U.S. Department of the Interior

U.S. Geological Survey

Scientific Investigations Report 2008–5118

Prepared in cooperation with the Osage Tribal Council

Aquifer Tests and Characterization of Transmissivity, AdaVamoosa Aquifer on the Osage Reservation, Osage County, 

Oklahoma, 2006

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Pawhuska

Wynona

Hominy 21

38

56

22

70

44

44

130

30

45

80

20

40

210

100-110

5

15

10

55

100

112-1,000
On the cover: Map of Osage Reservation, Osage County, with the Ada-Vamoosa a

quifer outlined.
Aquifer Tests and Characterization of 

Transmissivity, Ada-Vamoosa Aquifer on 

the Osage Reservation, Osage County, 

Oklahoma 2006

By Marvin M. Abbott and Kelli DeHay

Prepared in cooperation with the Osage Tribal Council

Scientific Investigations Report 2008–5118

U.S. Department of the Interior

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

DIRK KEMPTHORNE, Secretary

U.S. Geological Survey

Mark D. Myers, Director

U.S. Geological Survey, Reston, Virginia: 2008

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Although this report is in the public domain, permission must be secured from the individual copyright owners to 

reproduce any copyrighted materials contained within this report.

Suggested citation:

Abbott, M.M., and DeHay, Kelli, 2008, Aquifer tests and characterization of transmissivity, Ada-Vamoosa Aquifer 

on the Osage Reservation, Osage County, Oklahoma, 2006: U.S. Geological Survey Scientific Investigations Report 

2008-5118, 10 p.
iii

Contents

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

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

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

Description of the Aquifer in the Study Area ............................................................................................1

Ground-Water Hydrologic Terms ................................................................................................................3

Aquifer Data and Field Methods .................................................................................................................3

Aquifer Test Analysis Methods and Results..............................................................................................4

Characterization of Transmissivity..............................................................................................................4

References......................................................................................................................................................9

Figures

Figures 1–4. Maps showing:

1. Distribution of the outcrop area of the Ada-Vamoosa aquifer and the specific 

capacity data for the aquifer ......................................................................................................2

2. Distribution of the outcrop area of the Ada-Vamoosa aquifer and the calculated

and estimated transmissivity data for the aquifer..................................................................6

3. Comparison of the calculated and estimated transmissivity data with the data from

Oklahoma Geological Survey Circular 87 for the unconfined part of the 

Ada-Vamoosa aquifer ..................................................................................................................7

4. Comparison of the calculated and estimated transmissivity data with the data from

Oklahoma Geological Survey Circular 87 for the confined part of the Ada-Vamoosa

aquifer.............................................................................................................................................8

Tables

1. Ada-Vamoosa aquifer properties from wells in Creek, Payne, and Lincoln Counties ......3

2. Ada-Vamoosa aquifer test information, including pumping rate, water-level 

drawdown, specific capacity, estimated and calculated transmissivity, and 

calculation method used .............................................................................................................5
iv

Conversion Factors

Inch/Pound to SI

Multiply By To obtain

Length

foot (ft) 0.3048 meter (m)

Area

square mile (mi2

) 2.590 square kilometer (km2) 

Flow rate

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

Pressure

pound per square inch (lb/in2

) 6.895 kilopascal (kPa) 

Specific capacity

gallon per minute per foot 

[(gal/min)/ft)]

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

Transmissivity*

foot squared per day (ft2

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

Vertical coordinate information is referenced to the North American Vertical Datum of 1988 (NAVD 88).

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

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

thickness [(ft3

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

convenience.
Aquifer Tests and Characterization of Transmissivity, AdaVamoosa Aquifer on the Osage Reservation, Osage County, 

Oklahoma, 2006

By Marvin M. Abbott and Kelli DeHay

Abstract

The Ada-Vamoosa aquifer of northeastern Oklahoma 

is a sedimentary bedrock aquifer of Pennsylvanian age that 

crops out over 800 square miles of the Osage Reservation. 

The Osage Nation needed additional information regarding 

the production potential of the aquifer to aid them in future 

development planning. To address this need, the U.S. Geological Survey, in cooperation with the Osage Nation, conducted 

a study of aquifer properties in the Ada-Vamoosa aquifer. This 

report presents the results of the aquifer tests from 20 wells in 

the Ada-Vamoosa aquifer and one well in a minor aquifer east 

of the Ada-Vamoosa outcrop on the Osage Reservation. Well 

information for 17 of the 21 wells in this report was obtained 

from the Indian Health Service. Data collected by the U.S. 

Geological Survey during this investigation are pumping well 

data from four domestic wells collected during the summer 

of 2006. Transmissivity values were calculated from well 

pumping data or were estimated from specific capacity values 

depending on the reliability of the data. The estimated transmissivity values are 1.1 to 4.3 times greater than the calculated 

transmissivity values. The calculated and estimated transmissivity values range from 5 to 1,000 feet squared per day. 

Introduction

The Ada-Vamoosa aquifer of northeastern Oklahoma is a 

sedimentary bedrock aquifer of Pennsylvanian age that crops 

out over 800 square miles of the Osage Reservation (Bingham 

and Bergman, 1980, sheets 1 and 2). The Osage Nation needed 

additional information regarding the production potential of 

the aquifer to aid them in future development planning. A 

previous ground-water-quality study of the aquifer (Abbott, 

2000) provided water-quality data in rural domestic wells 

and compared water quality to proximity of oil wells. The 

Abbott (2000) study did not provide information regarding the 

potential water yield of the aquifer and this information can be 

used by the Osage Nation to evaluate the aquifer as a resource. 

To address this need, the U.S. Geological Survey (USGS), 

in cooperation with the Osage Nation, conducted a study of 

aquifer properties on the reservation. 

Purpose and Scope

The purpose of this report is to present the results of the 

aquifer tests and characterization of transmissivity from 20 

wells in the Ada-Vamoosa aquifer and one well in a minor 

aquifer east of the Ada-Vamoosa outcrop on the Osage Reservation. Transmissivity values were calculated from well 

pumping data or were estimated from specific capacity values 

depending on the reliability of the data. The well transmissivity values are compared to selected published aquifer hydraulic data (D’Lugosz and others, 1986) to present a regional 

spatial interpretation.

Description of the Aquifer in the 

Study Area

The study area was about the extent of the outcrop area of 

the Ada and Vamoosa Formations on the reservation. The eastern boundary is the outcrop of the lower units of the Vamoosa 

Formation. The western boundary is the limit of usable water 

in the aquifer. This approximately corresponds to the western 

limits of the Ada Formation. 

Descriptions of the aquifer were obtained from drilling 

information required by the U.S. Department of Health and 

Human Services, Indian Health Service (IHS) in Pawnee, 

Oklahoma, and other references as listed. IHS data includes 

date the well was tested, latitude, longitude, lithology thicknesses, well depth, screen interval, screen depth, pumping rate, 

and well-test drawdown information. 

The Ada-Vamoosa aquifer is composed of sedimentary 

bedrock of Pennsylvanian age that crops out from near Sulphur in south-central Oklahoma to the Osage Reservation (fig. 

1). The outcrop for the Ada-Vamoosa aquifer (fig. 1) system 
T. 29 N. T. 28 N. T. 27 N. T. 26 N. T. 25 N. T. 24 N. T. 23 N. T. 22 N. T. 21 N. T. 20 N.

R. 06 E. R. 07 E. R. 08 E. R. 09 E. R. 10 E. R. 11 E. R. 12 E.

R. 05 E.

R. 04 E.

R. 03 E.

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Arkansas River

0.4

0.19

0.11

0.51

0.21

0.92

0.05

0.87

0.14

0.03

0.05

0.18

0.48 0.23

0.33

0.08

0.44

0.78

0.16

0.29

0.87

Pawhuska

Hominy

Wynona

-96°15'

-96°15'

-96°30'

-96°30'

-96°45'

-96°45'

-97°0'

-97°0'

-96°0'

-96°0'

37°0'

37°0'

36°45'

36°45'

36°30'

36°30'

36°15'

36°15'

 

 

0 5 10 Miles

0 5 10 Kilometers

Map compiled by U.S. Geological Survey

Base from U.S. Geological Survey digital data, 1:100,000, 1983

Albers Equal Area Conic projection, NAD83 datum

EXPLANATION

0.78 Specific Capacity,

gallons per minute 

per foot of drawdown

Towns

Ada Formation

outcrop area

Vamoosa Formation

outcrop area

!(

!(

U.S. Geological Survey,

pump test data

U.S. Department of Health 

and Human Services, 

Indian Health Service, 

pump test data

Sulphur !

Payne County

Creek County

Lincoln County

Osage 

Reservation

Limit 

of 

outcrop 

area

Limit 

of 

outcrop 

area

Figure 1. Distribution of the outcrop area of the Ada-Vamoosa aquifer and the specific 

capacity data for the aquifer.
3 Aquifer Tests and Characterization of Transmissivity, Ada-Vamoosa Aquifer, Osage Reservation, Oklahoma, 2006

includes about 800 square miles of the Osage Reservation or 

about 35 percent of the surface area in a broad north-south 

band (Bingham and Bergman, 1980, plates 1 and 2). 

The Ada Formation, the upper unit of the aquifer, is about 

400 feet thick and consists of interbedded limestone and shale 

units near the Kansas border. The Ada Formation grades into 

fine-grained sandstones interbedded with limestone and shale 

near the southern border of the reservation (Bingham and 

Bergman, 1980, plate 1). The lower members of the Ada Formation are seen in limestone quarries west of Pawhuska. The 

Ada Formation probably supplies little of the water produced 

from the aquifer on the reservation. 

The Vamoosa Formation, the lower unit of the aquifer, is 

about 630 feet thick and consists of alternating layers of shale 

and fine- to coarse-grained sandstone with some limestone 

(Bingham and Bergman, 1980, plate 1). Sandstone units vary 

from 5 to 60 feet in thickness. The sandstone aquifer is confined by the alternating shale beds in the Vamoosa Formation, 

except where the sandstone units crop out. The sandstones are 

cemented with clay and calcite (Oakes, 1959; Greig, 1959; 

and Shelton and others, 1985). The sources of sediment for the 

aquifer were the Arbuckle and Ouachita Uplifts in southern 

and southeastern Oklahoma (D’Lugosz and others, 1986). 

The aquifer is thicker and sandstones comprise a greater 

percentage nearer the sediment sources to the south and southwest. The regional dip of the aquifer is generally less than 1 

degree to the west (D’Lugosz and others, 1986). Movement of 

water in the aquifer is assumed to be down the regional dip.

Ground-Water Hydrologic Terms

The following terms of ground-water hydrology are 

defined in Lohman and others (1972), Heath (1983), and 

Driscoll (1986) along with a discussion of basic ground-water 

hydrology. An aquifer is a geologic formation, group of formations, or part of a formation that contains sufficient saturated 

permeable material to yield significant quantities of water to 

springs and wells. An unconfined aquifer occurs where the 

aquifer is exposed to the atmosphere locally through the openings in the overlying regolith. A confined aquifer is isolated 

from the atmosphere at the point of discharge by impermeable rocks such as shales and clays. Static water level is the 

level at which water stands in a well when no water is being 

removed from the aquifer. Pumping water level is the level 

at which water stands in a well when pumping is in progress. 

Drawdown is the difference between the water level in a 

well before pumping and the water level in the well during 

pumping. Hydraulic conductivity is the capacity of a rock to 

transmit water, and is expressed as the volume of water at the 

existing kinematic viscosity that will move in unit time under 

a unit hydraulic gradient through a unit area measured at right 

angles to the direction of flow. Transmissivity is the rate at 

which water of the prevailing kinematic viscosity is transmitted through a unit width of an aquifer under a unit hydraulic 

gradient, and equals the hydraulic conductivity multiplied by 

the aquifer thickness. Specific capacity is the yield of a well 

per unit of drawdown. 

Aquifer Data and Field Methods

Aquifer data for the Ada-Vamoosa aquifer have been published in Oklahoma Geological Survey Circular 87 (D’Lugosz 

and others, 1986). Transmissivity values ranged from 117 to 

325 feet squared per day (table 1) for four wells outside the 

study area in Creek, Lincoln, and Payne Counties (fig. 1) 

(D’Lugosz and others, 1986).

The data for Circular 87 was compiled as a regional perspective of the aquifer. Circular 87 utilized about 600 borehole 

geophysical logs from oil wells to interpret the aquifer in the 

subsurface. Borehole geophysical data are obtained during 

the drilling of oil wells after the surface casing is in place, 

after the well is drilled to a total depth, and before the well is 

completed. Estimates of the lithology, sandstone thickness, 

lateral distribution of lithologies, and electrical conductivity of 

the water can be obtained from the geophysical log data. The 

shallowest rocks, which are protected by the surface casing, 

are not part of the data. The lithology of the shallow zone was 

assumed to be the same as that on logs in nearby wells down 

dip to the west. Circular 87 divided the aquifer into unconTable 1. Ada-Vamoosa aquifer properties from wells in Creek, Payne, and Lincoln Counties.

[gpm, gallons per minute; ft, foot; gpm/ft, gallons per minute per foot; ft2/d, feet squared per day, data from D’Lugosz and others, 1986; estimated transmissivity 

values = 242 ∗ pumping rate ÷ drawdown]

Location County Pumping rate 

(gpm)

Drawdown 

(ft)

Specific

capacity 

(gpm/ft)

Estimated 

transmissivity

(ft2

/d)

17N-07E-08CBD-1 Creek 110 161 0.68 165

12N-06E-27BCB-1 Lincoln 90 186 0.48 117

15N-06E-28DBD-1 Lincoln 40 57 0.70 170

17N-05E-03ACB-1 Payne 208 155 1.34 325
Characterization of Transmissivity 

fined and confined units based on the borehole geophysical 

data. 

In a shallow ground-water system with low dissolved 

solids concentrations, borehole geophysical logs do not distinguish thin sandstones from limestones. Throughout much 

of the regional extent of the aquifer south of the reservation, 

the Ada Formation is predominately a sandstone and shale 

sequence. On the Osage Reservation, the Ada Formation is a 

limestone and shale sequence except near the southern boundary along the Arkansas River. The lithology change was not 

noted in the discussion of the aquifer in Circular 87 and thus 

was probably not taken into account in the interpretation. 

Well information for 17 of the 21 wells in this report 

was obtained from the IHS (table 2). IHS monitors the design 

and installation of domestic wells on Indian lands. The data 

available are from information supplied by the drillers who 

installed the wells for IHS. All of these wells were drilled 

after 1996 and IHS required a standard construction design 

for domestic water wells in the area. Depth to water in most 

of the wells, when the wells were drilled, was about 100 feet 

below land surface. Most of the wells penetrated from 250 to 

400 feet of the aquifer. The data for some of the wells included 

complete drawdown and recovery data. 

Data collected by the U.S. Geological Survey during this 

investigation (table 2) are pumping well data from four domestic wells collected during the summer of 2006, which was a 

drought period for Oklahoma (Oklahoma Water Resources 

Board, 2007). Many landowners who were contacted during 

this period did not want aquifer tests performed on their well 

because of lower than normal water levels and poorer productivity of their wells. The landowners reported their wells could 

be pumped dry in a few hours, if pumped continuously, and 

the water-level recovery period would be more than 24 hours. 

Because of these concerns and the small number of domestic 

wells in the northwest part of the aquifer on the reservation, no 

aquifer tests were obtained from that area. 

Aquifer tests by the U.S. Geological Survey were performed by using a Druck PDCR 35® transducer with a measurement range of 0 to 25 pounds per square inch. This range 

allowed the transducer to be lowered 30 feet below the static 

water level in a well, which was determined by using a steel 

tape. The well was then pumped continuously until water-level 

drawdown stabilized. When the pump was turned off, the 

water level was allowed to recover to the initial static level. 

The water-level data were collected by a Campbell Scientific 

data logger during the drawdown and recovery periods. 

The transducer was field checked and calibrated before 

the first aquifer test. The transducer was lowered into each 

well with an electric water level tape to check the accuracy of 

the readings at the static water level and then lowered to the 

maximum functional depth of the transducer. Field calibration measurements were used to develop a regression between 

measured water depth and pressure and a correction factor for 

the pressure data (Freeman and others, 2004).

Aquifer Test Analysis Methods and 

Results

Based on drilling information, the 21 wells analyzed for 

aquifer properties in this report are considered to be completed in the confined part of the aquifer. Drilling depth of the 

21wells in this report ranged from 140 to 400 feet and averaged 234 feet. Depth of the casing ranged from 120 to 380 feet 

and averaged 214 feet. Static water level in the wells ranged 

from 54 to 200 feet and averaged 104 feet.

Transmissivity values for the 21 wells in this report are 

presented in table 2. AQTESOLV® software (HydroSolve, 

2006) was used to calculate transmissivity for 10 of the 21 

wells where sufficient drawdown or recovery data were 

available. For the AQTESOLV calculated transmissivities, 

the aquifer was assumed to have a thickness of 400 feet and a 

static water level of 100 feet below land surface. IHS drilling 

information indicates these assumptions are appropriate for the 

confined part of the aquifer. Accordingly, aquifer-test analysis 

methods described in Cooper and Jacobs (1946), Papadopulos 

and Cooper (1967), and Agarwal (1980) were used to analyze 

the drawdown and recovery data. The test data are on file at 

the U.S. Geological Survey, Oklahoma Water Science Center 

in Oklahoma City.

Eleven of the aquifer tests did not have adequate data to 

reliably calculate a transmissivity value. Transmissivity values 

for these wells (table 2) were estimated from the specific 

capacity of the pumping wells using equation 1 (Parkhurst and 

others, 1996). 

 (1)

where: T is transmissivity, in feet squared per day; 

 Q is discharge, in gallons per minute; and 

 s is drawdown, in feet. 

The estimated transmissivity values probably have a 

greater error range than the calculated values but do provide 

relative aquifer productivity information in the area of the 

well. The estimated transmissivity values are 1.1 to 4.3 times 

greater than the calculated transmissivity values in table 2 and 

have a mean of 1.9 times greater than the calculated values. 

Likewise, the estimated transmissivity values in table 1 

(D’Lugosz and others, 1986) were calculated using equation 

1. These estimated values also are greater than the calculated 

transmissivity values (table 2).

Characterization of Transmissivity

The calculated and estimated transmissivity values shown 

in table 2 in bold font are presented in figures 2, 3, and 4. 

These transmissivity values range from 5 to 1,000 feet squared 

per day. 

T Q

s = 242
Table 2. Ada-Vamoosa aquifer test information, including pumping rate, water-level drawdown, specific capacity, estimated and calculated transmissivity, and calculation method used.

[gpm, gallons per minute; ft, foot; gpm/ft, gallons per minute per foot; ft2/d, feet squared per day; bold font transmissivity data are values used in accompanying maps, estimated transmissivity values = 242 ∗ pumping rate ÷ drawdown, used were calculation 

values could not be determined; transmissivity calculations were made using software by HydroSolve, Inc., AQTESOLV® Version 4.01, copyright 1996-2006, Reston, Virginia]

Site ID Township and 

range

Aquifer test

by Date

Pumping

rate

(gpm)

Drawdown

(ft)

Specific

capacity 

(gpm/ft)

Estimated 

transmissivity 

(ft2/d)

Calculated 

transmissivity 

(ft2/d)

Transmissivity 

calculation

method

364823096105101 T27N-R10E U.S. Geological Survey 09/05/2006 3.5 12 0.29 70 44 Papadopulos-Cooper (1967)

362803096223501 T23N-R09E Indian Health Service 11/20/1996 12 75 0.16 40 --

362302096253701 T22N-R08E U.S. Geological Survey 08/31/2006 6.7 8.6 0.78 190 44 Cooper-Jacobs (1946)

364044096170101 T25N-R09E Indian Health Service 04/07/2000 14 31.5 0.44 110 70 Papadopulos-Cooper (1967)

362404096212201 T22N-R09E Indian Health Service 07/24/2004 5 62 0.08 20 --

364007096141101 T25N-R10E Indian Health Service 10/30/1997 14 42 0.33 80 --

362621096312701 T23N-R07E Indian Health Service 08/04/2004 10 44 0.23 55 --

362623096320001 T23N-R07E Indian Health Service 05/25/2005 13.6 28.1 0.48 120 100-110 Papadopulos-Cooper (1967)

362252096284601 T22N-R08E Indian Health Service 05/08/1998 8 45 0.18 45 --

363156096332901 T26N-R09E Indian Health Service 06/17/2002 2.5 55 0.05 10 --

363803096205501 T25N-R09E Indian Health Service 03/03/1998 5 165 0.03 5 --

364857096103001 T27N-R10E Indian Health Service 09/14/2005 5 36.9 0.14 35 22 Papadopulos-Cooper (1967)

363255096210602 T24N-R09E Indian Health Service 03/16/2004 13 15 0.87 210 --

364319096180601 T26N-R10E U.S. Geological Survey 01/12/2006 7.8 9 0.87 210 112-1,000 Papadopulos-Cooper (1967),

Agarwal (1980)

362330096222801 T24N-R07E Indian Health Service 08/17/1999 5 93 0.05 15 --

362444096342101 T22N-R07E Indian Health Service 02/23/1998 10 25 0.40 100 --

363230096222401 T24N-R09E U.S. Geological Survey 08/25/2006 11 12 0.92 220 56 Papadopulos-Cooper (1967),

Agarwal (1980)

361504096182501 T21N-R09E Indian Health Service 06/11/2003 15 70 0.21 50 38 Papadopulos-Cooper (1967)

362343096305801 T22N-R07E Indian Health Service 07/07/2006 10 19.4 0.51 120 130 Papadopulos-Cooper (1967)

363443096191801 T24N-R09E Indian Health Service 06/10/2004 12 107 0.11 30 --

362516096283701 T23N-R08E Indian Health Service 12/06/2005 6 31 0.19 50 21 Papadopulos-Cooper (1967)
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R. 05 E. R. 06 E. R. 07 E. R. 08 E. R. 09 E. R. 10 E. R. 11 E. R. 12 E.

R. 04 E.

R. 03 E.

T. 29 N. T. 28 N. T. 27 N. T. 26 N. T. 25 N. T. 24 N. T. 23 N. T. 22 N. T. 21 N. T. 20 N.

Pawhuska

Wynona

Hominy

Arkansas River

21

38

56

22

70

44

44

130

30

45

80

20

40

210

100-110

5

15

10

55

100

112-1,000

-96°15'

-96°15'

-96°30'

-96°30'

-96°45'

-96°45'

-97°0'

-97°0'

-96°0'

-96°0'

37°0'

37°0'

36°45'

36°45'

36°30'

36°30'

36°15'

36°15'

 

 

0 5 10 Miles

0 5 10 Kilometers

Map compiled by U.S. Geological Survey

Base from U.S. Geological Survey digital data, 1:100,000, 1983

Albers Equal Area Conic projection, NAD83 datum

Transmissivity,

calculated from 

pump test

feet per day

EXPLANATION

80

70

2

Transmissivity,

estimated from

specific capacity

feet per day

2

Towns

Ada Formation

outcrop area

Vamoosa Formation

outcrop area

!(

!(

U.S. Geological Survey,

pump test data

Indian Health Services,

pump test data

Limit 

of 

outcrop 

area

Limit 

of 

outcrop 

area

Figure 2. Distribution of the outcrop area of the Ada-Vamoosa aquifer and the calculated 

and estimated transmissivity data for the aquifer.
!(

!(

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!(

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!( !(

!(

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!(

!(

!(

R. 05 E. R. 06 E. R. 07 E. R. 08 E. R. 09 E. R. 10 E. R. 11 E. R. 12 E.

R. 04 E.

R. 03 E.

T. 29 N. T. 28 N. T. 27 N. T. 26 N. T. 25 N. T. 24 N. T. 23 N. T. 22 N. T. 21 N. T. 20 N.

0 - 75

0 - 75

75 - 150

> 225

150 - 225

150 - 225

150 - 225

150 - 225

150 - 225

150 - 225

150 - 225

150 - 225 150 - 225

> 225

> 225

150 - 225

0 - 75

75 - 150

150 - 225 > 225

Pawhuska

Wynona

Hominy

Arkansas River

21

38

56

22

70

44

44

130

5

30

15

10

45

55

80

20

40

100

210

100-110

112-1,000

96°15'W

96°15'W

96°30'W

96°30'W

96°45'W

96°45'W

97°0'W

97°0'W

96°0'W

96°0'W

37°0'N

37°0'N

36°45'N

36°45'N

36°30'N

36°30'N

36°15'N

36°15'N

 

 

 

0 5 10 Miles

0 5 10 Kilometers

Map compiled by U.S. Geological Survey

Base from U.S. Geological Survey digital data, 1:100,000, 1983

Albers Equal Area Conic projection, NAD83 datum

Modified from D'Lugosz and others, 1986, 

for the unconfined part of the aquifer

0 - 25

25 - 50

50 - 75

greater than 75

Sand 

thickness

in feet

Transmissivity,

feet squared

per day

Specific capacity,

gallons per minute

per foot of drawdown

0 - 75

75 - 150

150 - 225

greater than 225

0 - 0.3

0.3 - 0.5

0.5 - 0.7

greater than 0.7

!(

!(

U.S. Geological Survey,

pump test data

Indian Health Services,

pump test data

Transmissivity, estimated from

specific capacity, feet per day

EXPLANATION

Towns

Circular 87 data

in unconfined part of 

aquifer

80

70 Transmissivity, calculated 

from pump test, feet per day 2

2

Limit 

of 

outcrop 

area

Limit 

of 

outcrop 

area

Figure 3. Comparison of the calculated and estimated transmissivity data with the data from 

Oklahoma Geological Survey Circular 87 for the unconfined part of the Ada-Vamoosa aquifer.
!(

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R. 05 E. R. 06 E. R. 07 E. R. 08 E. R. 09 E. R. 10 E. R. 11 E. R. 12 E.

R. 04 E.

R. 03 E.

T. 29 N. T. 28 N. T. 27 N. T. 26 N. T. 25 N. T. 24 N. T. 23 N. T. 22 N. T. 21 N. T. 20 N.

100-110

112-1,000

Pawhuska

Wynona

Hominy

Arkansas River

0 - 150

150 - 300

150 - 300

150 - 300

300 - 450

300 - 450

300 - 450

> 450

> 450

> 450

150 - 300

> 450

> 450

21

38

56

22

70

44

44

130

5

30

15

10

45

55

80

20

40

100

210

96°15'W

96°15'W

96°30'W

96°30'W

96°45'W

96°45'W

97°0'W

97°0'W

96°0'W

96°0'W

37°0'N

37°0'N

36°45'N

36°45'N

36°30'N

36°30'N

36°15'N

36°15'N

0 5 10 Miles

0 5 10 Kilometers

Map compiled by U.S. Geological Survey

Base from U.S. Geological Survey digital data, 1:100,000, 1983

Albers Equal Area Conic projection, NAD83 datum

Modified from D'Lugosz and others, 1986, 

for the confined part of the aquifer

Transmissivity,

feet squared

per day

0 - 150

150 - 300

300 - 450

greater than 450

0 - 50

50 - 100

100 - 150

greater than 150

Sandstone

thickness,

feet

Specific capacity,

gallons per minute

per foot of drawdown

0 - 0.4

0.4 - 0.8

0.8 - 1.2

greater than 1.2

!(

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U.S. Geological Survey,

pump test data

Indian Health Services,

pump test data

Transmissivity, estimated from

specific capacity, feet per day

EXPLANATION

Towns Circular 87 data

in confined part 

of aquifer

80

70 Transmissivity, calculated 

from pump test, feet per day 2

2

Limit 

of 

outcrop 

area

Limit 

of 

outcrop 

area

Figure 4. Comparison of the calculated and estimated transmissivity data with the data from 

Oklahoma Geological Survey Circular 87 for the confined part of the Ada-Vamoosa aquifer.
9 Aquifer Tests and Characterization of Transmissivity, Ada-Vamoosa Aquifer, Osage Reservation, Oklahoma, 2006

The well located in T21N-R09E (fig. 2) with a transmissivity value of 38 feet squared per day is not in the AdaVamoosa outcrop area (Bingham and Bergman, 1980, plates 1 

and 2). However, the aquifer test results illustrate the producing potential of the minor aquifers lower in the Pennsylvanian 

rock sequence.

The aquifer test data from the well with 1,000 feet 

squared per day, northeast of Pawhuska, did not fit the 

assumptions of the analysis method. The variability in the 

calculation was because of a shift in the drawdown data during 

the pump test. Such a shift could result from the well receiving 

an increasing proportion of water from the overlying valley 

alluvium after initially withdrawing water mostly from the 

Ada-Vamoosa aquifer. Two transmissivity values are reported 

for this well. The lesser value uses only the earlier data in the 

calculation and the greater value uses all the data.

Figures 3 and 4 are modified from Circular 87 (D’Lugosz 

and others, 1986) and are presented here for discussion only 

with the data from the current study. The maps were modified 

from the publication to adhere to the eastern outcrop limit of 

the base of the aquifer in Bingham and Bergman (1980). 

Figure 3 is presented in Circular 87 as the unconfined 

part of the Ada-Vamoosa aquifer. As previously discussed, 

the western area of figure 3 along the Ada Formation outcrop 

(figs. 1 and 2) probably has less potential for water production 

than shown in Circular 87 because of the limestone and shale 

sequence. The eastern area on figure 3, along the Vamoosa 

Formation outcrop (figs. 1 and 2), is the recharge area for the 

aquifer on the reservation. Areas where the sandstones are 

cropping out are the unconfined part of the aquifer. These 

areas are generally east and northeast of Pawhuska and east of 

Wynona and Hominy. 

Figure 4 is shown in Circular 87 as the confined part of 

the Ada-Vamoosa aquifer. The transmissivity values in the 

current study are thought to be from the confined part of the 

aquifer because of data from the IHS drilling information indicating the depths to water and the depths of the wells. Therefore, the transmissivity values from the current study should 

be more similar to figure 4 than figure 3. Twelve of the wells 

from this study were within the range of predicted transmissivity values from Circular 87 (fig. 4). The matching wells 

on figure 4 are on the area of the aquifer with 0 to 150 feet 

squared per day. This also is the largest area on the map. Six of 

these are calculated transmissivity values and six are estimated 

transmissivity values. The western boundary of the aquifer is 

defined in Circular 87 as the limit of usable ground water containing 1,500 milligrams per liter or less of dissolved solids. 

However, two of the wells in the current study, located west of 

the limit of usable ground-water boundary, were completed as 

domestic wells, indicating the presence of usable water. The 

western boundary of usable water in the aquifer probably varies locally on the reservation.

Five areas on figure 4 are indicated with transmissivity 

values greater than 450 feet squared per day. The northwestern area is farther from the recharge area of the aquifer and 

is confined below the Ada Formation (fig. 2). In 2006, few 

wells existed in this area. Over pumping of existing wells or 

significant additional well development in this area of the 

aquifer could pull the naturally occurring saline water, which 

is expected to be down dip to the west (D’Lugosz and others, 

1986), up into the fresh water stored in the aquifer. The four 

areas with greater transmissivity values along the eastern half 

of the aquifer (fig. 4) are on the Vamoosa Formation outcrop 

area (fig. 2) and the recharge area of the aquifer (fig. 3). The 

well west of Wynona with an estimated transmissivity of 210 

feet squared per day indicates these areas may have potential 

for ground-water development. There are wells from the current study along the edges of these four areas with transmissivity values less than predicted in Circular 87. These data may 

indicate the areas are not as large or uniformly continuous as 

presented in Circular 87. 

References

Abbott, Marvin, 2000, Water quality of the Quaternary and 

Ada-Vamoosa Aquifers on the Osage Reservation, Osage 

County, Oklahoma, 1997: U.S. Geological Survey WaterResources Investigations Report 99-4231. 76 p. (Available 

at http://pubs.usgs.gov/wri/wri994231/pdf/wri99-4231.pdf )

Alley, William, 1994, Guidance for the preparation, approval, 

and archiving of aquifer test results, Office of Ground Water 

technical memo 94.02. (Available at http://water.usgs.gov/

admin/memo/GW/gw94.02.html )

Agarwal, R.G., 1980, A new method to account for producing 

time effects when drawdown type curves are used to analyze 

pressure buildup and other test data: Society for Petroleum 

Engineers, Society of Petroleum Engineers 55th Annual Fall 

Technical Conference, September 2 1-24, Dallas, Texas: 

SPE Paper 9289).

Bingham, R.H., and Bergman, D.L., 1980, Reconnaissance of 

the water resources of the Enid quadrangle, north-central 

Oklahoma: Oklahoma Geological Survey Hydrologic Atlas 

7, 4 sheets, scale 1:250,000.

Cooper, H.H. and Jacobs, C.E., 1946, A generalized graphical 

method for evaluating formation constants and summarizing 

well field history: American Geophysical Union Transactions, v. 27, p. 526-534.

D’Lugosz, J.J., McClafin, R.G., and Marcher, M.V., 1986, 

Geohydrology of the Vamoosa-Ada aquifer, east-central 

Oklahoma: Oklahoma Geological Survey Circular 87, 41 p.

Driscoll, F.G., 1986, Groundwater and wells (2nd ed.): St. 

Paul, Minn., Johnson Filtration Systems, Inc., 1,089 p. 

Fetter, C.W., 1994, Applied hydrogeology (3rd ed.): 

Engelwood Cliffs, N.J., Prentice Hall, 691 p.
References 10

Greig, P.B., 1959, Geology of Pawnee County, Oklahoma: 

Oklahoma Geological Survey Bulletin 83, 188 p.

Freeman, L.A., Carpenter, M.C., Rosenberry, D.O., Rousseau, 

J.P., Unger, Randy, and McLean. J.S., 2004, Use of submersible pressure transducers in water-resources investigations: U.S. Geological Survey Techniques of WaterResources Investigations, book 8, chap. A3, 52 p. (Available 

at http://pubs.usgs.gov/twri/twri8a3/ )

Heath, R.C., 1983, Basic ground-water hydrology: U.S. Geological Survey Water-Supply Paper 2220, 84 p. (Available at 

http://pubs.er.usgs.gov/usgspubs/wsp/wsp2220 )

HydroSolve, Inc., 2006, AQTESOLV Version 4.01, copyright 

1996-2006, Reston, Virginia.

Lohman, S.W., Bennett, R.R., Brown, R.H., Cooper, H.H., 

Jr., Drescher, W.J., Ferris, J.G., Johnson, A.I., McGuinness, C.L., Piper, A.M., Rorabaugh, M.I., Stallman, R.W., 

and Theis, C.V., 1972, Definitions of selected ground-water 

terms—Revisions and conceptual refinements: U.S. Geological Survey Water-Supply Paper 1988, 21 p.

McClymonds, N.E., and Franke, O.L., 1972, Water-transmitting properties of aquifers on Long Island, New York: U.S. 

Geological Survey Professional Paper 627-E, 24 p.

Oakes, M.C., 1959, Geology of Creek County: Oklahoma 

Geological Survey Bulletin 81, 134 p.

Oklahoma Water Resources Board, 2007, in Hydrologic 

drought of water year 2006— A historical context: Oklahoma Water Resources Board, 4 p.

Papadopulos, I.S. and Cooper, H.H., 1967, Drawdown in a 

well of large diameter: Water Resources Research, v. 3, 

no. 1, p. 241-244.

Parkhurst, D.L., Christenson, Scott, and Breit, G.N., 1996, 

Ground-water-quality assessment of the Central Oklahoma 

aquifer, Oklahoma: Geochemical and geohydrologic investigations: U.S. Geological Survey Water-Supply 

Paper 2357-C, 101 p.

Shelton, J.W., Ross, J.S. Garden, A.J., Franks, J.L., 1985, 

Geology and mineral resources of Payne County, Oklahoma: Oklahoma Geological Survey Bulletin 137, 92 p.

U.S. Environmental Protection Agency, Drinking Water Contaminants, accessed May 19, 2008, at http://www.epa.gov/

safewater/contaminants/index.htm