, however,

appear to be any significant correlation between

regolith thickness and well yield. This may be the

result of Borough requirements for casing length, the

amount of clay produced when the crystalline rocks

weather, poor connection between secondary openings

in the bedrock and the overlying regolith, or other

unknown factors. Depth to bedrock does change rapidly over very short horizontal distances, but does not

appear to follow a recognizable pattern (fig. 5). As

shown in the table below, depth to bedrock does vary

by geologic formation. Depth to bedrock tends to be

less in areas underlain by the metabasalt and greenstone schist. Topographic lows, such as valleys and

upland draws, generally are assumed to be zones of

either structural or lithologic weakness. This weakness

would tend to favor a greater depth to bedrock because

more rock volume would be exposed to the effects of

precipitation, which enhances physical and chemical

weathering. Depth to bedrock does not appear to vary

greatly by topographic setting.

Well Depth

Well depth is related directly to the depth and

yield of water-producing zones (fig. 4). If an insufficient yield is obtained, the well driller will continue

deepening the well until sufficient water is encountered or the well has sufficient storage capacity to meet

most needs of the homeowner. Depths of wells in the

study area are presented in the following table. Wells

drilled in the metabasalt and greenstone schist generally are completed at greater depths than in the other

rock types. However, the thickness of the greenstone

schist and Loudoun Formation are only estimated as

Casing lengths by geologic formation

[Depth to bottom of casing, in feet below land surface; —,

insufficient data available; P10, tenth percentile; P25, twentyfifth percentile; P75, seventy-fifth percentile; P90, ninetieth

percentile]

Geologic

formation

Numberof wellsP10P25MedianP75P90MinimumMaximum

Weverton

Formation

2 — — 86 — — 52 120

Loudoun

Formation

9 — 25 63 74 — 21 90

metabasalt 263 21 27 40 53 63 12 155

metarhyolite 29 27 40 47 60 77 21 89

greenstone

schist

47 21 28 40 42 64 20 80

Depth to bedrock by geologic formation

[Depth to bedrock, in feet; —, insufficient data available; P10,

tenth percentile; P25, twenty-fifth percentile; P75, seventyfifth percentile; P90, ninetieth percentile]

Geologic

formation

Numberof wellsP10P25MedianP75P90MinimumMaximum

Weverton

Formation

2 — — 83 — — 40 115

Loudoun

Formation

9 — 10 48 63 — 4 108

metabasalt 251 6 10 28 40 55 0 110

metarhyolite 29 10 30 35 50 66 8 77

greenstone

schist

43 10 16 25 31 57 5 65
12

Figure 5. Depth to bedrock, Borough of Carroll Valley, Adams County, Pennsylvania.
13

100 to 150 ft (table 1). This indicates that most wells

started in the greenstone schist or Loudoun Formation

probably are completed in the underlying bedrock

unit, which is predominantly metabasalt.

Topographic setting also can affect well depth.

The depths of wells drilled in the metabasalt are

greater if the well is on a hilltop (87 wells) than on a

slope (153 wells) or an upland draw (158 wells); the

median depths are 395, 300, and 302 ft, respectively.

Water-Producing Zones

Ground water in the bedrock aquifers is stored in

and moves through a network of secondary openings

commonly called water-bearing or water-producing

zones. These secondary openings include joints, faults,

cleavage planes, and fractures. Although fractured

bedrock may have a low porosity, the permeability of

secondary openings can be quite high. The water-producing zones presented in table 4 and figures 6

through 9 are from driller completion reports. Depths

of water-producing zones are sometimes best guesses

because some zones may be plugged with mud, silt,

and debris as a result of drilling. The mud, silt, and

debris can be removed by further drilling, by the later

introduction of water in the borehole, by secondary

enhancement, or continued use by the well owner. In

addition, water-producing zones that yield small

amounts of water may not be noticed by the driller if a

shallower zone produced a considerably greater volume of water.

The distribution of 533 water-producing zones in

327 wells up to 780-ft deep were analyzed using the

following criteria:

Footage Sampled

If there is a reported water-producing zone behind

casing, the analysis omits from consideration footage above the reported water level.

If the first reported water-producing zone is at or

below the casing, then (a) if the water level is

below the casing, footage above the water level is

omitted, (b) if the water level is within the cased

depth, footage within the casing is omitted.

To achieve this, the excluded depth is set to the

water level, and changed to the casing depth only

if the first water-producing zone reported is below

and the water level is above the casing.

Water-Producing Zones Counted

All water-producing zones reported are counted in

the interval that they occur in, whether or not considered in footage sampled. For example, if casing

is exactly 50 ft, and the water-producing zone is

exactly 50 ft, one water-producing zone is counted

in the interval 0 to 50 ft, but the footage sampled is

zero.

Missing Data

If well depth is missing, it is set to the value of the

last reported water-producing zone.

If water level and casing depth are both missing,

both are set to 50.0001 ft.

If water level or casing depth is missing, the missing one is set to the given one.

Density of Water-Producing Zones

The density of the water-producing zones was

determined as follows:

N x 50-ft / F (1)

where N is equal to the number of driller reported

water-producing zones per 50-ft of hole depth, and

F is equal to footage of hole sample.

For example, if N equals 1 and footage of hole sample equals 223, the density of the water-producing

zone per 50-ft of hole depth is 0.22.

The number and density of water-producing zones

in four of the five bedrock aquifers underlying the

study area are shown in figures 6 through 9. The

Weverton Formation was excluded from the figures because only two water-producing zones

were encountered in two wells. The depths of

water-producing zones in the two wells drilled in

the Weverton Formation are 120 and 135 ft below

land surface.

Driller reported depths of drilled wells by geologic formation

[Depth, in feet below land surface; —, insufficient data

available; P10, tenth percentile; P25, twenty-fifth percentile;

P75, seventy-fifth percentile; P90, ninetieth percentile]

Geologic

formation

Numberof wellsP10P25MedianP75P90MinimumMaximum

Weverton

Formation

2 — — 300 — — 200 400

Loudoun

Formation

9 — 160 275 400 — 120 470

metabasalt 268 180 240 320 460 560 80 780

metarhyolite 30 150 210 300 340 500 100 600

greenstone

schist

48 207 280 320 405 600 145 623
14

The depths of water-producing zones in nine

wells drilled as deep as 470 ft in the Loudoun Formation range from 70 to 400 ft below land surface (fig. 6).

Fifty percent of the 15 water-producing zones reported

are penetrated at depths of 140 ft or less and 90 percent

at depths of 373 ft or less. The greatest density of

water-producing zones (0.75 per 50 ft of well depth) is

from 51-100 ft below land surface. The density of

water-producing zones from 151 ft or greater are based

on the presence of two or fewer water-producing zones

per 50-ft interval. The overall density of water-producing zones in the Loudoun Formation is 0.41 per 50 ft of

well depth.

Figure 6. Number and density of water-producing zones per 50 feet of well depth in the Loudoun Formation,

Borough of Carroll Valley, Adams County, Pennsylvania.

DEPTH INTERVAL, IN FEET BELOW LAND SURFACE

NUMBER OF WATER-PRODUCING ZONES REPORTED

MEAN DENSITY OF WATER-PRODUCING ZONES

NUMBER OF WATER-PRODUCING ZONES

MEAN DENSITY

5

0

1

2

3

4

1.0

0

0.1

0.2

0.3

0.4

0.5

0.6

0.7

0.8

0.9

(PER 50 FEET OF WELL DEPTH)

0-50 51-100 101-150 151-200 201-250 251-300 301-350 351-400 401-450
15

The depths of water-producing zones in

245 wells drilled as deep as 780 ft in the metabasalt

range from 40 to 640 ft below land surface. Fifty percent of the 410 water-producing zones reported are

penetrated at depths of 200 ft or less and 90 percent at

depths of 371 ft or less (fig. 7). The greatest density of

water-producing zones (0.36 per 50 ft of well depth) is

from 101-150 ft below land surface. The density of

water-producing zones from 501 ft or greater are based

on the presence of four or fewer water-producing

zones per 50-ft interval. The overall density of waterproducing zones in the metabasalt is 0.29 per 50 ft of

well depth.

Figure 7. Number and density of water-producing zones per 50 feet of well depth in the metabasalt, Borough

of Carroll Valley, Adams County, Pennsylvania.

NUMBER OF WATER-PRODUCING ZONES

MEAN DENSITY

DEPTH INTERVAL, IN FEET BELOW LAND SURFACE

NUMBER OF WATER-PRODUCING ZONES REPORTED

MEAN DENSITY OF WATER-PRODUCING ZONES

0

100

20

40

60

0

0.5

0.1

0.2

0.3

0.4

(PER 50 FEET OF WELL DEPTH)

80

0-50 51-100 101-150 201-250 251-300 301-350 351-400 401-450 451-500 501-550 551-600 601-650 151-200
16

The depths of water-producing zones in 27 wells

drilled as deep as 500 ft in the metarhyolite range from

60 to 370 ft below land surface. Fifty percent of the

44 water-producing zones reported are penetrated at

depths of 159 ft or less and 90 percent at depths of

300 ft or less (fig. 8). The greatest density of water-producing zones (0.73 per 50 ft of well depth) is from

51-100 ft below land surface. The density of water-producing zones from 301 ft or greater are based on the

presence of three or fewer water-producing zones per

50-ft interval. The overall density of water-producing

zones in the metarhyolite is 0.38 per 50 ft of well depth.

The depths of water-producing zones in 44 wells

drilled as deep as 623 ft in the greenstone schist range

from 60 to 520 ft below land surface. Fifty percent of

the 62 water-producing zones reported are penetrated

at depths of 240 ft or less and 90 percent at depths of

415 ft or less (fig. 9). The greatest density of water-producing zones (0.43 per 50 ft of well depth) is from

251-300 ft below land surface. The density of waterproducing zones from 301 ft or greater are based on the

presence of four or fewer water-producing zones per

50-ft interval. The overall density of water-producing

zones in the greenstone schist is 0.25 per 50 ft of well

depth.

Figure 8. Number and density of water-producing zones per 50 feet of well depth in the metarhyolite,

Borough of Carroll Valley, Adams County, Pennsylvania.

DEPTH INTERVAL, IN FEET BELOW LAND SURFACE

NUMBER OF WATER-PRODUCING ZONES REPORTED

MEAN DENSITY OF WATER-PRODUCING ZONES

NUMBER OF WATER-PRODUCING ZONES

MEAN DENSITY

0-50 51-100 101-150 201-250 251-300 301-350 351-400 151-200

15

0

3

6

9

12

1.0

0

0.2

0.4

0.6

0.8

1.0

(PER 50 FEET OF WELL DEPTH)
17

In many cases, it is difficult to determine if

water-producing zones are connected to adjacent

wells; however, there are some indications of such connections. During the drilling of a well in Section W, two

adjacent homeowners with established wells reported

a considerable decrease in the level of water in their

wells. A third established well, about 200 ft west of the

Section W well, exhibited a dramatic increase in the

amount of mud, silt, and other particulates in the

water. This increase of mud, silt, and other particulates

is believed to be the result of developing the Section W

well (Carl Bower, Borough of Carroll Valley, oral commun., 2002). For another example of fracture interconnection between wells, well AD-1152 was being

monitored during the drilling of a new well approximately 150 ft to the northeast in Section B. During

pumping and hydrofracturing of the new well in Section B, the water level in well AD-1152 decreased

approximately 5 ft and had not recovered after 4 days

of rest.

Figure 9. Number and density of water-producing zones per 50 feet of well depth in the greenstone schist,

Borough of Carroll Valley, Adams County, Pennsylvania.

DEPTH INTERVAL, IN FEET BELOW LAND SURFACE

NUMBER OF WATER-PRODUCING ZONES REPORTED

MEAN DENSITY OF WATER-PRODUCING ZONES

NUMBER OF WATER-PRODUCING ZONES

MEAN DENSITY

0-50 51-100 101-150 151-200 201-250 251-300 301-350 351-400 401-450 451-500 501-550

15

0

3

6

9

12

0

0.1

0.2

0.3

0.4

(PER 50 FEET OF WELL DEPTH)

0.5
18

Discharge

The discharge (yield and specific capacity)

reported or measured by a driller is affected by well

construction (casing length, borehole diameter, well

depth), pumping rate, and physical characteristics of

the aquifer (thickness and type of regolith, size, number, and inter-connectedness of water-producing

zones). A large amount of casing may reduce the discharge of a well by sealing off shallow, productive

water-producing zones. The discharge of a well will

increase if the diameter of the borehole increases (more

surface area exposed to water-producing zones). Deep

wells have greater storage capacity than shallow wells

and can be pumped harder (greater reported yield)

than shallow wells, although this will result in a lower

specific capacity. A thick, highly permeable regolith

can increase the discharge of a well by acting as a water

reservoir and providing this water to a well through a

network of secondary openings (water-producing

zones).

The majority of yields and specific capacities

(table 4) analyzed are from short-term driller completion tests during which the driller blew water (using

air pressure to force water up and out of the borehole)

from the well. Although this method is not as accurate

as those conducted using submersible pumps and

metering the discharge, it provides a reasonable basis

for estimating and comparing the discharge and

hydrologic properties [hydraulic conductivity and

transmissivity (appendix A)] of individual geologic

formations.

Yield

Yield is the volume of water per unit of time

removed from a well and usually is determined by

blowing the well or by pumping a well. Yield is commonly an estimated, not a measured, value and is

reported in gallons per minute. Yield typically varies

by rock type and topographic setting. As shown in the

following table, the Loudoun Formation is the best

yielding bedrock aquifer; the median reported yield is

5.0 gal/min. The metabasalt is typically the lowest

yielding bedrock aquifer; the median reported yield is

3.0 gal/min. It is also interesting to note that more than

25 percent of the wells drilled in the metabasalt have

yields less than 1.25 gal/min, the Borough’s current

(2002) minimum required yield.

Topographic setting also can affect yield. As

shown in the following table, wells drilled in the

metabasalt and in upland draws generally have greater

yields than wells drilled on slopes or hilltops. For the

greenstone schist, however, yields tend to be lower in

upland draws.

The location of relatively higher yielding wells

does not appear to follow a recognizable pattern

(fig. 10). Wells that yield more than 5 gal/min are dispersed randomly among wells with considerably

lower yields.

Well-development techniques can increase yields

beyond those obtained through typical well development (Driscoll, 1986, p. 528-533). Some methods that

can be employed include acid or explosives (Driscoll,

1978), but there are many legal and safety concerns

involved with these two methods. Hydrofracturing,

which involves injecting fluids at high pressure into

newly opened fractures, may need a propping agent

such as sand to keep fractures open over time. This

Driller reported yields of drilled wells by geologic formation

[Yield, in gallons per minute; —, insufficient data available;

P10, tenth percentile; P25, twenty-fifth percentile; P75,

seventy-fifth percentile; P90, ninetieth percentile]

Geologic

formation

Numberof wellsP10P25MedianP75P90MinimumMaximum

Weverton

Formation

2 — — 3.0 — — 3.0 3.0

Loudoun

Formation

9 — 3.0 5.0 18 — 1.0 30

metabasalt 262 0.6 1.0 3.0 7.0 14.6 .0 150

metarhyolite 29 .9 1.6 4.5 14.3 20 .0 40

greenstone

schist

49 .8 1.5 3.0 6.0 15 .1 25

Driller reported yields by topographic setting for wells drilled

in the metabasalt and greenstone schist

[Yield, in gallons per minute; —, insufficient data available;

P10, tenth percentile; P25, twenty-fifth percentile; P75,

seventy-fifth percentile; P90, ninetieth percentile]

Topographic

setting

Numberof wellsP10P25MedianP75P90MinimumMaximum

metabasalt

Hilltop 85 1.0 1.5 3.0 7.0 15 0.0 20

Slope 150 .5 1.0 2.0 6.0 10 .0 150

Upland draw 26 .8 2.5 6.0 14.5 20 .0 50

Valley 3 — — 1.0 — — 1.0 8.0

greenstone schist

Hilltop 7 — 1.5 1.8 2.8 — 1.0 20

Slope 36 .5 1.5 3.2 6.0 11.5 .1 25

Upland draw 6 — — 3.0 — — 1.0 15
19

77°23'53" 77°22'53"

39°44'09"

39°45'09"

0 0.5 1 MILE

0 0.5 1 KILOMETER

Pennsylvania Route 16

Pennsylvania Route 116

Jack's Mountain Road

EXPLANATION

YIELD (GALLONS PER MINUTE)

CARROLL VALLEY SECTION BOUNDARY

ROADS

0.00 - 1.25

1.26 - 6.00

6.01 - 150

Figure 10. Spatial distribution of driller reported yields in gallons per minute, Borough of Carroll Valley,

Adams County, Pennsylvania.
20

method, however, has been used successfully in the

Borough (Randy Alexander, Alexander Well Drilling,

oral commun., 2001).

Specific Capacity

Specific capacity is a better measure of the productivity of a geologic formation than yield. Specific

capacity is calculated by dividing the yield by the

drawdown or the pumping water level (fig. 4). Specific

capacity for a well pumped at a constant yield generally decreases with time. Also, specific capacity generally decreases as the discharge increases in the same

well.

Specific capacities in the bedrock aquifers of the

study area are low. The specific capacities presented in

the following table indicate that borehole storage plays

an important part in the yield of most wells. Wells that

have specific capacities that are 0.04 (gal/min)/ft or

less obtain most of the yield from borehole storage and

hence are considered incapable of meeting most homeowner or other water-use demands (Low and others,

2002). One way around this restriction, however, is to

increase the depth of the well and to locate the pump

near the bottom of the borehole. This technique generally provides the well owner with sufficient storage

capacity to meet most of their domestic requirements.

(A 6-in. diameter borehole will contain 1.47 gal/ft.) As

shown below, more than half of the wells drilled into

the metabasalt, metarhyolite, and greenstone schist

have specific capacities that are less than

0.04 (gal/min)/ft.

Topographic setting also can affect specific

capacity. As shown in the following table, wells drilled

in the metabasalt and in upland draws generally have

greater specific capacities than wells drilled on slopes

or hilltops. For the greenstone schist, however, specific

capacities tend to be greater on hilltops. The median

specific capacity for wells drilled in the greenstone

schist and on hilltops (6 wells), slopes (30 wells), and

upland draws (5 wells) are 0.07, 0.01, and

0.01 (gal/min)/ft, respectively.

The location of wells with relatively greater specific capacities does not appear to follow a recognizable

pattern (fig. 11). In general, wells with greater reported

yields have greater specific capacities.

Because of the close relation between yield and

specific capacity, aquifer-development techniques that

enhance well yield also will increase specific capacity.

Secondary development may be a better or cheaper

alternative to drilling a new well.

Ground-Water Flow and Recharge

Precipitation is the primary source of groundwater recharge. Much of the precipitation, however,

returns to the atmosphere through evapotranspiration

or reaches streams as surface runoff or base flow

(fig. 12). Evapotranspiration is greatest in late spring,

summer, and early fall when plants are actively growing. Surface runoff, however, is greatest in late winter

or early spring when the ground is frozen and lowest

in late summer and early fall. The remaining precipitation infiltrates into the regolith and the underlying

bedrock, flowing from areas of high relief such as

Jack’s Mountain (high hydraulic head) to areas of low

relief such as valleys (low hydraulic head), through

joints, cleavage planes, faults, fractures, and other secondary openings. Onlot septic systems also may contribute to ground-water flow and recharge because

consumptive use of ground water by homeowners is

about 14 percent (U.S. Geological Survey, 1999b).

Specific capacities of drilled wells by geologic formation

[Specific capacity, in gallons per minute per foot of drawdown;

—, insufficient data available; P10, tenth percentile; P25,

twenty-fifth percentile; P75, seventy-fifth percentile; P90,

ninetieth percentile; <, less than]

Geologic

formation

Numberof wellsP10P25MedianP75P90MinimumMaximum

Weverton

Formation

2 — — 0.01 — — <0.01 0.02

Loudoun

Formation

7 — 0.04 .05 0.43 — <.01 .86

metabasalt 207 <0.01 <.01 .01 .06 0.25 <.01 7.5

metarhyolite 22 <.01 <.01 .02 .04 .25 <.01 .67

greenstone

schist

41 <.01 <.01 .01 .05 .12 <.01 .40

Specific capacities by topographic setting for wells drilled in

the metabasalt

[Specific capacity, in gallons per minute per foot of drawdown;

—, insufficient data available; P10, tenth percentile; P25,

twenty-fifth percentile; P75, seventy-fifth percentile; P90,

ninetieth percentile; <, less than]

Topographic

setting

Numberof wellsP10P25MedianP75P90MinimumMaximum

Hilltop 66 <0.01 <0.01 0.02 0.06 0.30 <0.01 0.27

Slope 120 <.01 <.01 .01 .04 .14 <.01 7.5

Upland draw 19 <.01 <.01 .04 .28 .60 <.01 .63

Valley 2 — — .04 — — <.01 .07
21

77°23'53" 77°22'53"

39°44'09"

39°45'09"

0 1 KILOMETER

0 1 0.5 MILE

0.5

Jack's Mountain Road

Pennsylvania Route 16

Pennsylvania Route 116

EXPLANATION

SPECIFIC CAPACITY (GALLONS PER MINUTE)

PER FOOT OF DRAWDOWN

CARROLL VALLEY SECTION BOUNDARY

ROADS

< 0 - 0.04

0.05 - 0.25

0.26 - 1.20

Figure 11. Spatial distribution of specific capacities in gallons per minute per foot of drawdown, Borough of

Carroll Valley, Adams County, Pennsylvania.
22

Ground-water flow generally results in a water

table that is a subdued replica of the land surface

(fig. 3). Water levels are influenced strongly by the

amount and duration of precipitation and topographic

setting. Where the water table intercepts the land surface, springs can occur. In the Borough, springs are

present in Section W where they parallel a north-south

trending fault (fig. 2). Two wells in Section H apparently intercept fractures with high hydraulic head

because they flow either year round (AD-793) or in the

spring (AD-898).

The ground-water system can be considered to

consist of two zones—unsaturated and saturated

(Davis and DeWiest, 1966). The unsaturated zone is

comprised of soil water, intermediate vadose water,

and capillary water (fig. 13). Soil water is most important to agriculture because it provides the water for

plant growth. Water is lost from this zone by evapotranspiration and percolation when oversaturation

occurs. The vadose water and capillary water generally

are found in the regolith and can not be used for

human consumption but play an important part as a

source of recharge to the underlying saturated zone

and bedrock aquifers. In the Borough, the unsaturated

zone is best represented by regolith that is composed of

granular to clayey soil, saprolite, disaggregated bedrock, and colluvium. Regolith can act as a storage

medium for water or it can transmit water vertically

and horizontally to the underlying bedrock (Driscoll,

1986, p. 59). Thick regolith facilitates infiltration of precipitation and storage and release of water to wells

completed in the underlying fractured bedrock.

Regolith also can play an important part in maintaining base flow to streams.

The saturated zone contains the shallow groundwater system and the deep ground-water system

(fig. 3). The top of the saturated zone is the water table.

In the saturated zone, water completely fills the voids

or secondary openings. (The saturated zone also may

move upward into the regolith, especially during

PRECIPITATION

EVAPOTRANSPIRATION

INFILTRATION

SURFACE RUNOFF

BASE FLOW

(42 inches/year)

(22 inches/year)

(7 inches/year)

(13 inches/year)

(13 inches/year)

TOTAL STREAMFLOW

(20 inches/year)

Figure 12. Annual hydrologic cycle for Pennsylvania (modified from Fleeger, 1999, p. 7).
23

extended wet periods.) The water pressure in the saturated zone is high enough to allow ground water to

enter a well as the water level in the well is lowered by

pumping. The saturated zone gradually grades into

areas or regions where ground-water flow is slow and

is essentially not available for use (figs. 13 and 14).

Water in these secondary openings may not flow

toward a well because individual pores are not connected.

The USGS logged three wells, AD-774, AD-808,

and AD-836, with a heatpulse flowmeter to evaluate

ground-water flow patterns and to determine the

depth of the deep ground-water system (appendix B).

Ideally, wells on hilltops will show downward flow

(ground-water recharge), wells on slopes will show

either downward or upward flow, and wells in valleys

will show upward flow (ground-water discharge). Well

AD-774, which is on a slope, shows upward and lateral

flow under nonpumping conditions (table B2). Well

AD-808, which is on a hilltop, shows only lateral flow

under nonpumping conditions (table B3). Well AD-836,

which is also on a hilltop, exhibited no vertical borehole flow under nonpumping conditions (table B4).

The three borehole geophysical logs suggest that

(1) very little hydraulic head difference exists between

water-producing zones, (2) the water-producing zones

are not well connected, or (3) both conditions may

occur.

The borehole geophysical logs of wells AD-774

(fig. B1; fig. 15), AD-808 (fig. B2), and AD-836 (fig. B3;

fig. 15) indicate also that, under nonpumping conditions, most water-producing zones are shallow. The

deepest water-producing zone under nonpumping

conditions was in well AD-774 at a depth of 254 ft bls.

Well AD-836 was the only well of the three to be

pumped. Under nonpumping conditions, no vertical

borehole flow was identified. Under pumping conditions, vertical borehole flow was measured to a depth

of 190 ft with possible vertical borehole flow as deep as

470 ft bls. The deepest reported water-producing zone

in the study area is in well AD-807 at a depth of

640 ft bls. The U.S. Government drilled a well (AD-347)

in the Catoctin Formation about a mile west of the Borough to a depth of over 9,000 ft. Water in this well

flows upward from a depth of at least 600 ft bls. When

this information is combined with the depth of driller

reported water-producing zones from figures 6 to 9, it

suggests the saturated zone exceeds a thickness of

700 ft, but a more practical limit may be a thickness of

400 to 500 ft bls. Additional information regarding

borehole geophysical logging is presented in

appendix B.

Soil water

Unsaturated

zone

Saturated zone

Water in unconnected

pores or fractures

Subsurface

water

Water table

Land surface

NOT TO SCALE

Figure 13. Classification of subsurface water (modified

from Driscoll, 1986, p. 60).

BEDROCK REGOLITH
24

Water Levels

Water levels fluctuate in response to recharge

from precipitation, pumping of wells, seasons, and

evapotranspiration. Water levels in wells completed in

the fractured bedrock quickly respond to precipitation

events (figs. 16-18). This response is primarily the

result of the interconnection and low-storage capacity

between shallow, high-angle fractures and the overlying, more permeable regolith. Other factors that can

induce rapid changes in water levels include (1) air

entrapment during recharge, (2) nearby pumping, and

(3) atmospheric pressure effects (Freeze and Cherry,

1979, table 6.2).

Water levels typically vary by season and generally rise during the late fall, winter, and early spring

when evapotranspiration is at a minimum and

recharge is at a maximum. Rising water levels, typical

of winter months, can be seen in the records for wells

AD-831, AD-832, and AD-846, which cover a period

from January 17, 2001, to February 10, 2001 (fig. 16). As

seen in the continuous water levels for wells AD-837

and AD-839, which cover a period from February 9,

2001, to March 15, 2001, water levels also may remain

fairly steady (AD-839) or even decline (AD-837). However, recharge events of 0.5 in. or greater can result in a

considerable rise in water levels (figs. 16 and 17).

Snowmelt also can recharge the underlying rocks. The

Borough received 4 in. of snow on January 6 and 2.5 in.

of snow on January 7, 2001. Daily high temperatures

for the period of January 6 to January 17 ranged from a

low of 29°F on January 10 to 56°F on January 13. The

recharge event related to this snowmelt begins to

appear in wells AD-831, AD-832, and AD-846 on January 19 (fig. 16).

Figure 14. Hydrogeologic cross-section from Jack’s Mountain east to Pennsylvania Route 116, Borough of

Carroll Valley, Adams County, Pennsylvania.
25

The typical summer decline in water levels is

evident in the continuous water level for well AD-788,

which covers a period from May 31, 2001, to August

15, 2001 (fig. 18). Also shown in this well, recharge

events tend to flatten, but not reverse, the overall

downward trend of the water level.

Wells AD-831 and AD-832 also show the effects

of pumping from neighboring wells. The water levels

in well AD-831 exhibit many peaks and troughs that

correspond to different periods of demand from one or

more neighboring wells during a 24-hour period of

time. The water level in well AD-832 exhibits only

slight and brief declines that occur about 4 days apart.

This suggests that well AD-832 is affected by at least

one well that is not in the immediate vicinity.

WELL AD-836

DEPTH, IN FEET BELOW LAND SURFACE

WELL AD-774

89

NP P

NF

NF

NF

NF

NF

NF

NF

NF

NF

NF

NF

109.40

550

0

50

100

150

200

250

300

350

400

450

500

EXPLANATION

STATIC WATER LEVEL—

Measured in well at the time of geophysical logging.

NO FLOW

PUMPING

NONPUMPING

DIRECTION OF BOREHOLE FLOW UNDER NONPUMPING OR PUMPING

CONDITIONS

NP

WATER-PRODUCING ZONE UNDER NONPUMPING OR PUMPING CONDITIONS

WATER-THEIVING ZONE UNDER NONPUMPING CONDITIONS

LATERAL FLOW

NF

NF

NF

NF

NF

NF

NP

72

REGOLITH

BEDROCK

CASING

LAND SURFACE

FRACTURES

FRACTURES

89

Figure 15. Well-bore flow in wells AD-836 and AD-774 under nonpumping and pumping conditions,

Borough of Carroll Valley, Adams County, Pennsylvania.

P
26

Figure 16. Precipitation and water levels in wells AD-831, AD-832, and AD-846. (Precipitation

data collected from sewer plant, Borough of Carroll Valley, Adams County, Pennsylvania.)
27

Figure 17. Precipitation and water levels in wells AD-837 and AD-839. (Precipitation data

collected from sewer plant, Borough of Carroll Valley, Adams County, Pennsylvania.)

Figure 18. Precipitation and water levels in well AD-788. (Precipitation data collected

from sewer plant, Borough of Carroll Valley, Adams County, Pennsylvania.)
28

The continuous water levels recorded in wells

AD-837 and AD-839 may also show the influence of

earth tides, which indicates confined ground water

(fig. 17). According to Todd (1980, p. 247), “Regular

semidiurnal fluctuations of small magnitude... result

from earth tides, produced by the attraction exerted on

the earth’s crust by the moon and, to a lesser extent, the

sun.” Peaks occur at low tide when the earth is compressed. Compression of the bedrock aquifers increases

the pressure on confined ground water, which results

in rising water levels in wells.

Water levels generally decline during the late

spring, summer, and early fall when plant growth is at

a maximum and recharge is at a minimum. Because of

plant consumption, very little water reaches the shallow or deep ground-water systems and precipitation

events, at best, tend to stair-step the seasonal decline

rather than reverse the decline (fig. 18). The

hydrograph of well AD-788 also shows a large number

of peaks and troughs. The water level is affected by one

or more wells; the decline on July 6 is the most pronounced.

Water levels also are influenced by topographic

setting. As shown in the table below, water levels generally are deeper for wells completed on hilltops than

wells completed on slopes, upland draws, or in valleys.

Because ground water flows from higher to

lower hydraulic head, the general direction of groundwater flow can be estimated from a map of the potentiometric surface. Synoptic water levels were collected

on November 14, 2000 (76 wells), and August 15, 2001

(74 wells), to aide in the evaluation of ground-water

flow paths and seasonal changes in water levels

(figs. 19 and 20). In general, ground-water flow paths

and the potentiometric surface during the fall closely

resemble that of summer. Depths to water in summer,

however, tend to be greater than in the fall; changes

range from less than 1 ft (well AD-793) to more than

80 ft (well AD-807). This change in water depth can

result in a retreat of water-level contours away from

the nearby creeks, toward ridge tops. The changes in

water levels between fall and summer, however, do not

appear to have been affected by geology or topography. Rather, the fluctuations are distributed randomly.

This is probably a result of the low transmissivity of

the water-producing fractures and the time between

when the pump was last run and when the water level

was measured.

Despite the season, ground-water flow directions

are dominated by Jack’s Mountain, which directs flow

to the southeast along a broad front. Flow along this

front is affected by the presence of faults and by

changes in topography. Geology may also affect the

location of springs because all three inventoried

springs are in the greenstone schist.

Seasonal and perennial springs and flowing

wells are interspersed in Section H (fig. 2), which is

near the base of Jack’s Mountain, with wells that have

water levels that are generally 30 to 40 ft below land

surface. One well, AD-1063, which was completed at

the beginning of August 2001, had a water level 320 ft

below land surface at the time of the August 15, 2001,

synoptic. Later measurements in well AD-1063 indicated a depth to water of approximately 37 ft.

The north-south trending fault through Sections

I and W has a pronounced effect on ground-water flow

paths. Springs and wet areas are common on either

side of the fault for most of its length. The hydraulic

gradient is steeper (water-table contours are more

closely spaced) in the vicinity of the fault, which suggests a change (reduction) in the relative permeability

of the rocks. Three wells (AD-798, AD-799, and

AD-821) in Sections I and W, near the north-south

trending fault, consistently have depths to water

greater than 100 ft. However, a little further south and

also along the fault (near the southeastern corner of

Section I) is well AD-797. The water level in well

AD-797 is much shallower, typically only 5 to 6 ft

below land surface.

The major ridge down the center of the study

area represents a ground-water divide that is present

throughout the year. The ground-water divide trends

in a southeasterly direction. Depths to water in wells

on this central ridge tend to be considerably greater

than depths to water in wells on the ridge flanks. Also,

it is not uncommon, regardless of the season, for wells

on the southern part (southeastern part of Section W,

Section E, most of Section P) of the central ridge to

Water level by topographic setting

[Depth, in feet below land surface; —, insufficient data

available; P10, tenth percentile; P25, twenty-fifth percentile;

P75, seventy-fifth percentile; P90, ninetieth percentile;

-, indicate water level above land surface]

Topographic

setting

Numberof wellsP10P25MedianP75P90MinimumMaximum

Hilltop 98 20 35.9 50 90 121.1 7 200

Slope 255 20 33.3 50 62 92.4 -2.3 280

Upland draw 33 20 20 40 54.1 80 5 103

Valley 4 — — 7.1 — — 5 10.2
29

700

650

600

800

750

550

500

850

900

800

650

600

700

750

77°23'53" 77°22'53"

39°44'09"

39°45'09"

0 1 0.5 MILE

0 0.5 1 KILOMETER

Jack's Mountain

600

Pennsylvania Route 116

Jack's

Mountain

Road

Pennsylvania Route 16

700

550

EXPLANATION

POTENTIOMETRIC SURFACE FOR

NOVEMBER 14, 2000

CARROLL VALLEY SECTION BOUNDARY

ROADS

FAULTS

INDEX CONTOUR

INTERMEDIATE CONTOUR

Figure 19. Potentiometric surface for November 14, 2000, Borough of Carroll Valley, Adams

County, Pennsylvania.
30

Figure 20. Potentiometric surface for August 15, 2001, Borough of Carroll Valley, Adams County,

Pennsylvania.
31

have depths to water of 100 ft or greater. Ground water

on the flanks of the central ridge flow to the southsouthwest towards Miney Branch or to the east-northeast towards Toms Creek. Several wells in Sections B

and WA (AD-773, AD-833, AD-845, AD-846), near a

small tributary to Toms Creek, have relatively shallow

water levels. During the synoptic measurements, water

levels in these wells ranged from 3.6 to 26.55 ft bls. The

small creek is probably a discharge area for ground

water.

Bedrock Water Budget

Under predevelopment conditions, the groundwater system is in long-term equilibrium: inflow

(recharge from precipitation that infiltrates through the

unsaturated zone to the water table and recharge from

losing streams, lakes, and wetlands) approximately

equals outflow (discharge to streams, lakes, wetlands,

and springs or base flow, plus evapotranspiration) or

simply:

P = SF + ET , (2)

where P is precipitation,

SF is stream outflow [(I) infiltration +

(RO) surface runoff], and

ET is evapotranspiration.

Humans change this equation by withdrawing

(pumping) water, adding impermeable surfaces,

changing vegetation, installing onlot septic systems,

and introducing irrigation. Because precipitation does

not increase, the consumptive use of pumpage must be

provided by a decrease in ground-water storage and a

decrease in base flow. Equation 1 now becomes:

P = SF + ET + Q , (3)

where P is precipitation,

SF is stream outflow [(I) infiltration +

(RO) surface runoff],

ET is evapotranspiration, and

Q is pumpage.

Pumpage also will reduce water levels. This

decline is necessary to induce ground water stored in

secondary openings to move toward the pumping

wells. Thus, the ground-water system serves as a water

reservoir and a water-distribution system (Alley and

others, 1999). For most ground-water systems, this

change is transient and the system will eventually

adjust. Additional stress is introduced by long-term

drought by reducing ground-water storage and base

flow. Because droughts represent an extreme hydrologic condition, they should be evaluated in any longterm management plan.

Although a detailed bedrock water budget

would provide additional geohydrologic information

to the Borough, it was beyond the scope of the study to

install the stream gages needed for the analysis. However, the efforts of previous workers can provide an

approximation of the terms in equation 2 and may

prove useful in determining ground-water availability.

Taylor and Royer (1981), who developed a water

budget for Adams County, estimated P as averaging

about 39 in. per year or 2,930 (gal/d)/acre. They also

estimated SF (includes surface runoff plus groundwater recharge) as 15 in. [1,130 (gal/d)/acre] and ET as

24 in. [1,800 (gal/day)/acre]. Taylor and Royer (1981,

p. 6) noted also that in drought years as much as 70 to

75 percent of precipitation can be lost to ET.

The 9-year average (1993-2001) precipitation for

the Borough is 46.54 in. (Howard Rodriguez, Borough

of Carroll Valley, written commun., 2002). This average

is very similar to those reported by Sloto (1994) who

determined the water budget for a number of surfacewater basins in Chester County also underlain by crystalline rocks. The averages from Sloto (1994) are presented in the following table.

In 2001, the Borough measured 31.16 in. of precipitation (Howard Rodriguez, Borough of Carroll Valley, written commun., 2002), a decrease in precipitation

of 15.38 in. or 33 percent between the 9-year average

and the year 2001. Applying a 33 percent reduction

from the three-basin average may be a good approximation for drought water budget and estimated

Average annual water budget and estimated recharge for

selected surface-water basins in Chester County,

Pennsylvania (modified from Sloto, 1994)

[All values are shown in inches and in (gallons per day per

acre)]

Basin

(P)

Precipitation

(SF)

Streamflow

(RO)

Surface

runoff

(ET)

Evapotranspiration

(I)

Recharge

Darby Creek

1975-88

47.9

(3,590)

23.2

(1,740)

8.7

(653)

24.9

(1,870)

16.3

(1,220)

Crum Creek

1982-88

45.8

(3,440)

18.7

(1,400)

6.7

(503)

27.1

(2,030)

14.0

(1,050)

West Branch

Brandywine Creek

1974-88

45.4

(3,410)

21.2

(1,590)

9.3

(698)

24.1

(1,810)

14.0

(1,050)

Three basin

average

46.4

(3,480)

21.0

(1,577)

8.2

(618)

25.4

(1,903)

14.8

(1,107)
32

recharge to the study area. This information is presented in the following table and equations (note numbers in table are not exact due to rounding).

P = SF + ET or (4)

31.2 = 14.1 + 17.1 or (5)

P = RO + I + ET or (6)

31.2 = 5.1 + 9.0 + 17.1 (7)

This water-budget approximation would suggest

that the infiltration for the Borough was about 9 in. or

675 (gal/d)/acre. For the typical 0.5-acre development

in the Borough, ground-water recharge would be about

338 gal/d. Mark Sigouin (Pennsylvania Department of

Environmental Protection, written commun., 2002)

estimates that the average water usage per person is

75 gal/d. For a typical family of four, water usage

would then be 300 gal/d or almost the entire infiltration rate of 338 gal/d. Although almost all of the

ground-water withdrawn for domestic usage is

returned to the regolith via onlot septic systems, the

typical domestic well does not have ready access to

this recycled water because (1) the well is sealed off

from the regolith by grout and steel casing, and (2) the

poor interconnection of secondary openings in the bedrock aquifers to the regolith.

Consumptive use for the study area is considered to be that part of water withdrawn that is evaporated or otherwise removed from the immediate water

environment (Solley and others, 1998, p. viii). The

USGS (1999b) estimates annual domestic consumptive

use at about 14 percent with most of it occurring during the summer months or a loss to infiltration of about

42 (gal/d)/acre. In a drought year, this consumptive

use would probably be higher owing to increased

watering of vegetation.

In summary, detailed work by Sloto (1994) and

Taylor and Royer (1981) suggests that infiltration in the

Borough, during a drought, may average about 9 in.

per year. Assuming that the typical family of four

resides on just 0.5 acre, then the infiltration rate (minus

42 gal of consumptive use) is 296 gal/d, or approximately equal to the water usage of 300 gal/d.

Another way to evaluate ground-water availability is to look at well construction and discharge patterns over time. In Pennsylvania, a good well driller

will attempt to meet the per capita usage requirement

of 75 gal/d by drilling a well that is either deep enough

so that a sufficient number of water-producing zones

are penetrated or deep enough so that borehole storage

is sufficient. If the development of the Borough has had

a minimal effect on the bedrock water budget, one

would expect only a small increase over time in well

depth and little change in reported yield. However, the

median depth of a well drilled in the Borough has

increased from a low of 209 ft (1980-84) to 400 ft (2000-

01) (table 2). This increase in well depth may be attributed to (1) a decline in water levels, (2) a decrease in

the productivity of shallow water-producing zones

(through a decrease in water levels), (3) warmer temperatures (greater consumptive use), (4) increasing frequency and severity of drought, (5) a transition phase

as the ground-water system adjusts to increased

pumping and drought, or (6) drillers have become

more aware of the low-yielding characteristics of the

crystalline-rock aquifers and have compensated by

drilling wells deeper.

Sources of Possible Anthropogenic Recharge

The potential for anthropogenic recharge to the

crystalline-rock aquifers was evaluated through certain

chemical and biological water-quality data collected by

the Borough and USGS (appendix C). About every

10 years, the Borough is required by law to collect and

analyze water from approximately 10 percent of the

existing wells for the presence of nitrate as N and

coliform bacteria (total and fecal).

In general, ground water unaffected by contaminant sources contains less than 2 mg/L of nitrate

(U.S. Geological Survey, 1999a, p. 34). Of the

35 samples analyzed for nitrate in 2001, 12 (33 percent)

had nitrate concentrations greater than 2.0 mg/L as N;

one well contained water that exceeded the U.S. Environmental Protection Agency (USEPA) maximum contaminant level (MCL) of 10 mg/L (table 3). Ground

water with concentrations of nitrate greater than

2 mg/L may indicate anthropogenic sources such as

fertilizer or sewage from septic systems. Leaking or

ineffective septic systems, in addition to elevating

nitrate concentrations, can cause elevated concentrations of total coliforms, fecal coliforms, and chloride in

ground water.

Drought water budget and estimated recharge for Borough of

Carroll Valley, Adams County, Pennsylvania

[All values are shown in inches and in (gallons per day per

acre)]

Basin

(P)

Precipitation

(SF)

Streamflow

(RO)

Surface

runoff

(ET)

Evapotranspiration

(I)

Recharge

Borough 2001 31.2

(2,340)

14.1

(1,060)

5.1

(383)

17.1

(1,280)

9.0

(675)
33

Table 2. Change, over time, in well depth, yield, and specific capacity, Borough of Carroll Valley, Adams County, Pennsylvania

[—, not available; yield, in gallons per minute; specific capacity, in gallons per minute per foot of drawdown; ft, feet]

Wells with reported yields Wells with specific capacities

Year well

drilled

Well depth

(median)

Number

of wells

Yield

(median)

Gallons per

100-ft well depth

Well depth

(median)

Number

of wells

Specific capacity

(median)

Specific capacity

per 100-ft well depth

1965-79 311 10 3 0.96 — — — —

1980-84 209 5 3 1.44 209 5 0.12 0.057

1985-89 250 50 6 2.4 250 46 .035 .014

1990-94 305 90 3 .98 320 69 .01 .0033

1995-99 340 149 2.5 .74 360 122 .01 .0028

2000-01 400 48 5 1.25 500 36 .01 .002

Table 3. Results of analyses for nitrate, coliform, chloride, and bromide in ground water of selected wells, Borough of Carroll

Valley, Adams County, Pennsylvania

[mg/L, milligrams per liter; mL, milliliter; <, less than; —, not analyzed; E, estimated]

U.S.

Geological

Survey well

number

Nitrate 1990

(mg/L)

Nitrate 2001

(mg/L)

Total coliform

1990 (colonies

per 100 mL)

Total coliform

2001 (colonies

per 100 mL)

Fecal coliform

2001 (colonies

per 100 mL)

Chloride

2001

(mg/L)

Bromide

2001

(mg/L)

AD-779 5.4 — 0 — — — —

AD-780 1.7 — 0 — — — —

AD-781 6.6 4.67 4 6 0 13.3 <0.030

AD-783 7.1 — 0 — — — —

AD-790 — 2.07 — 15 0 20.6 .044

AD-800 2.9 1.32 0 0 0 8.6 —

AD-826 7.2 — 0 — — — —

AD-829 — 3.19 — 0 0 4.6 —

AD-830 — 1.05 — 0 0 3.3 <.030

AD-844 — 1.42 — 0 0 5.3 —

AD-845 — 1.62 — 0 0 6.2 —

AD-852 1.7 — 0 — — — —

AD-869 — 5.58 — 135 3 35.9 <.030

AD-873 — 1.32 — 0 0 10.6 E .016

AD-877 — <1.00 — 0 0 5.3 —

AD-883 <1.00 — 6 — — — —

AD-892 — 4.75 — 0 0 21.0 E .026

AD-900 — <1.00 — 0 0 1.5 .015

AD-902 — <1.00 — 0 0 1.3 .010

AD-911 — <1.00 — 0 0 8.8 —

AD-912 — <1.00 — 6 0 5.9 —

AD-914 — 1.01 — 0 0 3.7 —

AD-922 — 5.59 — 0 0 8.6 <.030

AD-931 — 1.02 — 0 0 3.8 E .024

AD-941 — <1.00 — 0 0 10.3 —

AD-947 — 1.27 — 0 0 5.2 —

AD-950 — 1.96 — 0 0 4.9 —

AD-959 — 1.20 — 0 0 7.0 —

AD-960 — 7.31 — 0 0 6.8 E .025

AD-961 — 19.5 — 6 0 13.3 .046

AD-963 — 1.58 — 0 0 4.5 <.030

AD-969 — 1.68 — 0 0 5.2 —

AD-1013 1.6 2.55 0 0 0 5.3 —

AD-1021 — 4.55 — 22 0 8.5 —

AD-1033 — 1.67 — 0 0 5.6 —

AD-1037 — 2.71 — 0 0 13.2 E .025

AD-1077 1.2 1.22 0 0 0 5.7 <.030

AD-1084 — <1.00 — 0 0 2.1 .024

AD-1098 — 3.79 — 168 2 8.4 .040

AD-1122 — <1.00 — 0 0 4.0 —

AD-1138 — 1.02 — 0 0 3.7 —
34

The presence of total coliform bacteria indicates

the possibility of sewage contamination. In the study

area, total coliforms were detected in 7 of the 35 samples (20 percent) collected in 2001 (table 3). This percentage is similar to that found by Francy and others

(2000), who found a relation between the presence of

septic systems on the property and the detection of

coliforms in water wells. Bacteria survival times in

ground water range from days to years and are dependent on temperature, microbial activity, moisture content, pH, salt species and concentrations, soil

properties, bacterium type, organic matter, and

hydraulic conditions (Yates and Yates, 1988).

Fecal coliform bacteria are found only in the

intestines of warm-blooded animals and humans. The

presence of these bacteria indicate that sewage wastes

or other fecal material are present in the water. Fecal

coliform bacteria were found in water from 2 of the

35 wells sampled in 2001 (table 3). The two wells that

contained fecal coliform bacteria also contained the

greatest number of total coliform bacteria (table 3).

The presence of chloride (along with excessive

nutrients or bacteria) where it does not occur naturally

also may indicate anthropogenic sources of recharge.

Sources of chloride include septic systems (chloride

concentrations typically range from 50 to 100 mg/L are

common in septic tank effluent), animal waste, potash

fertilizer, and drainage from road-salting chemicals.

Concentrations of chloride in water from

35 wells range from 1.3 to 35.9 mg/L, the median is

5.65 mg/L (table 3). The Wilcoxon rank-sum test indicated a significant correlation between the presence of

coliform and the concentration of chloride. The median

concentration of chloride in wells that contained

coliform (7 wells) was 13.3 mg/L; in wells with no

coliform (28 wells), the median concentration of chloride was 5.3 mg/L.

In a typical winter, the Borough may use 44 tons

or more of road salt to keep their roads clear of snow

and ice. To identify sources of chloride, such as road

salt in ground water, weight ratios of chloride and bromide concentrations can be used (Whittemore, 1988;

Knuth and others, 1990; Davis and others, 1998; Jagucki and Darner, 2001). Chloride and bromide are useful indicators because they are (1) highly soluble,

(2) minimally affected by adsorption once dissolved in

water, (3) not altered by oxidation-reduction reactions,

and (4) not found in high concentrations in igneous

rocks (Hem, 1985). Differences in ratios of chloride to

bromide occur because bromide is even more soluble

in water than chloride (Davis and others, 1998, p. 339).

According to Davis and others (1998, table 3), ground

water from granitic and metamorphic rocks generally

should have a chloride-to-bromide (Cl:Br) ratio that

lies between 90 and 140. If road salt (halite) is reaching

the ground water, the water will become enriched in

chloride relative to bromide and will thus have a high

Cl:Br ratio.

Three binary mixing curves (ground water plus

halite, domestic sewage plus halite, and dilute ground

water) were prepared (fig. 21), following methods

described in Whittemore (1988, p. 340) and Jagucki and

Darner (2001, p. 38). The sample from well AD-900 was

chosen as the dilute ground water end-member

because it had one of the lowest Cl:Br ratios and chloride and bromide concentrations. Water from this well

also contains no detectable amounts of nitrate or

coliform. The Cl:Br ratio of the ground water plus

halite end-member was estimated as the mean of three

samples of road salt collected by Knuth and others

(1990, table 1). The Cl:Br ratio of the domestic sewage

end-member was selected following the method used

by Jagucki and Darner (2001, p. 38). Mixing curves

were calculated by using the formula presented by

Whittemore (1998, p. 340).

Jagucki and Darner (2001, p. 40) report that

waters with Cl:Br ratios greater than 400 and plotting

near or between ground water plus halite and domestic sewage plus halite lines should be considered to

have been affected by anthropogenic activities such as

road salting or leakage from septic systems. Other factors, such as nitrate concentrations and the presence of

coliform, also should be considered when determining

the effect of human activities on ground water. For

example, well AD-1098 with a Cl:Br ratio of 211 contains water with a nitrate concentration of 3.79 mg/L

and total coliform count of 168, which strongly suggests contamination from sewage.

To further discern anthropogenic sources of

ground-water recharge, 6 of the 18 wells selected for

analysis of Cl:Br ratios also were chosen to evaluate the

presence of wastewater compounds in well water.

Zaugg and others (2002) have developed a method for

the determination of 67 compounds typically found in

domestic and industrial wastewater such as non-ionic

surfactants, fungicides, herbicides, insecticides, flame

retardants, and combustion products. Other, more recognizable named compounds include caffeine, camphor, and menthol. The method was developed in

response to concern over endocrine-disrupting chemi-
35

cals in wastewater on aquatic organisms. However,

this method also may be useful for evaluating the effect

of sanitary and storm-sewer overflow on water quality.

The results of the analyses of the 67 wastewater

compounds are listed in table D1. The endocrine-disrupting potential and possible compound uses or

sources are listed in table D2. Although all six wells

contained water with detectable concentrations of

wastewater compounds, the concentrations for most of

the compounds were below the minimum reporting

levels of 1 or 0.5 μg/L (equivalent to parts per billion

or ppb). In addition, some of the wastewater compounds detected may be the result of the sampled

water being in contact with plastic pipe during the

transport of the water from the crystalline-rock aquifer

to the sample bottle.

Analysis of the water-quality data indicates that

infiltration from onlot septic systems and surface runoff from roads may be reaching wells in the Borough.

The exact flow paths taken by the recharge water and

the recharge volume, however, remain uncertain. For

example, the owners of well AD-900, which contains

no detectable concentrations of coliform or nitrate and

had the lowest concentration of chloride and bromide,

have utilized a holding tank for almost 10 years. Yet,

the water in well AD-900 contained 0.68 μg/L Phenol

(table D1). For another example, consider well AD-869.

The water in well AD-869 contained total and fecal

coliforms and elevated concentrations of nitrate and

chloride (table 3), suggesting contamination from onlot

septic systems. Yet, the concentrations of wastewater

compounds Bisphenol A and Triphenyl phosphate

were the lowest reported. In essence, although anthropogenic recharge may reach wells in the Borough, this

impact is reduced through dilution with native ground

water, breakdown via biological processes, and sorption to soils.

Figure 21. Binary mixing curves for chloride to bromide (Cl:Br) ratios, Borough of Carroll Valley,

Adams County, Pennsylvania (modified from Jagucki and Darner, 2001, fig. 14).
36

ESTABLISHMENT OF A

DROUGHT-MONITOR WELL

According to Alley and others (1999, p. 20),

droughts can be classified into three principal types

(1) meteorological (lack of precipitation), (2) agricultural (lack of soil moisture), and (3) hydrologic

(reduced streamflow or ground-water levels). A meteorological drought is the cause of agricultural and

hydrologic drought, but the severity of any type of

drought is strongly dependent on the timing of the

water deficiency. For example, a prolonged dry period

during the winter months has only a minor effect on

agriculture or ground-water levels because plants are

dormant and the ground may be frozen. If the hydrologic drought occurs during the summer, soil moisture

is consumed quickly through evapotranspiration and

an agricultural drought occurs. If the hydrologic

drought occurs when ground water typically is

recharged (fall through early spring), then

ground-water levels decline, shallow wells go dry,

and streamflow decreases. The normal (1960-90)

monthly precipitation for South Mountain and

the precipitation recorded at the Borough are

shown on figure 22. The 2001 precipitation deficit

began in the winter months and continued for

much of the spring (hydrologic drought), summer

(agricultural drought), and fall, cumulating in a

meteorological drought with a total precipitation

deficit of 13.58 in. The impact of the 2001 drought

on water levels can be seen in the hydrograph for

well AD-808 (fig. 23).

Meteorological and agricultural droughts

are not cumulative and can end relatively quickly

by a return to sufficient precipitation. Groundwater systems, however, tend to respond much

more slowly. Not only is there a time delay for the

precipitation to migrate downward from the soil

into the underlying aquifer, but the hydrological

drought is cumulative. Enough water must be

returned to ground-water storage to return

ground-water levels and stream base flows back

to near pre-drought levels before the hydrological

drought is over.

A common response to hydrologic drought

is to drill more wells or to drill existing wells

deeper. The success of this response depends on

the storage capacity of the underlying aquifer and

the extent of existing ground-water development.

If storage is large and development minimal,

droughts may have limited, if any, effect on well

owners. In the study area, however, the storage

capacity of the bedrock aquifers is extremely low

and the interconnection of the water-producing zones

with the overlying soil or regolith is limited. With additional population growth and the resultant increase in

ground-water consumption and impervious surfaces,

severity of hydrologic droughts will continue to

increase in the study area.

Pennsylvania Drought Monitor Network

In 1931, in response to concerns about groundwater-level declines caused by the drought of 1930, a

statewide well network was established in Pennsylvania to monitor water-level fluctuations. Today (2002),

in cooperation with the PaDEP, the USGS currently

operates one observation well in each of Pennsylvania’s 67 counties. Twenty-two wells are in the Ohio

River Basin, 30 wells are in the Susquehanna River

Basin, and 15 wells are in the Delaware River Basin.

0

0.5

1.0

1.5

2.0

2.5

3.0

3.5

4.0

4.5

5.0

JANUARY

FEBRUARY

MARCH

APRIL

MAY

JUNE

JULY

AUGUST

SEPTEMBER

OCTOBER

NOVEMBER

DECEMBER

MONTH

PRECIPITATION, IN INCHES

SOUTH MOUNTAIN

CARROLL VALLEY

Figure 22. Normal monthly precipitation for South Mountain (1960-

90) and monthly precipitation for Borough of Carroll Valley, Adams

County, Pennsylvania (2001) (Howard Rodriguez, Borough of Carroll

Valley, written commun., 2002).

Figure 23. Daily water levels in well AD-808, Borough of Carroll

Valley, Adams County, Pennsylvania.
37

The Commonwealth of Pennsylvania, in cooperation with the Susquehanna River Basin (SRBC) and

the Delaware River Basin (DRBC), uses five parameters

to assess drought conditions. These include stream

flows, precipitation, reservoir storage levels, water levels in the county ground-water observation network,

and Palmer Drought Index (a measure of soil moisture). Drought declarations are based on at least three

of the five parameters (PaDEP, 2001). Phases of

drought preparedness and objectives for water conservation are:

Drought watch - alerts government agencies,

water suppliers and users, and the public regarding the

onset of conditions indicating the potential for future

drought-related problems. A request for voluntary

water conservation is made to reduce usage by 5 percent.

Drought warning - prepares governmental agencies for coordinated response to imminent drought

conditions, potential water supply shortages, and initiates concerted voluntary conservation measures. The

objective is to reduce overall water uses by 10-15 percent.

Drought emergency - concentrated phase of

operations by state and local agencies to marshall

resources to respond to emergency conditions, avoid

depletion of water sources, assure minimum water

supplies to protect public health and safety, support

essential and high priority water uses, and avoid

unnecessary economic dislocations. Mandatory restrictions on nonessential water uses are possible. The

objective is to reduce consumptive water use by at least

15 percent.

Up-to-date hydrologic and drought-condition

information can be found on the USGS web site at

http://pa.water.usgs.gov. In addition to the current conditions, this site includes details of the monitoring program, criteria used in drought determination, and indepth definitions of the various drought levels.

Borough Observation-Well Network

and Drought-Monitor Well

As a result of a number of wells going dry in

1998, Borough officials were interested in establishing a

drought monitor well within the Borough to aid them

in evaluating the local severity of droughts. This well

would be completed in the metabasalt or metarhyolite

and be protected from outside influences such as property development and pumping from nearby wells. To

meet these objectives, the USGS converted 11 wells into

long-term (greater than 30 days) observation wells

with continuous monitoring of water levels. At least

once a month, the water levels in these wells were verified by personnel from the USGS or the Borough utilizing electric tapes. A number of the wells were later

removed from the observation well network because of

poor construction, pending development of the lot, or

utilization of instruments in other wells. By October of

2001, the observation-well network was reduced to six

wells. Of the final six wells, well AD-808 was selected

to be a drought monitor well for the Borough. This

selection was based on several criteria: (1) water level

in well reflects seasonal changes, (2) lot cannot be

developed (did not pass percolation or “perk” test),

(3) surrounding lots are developed, and (4) water level

is not affected by pumping from nearby wells.

Well AD-808 is at latitude 39°44'30", longitude

077°22'50", and is owned and operated by the Borough.

Well AD-808 has a continuous period of record from

October 2, 2000, to present. The well is completed in

the metabasalt, has a total depth of 234 ft, and is cased

to 20 ft. The well is currently (2002) instrumented with

a Stevens Type F analog chart recorder.

Sloto (1994) demonstrated that long-term waterlevel data from one or more reference or index wells

can be related to water levels measured in short-term

observation wells by using a regression equation. This

method is applicable for areas where water levels represent the natural fluctuation of the water table or

potentiometric surface.

Two wells that are part of the Pennsylvania

drought monitor network were considered as possible

reference wells, AD-146 and CU-2 (fig. 1). The Adams

County observation well (AD-146) is at latitude

39°58'46", longitude 077°04'06", at State Game Land

No. 249, near York Springs, Pa. The well has a continuous record of water levels from January 1968 to the current year. The well is completed in the Gettysburg

Formation of Late Triassic age, has a total depth of

100 ft, and is cased to 17 ft. The Cumberland County

observation well (CU-2) is at latitude 40°02'09", longitude 077°18'33", in Michaux State Forest near Pine

Grove Furnace, Pa.; the well is owned by the Commonwealth of Pennsylvania and operated by the USGS.

Water levels in this well were measured several times

per month from June 1951 to March 1955. Water levels

were recorded (continuous) beginning in July 1955 and

continue to the current year. The well is completed in

the metarhyolite, has a total depth of 37 ft, and is cased

to 19 ft.
38

Water levels in well AD-808 (fig. 23) were

compared to wells AD-146 and CU-2 for the same

time period and a similar pattern of recharge and

decline were observed. A regression equation was

then developed for each well. In conjunction with

the regression equation, a coefficient of determination was calculated to determine how the waterlevel data were related. A perfectly linear relation

would have a coefficient of determination of

1.0000. The coefficient of determination was 0.4522

between well AD-146 and AD-808, but 0.9586

between well CU-2 and AD-808 (fig. 24). On the

basis of this analysis of water levels in well CU-2

and well AD-808, the following regression equation was used:

Y = 2.2278X + 62.837 , (8)

where Y is the predicted

water level in well

AD-808 and X is the water

level observed in well

CU-2. In 2001, the water

level in well AD-808 fell

below the droughtwarning level (90th

percentile) in June and

stayed below the droughtwatch level (75th

percentile) from July

through September

(fig. 25). In November and

December, the water level

in well AD-808 was again

below the droughtwarning level.

Figure 24. Relation between water levels in Borough of Carroll

Valley, Adams County, Pennsylvania, well AD-808 and Cumberland

County, Pennsylvania observation well CU-2.

Figure 25. Drought-warning levels for well AD-808, Borough of Carroll Valley, Adams

County, Pennsylvania.
39

SUMMARY AND CONCLUSIONS

Population growth in the Borough of Carroll Valley has increased the demand for ground water. This

increased demand, however, has coincided with a

series of droughts that have reduced the availability of

ground water. Borough officials joined with the USGS

to study the geohydrology, ground-water availability,

ground-water flow, and the effect of the 2001 drought

in the Borough.

The depth and yield of a well is affected directly

by the size and distribution of water-producing zones

open to the well. Because of the highly resistant, massive, and competent nature of the bedrock, water-producing zones generally are not abundant, productive,

or inter-connected. As a result, many wells are deep,

subsurface stand or storage pipes. Wells drilled in the

metabasalt and greenstone schist generally are deeper

than those completed in the metarhyolite; the median

well depths in these rocks are 320, 320, and 300 ft,

respectively. Wells on hilltops generally are deeper

than wells on slopes or in valleys. The deepest well

drilled has a reported depth of 780 ft.

Depth to bedrock or regolith thickness is highly

variable, ranging from 0 to 115 ft and determining to a

large degree how much casing is required. Although

regolith commonly absorbs and stores precipitation,

there does not appear to be a relation between greater

regolith thickness and driller reported yield. Depth to

bedrock does vary by geologic formation, however,

with more casing required for wells completed in the

metarhyolite (median 35 ft) than in the metabasalt

(median 28 ft) or in the greenstone schist (median

25 ft).

Driller reports and borehole geophysics indicate

that water-producing zones typically are shallow. Fifty

percent of the water-producing zones in the metabasalt, metarhyolite, and greenstone schist are penetrated

by a depth of 200, 159, and 240 ft, respectively. Ninety

percent of the water-producing zones (in all three rock

types) are penetrated by a depth of 370 ft. Borehole

geophysical data also indicate very little hydraulic

head difference between water-producing zones, and

water-producing zones generally are not well connected.

The metabasalt, metarhyolite, and greenstone

schist are among the lowest yielding rocks in the Commonwealth; median reported yields are 3.0, 4.5, and

3.0 gallons per minute (gal/min), respectively. Welldevelopment techniques can increase yields beyond

those obtained through the typical well development

method of pumping and surging a well. Specific capacities are low; median specific capacities are 0.01 gallon

per minute per foot of drawdown [(gal/min)/ft] for

the metabasalt and greenstone schist and

0.02 (gal/min)/ft for the metarhyolite. More than

50 percent of the wells completed in the bedrock aquifers have specific capacities of 0.04 (gal/min)/ft or less.

This number indicates that most water comes from

borehole storage. Although topographic setting can

affect reported yields and specific capacities, this distribution does not appear to have any recognizable pattern in the study area.

Estimates of transmissivity from slug tests range

from 2 to 188 feet squared per day (ft2/d); the median

is 26 ft2/d. Driller drawdown tests indicate that 90 percent of the wells have values of transmissivity and

hydraulic conductivity less than 100 ft2/d and 1 foot

per day, respectively. Ground-water flow paths are

very complex and strongly affected by topography,

geology, sources of recharge, and pumping.

Water levels fluctuate in response to recharge

from precipitation, pumping of wells, and evapotranspiration. Water levels in wells completed in the fractured bedrock quickly respond to precipitation events.

Although precipitation events and changes in the season can greatly affect water levels, the effects are generally short lived. Despite the season, synoptic waterlevel measurements indicate that ground-water flow

directions are dominated by Jack’s Mountain and that

the major ridge down the center of the study area represents a ground-water divide. Ground-water flow

generally results in a water table that is a subdued replica of the land surface.

The principal source of ground-water recharge in

the Borough is precipitation. Inflow from topographically higher areas that border the Borough also occurs.

Approximately half of the 46 in. of precipitation

returns to the atmosphere through evapotranspiration,

and surface runoff to streams and base flow account

for the remainder.

In general, the ground-water system is under

stress. Humans effect the ground-water budget by

withdrawing water, adding impermeable surfaces,

changing vegetation, installing onlot septic systems,

and introducing irrigation. The consumptive use of

pumpage must be provided by a decrease in groundwater storage and a decrease in base flow. During 2001,

the estimated ground-water infiltration rate on a

0.5-acre lot was approximately 9 inches per year or
40

300 gallons per day (gal/d). A typical family of four

residing on just 0.5 acre also uses 300 gal/d. This analysis suggests that during drought years, the groundwater system is severely stressed and that declining

water levels, decreased ground-water availability, and

reduced base flow will continue for an unknown

period of time.

The use of data on selected chemical (nitrate,

chloride, bromide), biological (coliform), and wastewater compounds to identify potential sources of anthropogenic recharge showed mixed success. Total

coliform bacteria (7 of 35 wells), fecal coliform bacteria

(2 of 35), and elevated concentrations (greater than

2 mg/L) of nitrate (12 of 35 wells) were found. There

was a significant correlation between the concentration

of chloride and wells that contained coliform bacteria.

Chloride to bromide ratios from 18 wells ranged from

88 (dilute ground water) to 1,200 [ground water probably effected by anthropogenic source(s)]. The water in

six wells was analyzed for 67 wastewater compounds.

Although six wastewater compounds were found, concentrations were very low, ranging from 0.02 to

1.2 μg/L. The presence of total and fecal coliform bacteria, nitrate, and Cl:Br ratios indicate that some of the

ground-water recharge reaching domestic wells in the

study area is affected by anthropogenic sources that

may include fertilizer, road salt, or sewage. The flow

paths taken by the recharge water and volume of

recharge, however, remains uncertain.

Through the use of continuous water-level

recorders, borehole geophysical surveys, slug tests,

driller logs, and adjacent county observation wells, the

USGS was able to identify well AD-808 as a suitable

candidate for a drought-monitoring well in the Borough. In 2001, the water level in well AD-808 fell below

the drought-warning level (90th percentile) in June and

stayed below the drought-watch level (75th percentile)

from July through September. In November and

December, the water level in well AD-808 was again

below the drought-warning level.

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42

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43

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45

Table 4. Records of selected wells and springs, Borough of Carroll Valley, Adams County, Pennsylvania

Latitude and longitude: Location of well determined to the nearest second from topographic maps and to

the nearest tenth of a second by a Global Positioning System (GPS). Examples: 394428 represents

39°44'28", 394429.7 represents 39°44”29.7". Horizontal coordinate datum for wells located by GPS

is NAD 83, datum for other wells is NAD 27.

Date completed: Date of well construction as reported on driller’s log, in m/d/y, m/y, or y format.

Altitude of land surface: Land surface at well site, in feet above NGVD 29.

Topographic setting: S, slope; H, hilltop; V, valley; W, upland draw.

Hydrogeologic unit: 000MBSL, metabasalt; 000MTRL, metarhyolite; 000GRNS, greenstone schist;

377 WVRN, Weverton Formation; 377 LUDN, Loudoun Formation.

Depth of well: Depth of drilled well, in feet below land surface, as reported on driller’s log.

Casing length: Feet of casing used to complete well, as reported on driller’s log.

Static water level: Depth of water, in feet below land surface, as measured by USGS personnel or

reported by driller or owner.

Date water level measured: m/d/y, m/y, or y format.

Driller reported yield: in gallons per minute.

Specific capacity: in gallons per minute per foot of drawdown.

Depth to bedrock: Depth, in feet below land surface, to bedrock as reported on driller’s log.

<, less than; >, greater than; F, flowing well; —, no data.
46

Table 4. Records of selected wells and springs, Borough of Carroll Valley, Adams County,

Pennsylvania

USGS well

identification

number

Location

Driller Date

completed

Altitude

of land

surface

(feet)

Topographic

setting

Hydrogeologic

unit

Depth

of well

Latitude Longitude (feet)

AD-516 394428 0772318 Eichelberger 9/20/1978 730 S 000MBSL 550

AD-771 394453 0772245 Alexander 6/1986 580 S 000MBSL 230

AD-772 394450 0772254 — 2000 630 S 000MBSL —

AD-773 394452 0772315 Eichelberger 11/1998 670 V 000MBSL 400

AD-774 394439 0772239 — 2000 620 S 000MBSL 398

AD-775 394445 0772240 Alexander 2/16/2000 570 S 000MBSL 240

AD-776 394426 0772231 Alexander 3/21/2000 670 S 000MTRL 340

AD-777 394446 0772324 — 1988 805 S 000MBSL 80

AD-778 394445 0772318 Alexander 5/8/2000 780 S 000MBSL 500

AD-779 394444 0772308 Reichart 2000 745 S 000MTRL —

AD-780 394440 0772319 Alexander 2000 860 S 000MBSL 260

AD-781 394438 0772319 Alexander 10/3/1995 875 H 000MBSL 500

AD-782 394438 0772320 D.H. Woodward 1975 880 H 000MBSL —

AD-783 394438 0772320 — 2000 880 H 000MBSL —

AD-784 394436 0772318 Alexander 1998 850 H 000MTRL 600

AD-785 394433 0772254 Alexander 10/19/1995 750 S 000MBSL 300

AD-786 394432 0772244 Harley 6/26/2000 740 W 000MBSL 400

AD-787 394431 0772238 Alexander 8/6/1991 680 S 000MTRL 340

AD-788 394429.7 0772317.1 Alexander 2000 760 W 000MBSL 380

AD-789 394546 0772346 Woodward 1972 830 S 377WVRN 400

AD-790 394421 0772330 Alexander 8/1990 660 S 000MBSL 615

AD-791 394422 0772339 Alexander 2/1994 630 S 000GRNS 500

AD-792 394433 0772330 Alexander 11/7/1998 800 S 000MBSL 700

AD-793 394541 0772340 — 1990 790 S 000MBSL —

AD-794 394534 0772347 — 2/15/2000 820 W 000MBSL 225

AD-795 394435 0772427 Reichart 4/2/1997 690 S 377LUDN 300

AD-796 394433 0772427 Alexander 11/1989 680 W 000MBSL 100

AD-797 394431 0772414 Harley 6/28/2000 650 W 000MBSL 300

AD-798 394438.4 0772413.8 Alexander 10/27/1999 740 S 000MBSL 400

AD-799 394439 0772413 — 2000 700 H 000MBSL —

AD-800 394445.3 0772424.8 W. Funt 7/1988 820 S 000MBSL 170

AD-801 394451.3 0772420.9 Alexander 6/1991 890 H 000MBSL 500

AD-803 394418 0772234 Harley 6/27/2000 680 S 000MTRL 225

AD-804 394418 0772235 Alexander 2/26/2000 680 S 000MTRL 280

AD-805 394416 0772239 — 1972 680 S 000MTRL 200

AD-806 394426 0772239 Alexander 10/9/1995 730 S 000MBSL 260

AD-807 394425 0772258 Alexander 5/4/2000 780 S 000MBSL 750

AD-808 394429.9 0772249.8 Keyser 10/16/1969 790 H 000MBSL 234

AD-809 394428 0772250 Alexander 7/28/1995 780 H 000MBSL 300

AD-814 394458 0772424 — 7/2000 830 S 000GRNS 300

AD-815 394500 0772420 Alexander 3/28/1997 860 S 000GRNS 600

AD-816 394500.3 0772418.2 Alexander 11/2/1996 860 S 000MBSL 780

AD-817 394500.7 0772419.3 Alexander 6/18/1997 865 S 000GRNS 600

AD-818 394503.4 0772412.2 Alexander 5/3/2000 905 H 000MBSL 600

AD-819 394501.1 0772415.1 Alexander 8/14/2000 895 H 000MBSL 640
47

Table 4. Records of selected wells and springs, Borough of Carroll Valley, Adams County,

Pennsylvania—Continued

Casing Depth(s) to

water-producing

zone(s)

(feet)

Static water

level

(feet below

land surface)

Date water

level

measured

Driller

reported

yield

(gal/min)

Specific

capacity

(gal/min)/ft

Depth

to

bedrock

(feet)

USGS well

identification

number Length

(feet)

Diameter

(inches)

42 6 400; 485 91.95 8/15/2001 3 — — AD-516

50 6 — 55.87 8/15/2001 6 — — AD-771

— 6 — 64.16 8/15/2001 — — — AD-772

60 6 — 7.14 8/15/2001 1 — — AD-773

12 6 50 72.83 8/15/2001 — — — AD-774

60 6 110; 170; 225 32.64 8/15/2001 5 0.04 48 AD-775

60 6 140; 260 96.2 11/6/2000 7 .1 48 AD-776

— 6 — 65.05 8/15/2001 — — — AD-777

40 6 190; 260; 360 102.97 8/15/2001 3 .01 — AD-778

— 6 — 56.54 8/15/2001 — — — AD-779

— 6 — 49.59 8/15/2001 — — — AD-780

40 6 — 137.05 8/15/2001 .25 <.01 30 AD-781

— 6 — 109.5 8/15/2001 — — — AD-782

— 6 — 135.38 8/15/2001 — — — AD-783

40 6 — > 151 8/15/2001 .1 <.01 — AD-784

40 6 220 135.77 8/15/2001 1 <.01 30 AD-785

21 6 345; 365 10.2 8/15/2001 8 — 10 AD-786

40 6 250; 300 87.73 8/15/2001 1.5 .01 30 AD-787

30 6 300; 340 102.97 8/15/2001 15 — 15 AD-788

120 6 185 3 1972 3 <.01 115 AD-789

21 6 — 72.08 8/15/2001 0 <.01 8 AD-790

40 6 460 34.66 8/15/2001 5 — 25 AD-791

20 6 — 79.8 11/14/2000 .25 <.01 — AD-792

— 6 — -2.3F 8/15/2001 — — — AD-793

60 6 215 43.04 8/15/2001 12 — — AD-794

63 6 84; 140; 220 47.95 8/15/2001 3 — 4 AD-795

42 6 80 54.09 8/15/2001 12 .6 35 AD-796

42 6 230; 260 6.15 8/15/2001 15 — 30 AD-797

40 6 290 105.13 8/15/2001 2.1 — 10 AD-798

— 6 — 102.42 8/15/2001 — — — AD-799

55 6 70 66.56 8/15/2001 5 .04 48 AD-800

20 6 — 84.96 8/15/2001 1 <.01 10 AD-801

53 6 210 52 8/15/2001 20 — 45 AD-803

47 6 220; 240 57.34 8/15/2001 6 .04 35 AD-804

35 6 80 31.31 11/14/2000 3 — 35 AD-805

60 6 160; 225 49.4 8/15/2001 8 .06 50 AD-806

20 6 247; 640 224 8/15/2001 1.25 <.01 3 AD-807

20 6 98; 178; 225 12.31 8/15/2001 2 — 10 AD-808

27 6 — dry 7/28/1995 0 0 10 AD-809

31 6 — 44.16 8/15/2001 7 — — AD-814

21 6 — 92.76 8/15/2001 1.81 .01 10 AD-815

21 6 260 147.91 8/15/2001 .33 <.01 3 AD-816

28 6 — 81.81 8/15/2001 .85 <.01 15 AD-817

41 6 460; 560 16.7 8/15/2001 2 .01 25 AD-818

40 6 210; 350 76.4 8/15/2001 1.3 <.01 20 AD-819
48

AD-820 394451 0772415 Alexander 8/12/1995 810 S 000MBSL 220

AD-821 394443 0772418 Alexander 8/2000 800 S 000GRNS 360

AD-822 394455.3 0772402.3 Alexander 8/18/2000 790 W 000GRNS 160

AD-823 394442 0772403 Alexander 6/2000 780 S 000GRNS 500

AD-824 394437.4 0772400.9 Alexander 3/13/2000 820 S 000MBSL 500

AD-825 394448 0772351 Alexander 4/1990 890 H 000GRNS 310

AD-826 394440.4 0772327.3 — 1965 880 H 000MBSL 150

AD-827 394443.2 0772336.2 Alexander 1/1998 880 H 000MBSL 400

AD-828 394441.7 0772329.6 — 1975 880 H 000GRNS —

AD-829 394444.0 0772335.8 Alexander 12/21/1995 880 H 000MBSL 500

AD-830 394446.4 0772337.4 Alexander 2/1990 870 H 000MBSL 520

AD-831 394453.0 0772347.9 Alexander 3/14/2000 885 H 000MBSL 420

AD-832 394454 0772348 Alexander 12/19/1998 900 H 000MBSL 300

AD-833 394453.5 0772337.0 — 7/2000 820 S 000MBSL 160

AD-834 394518.4 0772351.3 Alexander 3/11/1997 960 H 000MBSL 400

AD-835 394513.2 0772347.4 — 2000 950 S 000MBSL —

AD-836 394513.9 0772353.8 — 6/6/1999 980 H 000MBSL 500

AD-837 394511 0772354 Alexander 1/14/2000 970 H 000MBSL 400

AD-838 394506.9 0772400.9 Alexander 4/28/2000 900 S 000MBSL 500

AD-839 394504.3 0772357.8 Alexander 4/17/1997 900 S 000MBSL 240

AD-840 394508 0772310 — 1984 760 H 000MBSL 180

AD-841 394506 0772313 — 5/1999 770 H 000MBSL 250

AD-842 394505 0772320 Alexander 9/24/2001 780 H 000MBSL 300

AD-843 394501 0772319 L. Adams 6/22/1992 750 H 000MBSL 350

AD-844 394500 0772318 Alexander 6/8/1999 750 H 000MBSL 500

AD-845 394456 0772318 Alexander 4/14/1999 710 S 000MBSL 220

AD-846 394453 0772320 Alexander 10/2/1996 680 V 000MBSL 400

AD-847 394453 0772239 Alexander 8/3/1992 550 S 000MBSL 200

AD-848 394453 0772250 Larry Adams 2/8/1993 600 S 000MBSL 175

AD-849 394430 0772228 L. Adams 5/1/1995 560 S 000MTRL 250

AD-850 394447 0772305 Alexander 4/9/1994 660 S 000MBSL 240

AD-851 394451 0772312 Alexander 9/1998 655 S 000MBSL 330

AD-852 394452 0772324 J.F. Harrison 5/1988 725 S 000MBSL 180

AD-853 394428 0772227 Alexander 8/1989 610 S 000MTRL 180

AD-854 394450 0772303 Alexander 10/29/1994 670 S 000MBSL 500

AD-855 394450 0772258 L. Adams 9/10/1993 660 S 000MBSL 350

AD-856 394449 0772251 Alexander 9/1988 620 S 000MBSL 305

AD-857 394425 0772229 Alexander 3/8/1999 660 S 000MTRL 200

AD-858 394423 0772226 Alexander 7/15/1994 640 S 000MTRL 160

AD-859 394447 0772314 Burcker 11/30/1990 720 S 000MBSL 185

AD-860 394445 0772320 Alexander 8/1989 820 S 000MBSL 250

AD-861 394446 0772244 Kohler 5/1995 580 S 000MBSL 200

AD-862 394444 0772255 Alexander 10/1/1993 630 S 000MTRL 500

AD-863 394444 0772316 Alexander 5/19/1999 780 S 000MBSL 580

AD-864 394444 0772323 Alexander 9/24/1998 845 S 000MBSL 440

Table 4. Records of selected wells and springs, Borough of Carroll Valley, Adams County,

Pennsylvania—Continued

USGS well

identification

number

Location

Driller Date

completed

Altitude

of land

surface

(feet)

Topographic

setting

Hydrogeologic

unit

Depth

of well

Latitude Longitude (feet)
49

60 6 195 60 8/12/1995 4 0.03 50 AD-820

40 6 280 107.11 8/15/2001 2 .01 20 AD-821

55 6 140 24.49 8/15/2001 20 .4 45 AD-822

27 6 — 42 8/15/2001 5 — — AD-823

40 6 176 65.21 8/15/2001 2.1 .01 30 AD-824

70 6 250 107.04 8/15/2001 3 .03 65 AD-825

— 6 — 73.93 8/15/2001 — — — AD-826

40 6 — 99.85 8/15/2001 3 — — AD-827

— 6 — 116.97 8/15/2001 — — — AD-828

72 6 260; 360 168.4 8/15/2001 2 .01 62 AD-829

40 6 200 96.8 8/15/2001 1 <.01 94 AD-830

40 6 265; 360 73.99 8/15/2001 4.6 .02 20 AD-831

55 6 180; 220; 280 64.55 8/15/2001 6 — 40 AD-832

40 6 — 26.55 8/15/2001 10 — — AD-833

42 6 140; 340 72.35 8/29/2001 2 .01 30 AD-834

— 6 — 97.2 8/15/2001 — — — AD-835

80 6 200; 460 95.9 8/29/2001 5 — 70 AD-836

91 6 111; 220; 330 68.6 8/15/2001 3.3 .01 75 AD-837

40 6 144; 164; 240 58 8/15/2001 8 .04 20 AD-838

63 6 120; 140; 220 47.8 8/15/2001 10 .11 50 AD-839

— 6 — 4.2 8/29/2001 — — — AD-840

40 6 160; 210 6.85 8/29/2001 8 — 20 AD-841

40 6 105; 240 2.72 1/29/2002 3 .02 20 AD-842

55 6 225 41.7 11/15/2000 4 .03 35 AD-843

40 6 260 53.6 8/15/2001 .5 <.01 20 AD-844

40 6 165 22.4 8/15/2001 25 .36 20 AD-845

62 6 120 1.2 8/15/2001 1 <.01 50 AD-846

54 6 140; 180 40 8/3/1992 8 .1 35 AD-847

42 6 145 43 2/8/1993 3 — 40 AD-848

63 6 100 50 5/1/1995 5 .03 60 AD-849

40 6 140 40 4/9/1994 3 .02 25 AD-850

30 6 300 — — 1 — 24 AD-851

81 6 98; 172 — — 30 — 64 AD-852

63 6 158; 168 40 9/1989 40 .67 54 AD-853

40 6 320 60 10/29/1994 .5 <.01 20 AD-854

40 6 240 60 9/10/1993 3 .01 40 AD-855

30 6 200 25 9/1988 1 .01 20 AD-856

60 6 160; 180 20 3/8/1999 20 .25 50 AD-857

80 6 100; 145 60 7/15/1994 15 .25 70 AD-858

48; 108 6; 4 125; 165 125 11/30/1990 13 .52 48 AD-859

21 6 80; 125; 165; 225 70 8/1989 8 .09 10 AD-860

51 6 61; 112; 165 22 5/1995 7 — 60 AD-861

60 6 260; 320 40 10/1/1993 1 <.01 50 AD-862

40 6 200; 430 116 5/19/1999 1 <.01 20 AD-863

47 6 300; 360 60 9/24/1998 1 <.01 40 AD-864

Table 4. Records of selected wells and springs, Borough of Carroll Valley, Adams County,

Pennsylvania—Continued

Casing Depth(s) to

water-producing

zone(s)

(feet)

Static water

level

(feet below

land surface)

Date water

level

measured

Driller

reported

yield

(gal/min)

Specific

capacity

(gal/min)/ft

Depth

to

bedrock

(feet)

USGS well

identification

number Length

(feet)

Diameter

(inches)
50

AD-865 394446 0772326 Alexander 11/5/1992 800 S 000MBSL 200

AD-866 394441 0772322 Alexander 2/1988 880 H 000MBSL 475

AD-867 394441 0772321 Alexander 10/27/1998 875 H 000MBSL 600

AD-868 394440 0772318 Alexander 11/1984 850 S 000MBSL 250

AD-869 394440 0772318 Alexander 11/1984 850 S 000MBSL 250

AD-870 394441 0772246 L. Adams 8/11/1994 640 S 000MBSL 250

AD-871 394439 0772254 Alexander 2/21/1997 670 S 000MBSL 260

AD-872 394439 0772257 Alexander 8/1989 675 S 000MTRL 120

AD-873 394439 0772301 Alexander 9/24/1991 680 S 000MTRL 325

AD-874 394436 0772316 Alexander 4/15/2001 850 S 000MTRL 600

AD-875 394436 0772259 Alexander 8/1990 805 S 000MTRL 330

AD-876 394438 0772243 L. Adams 2/1/1994 675 S 000MBSL 300

AD-877 394435 0772300 Alexander 7/25/1996 750 S 000MTRL 300

AD-878 394434 0772303 Alexander 9/20/1994 720 W 000MTRL 300

AD-879 394431 0772251 Alexander 11/1990 800 H 000MBSL 530

AD-880 394429 0772248 Alexander 2/23/1993 790 H 000MBSL 400

AD-881 394427 0772241 Alexander 5/9/1992 740 S 000MBSL 265

AD-882 394432 0772236 Alexander 9/1989 670 S 000MTRL 300

AD-883 394433 0772324 Alexander 11/10/1998 840 S 000GRNS 320

AD-884 394431 0772324 Alexander 10/28/1998 820 S 000GRNS 600

AD-885 394436 0772318 Kohler 11/21/1997 840 S 000MBSL 400

AD-886 394433 0772318 Alexander 3/13/1998 810 S 000MBSL 360

AD-887 394424 0772319 Alexander 1/7/1997 700 S 000MBSL 260

AD-888 394423 0772337 Reichart 6/28/1995 640 W 000MBSL 500

AD-889 394421 0772338 Alexander 3/3/1993 610 W 000GRNS 405

AD-890 394426 0772336 Alexander 5/1989 660 W 000MBSL 535

AD-891 394427 0772336 Alexander 8/6/1997 690 S 000MBSL 460

AD-892 394436 0772325 Alexander 5/17/2000 850 S 000MBSL 750

AD-893 394435 0772327 Alexander 10/7/1995 825 S 000MBSL 600

AD-894 394429 0772331 Alexander 12/1988 730 S 000MBSL 535

AD-895 394426 0772329 Alexander 9/12/1995 740 S 000MBSL 400

AD-896 394427 0772324 Alexander 11/9/1998 790 S 000MBSL 400

AD-897 394539 0772333 Alexander 5/1989 740 S 000MBSL 250

AD-898 394533 0772340 Alexander 4/25/1991 800 S 000MBSL 425

AD-899 394533 0772349 Alexander 5/1988 840 S 000MBSL 145

AD-900 394536 0772348 Alexander 9/1989 840 S 000MBSL 105

AD-901 394544 0772346 L. Adams 4/1989 830 S 000MBSL 125

AD-902 394547 0772345 Alexander 10/16/1992 840 S 000MBSL 260

AD-903 394548 0772345 Alexander 8/6/1996 840 S 377LUDN 120

AD-904 394551 0772343 Alexander 6/1988 850 S 377LUDN 145

AD-905 394551 0772341 Alexander 4/3/2000 840 S 377LUDN 160

AD-906 394556 0772339 Alexander 11/19/1997 800 S 377WVRN 200

AD-907 394550 0772340 Alexander 12/1989 820 S 000MBSL 85

AD-908 394426 0772415 Alexander 11/1987 620 W 000GRNS 380

AD-909 394434 0772434 Alexander 6/10/1996 660 S 000MBSL 660

Table 4. Records of selected wells and springs, Borough of Carroll Valley, Adams County,

Pennsylvania—Continued

USGS well

identification

number

Location

Driller Date

completed

Altitude

of land

surface

(feet)

Topographic

setting

Hydrogeologic

unit

Depth

of well

Latitude Longitude (feet)
51

52 6 120; 182 60 11/5/1992 12 0.15 40 AD-865

21 6 230; 300 25 2/1988 2.5 .01 5 AD-866

20 6 360 200 10/27/1998 .92 <.01 — AD-867

25 6 60; 70 30 11/1984 .5 <.01 10 AD-868

23 6 60; 70; 130 30 11/1984 1 .01 16 AD-869

60 6 240 50 8/11/1994 1.5 — 60 AD-870

63 6 90; 240 60 2/21/1997 3 .02 50 AD-871

46 6 90 15 8/1989 12 .2 40 AD-872

42 6 60; 81 40 9/24/1991 2 .01 31 AD-873

40 6 — 280 4/15/1994 .03 <.01 20 AD-874

40 6 110 20 8/1990 2 .01 30 AD-875

42 6 285 45 2/1/1994 4 .02 30 AD-876

21 6 150; 260 40 7/25/1996 5 .03 10 AD-877

30 6 80; 140 40 9/20/1994 3 .02 30 AD-878

21 6 — 90 11/1990 .3 <.01 8 AD-879

20 6 200 40 2/23/1993 .75 <.01 10 AD-880

60 6 140; 240 50 5/9/1992 8 .06 45 AD-881

21 6 — — — .14 <.01 12 AD-882

20 6 100 110 11/10/1998 .25 <.01 — AD-883

20 6 300 200 10/28/1998 .1 <.01 — AD-884

32 6 168 50 11/21/1997 .75 <.01 18 AD-885

54 6 115; 260 40 3/13/1998 2 .01 40 AD-886

21 6 230 30 1/7/1997 6 .09 4 AD-887

33 6 139; 473 20 6/28/1995 4 — 14 AD-888

— 6 — 30 3/3/1993 1.5 <.01 — AD-889

68 6 515 40 5/1989 1 <.01 62 AD-890

60 6 420 20 8/6/1997 1 <.01 50 AD-891

40 6 140; 340; 500 78 5/20/2000 2 <.01 10 AD-892

— 6 — — — .25 <.01 — AD-893

25 6 200; 505 100 12/1988 4 .02 20 AD-894

20 6 290 60 9/12/1995 .75 <.01 6 AD-895

20 6 310 200 11/9/1998 6 .12 5 AD-896

21 6 140 20 5/1989 3 .02 0 AD-897

40 6 400 10 4/25/1991 2.5 .01 10 AD-898

44 6 65; 110 15 5/1988 15 .23 38 AD-899

42 6 50; 80; 90 20 9/1989 150 7.5 30 AD-900

115 6 120 10 4/1989 45 .9 110 AD-901

88 6 200 15 10/16/1992 3 .02 77 AD-902

84 6 90 30 8/6/1996 30 .86 108 AD-903

90 6 120 20 6/1988 18 .45 85 AD-904

74 6 115; 140 30 4/3/2000 20 .4 63 AD-905

52 6 135 20 11/19/1997 3 .02 40 AD-906

43 6 50; 65 21 12/1989 60 6.67 35 AD-907

40 6 160; 180 30 11/1987 2 <.01 30 AD-908

40 6 200 55 6/10/1996 2 .01 25 AD-909

Table 4. Records of selected wells and springs, Borough of Carroll Valley, Adams County,

Pennsylvania—Continued

Casing Depth(s) to

water-producing

zone(s)

(feet)

Static water

level

(feet below

land surface)

Date water

level

measured

Driller

reported

yield

(gal/min)

Specific

capacity

(gal/min)/ft

Depth

to

bedrock

(feet)

USGS well

identification

number Length

(feet)

Diameter

(inches)
52

AD-910 394439 0772437 Alexander 10/1988 690 S 000MBSL 210

AD-911 394444 0772438 Alexander 3/30/2000 720 S 000MBSL 650

AD-912 394450 0772432 Alexander 7/18/1997 750 S 000MBSL 380

AD-913 394451 0772432 Alexander 5/1/1996 760 S 000MBSL 360

AD-914 394452 0772430 Alexander 5/29/1997 770 S 000MBSL 460

AD-915 394446 0772431 Alexander 8/1989 760 S 377LUDN 430

AD-916 394436 0772425 Alexander 5/24/1996 750 W 000MBSL 600

AD-917 394437 0772433 Alexander 8/1990 690 S 377LUDN 275

AD-918 394436 0772422 Alexander 10/5/1996 700 W 000MBSL 220

AD-919 394434 0772422 Alexander 2/12/1997 680 W 000MBSL 240

AD-920 394430 0772422 Alexander 5/1990 750 S 000MBSL 280

AD-921 394429 0772418 Alexander 11/2/1998 650 S 000GRNS 380

AD-922 394432 0772418 Alexander 9/18/1995 670 S 000GRNS 400

AD-923 394432 0772420 Alexander 11/1989 680 S 000GRNS 312

AD-924 394435 0772420 Alexander 10/24/1995 700 S 000GRNS 300

AD-925 394435 0772418 Alexander 5/1990 700 S 000GRNS 292

AD-926 394437 0772423 Alexander 3/10/1998 750 W 000MBSL 200

AD-927 394439 0772421 Alexander 11/6/1995 750 W 000GRNS 280

AD-928 394439 0772416 Alexander 6/12/1996 750 S 000MBSL 225

AD-929 394432 0772412 Reichart 4/22/1992 660 W 000MBSL 175

AD-930 394444 0772422 Reichart 1/7/1993 820 S 000MBSL 200

AD-931 394448 0772427 Alexander 11/1989 820 S 377LUDN 470

AD-932 394452 0772429 Alexander 8/11/1995 780 S 000MBSL 300

AD-933 394456 0772425 J.F. Harrison 3/16/2000 830 S 000GRNS 623

AD-934 394418 0772231 Harley 6/27/2000 660 S 000MTRL 225

AD-936 394421 0772248 Alexander 6/3/1996 730 S 000MBSL 200

AD-937 394424 0772245 Alexander 12/24/1997 760 H 000MBSL 300

AD-938 394426 0772241 Alexander 4/1988 750 S 000MBSL 165

AD-939 394426 0772244 Reichart 9/1989 770 H 000MBSL 175

AD-940 394426 0772246 Alexander 12/23/1997 770 H 000MBSL 140

AD-941 394424 0772248 J.F. Harrison 1/1991 750 S 000MTRL 373

AD-942 394429 0772309 Alexander 9/11/1997 770 S 000MTRL 400

AD-943 394423 0772300 Alexander 9/16/1996 750 S 000MBSL 240

AD-944 394423 0772254 Alexander 10/28/1996 710 W 000MBSL 380

AD-945 394424 0772256 Alexander 5/25/1991 740 S 000MBSL 370

AD-946 394424 0772253 Alexander 8/28/1997 720 W 000MBSL 340

AD-947 394426 0772250 Alexander 12/1989 750 W 000MBSL 550

AD-948 394427 0772247 Reichart 9/1990 770 H 000MBSL 500

AD-949 394427 0772247 Reichart 10/1990 770 H 000MBSL 175

AD-950 394428 0772250 Alexander 11/15/1996 780 H 000GRNS 620

AD-951 394429 0772254 Alexander 1/1986 810 H 000MBSL 410

AD-952 394430 0772259 Alexander 6/20/1998 820 H 000MTRL 500

AD-953 394430 0772300 Alexander 6/18/1998 820 H 000MTRL 500

AD-955 394502 0772417 Alexander 8/3/1996 900 S 000GRNS 620

AD-956 394501 0772415 Alexander 9/14/2000 895 H 000MBSL 640

Table 4. Records of selected wells and springs, Borough of Carroll Valley, Adams County,

Pennsylvania—Continued

USGS well

identification

number

Location

Driller Date

completed

Altitude

of land

surface

(feet)

Topographic

setting

Hydrogeologic

unit

Depth

of well

Latitude Longitude (feet)
53

42 6 — 40 10/1988 4 0.03 35 AD-910

40 6 200; 430 32 3/30/2000 3.75 .02 25 AD-911

48 6 340; 360 80 7/18/1997 30 .3 35 AD-912

60 6 330 60 5/1/1996 8 .06 45 AD-913

65 6 445 60 5/29/1997 60 1 55 AD-914

63 6 200; 400 40 8/1989 6 .05 57 AD-915

42 6 560 60 5/24/1996 2 <.01 30 AD-916

25 6 105 55 8/1990 1 .01 15 AD-917

42 6 205 40 10/5/1996 30 .6 28 AD-918

43 6 225 60 2/12/1997 7 .06 27 AD-919

41 6 265 30 5/1990 12 .4 34 AD-920

40 6 360 60 11/2/1998 8 .06 20 AD-921

40 6 265 60 9/18/1995 1 <.01 25 AD-922

21 6 260; 280 50 11/1989 2 .01 14 AD-923

40 6 240; 255 40 10/24/1995 5 .03 25 AD-924

40 6 260 40 5/1990 3 .04 32 AD-925

42 6 110; 180 20 3/10/1998 9 .11 30 AD-926

63 6 105; 255 40 11/6/1995 1.5 .01 50 AD-927

21 6 155 50 6/12/1996 2 .02 8 AD-928

21 6 41; 55; 75 5 4/22/1992 6 — 6 AD-929

21 6 57; 85 33 1/7/1993 5 — 8 AD-930

21 6 450 140 11/1989 4 .03 10 AD-931

60 6 270 60 8/11/1995 20 .67 50 AD-932

80 6 430 146 3/16/2000 1.5 .02 59 AD-933

53 6 210 80 6/27/2000 20 — 45 AD-934

42 6 80; 100 60 6/3/1996 5 .05 20 AD-936

40 6 200; 260 40 12/24/1997 1.5 .01 30 AD-937

21 6 140 20 4/1988 12 .15 10 AD-938

21 6 91; 114; 140 48 9/1989 12 — 4 AD-939

40 6 110; 120 60 12/23/1997 12 .25 30 AD-940

40 6 338; 370 80 1/1991 5 .02 18 AD-941

40 6 200; 330 40 9/11/1997 4 .03 10 AD-942

20 6 200 40 9/16/1996 3 .02 10 AD-943

21 6 160 40 10/28/1996 .5 <.01 5 AD-944

27 6 260 40 5/25/1991 1 <.01 15 AD-945

23 6 150 50 8/28/1997 1 <.01 1 AD-946

21 6 21 80 12/1989 .23 <.01 16 AD-947

21 6 55; 432 130 9/1990 1.25 — 13 AD-948

21 6 44; 69; 107; 142 35 10/1990 6.5 — 9 AD-949

27 6 — 60 11/15/1996 .33 <.01 10 AD-950

21 6 260 100 1/1986 .5 <.01 5 AD-951

28 6 260 100 6/20/1998 1 <.01 10 AD-952

48 6 300 100 6/18/1998 1 <.01 35 AD-953

21 6 300 60 8/3/1996 .33 <.01 5 AD-955

40 6 210; 350 76.4 8/15/2001 1.3 <.01 20 AD-956

Table 4. Records of selected wells and springs, Borough of Carroll Valley, Adams County,

Pennsylvania—Continued

Casing Depth(s) to

water-producing

zone(s)

(feet)

Static water

level

(feet below

land surface)

Date water

level

measured

Driller

reported

yield

(gal/min)

Specific

capacity

(gal/min)/ft

Depth

to

bedrock

(feet)

USGS well

identification

number Length

(feet)

Diameter

(inches)
54

AD-957 394459 0772417 Alexander 6/26/1996 880 H 000MBSL 600

AD-958 394458 0772418 Alexander 6/1987 880 H 000MBSL 515

AD-959 394453 0772417 Alexander 9/10/1996 830 S 000MBSL 200

AD-960 394448 0772418 Alexander 3/11/1998 850 S 000MBSL 240

AD-961 394448 0772419 Alexander 2/15/1996 860 S 000MBSL 200

AD-962 394446 0772420 Alexander 2/22/2000 840 S 000MBSL 500

AD-963 394444 0772420 Alexander 5/1990 820 S 000MBSL 330

AD-964 394443 0772421 Alexander 4/4/1991 800 W 000MBSL 305

AD-965 394442 0772421 Alexander 4/3/1991 790 S 000MBSL 260

AD-966 394441 0772422 Alexander 11/1990 770 W 000MBSL 300

AD-967 394441 0772419 Alexander 4/10/1992 780 S 000GRNS 200

AD-968 394443 0772415 Alexander 4/12/1996 760 S 000MBSL 400

AD-969 394446 0772406 Alexander 6/4/1998 750 S 000MBSL 400

AD-970 394448 0772406 Alexander 6/1986 770 S 000MBSL 395

AD-971 394454 0772406 Alexander 9/10/1991 770 W 000GRNS 265

AD-972 394504 0772405 Alexander 1/1990 850 S 000MBSL 450

AD-973 394502.4 0772402.1 — 2000 880 S 000MBSL —

AD-974 394500 0772401 Alexander 8/13/1999 880 S 000MBSL 240

AD-975 394454 0772402 Alexander 10/24/1995 790 S 000MBSL 200

AD-976 394451 0772403 L. Adams 3/28/1997 780 S 000MBSL 175

AD-977 394449 0772402 Alexander 6/5/1995 800 S 000MBSL 220

AD-978 394440 0772403 Alexander 7/24/1997 810 S 000MBSL 500

AD-979 394438 0772400 Alexander 7/1990 820 S 000MBSL 350

AD-980 394442 0772354 J.F. Harrison 6/26/1996 840 S 000MBSL 298

AD-981 394444 0772352 Alexander 6/11/1997 860 S 000MBSL 340

AD-982 394445 0772356 Alexander 7/1/1996 870 H 000GRNS 400

AD-983 394442 0772357 Alexander 2/15/1991 860 S 000MBSL 205

AD-984 394441 0772359 Alexander 8/24/1995 840 S 000MBSL 240

AD-985 394446 0772358 Alexander 9/18/1991 850 S 000GRNS 400

AD-986 394446 0772358 Alexander 4/6/2001 850 S 000GRNS 300

AD-987 394450 0772356 Alexander 4/12/2000 850 S 000MBSL 260

AD-988 394446 0772347 Alexander 7/1990 860 H 000MBSL 465

AD-989 394444 0772344 Alexander 2/1990 860 H 000MBSL 270

AD-990 394444 0772340 Alexander 4/22/1992 880 H 000MBSL 200

AD-991 394444 0772341 Alexander 1/14/1997 880 H 000MBSL 500

AD-992 394443 0772339 Alexander 1/11/1997 880 H 000MBSL 500

AD-993 394442 0772339 Alexander 1/21/1998 880 H 000MBSL 400

AD-994 394441 0772333 Alexander 7/1989 850 H 000MBSL 395

AD-995 394458 0772351 Alexander 7/1993 900 H 000MBSL 715

AD-996 394452 0772354 Alexander 8/9/1995 850 S 000MBSL 300

AD-997 394453 0772353 Alexander 4/13/2000 860 S 000MBSL 400

AD-998 394451 0772348 Alexander 10/23/1995 900 H 000GRNS 180

AD-999 394447 0772338 Alexander 3/10/1997 860 H 000MBSL 380

AD-1000 394446 0772336 Alexander 9/29/1992 850 H 000MBSL 400

AD-1001 394448 0772333 Alexander 8/29/1997 810 S 000MBSL 360

Table 4. Records of selected wells and springs, Borough of Carroll Valley, Adams County,

Pennsylvania—Continued

USGS well

identification

number

Location

Driller Date

completed

Altitude

of land

surface

(feet)

Topographic

setting

Hydrogeologic

unit

Depth

of well

Latitude Longitude (feet)
55

31 6 500 60 6/26/1996 0.5 <0.01 15 AD-957

21 6 400 60 6/1987 1 <.01 10 AD-958

61 6 90; 140 50 9/10/1996 5 .07 35 AD-959

80 6 115; 210 30 3/11/1998 6 .03 70 AD-960

42 6 140 30 2/15/1996 15 .15 30 AD-961

40 6 200; 300; 380 40 2/22/2000 1.3 <.01 20 AD-962

29 6 165 40 5/1990 1.5 .01 23 AD-963

21 6 100; 180 20 4/4/1991 2 .01 10 AD-964

22 6 125; 240 25 4/3/1991 8 .06 10 AD-965

21 6 140; 284 — — 5 — 10 AD-966

26 6 140 30 4/10/1992 8 .1 16 AD-967

40 6 210 30 4/12/1996 1 <.01 27 AD-968

40 6 320 62 6/4/1998 1 <.01 5 AD-969

21 6 185; 360 60 6/1986 4 .03 10 AD-970

40 6 180; 240 30 9/10/1991 3 .02 25 AD-971

100 6 — 70 1/1990 1 <.01 90 AD-972

— 6 — 71.3 11/16/2000 — — — AD-973

67 6 190; 220 50 8/13/1999 20 .4 55 AD-974

60 6 75; 179 50 10/24/1995 6 .06 45 AD-975

63 6 135 50 3/28/1997 6.5 .07 55 AD-976

52 6 205 40 6/5/1995 2 .01 41 AD-977

34 6 200; 350 80 7/24/1997 1.5 <.01 20 AD-978

21 6 260 100 7/1990 1 .01 4 AD-979

63 6 123; 264; 282 80 6/26/1996 36 .21 40 AD-980

21 6 260 60 6/11/1997 2.5 .01 5 AD-981

40 6 365 40 7/1/1996 15 .1 25 AD-982

42 6 100; 180 40 2/15/1991 25 .36 20 AD-983

41 6 110; 160 60 8/24/1995 3 .02 30 AD-984

20 6 370 40 9/18/1991 3 .01 10 AD-985

40 6 100 25 4/6/1991 1 <.01 30 AD-986

65 6 110; 180; 250 50 4/12/2000 6 .04 50 AD-987

60 6 60 40 7/1990 1 <.01 50 AD-988

40 6 220; 250 15 2/1990 6 .04 34 AD-989

40 6 80; 115; 180 40 4/22/1992 20 .25 25 AD-990

84 6 130; 380 122.39 8/15/2001 2 .01 70 AD-991

68 6 300; 420 142 1/11/1997 2 .01 55 AD-992

40 6 100; 260 60 1/21/1998 3 .01 10 AD-993

42 6 350 80 7/1989 3 .01 30 AD-994

20 6 265 — — 0 0 6 AD-995

53 6 240 60 8/9/1995 6 .04 40 AD-996

40 6 240; 340 40 4/13/2000 5 .04 25 AD-997

40 6 65; 85 40 10/23/1995 6 .1 15 AD-998

44 6 140; 250 30 3/10/1997 6 .04 30 AD-999

40 6 200 80 9/29/1992 1 <.01 25 AD-1000

60 6 110; 290 45 8/29/1997 2 .01 50 AD-1001

Table 4. Records of selected wells and springs, Borough of Carroll Valley, Adams County,

Pennsylvania—Continued

Casing Depth(s) to

water-producing

zone(s)

(feet)

Static water

level

(feet below

land surface)

Date water

level

measured

Driller

reported

yield

(gal/min)

Specific

capacity

(gal/min)/ft

Depth

to

bedrock

(feet)

USGS well

identification

number Length

(feet)

Diameter

(inches)
56

AD-1002 394448 0772334 Alexander 8/30/1997 820 S 000MBSL 260

AD-1003 394452 0772343 Alexander 12/1984 880 S 000MBSL 189

AD-1004 394455 0772345 Alexander 5/14/1996 900 H 000MBSL 360

AD-1005 394454 0772343 Alexander 5/12/1997 880 S 000GRNS 280

AD-1006 394451 0772336 Alexander 3/26/1996 800 S 000MBSL 380

AD-1007 394523 0772333 Alexander 2/1989 840 S 000MBSL 168

AD-1008 394521 0772328 Alexander 2/26/1999 830 S 000MBSL 500

AD-1009 394519 0772329 Alexander 4/1987 840 S 000MBSL 208

AD-1011 394517 0772343 Alexander 8/1987 900 S 000MBSL 425

AD-1012 394517 0772347 Alexander 3/1989 910 S 000MBSL 250

AD-1013 394512 0772336 Alexander 7/1989 880 S 000GRNS 410

AD-1014 394510 0772359 Alexander 8/17/1991 940 S 000MBSL 345

AD-1015 394508 0772351 Alexander 5/13/1992 950 H 000MBSL 340

AD-1016 394509 0772353 Alexander 9/23/1998 950 H 000MBSL 320

AD-1017 394510 0772356 Alexander 3/16/1992 960 H 000MBSL 260

AD-1018 394511 0772347 Alexander 6/5/1995 970 S 000MBSL 600

AD-1019 394509 0772346 Alexander 11/14/1994 950 H 000MBSL 400

AD-1020 394511 0772343 Alexander 8/1989 930 S 000MBSL 312

AD-1021 394509 0772342 Alexander 10/1989 900 S 000GRNS 205

AD-1022 394506 0772348 Alexander 7/1984 940 H 000GRNS 208

AD-1023 394505 0772350 Kohler 7/7/1999 930 H 000GRNS 400

AD-1024 394504 0772352 Alexander 10/1989 910 S 000GRNS 350

AD-1025 394507 0772400 Alexander 8/1989 910 S 000MBSL 250

AD-1026 394504 0772346 Alexander 2/1989 920 H 000MBSL 250

AD-1027 394502 0772346 J.F. Harrison 1/1989 910 H 000MBSL 261

AD-1028 394500 0772350 Alexander 8/1985 910 H 000MBSL 205

AD-1029 394457 0772342 Alexander 8/1984 880 S 000GRNS 209

AD-1030 394508 0772335 Alexander 5/16/1997 860 S 000MBSL 340

AD-1031 394509 0772333 Alexander 6/25/1996 860 S 000MBSL 380

AD-1032 394514 0772330 Alexander 2/3/1998 840 S 000GRNS 200

AD-1033 394516 0772328 Alexander 8/26/1997 820 S 000GRNS 300

AD-1034 394500 0772337 Alexander 3/1990 810 S 000GRNS 145

AD-1035 394454 0772338 J.F. Harrison 7/6/1989 820 S 000MBSL 517

AD-1036 394506 0772330 Alexander 2/14/1998 800 S 000GRNS 240

AD-1037 394515 0772312 Alexander 11/1990 720 V 000MBSL 290

AD-1038 394513 0772309 Alexander 4/29/1998 720 S 000MBSL 300

AD-1039 394513 0772325 Alexander 2/1/1996 790 S 000MBSL 380

AD-1040 394512 0772323 Alexander 9/9/1998 780 W 000MBSL 140

AD-1041 394512 0772320 Alexander 4/1990 770 W 000MBSL 250

AD-1042 394510 0772310 Alexander 2/25/2000 750 H 000MBSL 600

AD-1043 394509 0772312 Alexander 7/7/1998 760 H 000MBSL 380

AD-1044 394509 0772315 L. Adams 9/1989 770 H 000MBSL 400

AD-1045 394509 0772315 L. Adams 8/1989 770 H 000MBSL 400

AD-1046 394510 0772316 Alexander 11/25/1996 780 H 000MBSL 500

AD-1047 394511 0772324 Alexander 4/1990 790 H 000MBSL 300

Table 4. Records of selected wells and springs, Borough of Carroll Valley, Adams County,

Pennsylvania—Continued

USGS well

identification

number

Location

Driller Date

completed

Altitude

of land

surface

(feet)

Topographic

setting

Hydrogeologic

unit

Depth

of well

Latitude Longitude (feet)
57

40 6 105; 200 50 8/30/1997 1 0.01 30 AD-1002

28 6 40; 140; 170 80 12/1984 10 .2 20 AD-1003

63 6 270 60 5/14/1996 2 .01 52 AD-1004

63 6 180; 260 80 5/12/1997 8 .08 50 AD-1005

40 6 260 10 3/26/1996 1 <.01 28 AD-1006

21 6 45; 90; 145 20 2/1989 10 .25 10 AD-1007

40 6 450 89 2/26/1999 1.5 .01 10 AD-1008

27 6 40; 130 20 4/1987 8 .06 21 AD-1009

42 6 400 60 8/1987 50 .36 35 AD-1011

74 6 80; 170; 230 40 3/1989 6 .05 68 AD-1012

35 6 200 60 7/1989 .5 <.01 30 AD-1013

40 6 140; 200 40 8/17/1991 2 .01 25 AD-1014

40 6 223; 325 40 5/13/1992 4 .02 28 AD-1015

60 6 140; 290 50 9/23/1998 6 .04 50 AD-1016

52 6 100; 150; 240 50 3/16/1992 15 .15 35 AD-1017

40 6 — 50 6/5/1995 .2 <.01 3 AD-1018

40 6 140 50 11/14/1994 1 <.01 30 AD-1019

63 6 280 40 8/1989 3 .02 58 AD-1020

22 6 185 30 10/1989 6 .05 15 AD-1021

21 6 60; 160; 180 35 7/1984 3 .12 7 AD-1022

42 6 285 116 7/7/1999 2.4 .01 28 AD-1023

23 6 280 60 10/1989 2 .01 16 AD-1024

42 6 150; 200 35 8/1980 4 .03 36 AD-1025

21 6 160; 230 20 2/1989 12 .12 5 AD-1026

60 6 97; 184; 237 — — 12 — 48 AD-1027

60 6 165 30 8/1985 10 .14 50 AD-1028

69 6 75; 160; 180 70 7/1984 4.5 .15 60 AD-1029

21 6 140 30 5/16/1997 2 .01 5 AD-1030

60 6 260 40 6/25/1996 4 .03 45 AD-1031

40 6 130; 180 20 2/3/1998 6 .08 10 AD-1032

45 6 130; 200 30 8/26/1997 4 .03 30 AD-1033

73 6 115 20 3/1990 15 .25 58 AD-1034

82 6 370; 465 50 7/6/1989 1.5 <.01 73 AD-1035

40 6 120; 190 20 2/14/1998 4 .05 30 AD-1036

25 6 119; 169 5 11/1990 8 .07 10 AD-1037

41 6 130; 190 40 4/29/1998 2 .01 30 AD-1038

59 6 85; 310 5 2/1/1996 2 .01 49 AD-1039

40 6 110; 130 30 9/9/1998 15 .25 28 AD-1040

36 6 37; 65; 200; 225 20 4/1990 15 .3 31 AD-1041

73 6 565 30 2/25/2000 1.9 .01 60 AD-1042

40 6 130 30 7/7/1998 1 <.01 30 AD-1043

40 6 50 20 9/1989 .5 <.01 30 AD-1044

40 6 125 45 8/1989 .5 <.01 20 AD-1045

21 6 300 24 11/25/1996 .5 <.01 1 AD-1046

40 6 230 40 4/1990 .5 <.01 33 AD-1047

Table 4. Records of selected wells and springs, Borough of Carroll Valley, Adams County,

Pennsylvania—Continued

Casing Depth(s) to

water-producing

zone(s)

(feet)

Static water

level

(feet below

land surface)

Date water

level

measured

Driller

reported

yield

(gal/min)

Specific

capacity

(gal/min)/ft

Depth

to

bedrock

(feet)

USGS well

identification

number Length

(feet)

Diameter

(inches)
58

AD-1048 394507 0772320 Alexander 2/23/1996 780 H 000MBSL 140

AD-1049 394506 0772317 L. Adams 11/15/1996 780 H 000MBSL 500

AD-1050 394506 0772315 Alexander 12/22/1995 780 H 000MBSL 300

AD-1051 394505 0772319 Alexander 11/5/1998 770 H 000MBSL 300

AD-1052 394507 0772326 Alexander 7/10/1995 780 H 000MBSL 160

AD-1053 394502 0772320 C. Jones 5/1986 760 H 000MBSL 205

AD-1054 394457 0772315 Alexander 5/15/1996 720 S 000MBSL 580

AD-1055 394457 0772317 Alexander 10/3/1997 720 S 000MBSL 180

AD-1056 394500 0772321 Alexander 8/31/1994 740 H 000MBSL 100

AD-1057 394456 0772320 Alexander 10/3/1996 710 S 000MBSL 180

AD-1058 394455 0772326 Alexander 7/1990 740 S 000GRNS 475

AD-1060 394448 0772400 Alexander 6/15/2001 820 S 000MBSL 320

AD-1061 394446 0772355 Alexander 6/18/2001 880 H 000GRNS 600

AD-1062 394442 0772336 Negley 8/2000 870 H 000MBSL 273

AD-1063 394533 0772346 Alexander 8/2001 810 W 000MBSL 700

AD-1064 394425 0772224 Alexander 3/18/1999 530 S 000MTRL 220

AD-1065 394438 0772248 Alexander 5/4/1994 690 S 000MBSL 320

AD-1066 394435 0772310 Alexander 1/12/1994 760 W 000MTRL 320

AD-1067 394418 0772318 Alexander 5/1989 590 S 000MBSL 535

AD-1074 394429 0772247 Alexander 2/23/1993 750 H 000MBSL 400

AD-1075 394435 0772324 Alexander 11/11/1999 830 S 000GRNS 300

AD-1076 394432 0772319 — 1968 790 S 000MBSL 610

AD-1077 394430 0772317 Keyser 1972 780 S 000MBSL 302

AD-1078 394422 0772335 Keyser 1968 640 S 000MBSL 190

AD-1079 394420 0772339 Alexander 10/1/1994 610 S 000GRNS 400

AD-1080 394426 0772339 Keyser 1968 670 W 000GRNS 300

AD-1081 394426 0772334 — 11/3/1994 700 S 000MBSL 400

AD-1082 394436 0772332 L. Adams 5/31/1994 820 S 000GRNS 250

AD-1083 394431 0772328 Eichelberger 12/2/1998 820 S 000MBSL 625

AD-1084 394545 0772339 L. Adams 5/12/1995 780 S 000MBSL 200

AD-1085 394544 0772333 Keyser 1968 750 S 000MBSL 280

AD-1086 394435 0772435 Alexander 3/17/1995 670 S 000MBSL 560

AD-1087 394436 0772432 Reichart 4/5/1996 690 S 377LUDN 400

AD-1088 394435 0772423 Alexander 2/14/1995 690 W 000MBSL 220

AD-1089 394433 0772418 Alexander 6/2/1999 690 S 000GRNS 320

AD-1090 394436 0772418 L. Adams 2/7/1996 730 S 000GRNS 250

AD-1091 394438 0772417 Alexander 6/1/1999 750 S 000GRNS 500

AD-1092 394453 0772429 Alexander 6/26/2001 780 S 000MBSL 340

AD-1093 394418 0772239 Alexander 7/1/1994 710 S 000MTRL 260

AD-1094 394414 0772228 C. Barber 5/13/996 640 S 000MTRL 150

AD-1095 394414 0772226 C. Barber 5/10/1996 620 S 000MTRL 150

AD-1096 394412 0772228 L. Adams 5/6/1992 600 S 000MTRL 100

AD-1097 394423 0772250 L. Adams 3/10/993 730 S 000MBSL 400

AD-1098 394420 0772259 Alexander 4/6/1999 720 S 000MBSL 300

AD-1099 394421 0772301 Alexander 4/9/1999 750 S 000MBSL 510

Table 4. Records of selected wells and springs, Borough of Carroll Valley, Adams County,

Pennsylvania—Continued

USGS well

identification

number

Location

Driller Date

completed

Altitude

of land

surface

(feet)

Topographic

setting

Hydrogeologic

unit

Depth

of well

Latitude Longitude (feet)
59

42 6 58; 90; 130 20 2/23/1996 8 0.13 30 AD-1048

100 6 125; 400 50 11/15/1996 2 .04 75 AD-1049

25 6 240 — — 2 — 14 AD-1050

28 6 90; 245 20 11/5/1998 3 .02 18 AD-1051

42; 155 6; 4 70; 110 20 7/10/1995 12 .3 32 AD-1052

21 6 165 15 5/1986 10 .12 10 AD-1053

21 6 106; 360 20 5/15/1996 4 .02 2 AD-1054

20 6 108; 170 30 10/3/1997 30 1 3 AD-1055

29 6 80 20 8/31/1994 6 .12 17 AD-1056

41 6 76; 150 10 10/3/1996 6 .07 30 AD-1057

30 6 425 40 7/1990 .5 <.01 20 AD-1058

41 6 120; 280; 40 6/15/2001 12 .07 10 AD-1060

42 6 130; 330 93 6/18/2001 2.14 .01 5 AD-1061

63 6 — 182 8/15/2001 10 — — AD-1062

40 6 400 43 9/5/2001 0 0 5 AD-1063

77 6 110; 180 40 3/18/1999 6 — 65 AD-1064

20 6 100; 140; 240 60 5/4/1994 3 .02 8 AD-1065

20 6 240 80 1/12/1994 1.5 .01 8 AD-1066

68 6 515 40 5/1989 1 <.01 62 AD-1067

20 6 200 40 2/23/1993 .75 <.01 10 AD-1074

— 6 150; 160 80 11/11/1999 2 .03 — AD-1075

17 6 150 100 1968 0 0 7 AD-1076

29 6 93; 248 47 1972 3 — 28 AD-1077

23 6 73; 108; 178 25 1968 6 — 13 AD-1078

40 6 360 40 10/1/1994 2 .01 30 AD-1079

41 6 78 60 1968 1 — 30 AD-1080

60 6 240 50 11/3/1994 1 — 50 AD-1081

60 6 242 40 5/31/1994 25 — 55 AD-1082

40 6 434; 487 5 12/2/1998 1.5 — — AD-1083

70 6 165 50 5/12/1995 6 — 60 AD-1084

21 6 240 35 1968 2 — 10 AD-1085

29 6 460; 530 40 3/17/1995 3.5 .01 19 AD-1086

21 6 72; 245; 332 60 4/5/1996 2 — 7 AD-1087

40 6 205 80 2/14/2001 50 .63 28 AD-1088

40 6 305 80 6/2/1999 20 — 20 AD-1089

65 6 240 75 2/7/1996 20 — 60 AD-1090

40 6 420; 460 97 6/1/1999 3.3 .01 20 AD-1091

60 6 295; 298 131 6/26/2001 8 .12 40 AD-1092

60 6 65; 75 50 7/1/1994 2 .01 50 AD-1093

87 6 90; 115 65 5/13/1996 20 — 75 AD-1094

89 6 118 65 5/10/1996 20 — 77 AD-1095

50 6 80; 89 40 5/6/1992 20 — 40 AD-1096

48 6 150 50 3/10/1993 1.5 — 40 AD-1097

20 6 160; 240; 260 60 4/6/1999 1.5 <.01 3 AD-1098

20 6 450 129 4/9/1999 1 <.01 2 AD-1099

Table 4. Records of selected wells and springs, Borough of Carroll Valley, Adams County,

Pennsylvania—Continued

Casing Depth(s) to

water-producing

zone(s)

(feet)

Static water

level

(feet below

land surface)

Date water

level

measured

Driller

reported

yield

(gal/min)

Specific

capacity

(gal/min)/ft

Depth

to

bedrock

(feet)

USGS well

identification

number Length

(feet)

Diameter

(inches)
60

AD-1100 394426 0772310 L. Adams 5/1/1992 720 S 000MTRL 300

AD-1101 394422 0772258 Alexander 7/26/1995 740 S 000MBSL 300

AD-1102 394424 0772257 L. Adams 10/6/1992 760 S 000MBSL 350

AD-1103 394428 0772303 Alexander 5/25/1995 800 H 000MBSL 521

AD-1104 394427 0772256 L. Adams 3/1/1994 790 H 000MBSL 300

AD-1105 394454 0772420 L. Adams 10/11/1991 880 H 000MBSL 300

AD-1106 394445 0772406 Alexander 9/4/2001 770 S 000GRNS 560

AD-1107 394502 0772401 Kohler 4/28/1995 880 S 000MBSL 225

AD-1108 394502 0772405 Alexander 1/13/1995 860 S 000MBSL 260

AD-1109 394454 0772358 Alexander 5/19/1995 820 S 000MBSL 300

AD-1110 394453 0772359 Alexander 11/3/1994 810 S 000MBSL 380

AD-1111 394449 0772403 Alexander 3/25/1995 790 S 000MBSL 280

AD-1112 394451 0772358 Alexander 4/12/2000 810 S 000MBSL 260

AD-1113 394437 0772358 Alexander 3/8/1999 820 S 000MBSL 520

AD-1114 394437 0772358 Alexander 7/22/1999 820 S 000MBSL 500

AD-1115 394442 0772355 Alexander 3/15/1994 840 S 000MBSL 400

AD-1116 394447 0772355 L. Adams 1/16/1995 890 H 000GRNS 300

AD-1117 394442 0772401 L. Adams 2/9/1993 820 S 000MBSL 175

AD-1118 394448 0772357 Alexander 5/19/1993 860 S 000MBSL 400

AD-1119 394449 0772356 Alexander 9/14/1995 860 S 000MBSL 460

AD-1120 394441 0772335 Alexander 4/12/1999 860 H 000MBSL 360

AD-1121 394453 0772352 Alexander 5/3/1995 870 H 000MBSL 260

AD-1122 394449 0772343 L. Adams 4/28/1993 890 H 000MBSL 300

AD-1123 394458 0772351 Alexander 8/18/1993 900 H 000MBSL 300

AD-1124 394457 0772350 Alexander 8/22/1993 910 H 000MBSL 320

AD-1125 394519 0772350 Alexander 11/21/1997 940 S 000MBSL 360

AD-1126 394514 0772354 Alexander 8/1985 980 H 000MBSL 205

AD-1127 394511 0772359 Keyser 1972 960 H 000MBSL 320

AD-1128 394507 0772355 Alexander 9/6/1994 940 H 000MBSL 400

AD-1129 394509 0772403 Alexander 12/28/1994 920 S 000MBSL 400

AD-1130 394503 0772357 Alexander 4/28/1993 890 W 000MBSL 280

AD-1131 394517 0772330 Alexander 10/30/2001 850 S 000GRNS 400

AD-1132 394509 0772331 Abbots 11/8/1991 840 S 000MBSL 305

AD-1133 394509 0772328 L. Adams 4/5/1995 820 S 000MBSL 175

AD-1134 394512 0772309 Alexander 9/1/1999 720 S 000MBSL 380

AD-1135 394510 0772312 Alexander 8/31/1999 760 H 000MBSL 600

AD-1136 394509 0772319 Alexander 6/13/2000 780 H 000MBSL 600

AD-1137 394503 0772323 Alexander 2/7/1995 760 H 000MBSL 400

AD-1138 394459 0772312 Alexander 10/11/1993 740 S 000MBSL 500

AD-1139 394456 0772312 Alexander 9/17/1994 700 S 000MBSL 560

AD-1140 394458 0772320 L. Adams 5/4/1992 730 S 000MBSL 125

AD-1141 394459 0772320 Alexander 9/16/1994 740 H 000MBSL 160

AD-1142 394459 0772327 Alexander 3/30/1994 770 S 000MBSL 220

AD-1143 394500 0772329 Alexander 4/1987 780 W 000MBSL 100

AD-1144 394456 0772329 Keyser 1972 790 H 000MBSL 402

Table 4. Records of selected wells and springs, Borough of Carroll Valley, Adams County,

Pennsylvania—Continued

USGS well

identification

number

Location

Driller Date

completed

Altitude

of land

surface

(feet)

Topographic

setting

Hydrogeologic

unit

Depth

of well

Latitude Longitude (feet)
61

40 6 80; 270 45 5/1/1992 3 — 30 AD-1100

42 6 170 30 7/26/1995 2.5 — 40 AD-1101

40 6 190 45 10/6/1992 2 — 33 AD-1102

44 6 251 50 5/25/1995 1 — 25 AD-1103

40 6 100 40 3/1/1994 1 — 35 AD-1104

60 6 110; 230 30 10/11/1991 2 — 50 AD-1105

40 6 260; 460; 520 30 9/4/2001 1.33 <0.01 20 AD-1106

80 6 111; 210 62 4/28/1995 5 — 62 AD-1107

40 6 140; 200 70 1/13/1995 3 — 28 AD-1108

40 6 190 50 5/19/1995 1.1 <.01 28 AD-1109

27 6 340; 350 60 11/3/1994 7 .05 17 AD-1110

60 6 200; 255 60 3/25/1995 2.5 .02 45 AD-1111

65 6 110; 180; 250 50 4/12/2000 6 — 50 AD-1112

40 6 300 34 3/8/1999 .52 <.01 20 AD-1113

40 6 195; 367 62 7/22/1999 .54 <.01 20 AD-1114

43 6 300 40 3/15/1994 3 — 20 AD-1115

55 6 155 50 1/16/1995 1 — 50 AD-1116

44 6 165 40 2/9/1993 20 — 40 AD-1117

30 6 100; 330 80 5/19/1993 .75 <.01 20 AD-1118

42 6 265 60 9/14/1995 .75 <.01 25 AD-1119

40 6 305 170 4/12/1999 8 .27 20 AD-1120

60 6 120; 243 50 5/3/1995 4 .03 50 AD-1121

40 6 265 50 4/28/1993 3.5 — 36 AD-1122

20 6 160; 230; 285 60 8/18/1993 5 .04 8 AD-1123

20 6 240; 305 65 8/22/1993 10 .07 10 AD-1124

60 6 190; 285 60 11/21/1997 3 .02 50 AD-1125

60 6 165 30 8/1985 10 .14 50 AD-1126

34 6 285 65.5 11/6/2000 4 — 33 AD-1127

60 6 250 48 9/6/1994 1 <.01 45 AD-1128

40 6 160; 380 80 12/28/1994 4 .02 28 AD-1129

40 6 200; 230; 245 40 4/28/1993 5 .04 30 AD-1130

40 6 290 40 10/30/2001 5 .02 20 AD-1131

60 6 — 72 11/8/1991 5 — 50 AD-1132

60 6 165 50 4/5/1995 5 — 56 AD-1133

43 6 300 12 9/1/1999 2.1 — 30 AD-1134

54 6 300 27 8/31/1999 2.1 — 40 AD-1135

40 6 480; 560 44 6/13/2000 2.3 .01 20 AD-1136

40 6 200 7 2/7/1995 1.5 <.01 30 AD-1137

20 6 200; 380 40 10/11/1993 2 .01 10 AD-1138

40 6 — — — — — 25 AD-1139

40 6 110 30 5/4/1992 15 — 29 AD-1140

33 6 80 20 9/16/1994 5 .08 20 AD-1141

40 6 160 F 3/30/1994 1.5 .01 25 AD-1142

40 6 60; 80 20 4/1987 25 .5 35 AD-1143

21 6 105 10 1972 1 — 4 AD-1144

Table 4. Records of selected wells and springs, Borough of Carroll Valley, Adams County,

Pennsylvania—Continued

Casing Depth(s) to

water-producing

zone(s)

(feet)

Static water

level

(feet below

land surface)

Date water

level

measured

Driller

reported

yield

(gal/min)

Specific

capacity

(gal/min)/ft

Depth

to

bedrock

(feet)

USGS well

identification

number Length

(feet)

Diameter

(inches)
62

AD-1145 394458 0772333 Alexander 9/26/1994 800 H 000MBSL 260

AD-1146 394452 0772333 Alexander 9/10/2001 760 W 000MBSL 500

AD-1147 394453 0772312 Alexander 6/1986 660 W 000MBSL 230

AD-1148 394505 0772338 Alexander 12/1/2001 820 W 000MBSL 300

AD-1149 394512 0772349 Alexander 12/26/2001 960 H 000MBSL 520

AD-1150 394534 0772338 Alexander 9/1/2001 780 S 000MBSL 460

AD-1151 394504.6 0772317.9 Alexander 1/2001 770 H 000MBSL 600

AD-1152 394433 0772309 — 1980 770 S 000MTRL 275

AD-1153 394504 0772414 Alexander 10/2001 910 H 000MBSL 240

AD-SP17 394504 0772326 — 1980 760 W 000GRNS —

AD-SP18 394511.0 0772408.3 — 1900 910 S 000GRNS —

AD-SP19 394450.1 0772409.1 — 1980 740 V 000GRNS —

Table 4. Records of selected wells and springs, Borough of Carroll Valley, Adams County,

Pennsylvania—Continued

USGS well

identification

number

Location

Driller Date

completed

Altitude

of land

surface

(feet)

Topographic

setting

Hydrogeologic

unit

Depth

of well

Latitude Longitude (feet)
63

20 6 140 40 9/26/1994 1 0.01 10 AD-1145

34 6 140; 340; 460 20 9/10/2001 5 .01 10 AD-1146

50 6 208 40 6/1986 6 .04 44 AD-1147

40 6 110; 220 20 12/1/2001 5 .03 20 AD-1148

20 6 300; 440 101.31 1/16/2002 2 .01 2 AD-1149

20 6 430 19.27 1/16/2002 12 .06 5 AD-1150

40 6 — 35.91 1/28/2002 0 0 20 AD-1151

— 6 — 51.33 8/15/2001 — — — AD-1152

40 6 — 59.75 1/16/2002 15 — — AD-1153

— — — — — 5 — — AD-SP17

— — — — — 5 — — AD-SP18

— — — — — 10 — — AD-SP19

Table 4. Records of selected wells and springs, Borough of Carroll Valley, Adams County,

Pennsylvania—Continued

Casing Depth(s) to

water-producing

zone(s)

(feet)

Static water

level

(feet below

land surface)

Date water

level

measured

Driller

reported

yield

(gal/min)

Specific

capacity

(gal/min)/ft

Depth

to

bedrock

(feet)

USGS well

identification

number Length

(feet)

Diameter

(inches)
64

APPENDIX A—HYDRAULIC CONDUCTIVITY AND TRANSMISSIVITY

Hydraulic conductivity and transmissivity give

an indication of the ability or capacity of an aquifer to

transmit water. Hydraulic conductivity (K) is defined

as the volume of water that will move in a unit time

under a unit hydraulic gradient through a unit area, at

the prevailing temperature or K = m/d (Heath, 1983,

p. 12). Thus, the units of hydraulic conductivity are

those of velocity (or distance divided by time). Note,

the factors involved in the definition of hydraulic conductivity include the volume of water (Q) that will

move in a unit of time (such as a day) under a unit

hydraulic gradient (dh/dl or change in hydraulic head

over a horizontal distance). So hydraulic conductivity

can also be expressed as:

K = Qdl/Adh = [(feet3/day) x feet]/

(feet2 x feet) = feet/day (1)

The transmissivity (T) of an aquifer is equal to the

hydraulic conductivity (K) of the aquifer multiplied by

the saturated thickness (b) of the aquifer or T = Kb. For

this report, the saturated thickness of an aquifer was

the length of the well’s borehole minus the depth to

water. Transmissivity will change considerably if one

replaces length of well borehole with the depth of the

deepest water-producing zone (640 ft in the

metabasalt, fig. 7) or thickness of the geologic unit

(greater than 1,000 ft for the metabasalt, table 1).

Hydraulic conductivity and transmissivity were

calculated from single-well driller drawdown tests

(single-well aquifer or specific-capacity tests) by use of

a modified Theis formula (Theis and others, 1963) and

are shown in table A1. It should be noted, however, the

ideal hydrogeological conditions and theoretical

assumptions used by Theis and others (1963) rarely are

encountered at a well site. Some major assumptions

used to determine hydraulic conductivity and transmissivity from specific capacity tests for this report

include: (1) ground-water flow to the open interval of

the well is radial, (2) vertical flow is excluded from

consideration, (3) no well loss due to turbulence, and

(4) the producing unit is of infinite areal extent. It

should also be noted that the number of tests presented

in table A1 is a much smaller sampling than one would

expect from the data presented in table 4. Wells were

excluded from analysis if the percentage contributed

from borehole storage exceeded 100 percent and if the

amount of water reportedly discharged by the driller

was less than the amount of water stored in the borehole [(static water level - reported drawdown) x

1.47 gal/ft for 6-in. diameter casing].

Well slug tests provide a quick and inexpensive

method of estimating the transmissivity in the immediate vicinity of a well. By conducting these tests at several wells, the spacial distribution of transmissivity

and hydraulic conductivity (heterogeneity) can be

evaluated. The slug test results (table A2) were conducted by causing a sudden change in water level with

a 4-ft long, 4-in. diameter displacement barrel. The barrel was either rapidly sunk into or removed from

beneath the water to induce a sudden water-level

change. The water-level response was measured with a

15 pounds per square inch (psi) pressure transducer

and recorded with a data logger at 5-second intervals.

The tests were analyzed by the Bouwer and Rice

method (Bouwer, 1989).
65

Table A1. Summary of driller drawdown tests (utilizing a storativity of 0.00001) in determining transmissivity

and hydraulic conductivity, Borough of Carroll Valley, Adams County, Pennsylvania

[P10, tenth percentile; P25, twenty-fifth percentile; P75, seventy-fifth percentile; P90, ninetieth percentile;

ft/day, foot per day; ft2/day, foot squared per day; —, not applicable]

Geologic formation Number

of wells P10 P25 Median P75 P90 Minimum Maximum

Transmissivity (ft2/day1)

Weverton Formation 1 — — 5.18 — — 5.18 —

Loudoun Formation 5 — — 101 — — 5.32 243

metabasalt 131 1.42 3.24 9.49 34.3 96.2 .69 2,340

metarhyolite 12 2.35 3.97 8.72 52.8 66.9 2.18 182

greenstone schist 26 1.79 3.01 6.79 23.9 34.2 .48 108

Hydraulic conductivity (ft/day)

Weverton Formation 1 — — .04 — — .04 —

Loudoun Formation 5 — — 1.18 — — .02 6.75

metabasalt 131 .00 .01 .04 .24 .63 .00 47.5

metarhyolite 12 .01 .01 .04 .52 .82 .01 1.55

greenstone schist 26 .00 .01 .03 .14 .23 .00 1.03

1 Saturated thickness (b) of the aquifer is calculated as the length of the borehole of the well (well depth in table 4)

minus the depth to water. Transmissivity will change if one uses depth of deepest water-producing zone (640 ft for

metabasalt) or estimated thickness of geologic unit (greater than 1,000 ft for metabasalt) instead of the length of the

borehole of the well.

Table A2. Summary of U.S. Geological Survey slug tests and driller

drawdown tests in determining transmissivity of the metabasalt,

Borough of Carroll Valley, Adams County, Pennsylvania

[ft2/day, foot squared per day; —, not applicable]

Well

Transmissivity (ft2/day)1

U.S. Geological

Survey slug test

Driller

drawdown

test

AD-774 25 —

AD-806 42 13.89

AD-808 20 —

AD-818 2 1.17

AD-836 87 —

AD-837 17 2.52

AD-842 9 4.26

AD-846 4 —

AD-1060 188 19.14

AD-1062 120 —

AD-1063 4 —

AD-1148 90 6.46

AD-1149 27 1.66

AD-1153 85 —

1 Saturated thickness (b) of the aquifer is calculated as the length of

the borehole of the well (well depth in table 4) minus the depth to water.

Transmissivity will change if one uses depth of deepest water-producing zone

(640 ft for metabasalt) or estimated thickness of geologic unit (greater than

1,000 ft for metabasalt) instead of the length of the borehole of the well.
66

APPENDIX B—BOREHOLE GEOPHYSICAL LOGS

Borehole geophysical logs provide information

on location and orientation of fractures, water-producing and water-receiving zones, intervals of vertical

borehole flow, quantification of borehole flow, lithologic correlation, and data on well construction. The

subsurface information that can be determined using

borehole geophysics and the geophysical methods

employed are summarized in the following table.

The acoustic televiewer is a sonic imaging tool

that scans the borehole wall with an acoustic beam.

The reflected acoustic waves are recorded digitally on a

portable computer, and images of the wave’s transit

time and amplitude are produced. The logs are corrected for magnetic orientation, magnetic declination

(true north), and borehole deviation from vertical by

the logging software. Fractures are detected by longer

transit times and decreased signal amplitudes. Because

the returned data are oriented to true north and corrected for borehole deviation from vertical, strike and

dip for each fracture or bedding plane can be determined. The acoustic televiewer can be used in 6- to

9-in. boreholes.

Caliper logs record the average borehole diameter, which may be related to fractures, lithology, or

drilling methods. Caliper logs can be used to identify

fractures and possible water-producing or waterreceiving zones and correct other geophysical logs for

changes in borehole diameter. They also can be correlated with fluid-temperature logs and heatpulse flowmetering to identify fractures and water-producing

and water-receiving zones.

The natural-gamma or gamma log measures the

natural-gamma radiation (photons) emitted from all

rocks. The most common emitters of gamma radiation

are uranium-238, thorium-232, their daughter elements, and potassium-40. These radioactive elements

are concentrated in clays by adsorption, precipitation,

and ion exchange. Fine-grained sediments such as

shale or siltstone usually emit more gamma radiation

than sandstone, limestone, or dolomite. The gamma

log can be run in or out of water or casing. However,

casing does reduce the gamma response. The gamma

log is used to correlate geologic units between wells

(Keys, 1988).

The single-point-resistance log records the electrical resistance of a formation between the probe in a

water filled borehole below casing and an electrical

ground at land surface. Generally, electrical resistance

increases with formation grain size and decreases with

borehole diameter, water-producing fractures, and

increasing dissolved-solids concentration of borehole

water fluid. The single-point-resistance log is used to

corollate geology between wells and may help identify

water-producing zones. (Keys, 1988).

Fluid-temperature logs provides a continuous

record of the temperature of vertical variation in the

water in a borehole. Temperature logs are used to identify water-producing and water-receiving zones and to

determine zones of vertical borehole flow. Intervals of

vertical borehole flow are characterized by little or no

temperature gradient. (Williams and Conger, 1990).

The direction and rate of borehole-water movement was determined by the use of a heatpulse flowmeter. The heatpulse flowmeter operates by heating a

small sheet of water between two sensitive thermistors

(heat sensors). A measurement of direction and rate is

computed when a peak temperature is recorded by one

of the thermistors. The range of flow measurement is

about 0.01-1.5 gal/min in a 2- to 10-in.-diameter borehole (Conger, 1996).

Some heatpulse-flowmeter measurements may

be influenced by (1) poor seal integrity between the

borehole and heatpulse flowmeter and (2) contributions of water from storage within the borehole. If the

seal between the borehole and flowmeter is not complete, some water can bypass the flowmeter, resulting

in measurements of flow that are less than the actual

rate. Although the heatpulse flowmeter is a calibrated

probe, the data are primarily used as a relative indicator to identify water-producing zones.

Borehole geophysical logs and applicable subsurface

information

[A, acoustic televiewer log; C, caliper log; G, natural gamma log;

R, single-point resistance log; T, temperature log; V, heatpulse

flowmeter]

Borehole

geophysical

log

Subsurface information

A, C Location and orientation of fractures and waterproducing zones

R, T Location of water-producing and water-receiving

zones

T, V Intervals of vertical borehole flow

V Quantification of borehole flow

G, R Lithologic correlation

C, G Casing length

C Borehole diameter
67

Three wells were logged AD-774, AD-808,

AD-836. A summary of the depths logged, casing

depth, depths to water, and geophysical logs run are

presented in table B1.

Table B1. Wells logged at Borough of Carroll Valley, Adams

County, Pennsylvania

[A, acoustic televiewer; C, caliper; G, natural gamma; R, single-point

resistance; T, temperature; V, heatpulse flowmeter; ft bls, feet below

land surface]

U.S.

Geological

Survey well

identification

number

Depth

logged

(ft bls)

Depth of

casing

(ft bls)

Depth

to water

(ft bls)

Geophysical

logs run

AD-774 397 12 72 A, C, G, R, T, V

AD-808 231 19 136 A, C, G, R, T, V

AD-836 502 80 89 A, C, G, R, T, V
68

WELL AD-774

The caliper log shows the total depth of the borehole is 397 ft and it is cased with 6-in. diameter casing

to 12 ft bls (fig. B1). The depth to water at the time of

data collection was 72 ft bls. The caliper log shows

major fractures at 22-24, 28-29, 31-32, and 50-51 ft bls,

minor fractures throughout the open-hole section of

the borehole, and a change in drilling bit diameter at

68 ft bls. The natural-gamma log shows increased

counts at 91 to 124, 192 to 278, and 333 to 395 ft bls that

indicate lithologic changes, probably from metabasalt

to metarhyolite. The single-point-resistance log shows

major deflections (lower electrical resistance) at 95 to

110, 225, and 245 ft bls. The fluid-temperature log

shows changes in slope at 93, 121, 203, 223, 238, and

246 ft bls that correlate to fractures shown on the caliper log and zones of lower electrical resistance on the

single-point-resistance logs. Under nonpumping conditions, the heatpulse flowmeter measured upward

borehole flow at 112, 134, 150, and 254 ft bls, no flow at

82, 232, 310, 336, and 370 ft bls, and possible lateral

flow at 180, 196, and 214 ft bls (table B2). The geophysical logs and the heatpulse-flowmeter data indicate

water enters the borehole through fractures at 128, 202,

and below 254 ft bls and moves upward. The greatest

quantity of water exits the borehole through fractures

at 92 to 109 ft bls. A minor quantity of water exits the

borehole through a fracture at about 236 ft bls. The

borehole geophysical logs indicate also that most

water-producing and water-receiving zones are at

lithologic contacts.

Table B2. Summary of heatpulse-flowmeter measurements within borehole AD-774

collected on January 16, 2002, Section B, Borough of Carroll Valley,

Adams County, Pennsylvania

[ft bls, feet below land surface; gal/min, gallon per minute; —, not applicable]

Depth

(ft bls)

Flow rate under

nonpumping

conditions

(gal/min)

Flow direction

under nonpumping

conditions

Comments

82 No flow Not determined —

112 0.16 Up —

134 .08 Up —

150 .07 Up —

180 Not determined Not determined Turbulence,

possible lateral

flow

196 Not determined Not determined Turbulence,

possible lateral

flow

214 Not determined Not determined Turbulence,

possible lateral

flow

232 No flow Not determined —

254 .07 Up Turbulence,

possible lateral

flow

310 No flow Not determined —

336 No flow Not determined —

370 No flow Not determined —
69METABASALT

METARHYOLITE

EXP

STATIC 

Measloggi

BOREH

NONdepth flow 

DIRECT

NON

TURBU

0.16

 N38E/42NW

 N52W/34NE

NF

Figure B1. Lithology and borehole geophysical logs and direction of nonpumping flow within borehole AD-774 collected on January 1Carroll Valley, Adams County, Pennsylvania.

METABASALT

METABASALT

METABASALT

METABASALT

METARHYOLITE

METARHYOLITE

METARHYOLITE

ACOUSTIC

TELEVIEWER

NATURAL GAMMA,

IN COUNTS PER

SECOND

SINGLE-POINT

RESISTANCE,

IN OHMS

FLUID

TEMPERATURE,

IN DEGREES

CELSIUS HOLE DIAMETER, IN INCHES

DEPTH, IN FEET BELOW LAND SURFACE

LITHOLOGY

8 0 400 200 2,000 4,000 2,000 3,000 8 13 10 12 0

420

20406080

100120140160180200220240260280300320340360380400

5 6 9 11

NF

NF

NF

NF

NF

0.16

.07

72

7

.07

.08

REGOLITH

 N7W/35SW

N38E/42NW

 N52W/34NE

72
70

WELL AD-808

The caliper log shows the total depth of the borehole is 231 ft and it is cased with 6-in. diameter casing

to 19 ft bls (fig. B2). The depth to water at the time of

data collection was 136 ft bls. The caliper log shows a

major fracture at 150 to 151 ft bls and minor fractures

throughout the open-hole section of the borehole. The

natural-gamma log shows increased counts at 179 to

189 and 211 to 230 ft bls that indicate lithologic

changes, probably from metabasalt to metarhyolite.

The single-point-resistance log shows major deflections (lower electrical resistance) in slope at 150, 180 to

182, 197, 204, and 210 ft bls. The fluid-temperature log

shows changes in slope at 181, 184, 197, 207, 212, 221,

and 229 ft bls that correlate to minor fractures shown

on the caliper log and zones of lower electrical resistance on the single-point-resistance logs. Under nonpumping conditions, the heatpulse flowmeter

measured no borehole flow at 166, 186, 199, and

216 ft bls and possible lateral flow at 146 ft bls (table

B3). The geophysical logs suggest that minor quantities

of water enter the borehole through fractures at 150 to

151, 195, 204, and 211 ft bls. The borehole geophysical

logs indicate also that some water-producing zones

occur at lithologic contacts between the metabasalt and

metarhyolite.

Table B3. Summary of heatpulse-flowmeter measurements within borehole AD-808

collected on January 29, 2002, Section P, Borough of Carroll Valley,

Adams County, Pennsylvania

[ft bls, feet below land surface; gal/min, gallon per minute; —, not applicable]

Depth

(ft bls)

Flow rate under

nonpumping

conditions

(gal/min)

Flow direction

under nonpumping

conditions

Comments

146 Not determined Not determined Turbulence,

possible lateral

flow

166 No flow Not determined —

186 No flow Not determined —

199 No flow Not determined —

216 No flow Not determined —
71

Figure B2. Lithology and borehole geophysical logs and direction of nonpumping flow within borehole AD-808 collected on January 2Borough of Carroll Valley, Adams County, Pennsylvania.

ACOUSTIC

TELEVIEWER

NATURAL GAMMA,

IN COUNTS PER

SECOND

SINGLE-POINT

RESISTANCE,

IN OHMS

FLUID

TEMPERATURE,

IN DEGREES

CELSIUS HOLE DIAMETER, LITHOLOGY IN INCHES

5 8 6 0 400 0 2,000 9 12 10

240

0

20406080

100120140160180200220

DEPTH IN FEET, BELOW LAND SURFACE

7 11

NF

NF

NF

NF

136

METARHYOLITEMETARHYOLITE

METABASALT

METABASALT

REGOLITH

N49E/61NWN13E/76NW

N5W/34SW

N20E/32NWN25E/49NWN39E/32NW

STATI

Mege

BORE

MECOflow 

TURB

LAT

POSS

Sho

FRAC

Sho

WATE

NO

NF NO FL

N49E/61NW

N39E/32NW

136
72

WELL AD-836

The caliper log shows the total depth of the borehole is 502 ft and it is cased with 6-in. diameter casing

to 80 ft bls (fig. B3). The depth to water at the time of

data collection was 89 ft bls. The caliper log shows fractures at 86, 97, 101, 260, and 380 ft bls and minor fractures at 115, 122, 142 to 144, 182 to 184, 199, and

212 ft bls. The natural-gamma log shows increased

counts at 128 to 415 ft bls that indicate lithologic

changes, probably from metabasalt to metarhyolite.

The single-point-resistance log exhibits a large number

of deflections in slope from about 120 to 420 ft bls,

which suggests some flow (probably lateral flow). The

fluid-temperature log shows a consistent geothermal

gradient with only minor interruptions in slope at 222

to 280, 400 to 415, and 470 ft bls that may be due to lateral borehole flow. Under nonpumping conditions, the

heatpulse flowmeter measured no borehole flow at 110,

134, 170, 190, 220, 268, 360, 400, 450, 474, and 490 ft bls

(table B4).

A submersible pump was placed at 120 ft bls,

and the borehole was pumped at an initial rate of

1.1 gal/min. The static water level in the well was

88.75 ft bls. The water level declined 10.05 ft after

46 minutes. Under pumping conditions, the heatpulse

flowmeter measured minor upward borehole flow at

134 ft bls and no flow at 170 ft bls. The pumping rate

was increased to 2.5 gal/min with a beginning water

level of 98.80 ft bls. Under increased pumping conditions, the heatpulse flowmeter measured minor

upward borehole flow at 170 ft bls and no flow at

190 ft bls; water levels declined 10.6 ft in 28 minutes.

The pumping rate was again increased to 3 gal/min

with a beginning water level of 109.40 ft bls; the water

level declined 3.75 ft in 14 minutes. Under increased

pumping conditions, the heatpulse flowmeter measured minor upward flow at 190 ft bls. The geophysical

logs and the heatpulse-flowmeter data indicate a minor

quantity of water enters the borehole through fractures

at 142, 163, and below 190 ft bls (probably 470 ft bls).

When the pumping rate was 1.1 gal/min, 66 percent of

the water was produced from above 134 ft bls; at a

pumping rate of 2.5 gal/min, 71 percent of the discharge water was produced from above 170 ft bls; at a

pumping rate of 3 gal/min, 81 percent of the discharge

water was produced from above 190 ft bls.

Table B4. Summary of heatpulse-flowmeter measurements within borehole AD-836

collected on January 10, 2002, Section WA, Borough of Carroll Valley,

Adams County, Pennsylvania

[ft bls, feet below land surface; gal/min, gallon per minute; —, not applicable]

Depth

(ft bls)

Flow rate under

nonpumping conditions

(gal/min)

Flow direction under

nonpumping conditions

Pumping rate

(gal/min)

110 No flow Not determined —

134 No flow Not determined —

170 No flow Not determined —

190 No flow Not determined —

220 No flow Not determined —

268 No flow Not determined —

360 No flow Not determined —

400 No flow Not determined —

450 No flow Not determined —

474 No flow Not determined —

490 No flow Not determined —

Depth

(ft bls)

Flow rate under

pumping conditions

(gal/min)

Flow direction under

pumping conditions

Pumping rate

(gal/min)

134 0.22 Up 1.1

170 No flow Not determined 1.1

170 .16 Up 2.5

190 No flow Not determined 2.5

190 .19 Up 3.0
73

Figure B3. Lithology and borehole geophysical logs and direction of nonpumping and pumping flow within borehole AD-836 collected 

2002, Section WA, Borough of Carroll Valley, Adams County, Pennsylvania.

NF

N51E/47NW

N20E/30SE

ACOUSTIC

TELEVIEWER

NATURAL GAMMA,

IN COUNTS PER

SECOND

SINGLE-POINT

RESISTANCE,

IN OHMS

FLUID

TEMPERATURE,

IN DEGREES

CELSIUS HOLE DIAMETER, IN INCHES

DEPTH, IN FEET BELOW LAND SURFACE

LITHOLOGY

5 8 6 0 400 200 500 2,000 1,000 9 12 10

0

550

50

100150200250300350400450500

7 11

89

METARHYOLITE

REGOLITH

METABASALT

NP P

NF

NF

NF

NF

NF

NF

NF

NF

NF

NF

NF

0.22

.16.19

109.40

METABASALT N51E/47NW

N67W/28NE

N13E/50SE

N20E/30SE

N68W/78NE

N32E/46NW

N67E/12SE

N17E/42SE

N8W/25NE

N29E/51NW

89

NP

P
74

APPENDIX C—SOURCE AND SIGNIFICANCE OF SELECTED INDICATORS

OF GROUND-WATER QUALITY

[mg/L, milligrams per liter; MCL, maximum contaminant level; SMCL, secondary maximum contaminant level;

mL, milliliters; U.S. Environmental Protection Agency, USEPA; N, nitrogen]

Constituent or property Concentration limits and water-use

implications Implications for ground-water geochemistry

Bromide, dissolved mg/L Regulatory standards not established for

drinking water.

Generally derived from precipitation, dissolution of evaporites or

intrusion of brines. The ratio of chloride to bromide can be

used to evaluate the origin of dissolved salts in ground water

(Davis and others, 1998).

Chloride, dissolved mg/L The SMCL is 250 mg/L. Water with less

than 150 mg/L is suitable for most

purposes. A chloride content of more

than 250 mg/L is generally objectionable

for public supply, and water with a

chloride content of more than 350 mg/L

is objectionable for most irrigation and

industrial uses. Water containing

500 mg/L or more of chloride generally

has a disagreeable taste. In large

quantities chloride increases the

corrosiveness of water.

The most important natural sources of chloride are from

sedimentary rocks. Chloride is a rare constituent of nonevaporite rocks. Relatively large amounts of chloride are

derived from sewage, industrial wastes, brines and highway

deicing practices. Typical concentrations of chloride in ground

water range from 10-2,000 mg/L (Cook and Miles, 1980,

p. 17).

Total coliform bacteria,

colonies/100 mL

The MCL for coliform bacteria in drinking

water is zero (or no) total coliform per

100 mL of water.

Total coliform bacteria are indicator organisms that, when

present, indicate that there is a possibility, but not a certainty,

that disease-causing organisms may also be present in the

water due to contamination from human or animal wastes.

Coliform bacteria can also occur naturally in the soil, so their

presence does not necessarily indicate a sewagecontamination problem or imminent health risk (USEPA,

2000).

Fecal coliform bacteria,

colonies /100 mL

The MCL for coliform bacteria in drinking

water is zero (or no) total coliform per

100 mL of water.

Fecal coliform bacteria are bacteria whose presence indicates

that the water may be contaminated with human or animal

wastes. Disease-causing microbes in these wastes can cause

diarrhea, cramps, nausea, headaches, or other symptoms.

These microbes may pose a special health risk for infants,

young children, and people with severely compromised

immune systems (USEPA, 2000).

Nitrate, dissolved mg/L as N Small concentrations of nitrate have no

effect on the usefulness of water. Most

ground water contains less than 2 mg/L

nitrate. Waters containing more than

10 mg/L nitrate may cause

methemoglobinemia (blue baby

syndrome)- a disease often fatal in

infants under 6 months.

Presence of nitrate indicates oxidizing conditions in the aquifer.

Decaying organic matter, animal waste, sewage, septic tanks,

and fertilizers are principle sources of nitrate. Elevated

concentrations are indicative of anthropogenic sources of

nitrate (USEPA, 2000).
75

APPENDIX D—RESULTS OF ANALYSES FOR WASTEWATER COMPOUNDS, ENDOCRINEDISRUPTING POTENTIAL, AND POSSIBLE COMPOUND USES

Table D1. Wastewater compounds in selected wells, Borough of Carroll Valley, Adams County, Pennsylvania

[μg/L, micrograms per liter; <, less than; E, estimated; ND, not detected]

Compound

Minimum

reporting

level

(μg/L)

AD-781

(μg/L)

AD-790

(μg/L)

AD-830

(μg/L)

AD-900

(μg/L)

AD-922

(μg/L)

AD-1098

(μg/L)

1,4-Dichlorobenzene 0.5 ND ND ND ND ND ND

Ethynyl estradiol 5 ND ND ND ND ND ND

17beta-Estradiol 5 ND ND ND ND ND ND

1-Methylnaphthalene .5 ND ND ND ND ND ND

2,6-Dimethylnaphthalene .5 ND ND ND ND ND ND

2-Methylnaphthalene .5 ND ND ND ND ND ND

3-beta-Coprostanol 2 ND ND ND ND ND ND

3-Methyl-1 H-indole (skatol) 1 ND ND ND ND ND ND

3-tert-Butyl-4-hydroxyanisole (BHA) 5 ND ND ND ND ND ND

4-Cumylphenol 1 ND ND ND ND ND ND

4-n-Octylphenol 1 ND ND ND ND ND ND

4-tert-Octylphenol 1 ND ND ND ND ND ND

5-Methyl-1 H-benzotriazole 2 ND ND ND ND ND ND

Acetophenone .5 ND ND ND ND ND ND

Acetyl-hexamethyltetrahydonaphthalene (AHTN).5 ND ND ND ND ND ND

Anthracene .5 ND ND ND ND ND ND

Anthraquinone .5 ND ND ND ND ND ND

Benzo[a]pyrene Pyrene .5 ND ND ND ND ND ND

Benzophenone .5 ND ND ND ND ND E 0.02

beta-Sitosterol 2 ND ND ND ND ND ND

beta-Stigmastanol 2 ND ND ND ND ND ND

Bisphenol A 1 E 0.067 E 0.13 E 0.099 ND E 0.49 1.2

Bromacil .5 ND ND ND ND ND ND

Bromoform .5 ND ND ND ND ND ND

Caffeine .5 ND ND ND ND ND ND

Camphor .5 ND ND ND ND ND ND

Carbaryl 1 ND ND ND ND ND ND

Carbazole .5 ND ND ND ND ND ND

Chlorpyrifos .5 ND ND ND ND ND ND

Cholesterol 2 ND ND ND ND ND ND

Cotinine 1 ND ND ND ND ND ND

Diazinon .5 ND ND ND ND ND ND

Dichlorvos 1 ND ND ND ND ND ND

d-Limonene .5 ND ND ND ND ND ND

Equilenin 5 ND ND ND ND ND ND

Estrone 5 ND ND ND ND ND ND

Ethynyl estradiol 5 ND ND ND ND ND ND

Fluoranthene .5 ND ND ND ND ND ND

Hexahydrohexamethylcycloopentabenzopyran (HHCB).5 ND ND ND ND ND ND

Indole .5 ND ND ND ND ND ND

Isoborneol .5 ND ND ND ND ND ND

Isophorone .5 ND ND ND ND ND ND

Ispropylbenzene (cumene) .5 ND ND ND ND ND ND
76

Isoquinoline 0.5 ND ND ND ND ND ND

Menthol .5 ND ND ND ND ND ND

Metalaxyl .5 ND ND ND ND ND ND

Methyl salicylate .5 ND ND ND ND ND ND

Metolachlor .5 ND ND ND ND ND ND

N,N-diethyl-meta-toluamide (Deet) .5 E 0.13 E 0.067 E 0.076 ND E 0.22 E 0.42

Naphthalene .5 ND ND ND ND ND ND

Nonylphenol, diethoxy-(total, NPEO2) 5 ND ND ND ND ND ND

Octylphenol, diethoxy-(OPEO2) 1 ND ND ND ND ND ND

Octylphenol, monoethoxy-(OPEO1) 1 ND ND ND ND ND ND

para-Cresol 1 ND ND ND ND ND ND

para-Nonylphenol (total) 5 ND ND ND ND ND ND

Pentachloropohenol 2 ND ND ND ND ND ND

Phenanthrene .5 ND ND ND ND ND ND

Phenol .5 ND E .28 E .35 0.68 E .40 E .42

Prometon .5 ND ND ND ND ND ND

Pyrene .5 ND ND ND ND ND ND

Tetrachloroethylene .5 ND ND ND ND ND ND

Tri(2-butoxyethyl) phosphate .5 ND ND ND ND E .15 E .086

Tri(2-chloroethyl) phosphate .5 ND ND ND ND ND ND

Tri(dichloroisopropyl) phosphate .5 ND ND ND ND ND ND

Tributyl phosphate .5 ND ND ND ND ND E .1

Triclosan 1 ND ND ND ND ND ND

Triethyl citrate (ethyl citrate) .5 ND ND ND ND ND ND

Triphenyl phosphate .5 E .041 E .064 E .042 ND E .06 E .12

Table D1. Wastewater compounds in selected wells, Borough of Carroll Valley, Adams County, Pennsylvania—Continued

[μg/L, micrograms per liter; <, less than; E, estimated; ND, not detected]

Compound

Minimum

reporting

level

(μg/L)

AD-781

(μg/L)

AD-790

(μg/L)

AD-830

(μg/L)

AD-900

(μg/L)

AD-922

(μg/L)

AD-1098

(μg/L)
77

Table D2. Wastewater compound endocrine-disrupting potential and possible compound uses (modified from Zaugg and

others, 2002, table 1)

[EDP, endocrine-disrupting potential; K, known, S, suspected; %, percent; —, no data; CP, combustion product;

PAH, polycyclicaromatic hydrocarbon; >, greater than; F, fungicide; H, herbicide; I, insecticide; GUP, general use pesticide;

WW, wastewater; UV, ultraviolet]

Compound EDP Possible compound uses or sources

1,4-Dichlorobenzene S Moth repellent, fumigant, deodorant

Ethynyl estradiol — Oral contraceptive

17beta-Estradiol — Estrogen replacement therapy, estrogen metabolite

1-Methylnaphthalene — 2-5 percent of gasoline, diesel fuel, or crude oil

2,6-Dimethylnaphthalene — Present in diesel/kerosene (trace in gasoline)

2-Methylnaphthalene — 2-5 percent of gasoline, diesel fuel, or crude oil

3-beta-Coprostanol — Carnivore fecal indicator

3-Methyl-1 H-indole (skatol) — Fragrance, stench in feces and coal tar

3-tert-Butyl-4-hydroxyanisole

(BHA)

K Antioxidant, general preservative

4-Cumylphenol K Nonionic detergent metabolite

4-n-Octylphenol K Nonionic detergent metabolite

4-tert-Octylphenol K Nonionic detergent metabolite

5-Methyl-1 H-benzotriazole — Antioxidant in antifreeze and deicers

Acetophenone — Fragrance in detergent and tobacco, flavor in beverages

Acetyl-hexamethyltetrahydonaphthalene (AHTN)— Musk fragrance (widespread usage) persistent in ground water

Anthracene — Wood preservative, component of tar, diesel, or crude oil, CP

Anthraquinone — Manufacturing dye/textiles, seed treatment, bird repellent

Benzo[a]pyrene Pyrene K Regulated PAH, used in cancer research, CP

Benzophenone S Fixative for perfumes and soaps

beta-Sitosterol — Plant sterol

beta-Stigmastanol — Plant sterol

Bisphenol A K Manufacturing polycarbonate resins, antioxidant, flame retardant

Bromacil — H (GUP), > 80% noncrop usage on grass/brush

Bromoform — WW ozination by-product, military/explosives

Caffeine — Beverages, diuretic, very mobile/biodegradable

Camphor — Flavor, odorant, ointments

Carbaryl K I, crop and garden uses, low persistence

Carbazole — I, manufacturing dyes, explosives, and lubricants

Chlorpyrifos K I, domestic pest and termite control (domestic use restricted as of 2001)

Cholesterol — Often a fecal indicator, also a plant sterol

Cotinine — Primary nicotine metabolite

Diazinon K I, > 40% nonagricultural usage, ants, flies

Dichlorvos S I, pet collars, flies, also a degradate of naled or trichlofon

d-Limonene — F, antimicrobial, antiviral, fragrance in aerosols

Equilenin — Hormone replacement therapy drug

Estrone — Biogenic hormone

Ethynyl estradiol K Oral contraceptive

Fluoranthene — Component of coal tar and asphalt (only traces in gasoline or diesel fuel), CP

Hexahydrohexamethylcycloopentabenzopyran (HHCB)— Musk fragrance (widespread usage) persistent in ground water

Indole — Pesticide inert ingredient, fragrance in coffee

Isoborneol — Fragrance in perfumery, in disinfectants

Isophorone — Solvent for lacquer, plastic, oil, silicon, resin

Ispropylbenzene (cumene) — Manufacturing phenol/acetone, fuels and paint thinner

Isoquinoline — Flavors and fragrances
78

Menthol — Cigarettes, cough drops, liniment, mouthwash

Metalaxyl — H, F (GUP), mildew, blight, pathogens, golf/turf

Methyl salicylate — Liniment, food, beverage, UV-absorbing lotion

Metolachlor — H (GUP), indicator of agricultural drainage

N,N-diethyl-meta-toluamide (Deet) — I, urban uses, mosquito repellent

Naphthalene — Fumigant, moth repellent, major component (about 10%) of gasoline

Nonylphenol, diethoxy-(total,

NPEO2)

K Nonionic detergent metabolite

Octylphenol, diethoxy-(OPEO2) K Nonionic detergent metabolite

Octylphenol, monoethoxy-

(OPEO1)

K Nonionic detergent metabolite

para-Cresol S Wood preservative

para-Nonylphenol (total) K Nonionic detergent metabolite

Pentachloropohenol S H, F, wood preservative, termite control

Phenanthrene — Manufacturing explosives, component of tar, diesel fuel, or crude oil, CP

Phenol — Disinfectant, manufacturing several products, leachate

Prometon — H (noncrop only), applied prior to blacktop

Pyrene — Component of coal tar and asphalt (only traces in gasoline or diesel fuel), CP

Tetrachloroethylene — Solvent, degreaser, veterinary anthelmintic

Tri(2-butoxyethyl) phosphate — Flame retardant

Tri(2-chloroethyl) phosphate S Plasticizer, flame retardant

Tri(dichloroisopropyl) phosphate S Flame retardant

Tributyl phosphate — Antifoaming agent, flame retardant

Triclosan S Disinfectant, antimicrobial (concern for acquired microbial resistance)

Triethyl citrate (ethyl citrate) — Cosmetics, pharmaceuticals

Triphenyl phosphate — Plasticizer, resin, wax, finish, roofing paper, flame retardant

Table D2. Wastewater compound endocrine-disrupting potential and possible compound uses (modified from Zaugg and

others, 2002, table 1)—Continued

[EDP, endocrine-disrupting potential; K, known, S, suspected; %, percent; —, no data; CP, combustion product;

PAH, polycyclicaromatic hydrocarbon; >, greater than; F, fungicide; H, herbicide; I, insecticide; GUP, general use pesticide;

WW, wastewater; UV, ultraviolet]

Compound EDP Possible compound uses or sources