Water-Supply and Irrigation Paper No. 148 ^ { S

DEPARTMENT OF THE INTERIOR

UNITED STATES GEOLOGICAL SURVEY

CHARLES D. WALCOTT, DlBECTOB

GEOLOGY AND WATER RESOURCES 

OF OKLAHOMA

BY

CHARLES NEWTON GOULD

WASHINGTON

GOVERNMENT PRINTING OFFICE 

1905
Water-Supply and Irrigation Paper No. 148

DEPAETMENT OF THE INTEEIOE

UNITED tSTATES GEOLOGICAL SURVEY

CHARLES D. WALCOTT, DIRECTOR

GEOLOGY AND WATER RESOURCES 

OF OKLAHOMA

BY

CHARLES NEWTON GOULD

WASHINGTON

GOVERNMENT PRINTING OFFICE

1905
CONTENTS.

Page.

Introduction. -------.-____._._____..________________._____...__.______.____ 11

Location and general description ___--'._._.--__.-.___ 11

Sources of data ._________-___..--_.----.__-_.._--___- 11

Topography ....... .__...__-.__ ___ ............................-_........- 12

General features..-..-..--.-.--...,-_...---.-.-....-----.-.--...---.. 12

Uplands. -.--.__-_-_.__._.._.___.______._______.__,___.____.__._.__. 13

Wichita Mountain region _-__._______..__._-.-_------._-.._-- 15

Flint-Sandstone Hills region.. -..---.. ..---__-_.----------__.. 16

Low Plains region-............................._... _ _____ 16

Gypsum Hills region .--_.__.__________.__.__----_----__--... 17

High Plains region.____--__--___---.-___.-.--.- ..-._...--.... 17

Dakota Sandstone region. .___..._.___.-.._,-.--.-_-.-.-.... 18

Valleys.--. ..... ^-.................... .__..-... _______ ____________ _ 18

Arkansas Valley-..._-.____.____._______..__.____ .-____._____ 18

Salt Fork Valley.-___-____-___-_______...__-----_----__--___. 19

Cimarron Valley.._.._--___--____---___._.-____----_.---_..__ 19

North Canadian Valley -_-------_--__-----__----_---------_.- 20

South Canadian Valley. ______ ....--...---...--._.--_....-.-.. 20

Washita Valley................ .................._........... 21

RedRiverVaUey--..---...--..---.-..-.-----------.-.---.... 21

Conclusion .------------------..-----...---.--_ _..___.-__--__ 22

Geology._.___-_ .--..-...........................-..............._...... 22

General statement _---..---...-..........-....--..-.-__-..--...--. .. 23

Relations of pre-Carboniferous rocks -__.,_.____----.-_ .............. 23

Igneous rocks...-..-_......________._._...____--____---------__-.- _. 25

Gabbro_ .................................................... 25

Granite-porphyry --__--____...___-__..----_----_-_.---.---.._ 25

Granite-..-.--.-.----.---..-.--..-----.-.-.--.--..---..--..-. 26

Sedimentary rocks-----.--.------------------.---_-------.--------..- 26

Cambrian rocks._________.____.___._,_____-_.___.____.._____-____._ 26

Reagan sandstone,_..-.--...--.....--...---....---.---_-. 26

Cambro-Ordovician rocks .--.......-.......-.-_.----_.---..----.. 27

Arbuckle limestone --........-.--..-.--_------.---------. 27

Ordovician rocks.__. --.-.....-...--.....--.....-................ 27

Viola limestone ---_-.._--____-----.----_---__---_--__---- 27

Carboniferous rocks.,..-..............-.._-...-...-----..--..-.----. 28

Pennsylvanian series.-----.-_-.-----..-.---------.--..-.----- 28

General relations .-.....-........._......--....-.---_--.-. 28

Relation to the Permian--_____ ^__-___.--_____-----_---__ 28

Description of Pennsylvanian rocks in Oklahoma.__._.____ 32

Hominy district..._-.._____-__.--_.__.---__---_-..__ 32

Chandler district .. ,..,...-..----.----------.------ 33
4 CONTENTS.

Geology Continued. Page. 

Sedimentary rocks Continued.

Carboniferous rocks Continued.

Permian series. -_--.--.-..---.-_---.-------._-__-__---------- 34

Permian rocks of Kansas-.-..--.-----_ _._--___-_--_.__-_ 34

General relations of Permian rocks in Oklahoma - _ ...... 35

Classification .-..___-_--.--_-_-. ....._......... -_.._._. 37

Enid formation ......_____-__-_--_-.__ __-._--_---.__.-_. 39

Blaine formation ___.____.__________._____.._-__.__ _ _.. _ 44

Ferguson gypsum member._-.-____.____--.__--__.__ 46

Medicine Lodge gypsum member._.___._____-_____-__ 47

Shimer gypsum member -.._..____--___.-_____--_..-. 51

Woodward formation .--__-__._.-_...____.__ ._--____.-_. 52

Dog Creek shale member..__-_____-._-..-._-.---__-_. 52

Whitehorse sandstone member _-____--___._.__--..-_. 55

Day Creek dolomite member ...... .................. 57

Greer formation -.._...-.-..-.__.._..__._ ...._........ 59

Chaney gypsum member.-,...--.--.--._-.....--..... 66

Riser gypsum member......................... ..... 67

Haystack gypsum member __..__.__._-........-....._ 69

Cedartop gypsum member ___________________________ 69

Collingsworth gypsum member. ___-._-.._....-.._.... 70

Mangum dplomite member.--_--__-________.______._- 71

Quartermaster formation -__-._.-.-._.-__.__-_.-__-____._ 72

Red beds of uncertain relations. --.--.--_.-.---_-----.---. 73

Lawton area-________..____-__--_____-.__...__.___..__ 73

Lavernearea ________________________________________ 73

Conglomerate______________________________ ._....... 73

Gypsum in the red beds ___ -_._....__-..--.--.-. ........ 74

Paleontology of the red beds... - -.-...-..-..-..----..---. 75

Age of the red beds ..-__-_...-.--.--_-.__ ..._......_... 77

Cretaceous rocks..... .----..--.---.....----.--.----.----...-..-.. 77

Comanche series (Lower Cretaceous) -_._--.---_-._..-...._-___ 78

Upper Cretaceous._..__._.__.__ .............. ........._.... 78

Dakota sandstones...-...-.---------.--,-.----.--.'-.....- 78

Tertiary rocks -.__-_--__...._. ____.__._ ._............_......... 79

Physical properties. .......,....^..................... 80

Origin-..-.....-..-.-..-...-.-..--........-.......... 81

Extent and thickness.-_---._.-.---....--..-.-.-......_ 81

Lava of Black Mesa._..________-.________.______.____.__. 81

Quaternary rocks _..--_..---.--.-.-.-.--.-.....-...----_.--.--__. 82

Sandhills.-....--..---.---.---.--..-.-...._..-.--.-.---. 82

Alluvium.----.--....-.-_--.-_..--_--.----..-.----------- 84

Water supply.....--..-...---._-..-..-...-.--.--.----------_----------.-. 84

General conditions..--------.--------.------..---_--..........---.... 84

Wichita Mountain region .....--__-------------..-----.....__ 85

Flint-Sandstone Hills region _--.-----.---.--_--_.-_--.---__-. 86

Low Plains region -......_-..-.- .--.-..-_---.---...-.-.--.-.. 86

Gypsum Hills region......--.--..---..-_-- .................. 87

High Plainsregion.---_.-.-----_-._-..-----_--_-..-.__--.-.._ 88

Dakota Sandstone region. -.--..--...---........-..-..--....-- 88
CONTENTS. 5

Water supply Continued. Page.

Streams _--.__-___________--____._-_..-.:______________._-___-____-_-_ 89

Arkansas River._.-_____.....___-__.________.._________._-___ 89

SaltFork River.-....-.__.-.____-___-_--_--__-_......__ .____ 89

Cimarron River. ______...____-_.___-__...._-... ._.._-..._.__ 90

North Canadian River ..__.-____-____-__-___._-________.-_.. 91

South Canadian River_____________________________________ .. 92

Washita River.. ................................ ............ 93

Red River........... .... .................................. 93

Stream measurements..--.--.-------. .-.---...-.. ..._________ 94

Springs. --_-_--.. _._.___..___.._._-.._-__________-___-__---___...- 94

Fresh-water springs. -..-.----.-----.----.--..--..-_----------..- 95

Wichita Mountain springs .__._____________---_-. .-..---.... 95

Limestone springs --.--.-___________________-_____-.-----.-. 95

Sandstone springs...._-.---...-.-_.-------._.------------.-.. 97

Red beds springs..-_ -____.__,---_._-----.------------------- 97

Gypsum springs_.___-- .--_....------------.-----_-.----..--. 98

Tertiary springs .--______ __.__-___._________-__--_.-_--_.-..- 98

Alluvial springs. -.... _--_____-____-____-_____--__------_-_--- 99

Salt springs and plsliris ........._................................. 100

Woods County plain _.............._....._.......___......... 101

Woodward County plains -.__---__-_______________----------- 101

Blaine County plain-__________-______..__.________.-_____._-. 102

Roger Mills County plain _____----------_-_---.---------__.-- 103

Greer County plains _ .. -__._----____-__--_____---__-------- 104

Sulphur springs ------------ -________..._----_____----_-_-_--_---- 104

Granite sulphur spring. _.._.,___.-_-_..-_..___._!_..___.-.___ 105

Rainy Mountain sulphur spring .--....--.......---..-.....-.. 105

Apache sulphur spring ...................................... 105

Deep wells. --_-.-..----------.-.......------.--------.-.--------.-_.. 105

'Greneral conditions _____--_-_______-_--___-__.__--_:-_-._-.___---. 105

Water wells -..--.....-.--.---...-......-----.......------------- 106

FortReno well-------------------------------------- 106

Kingfisher well ...____.-_-_-.----- ---..---_-----_.---_ 106

Optima well -......--.--....-----.-.._.-..----..-.-.. 106

Childress,Tex., well.--------------------------------- 106

Oil and gas wells. _..-..-........_...--_---_---------...--.----.--- 106

Wells in the Osage Nation.__-___--_-.--_____-__-----. 106

Cleveland well-........-....-------------.--.-------- 107

Newkirk well....----..........-.--.-.---.-.-...-.--- 107

Shawnee well..__..__.__._-.-_-_--------.------------ 107

Jetwell .............. ...........---.-._--_......... 107

Anthony. Kans., well. _______._-----_---_.-_--_.------ 107.

Conclusion ...................................................... 107

Artesian water -.....-.....-.....-.--......._...--_-._--.-_--.-....-. 108

Water conditions, by counties.--_ -.....---.-------._-----------_----- 109

Osage Nation ........-.......-..__..-...---..-.-....-----_.-...--- 109

Kay County -.-..........---.-...-....--.-------------.---.---... 110

Noble County......-_---...--.....-.-.....-............-.--...--- 112

Pawnee County.....--._______-...._---.-..___-_--__-____ ...-._ 112

Payne County .----..------------.--.-_---------------------..... 113
6 CONTENTS.

Water supply Continued.

Water conditions by counties Continued. Page.

Lincoln County_____.___--________-____--__----__-_____--_----___ 114

Pottawatomie County _-.__--__-__________-_--_--._______ ______ 114

Cleveland County.._____.____----___--_____-__-----._____-__.___. 115

Oklahoma County _________ _____________________________________ 116

Logan County._____________.__._________....__.__..______....__. 117

Canadian County ................................................ 117

Kingfisher County _______________________________________________ 118

Garfield County -- .- _____- -.______ _.__.. ___. 119

Grant County .........................................^......... 120

Woods County, __________________ _ - _____ ____ ____ 121

Blaine County ................................................... 123

Caddo County _________-._-______..___-____...._____-_.________ ... 124

Comanche County _-_---_-------_______--_-------_-----_______-. 125

Kiowa County_._.._.........____........__...................... 126

Greer County .................................................... 126

WasMta County _._.__.__.....__..._._........._.__..___......... 127

Custer County.____________..... ________________________________ 128

Dewey County. .................................................. 128

Roger Mills County -------_ . _-- -- ---- ------- 129

Day County .________.__.________.___________.____.._.__---.__--_ 130

Woodward County.______ .............. _..._._......-._..___-_. 130

Beaver County -------.-_-__--_---.--_...---._-__--.______--_-_-- 131

Irrigation ----.----__......_....___-......._.-......._-----._..--.-.---._ 133

General statement ____-_-__--___--------.,.-..__--------_---._------_ 133

Irrigation from rivers......._..._........_........_----.._.._---.---- 133

Irrigation from reservoirs ............................................ 135

Medicine Bluff site. __-_-__--.--.-.,--...___----____._.______. 136

Lower narrows of Otter Creek ----.___-----_---_.------------ 136

Quartz Mountain site ......................... .............. 137

Cimarron River site ---..........--....._----------._.--..--.- 138

Utilization of storm waters ___-__-__._.----_----._----.------ 138

Irrigation from springs ................................... .......... 139

Irrigation from wells __--__--_________----___.----------_------_.---. 140

Climate .............._..............................--.-.......--.--.--- 141

Water analyses .--_-...._-_..-_---.....--.----..-..--_---------.--------- 142

Method ..-....____.....__... ._.... . -.---...---.- 142

Definition of terms ___._.......-_--..--.-..--.---_.----------- 142

Comparison of red beds wells_-----....._--.------.----.------ 143

Analyses ______._.._...................._.---_--..-------..-. 146

Well records .--...---.-_.----------..-..-----.--__---------------------- 155

Index ---.-.------_.-._..-.----.-._.---.-----_-.--_.-_---------- -------- 175
ILLUSTRATIONS.

Page. 

PLATE I. Preliminary geologic map and sections of Oklahoma ------------ 12

II. A, Granite weathering on top of Quanah Mountain; B, Devils

Canyon Mountain...__. _____.._...___._.____.___-.--.-..__-_-- 14

III. A, Upland basins; B, Gypsum bluffs on North Fork of Bed River. 16

IV. A, Dakota erosion near Kenton, Okla.; B, Erosion forms in Dakota Cretaceous.--.._..______._.__._.__._..--.--..--------.-- 18

V. A, Prairie stream just beginning to cut; B, Pit holes along

prairiearroyo_____________ __-______.__._____.___..------.--- 30

VI. Map of the Wichita Mountains ------------- .--__-----------.-- 24

VII. A, Typical red-beds erosion; B, Bed-beds slope below massive

gypsum ---_-----.._.._._________.__..__.--.-..----.--------- 42

VIII. A. Gypsum concretions covering the slopes of red clay, Glass

Mountains; B, Selenite and satin spar in red clay ------------- 44

I.. A, Cedar Hill, east of Watonga, Okla., showing Ferguson gypsum 

on the slope and Medicine Lodge gypsum as a cap; B, Anhydrite 

member of the Medicine Lodge gypsum. ._-_--__---._------.-- 48

X. A, Erosion forms in Caddo County buttes; B, Dakota sandstone

hnis......................................................... 56

XI. Entrance to gypsum cave near Weatherford, Okla ....-...---_.. 62

XII. A, B, Cross-bedding in mortar beds....--.---.--....--.....-..-- 80

XIII. A, B, Mortar-bed topography ..... ............................ 80

XIV. A, Tertiary pebbles in place; B, Mortar-bed structure..-..-_...- 80

XV. High Plains windmills ......................................... 88

XVI. Map showing drainage areas of streams crossing Oklahoma ..... 90

XVII. A, Bluff of Dakota sandstone; B, Bed beds-Dakota unconformity. 92

XVIII. A, Dam site at Quartz Mountain; B, Scene along the upper

course of South Canadian Biver...-.......-.-_---.-..-.-...-- 92

XIX. A, B, Tertiary springs and contiguous topography .............. 98

XX. A, B, Salt Plains on the Cimarron--............................ 100

XXI. A, Salt spring issuing from beneath gypsum ledge; B, Log and

earth dam on upper Cimarron Biver............--.......----- 102

XXII. Wellsections .._. .................................._...-......- 106

FIG. 1. Map of Oklahoma, showing physiographic features................ 14

2. Generalized section of the Oklahoma Permian red beds ............ 40

3. Section 3 miles west of Altona, Okla .---.-..----- ..----..._.-.-.- 45

4. Section near Watonga, in sec. 32, T. 16 N., B. 10 W............... 46

5. Cedar Hill section, in SW. i sec. 18, T. 16 N., R. 10 W ............ 47

6. Hitchcock section, 4 miles south of Hitchcock, Okla., along Bock

Island Bailroad _-.--__-_---.-__._-------.--------------------- 48

7. Bitter Creek section, 6 miles southwest of Ferguson, Okla., on west

 branch of Bitter Creek ._..---...------...-.--.-.----.--------.- 50

7
8 ILLUSTRATIONS.

Page. 

FIG. 8. The^Rubey section, in South Canyon, head of Salt Creek, at the

Rubey Stucco-Plaster mill, Ferguson, Okla.----.-_...-------_--- 51

9. Section of gypsum cave. .--____---__.__- .__-_-____--____-----__--- 52

10. Roscoe section, 1 mile south and 11 miles west of Roscoe, Okla..... 53

11. Glass Mountain section, on northwest side of mountain -_-_.._____ 54

12. Granton section; gypsum-capped butte 1 mile east of Granton,

Okla.-..........-.'............................................ 55

13. Section of hill west of the mouth of Greaver Creek- ...... ........ 56

14. Section on Main Creek one-half mile northeast of Bat Cave ..._--. 58

15. Section on Sand Creek, 5 miles northwest of Quinlan, Okla. ..._--- 60

16. Section on butte at mouth of Doe Creek, Woodward County, Okla_ _ 61

17. Section at high bluff at southeast corner of the Salt Plain --------- 62

18. Section of bluff 5 miles northwest of Weatherford, Okla........... 63

19. Section of butte 5 miles southeast of Cloud Chief, Okla_........... 64

20. Little Washita River section, taken west of Frisco Railroad crossing. 65

21. Section of bluff at the Salt Plain, 5 miles south of Carter, Okla .. _ _ 66

22. Haystack section, 6 miles south of Delhi, Okla ......--...----..... 67

23. Section at Salton, Greer County, Okla _............._..__........ 68

24. Section at mouth of Hackberry Creek, Greer County, Okla....,.. - 69

25. Section 10 miles south of Mangurn, Okla., in bluffs between Salt

Fork and Horse Branch -_.__-------.--._----...------------.--- 70

26. Section on Boggy Creek, 9 miles northeast of Eldorado, Okla __._.. 71

27. Tertiary structure, showing formation of mortar beds...-_.....-.. 80

28. Section of Black Mesa, 3 miles north of Kenton, Okla............. 82

29. Ideal section of Tertiary springs..-.------------------------------ 99

30. Section at Cleo springs, Cleo, Okla -.----.---.---..----------..-.- 122

31. Map showing the arid, semiarid, and humid regions of the United

States _-.._____________._._._____--_____--.---.--.------- -- 141

32. Map showing the mean annual rainfall of the United States....... 142
LETTER OF TRANSMITTAL.

DEPARTMENT or THE INTERIOR,

UNITED STATES GEOLOGICAL SURVEY,

RECLAMATION SERVICE, 

Washington, D. 6'., August 19, 1904.

SIR : I transmit herewith a manuscript, with illustrations, by Prof. 

C. IS". Goulcl, on the " Geology and Water Resources of Oklahoma," 

and recommend its publication in the series of water-supply papers.

The paper was prepared under the direction of Mr. IS". H. Darton, 

geologist in charge of the western section of the division of hydrology. 

It throws light upon the water resources of this section, regarding 

which but little has hitherto been known, and will be of considerable 

value in the development of this portion of the country. 

Very respectfully,

F. H. NEWELL,

Chief Engineer. 

Hon. CHARLES D. WALCOTT,

Director United States Geological Survey.

9
GEOLOGY AND WATER RESOURCES OF 

OKLAHOMA.

By CHARLES NEWTON GOTJLD.

INTRODUCTION.

Location mid general description. Oklahoma is situated in the 

southern part of the Great Plains, its northern boundary being the 

thirty-seventh parallel of north latitude. On the west the greater 

part of the Territory is bounded by the one hundredth meridian, but 

the northwest corner, Beaver County, 35 miles in width, extends west 

of this meridian for a distance of 16.5 miles. The southern and eastern boundaries are irregular, and are sometimes rivers and sometimes 

parallels or meridians. In places it extends south to the thirty-fourth 

parallel and east to the ninety-sixth meridian.

The area of the Territory at the present time is 39,030 square miles, 

about that of Ohio; the population is 365,000, and the assessed value 

of taxable property $85,000,000. Its resources are chiefly agricultural, although minerals are known to exist in various localities. Oil 

and gas are present in various parts of the Territory, but Oklahoma's 

greatest mineral wealth consists of inexhaustible deposits of gypsum 

and salt, which occur chiefly in the western part of the Territory.

Sources of data. The work which forms the basis for this report 

was carried on in the field and office during the years 1900-1903. In 

1900 the writer was a member of a field party of the Oklahoma Geological Survey, and in 1901, in connection with Mr. Joseph A. Taff. 

spent a month making a map of the Wichita Mountains. In 1902 he 

had charge of the field parties of the Oklahoma Geological Survey, 

which studied the gypsum deposits in the western part of the Territory; and in 1903 made a reconnaissance in western Oklahoma, southwestern Kansas, southeastern Colorado, northern New Mexico, and 

the Panhandle of Texas to determine the water conditions along the 

upper courses of South Canadian, North Canadian, and Cimarron 

rivers." In addition, many short trips have been made to various

0 Gould, Ohas. N., Reconnaissance in western Oklahoma and adjacent areas: Second 

Ann. Rept. Reclamation Service, 1904, pp. 423-432.

11
U.S. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. 143 PL.

LEGEND

Salt plains

PRELIMINARY 

GEOLOGIC MAP AND SECTIONS

OF

OKLAHOMA TERRITORY

BY C.FGOTJLD.

Prepared, under tlie direction of N.II.Darton 

Base COBDtpiled from CT.S.G.S. maps, railroad Levels, special surveys, and various sources.

Contour interval 100 feet.

flatiun is mean sea, level.

Comanchfi series 

(ffivuiff piano tollorrtson 

tn.l&nton area)

Red beds of uncertain 

relation

**''jjj*&&JM Marion aad~Welliiigton

formation S. ^

Houituy formalio.ii

A

("' Spring's from i^heous rocks 

+ Spring's rrom ifcrnestoiip 

 Tertiary 

O Gypsum spring's 

Red beds springs

& 

X Flint Hllta

ANDREW B.GRAHAM CO.. LITHOGRAPHERS. WASHINGTON. D C.
12 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

parts of the Territory. Since November, 1902, more than 11,000 

blanks and requests for information regarding wells and springs have 

been sent out and approximately 5,000 replies have been received.

The writer has been very ably assisted by several advanced students 

in the University of Oklahoma. Mr. Pierce Larkin has had charge 

of the subject of springs, Mr. Charles A. Long of deep wells, Mr. 

Charles T. Kirk of rivers. All of these gentlemen and Mr. Chester 

A. Eeeds, who has also assisted in the office the past year, were members of the field party during the season of 1903. Mr. Kirk and Mr. 

Eeeds have drawn the greater part of the maps and figures. Seven 

of the plates are from photographs made by Dr. A. H. Van Vleet, of 

the Oklahoma Geological Survey.

The water analysis has been made under the direction of Dr. 

Edwin DeBarr, professor of chemistry in the University of Oklahoma, largely by his assistants, Mr. E. S. Sherwiii and Mr. E. E. 

Gridley, students in the university; and by Professors Fields and 

Holter, of the Oklahoma Agricultural and Mechanical College. The 

gypsums and clays were analyzed by Mr. Sherwin, while the water 

analyses were compiled by Mr. Gridley.

TOPOGRAPHY.

GENERAL FEATURES.

The topographic features of Oklahoma are due to the fact that it 

is part of a region which was formerly a plain which was worn 

down nearly to sea level, then elevated, and again eroded. The surface slopes eastward at an average rate of about 8 feet to the mile. 

The highest point in the Territory, approximately 4,500 feet, is on 

Black Mesa, a lava-covered table-land which extends from Colorado 

into the extreme northwestern corner of Beaver County. The lowest 

elevation, about 700 feet, is in the southeastern corner of Osage 

Nation, where Arkansas Eiver flows from Oklahoma into Indian 

Territory. Cross sections made at various points in Oklahoma are 

shown in PL I.

In general, the rocks of eastern Oklahoma, Kansas, and the Indian 

Territory dip to the. west or southwest, while the country slopes to 

the east. In most localities the dip is from 10 to 20 feet to the mile. 

If the surface were level, an outcropping ledge would be 10 to 20 

feet below the surface 1 mile to the west of its place of outcrop. Because of this fact the highest rock on a north- or south-facing escarpment is found lower and lower in the valley to the west, until it finally 

disappears under the bed of a stream, and still farther west may be 

penetrated in a well many feet underground. In the meantime other
UPLANDS. 13

ledges outcrop and in turn dip into the valley, disappear beneath the 

stream bed, and are succeeded by others still higher.

This peculiar combination of slope of surface and dip of rock, 

together with the erosion of the exposed ledges, gives the marked 

" stair-step " structure to so much of the Great Plains. Westward 

the hills rise constantly higher and higher. Such conspicuous forms 

of relief as the Flint Hills, the Dakota Sandstone Hills, or the 

Gypsum Hills of Kansas and Oklahoma are simply somewhat exaggerated examples of this phenomenon. These hills are more conspicuous because, local conditions of sedimentation or erosion have 

made them higher than the surrounding region, but there are scores 

of less-marked escarpments.

The forms of relief of Oklahoma are the result of two factors: 

First, certain broad structural zones striking in a general northeastsouthwest direction, and, second, the alternation of high divides and 

shallow valleys resulting from stream erosion. Six streams of 

considerable size cross these structural zones, approximately at right 

angles, and produce a sort of checkerboard of upland and valley, 

flat prairie and broken country, which extends north into Kansas 

and south into Texas. This arrangement, however, can be distinguished in its broader outlines only by one who is thoroughly familiar \vith the topography of the entire region. The only exception 

to this general topographic plan is the Wichita Mountain region, 

wThere a dome-shaped mass of igneous and lower Paleozoic rocks has 

been thrust up from below, afterwards surrounded by sedimentary 

rocks and still later extensively eroded, so that the range appears to be 

a series of buried mountains with their tops sticking above a vast 

plain.

The topography of Oklahoma will be discussed with regard to the 

features due to the structural zones and with reference to valley 

erosion. On the contour map (PL I) the general configuration of 

the Territory is shown. Contour lines are lines of equal elevation 

above a certain datum, and the uniform altitudinal space between 

adjacent contour lines is called the contour interval. On this map 

the datum is sea level and the contour interval is 100 feet. If a person should follow one of these contour lines he would go neither 

uphill nor downhill, but on a level. If an area is gently sloping, the 

lines are far apart; if it is a steep slope, they are crowded together; 

and if the slope is actually perpendicular the lines will touch. They 

encircle the hills and recede into the reentrant angles of valleys, indicating both the shape and elevation of the relief forms.

UPLANDS.

With the exception of the Wichita Mountains, there are comparatively few conspicuous relief forms in Oklahoma, In the Osage
14 GEOLOGY AND WATEK RESOURCES OF OKLAHOMA.

Nation, in the northeastern part of the Territory, and the counties 

bordering Arkansas River the smaller streams have cut canyons 

into the hard limestone and sandstone, and throughout the central 

and southwestern part of the Territory are ranges of gypsum hills 

that rise steeply above the level plain to the east 200 or 300 feet. 

In the extreme northwestern corner of Beaver County Cimarron 

River has cut a canyon of considerable size through Cretaceous rocks.

With the exceptions just mentioned, the surface is usually one of 

low relief. In the central and western part of the Territory there are 

areas, sometimes thousands of square miles in extent, of practically 

level plain occupied by prosperous farms, with growing villages and 

cities.

Following a general classification only, without attempting to outline definite physiographic areas, because they all grade insensibly,

MAP SHOWING

PHYSIOGEAPHIC KEGIONS

IN OKLAHOMA

By C. N. Oculd

1904.

Scale

LEGEND 

fgH wichita Mountain region

Flint sandstone hill region

Low plains region

Gypsum hills region

High plains region

Dakota sandstone hillB.regiou

FIG. 1. Map of Oklahoma, showing physiographic features.

Oklahoma may be divided into the following topographic regions: 

(1) Wichita Mountain region; (2) Flint-Sandstone Hills region; 

(3) Low Plains region; (4) Gypsum Hills region; (5) High Plains 

region, and (6) the Dakota Sandstone region. These regions are 

shown in fig. 1. It is possible that the third and fourth of these divisions correspond, at least in part, to Professor Hill's Arapahoe and 

Canadian belts.0 Doctor Adams has proposed & a classification for 

Kansas physiographic divisions, according to which the northern part 

of Oklahoma is included under Osage Prairie, Flint Hills Uplands, 

Great Bend Prairie, Oklahoma Prairie, Red Hills Upland, and High 

Plains. It has not been found practicable to follow the classification

0 Hill, R. T., Geography and geology of the Black and Grand prairies. Texas: Twentyfirst Ann. Kept. TT. S. Geol. Survey, pt. 7, 1901, p. 93.

6 Adams, G. I., Physiographic divisions of Kansas: Trans. Kansas Acad. Sci., vol. 18. 

1903, p. 109.
U. S. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. U8 PL. II

A. GRANITE WEATHERING ON TOP OF QUANAH MOUNTAIN.

B. DEVILS CANYON MOUNTAIN.
UPLANDS. 15

of either Hill or Adams, and for this reason new terms are used. It 

is, however, not the intention of the writer to propose these names as 

any but convenient working terms for purpose of discussion.

WICHITA MOUNTAIN REGION.0

The Wichita Mountains constitute the westernmost of three domes 

or uplifts, each of which forms a separate group of mountains. Of 

these the easternmost, to which the term " Ouachitas '" has sometimes 

been applied, lies in southwestern Arkansas and the southern part of 

the Choctaw Nation. In the Chickasaw Nation occur the Arbuckle 

Mountains and in southwestern Oklahoma the Wichita Mountains. 

Some authorities, however, notably Hill, use the term " Ouachita 

Mountains " to apply to the entire series of uplifts and designate the 

easternmost of these as the Massern ranges.6

The Wichita Mountains differ from all others in the Territory in 

that they are composed of igneous rocks, chiefly granite and porphyry. 

They have been eroded, for the most part, into peaks which vary in 

height from a few hundred to perhaps 1,200 feet. The main range 

extends west from near Fort Sill for a distance of about 30 miles, has 

an average width of 12 miles, and includes among others such peaks 

as Mount Scott, Mount Sheridan, Mount Baker, Haystack Mountain, 

Signal Mountain, Saddle Mountain, and Quanah Mountain (PL II, 

A ). West of this main range to beyond the North Fork of Red River 

are scattered a number of smaller ranges and peaks, such as Raggedy 

Mountains, Mount Tepee, Devils Canyon Mountain (PL II, #), 

Quartz Mountain, and Headquarters Mountain. From a distance 

these granite peaks present the regular saw-toothed appearance noticed along the Front Range of the Rockies or in the Sierra Nevadas, 

with the difference that the Wichita topography is more subdued.

On the north and east for a distance of 30 miles or more is a parallel range of hills composed chiefly of hard massive limestone, and 

on the east and south are small rounded knobs of similar limestone. 

These limestone areas are remnants of a series of Paleozoic rocks 

which once extended as a dome over the igneous rocks, but which have 

been deeply eroded since the dome was uplifted.

On all sides and between these ranges of granite and limestone the 

rocks are composed of " red beds"" shale and sandstone, with local 

deposits of conglomerate. In other words, at the time the red beds 

were being deposited the Wichitas were probably islands in the sea. 

The numerous creeks which head in these mountains flow either south 

into Red River or north into the Washita.

0 For detailed discussion of the Wichitas see Taff, Joseph A., Prof. Paper U. S. Geol. 

Survey No. 31, 1904. The writer, as a member of Mr. Taff's party in 1901, assisted in 

preparing a geologic map of these mountains.

6 Op. cit., p. 37.
16 GEOLOGY AND WATER RESOURCES OF OKLAHOMA. 

FLINT-SANDSTONE HILLS REGION.

This region includes the Osage and Kaw reservations lying east of 

Arkansas River, Kay, Noble, Pawnee, Payne, Lincoln, and Pottawatomie counties, and the eastern part of Logan, Oklahoma, and Cleveland counties. It comprises in its northern part the southern extension of the Flint Hills, which stretch from Nebraska across Kansas 

into Oklahoma. Near the Kansas-Oklahoma line the Flint Hills consist mostly of limestone ledges containing large numbers of flint 

concretions, interbedcled with shales and sandstones, but in the Osage 

Nation the limestones thin out and most of the ledges disappear 

before Arkansas River is reached, a few only continuing as far as 

Cimarron River. South of that stream the rocks are almost entirety 

red shales and sandstones.

The part of Oklahoma north of the Arkansas is characterized by 

typical limestone topography rounded hills and knobs, steep shale 

slopes with numerous rock terraces, and rather narrow valleys. 

The principal streams are Bird, Hominy, Salt, Beaver, Turkey, and 

Buck creeks. The rocks dip gently to the west and southwest, and 

the stair-step arrangement of the strata, so characteristic of certain 

parts of Kansas, is well exhibited. West and south of the Arkansas 

the relief is not so pronounced, as the limestone ledges become thinner 

and are replaced by sandstones and shales. Streams have cut valleys 

into the sandstone ledges, and steep but low bluffs are conspicuous. 

In the western part of the region the topography is characteristically 

that of the red beds, with few forms of relief except low banks along 

the streams.

LOW PLAINS REGION.

In the Low Plains region, which includes western Kay, Noble, 

Logan, Oklahoma, and Cleveland counties, eastern Canadian, Blaine, 

and Woods counties, and the greater part of Kingfisher, Garfield, 

and Grant counties, as well as the western part of the Chickasaw 

Nation, the topography is rolling. Steep bluffs are rare, and high 

knobs are practically unknown. Rivers of considerable size Salt 

Fork, Cimarron, North Canadian, and South Canadian flow across 

this region from northwest to southeast and have carved broad and 

shallow valleys. The high divides are the remnants of the old high 

table, and, because their slope to the east is so gentle as to be practically unnoticeable, a person may travel across the country for 20 

miles along some lines without ascending or descending abruptly 

20 feet from the general level. The south bluff of these rivers, for 

the greater part of their course, is cut up by canyons, while the slope 

north is generally unbroken and is covered with sand hills (p. 84).
U. S. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. 148 PL.

A. UPLAND BASINS.

B. GYPSUM BLUFFS ON NORTH FORK OF RED RIVER.
UPLANDS. 17

GYPSUM HILLS REGION.

The Gypsum Hills region includes parts or all of Woods, Woodward, Blaine, Dewey, Day, Canadian, Caddo, Kiowa, Comanche, 

Greer, Washita, Ouster, and Roger Mills counties, in each of which 

there are exposures of gypsum. In this section the relief is more 

marked than in the Low Plains region, owing chiefly to the unequal 

erosion consequent upon the relatively hard ledges of gypsum which 

outcrop in this part of the territory and to the hard sandstone and 

dolomite which lie above the gypsum. The relation between these 

rocks will be explained under the heading u Geology " (pp. 44, 71). 

The general strike of all the gypsum beds is north and south, the 

most eastern exposure being just north of El Reno, the county seat 

of Canadian County, while to the southwest the gypsum ledges extend, through Greer County, into the Panhandle of Texas.

There are two prominent types of gypsum topography in Oklahoma the wall-canyon type and the round-mound type. The wallcanyon type occurs chiefly in Blaine, Woods, and Woodward counties 

along the range of gypsum hills designated in this report the Blaine 

Gypsum Hills, and again in southern Roger Mills and northern 

Greer counties (PI. Ill, B). This type of topography is characterized by steep bluffs of red clay capped by massive ledges of 

gypsum. These bluffs rise steeply above the plain, and numerous 

streams have cut deep and narrow canyons into them. The second 

type of gypsum topography is marked by low, white, rounded, gypsum 

knolls standing out on the plain, or by gentle slopes of gypsum along 

shallow streams. Such exposures are characteristic of parts of 

Dewey, Custer, Washita, Caddo, and southern Greer counties.

HIGH PLAINS REGION.

This region includes the most elevated portions of the Territory, 

and is typically developed in Beaver, Woodward, and northern Day 

counties, lying west of and at a higher level than the line of gypsum 

hills. Beaver County, an area 165 miles long and 35 miles wide, lies 

entirely on the high, level plateau, sloping gradually from a height 

of about 4,000 feet on the west to a little more than 2,000 on the east. 

Into this plateau Cimarron and Beaver rivers have cut their channels, 

usually shallow and broad, while numerous small tributar}7 creeks 

are now at work dissecting the level upland. Large areas remain, 

however, which appear to be as level as a floor and on which the only 

drainage is into playa lakes, or, as they are sometimes called in the 

West, " buffalo wallows " (PL III, A).

IEB 148 05 M 2
18 GEOLOGY AND WATER RESOURCES OF OKLAHOMA. 

DAKOTA SANDSTONE REGION.

In the extreme western end of Beaver County, along the Cimarron 

and the Currumpaw (a head tributary of the Beaver), is a small area 

which contains topographic features unlike those found elsewhere in 

Oklahoma, for in this locality the streams have cut canyons into the 

Dakota sandstone. The Cimarron Canyon has a length of 30 miles 

or more in Oklahoma and of 60 miles in New Mexico. The hills, as 

shown on Pis. IV, B, and X, B are 200 to 500 feet high, and are usually 

capped by heavy ledges of gray or brown sandstone, which have been 

carved into fantastic shapes by numerous small creeks.

In the extreme northwestern part of Beaver County these sandstone rocks are covered with 100 feet or more of basaltic lava, forming; 

the eastern end of Black Mesa, a level table-land which extends, into 

Oklahoma from Colorado and New Mexico (fig. 28).

VALI^EYS.

All the drainage of Oklahoma flows into Mississippi River, reaching that stream by Arkansas and Red rivers. The Arkansas crosses 

the northeast portion of Oklahoma, separating the Osage and Kaw 

reservations from the remainder of the Territory. Red River forms 

the extreme southwestern boundary of Oklahoma. The chief tributaries of the Arkansas in Oklahoma and the Indian Territory are. 

Salt Fork, Cimarron, North Canadian, and South Canadian rivers, 

the two latter streams joining before finally reaching the Arkansas 

in the eastern part of the Territory. The Washita and North Fork 

of Red River flow into Red River.

The general direction of all these streams is southeasterly that is, 

practically at right angles to the strike of the rocks. With the 

exception of the Washita, they are all typical streams of the plains, 

each with a relatively broad and shallow valley, containing a broad, 

sand-choked channel and, except in times of flood, carrying a relatively small amount of water. The character of these valleys is 

determined largely by the rocks across which they have been cut, 

being comparatively narrow and deep in the Gypsum Hills or Flint 

Hills regions and broad and shallow in the more level"country in 

central and western Oklahoma. These valleys will be discussed in 

regular order beginning on the north. PL XVI shows the drainage 

areas of the various streams.

ARKANSAS VALLEY.

Arkansas River flows in a broad, shallow channel from the point 

where it debouches from the jnountams, in Colorado, to the Flint
U. 6. GEOLOGICAL SURVEV WATER-SUPPLY PAPER NO. 148 PL. IV

A. DAKOTA EROSION NEAR KENTON, OKLA., SHOWING 

CROSS-BEDDING.

B. EROSION FORMS IN DAKOTA CRETACEOUS.
VALLEYS. 19

Hills, at Arkansas City, Kans., a few miles north of the Oklahoma 

line. From this point to the southeast corner of the Osage Nation 

it flows in a tortuous channel among limestone hills. The distance 

is about 83 miles direct, but as traversed by the river it is nearly 

twice as great. This part of its course is characterized by broad 

and sweeping oxbow bends, one, for instance, being 9 miles around, 

while at the nearest point it is not more than 1^ miles across. The 

valley between the bluffs, which are 150 to 300 feet high, is 1 to 5 miles 

wide, being narrowest between the Osage country and Kay County.

SALTJ FORK VALLEY.

The valley of the Salt Fork of the Arkansas, which extends 

through northern Woods, central Grant, and southern Kay counties, 

is broad and shallow and is for the most part bordered on the north 

slope by sand hills and on the south side by canyons cut into steep 

and uneven slopes. Near the point where this river enters Woods 

County from Kansas the valley is bordered by the Gypsum Hills, 

particularly on the south side, while farther downstream it is 2 to 5 

miles wide and the hills on either side reach an altitude of 50 to 100 

feet above the level of the stream. The tributaries are Medicine 

Lodge, Mule, Sand, Crooked, Deer, Osage, Buck, Chikaskia, and Bois 

d'Arc creeks. In eastern Woods County the Salt Fork flows across 

the northern edge of the Great Salt Plains, where the water acquires 

saline character, whence the name Salt Fork.

CIMARRON VALLEY.

N

Cimarron River rises among volcanic peaks in northern New 

Mexico, flows east through a narrow canyon cut into Dakota sandstone, and enters Oklahoma 4 miles south of the Colorado line, near 

the town of Kenton. From this point it flows nearly straight east 

for more than 30 miles in a canyon cut in the sandstone plateau. 

In this part of its course the valley averages 3 iniles in width and the 

rugged hills, which disappear near the point where the Cimarron 

flows from Oklahoma into Colorado, are 300 to 400 feet high. From 

this point to the place where the river cuts through the Gypsum 

Hills it flows in a broad and shallow valley carved into the level 

upland. After leaving Oklahoma the Cimarron flows through southeastern Colorado and southwestern Kansas for nearly 100 miles. 

It enters the Territory again about 15 miles west of the northeast 

corner of Beaver County, but soon turns northward to pass into 

Kansas. For the third time it enters Oklahoma, in the north-central 

part of Woodward County, where it breaks through the Blaine 

.Gypsum Hills. Throughout its entire course in Woodward County,
20 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

a distance of more than 40 miles, it flows in a canyon cut in the 

Gypsum Hills. This canyon gradually widens to the east, and near 

the western line of Woods County these hills recede from the river 

and swing to the north. On the south side, however, they parallel the 

river as far as the Glass Mountains in south-central Woods County, 

forming conspicuous gypsum-capped bluffs, then gradually recede 

from the Cimarroii and approach the South Canadian. East of the 

Glass Mountains the Cimarroii flows across a level country, and the 

valley is broad and shallow, being only occasionally lined with bluffs, 

as in the vicinity of Guthrie.

The drainage area of the Cimarroii -is broader than that of any 

other Oklahoma stream, and it includes a considerable number of 

tributary creeks, the chief of which are Buffalo, Eagle Chief, Salt, 

Turkey, Kingfisher, Cottonwood, Skeleton, and Stillwater. Along 

its eastern course the river flows into the southern extension of the 

limestone hills, where the topography consequently is more uneven 

and bluffs 100 or more feet high are not uncommon.

NORTH CANADIAN VALLEY.

North Canadian River is formed by the junction of Beaver and 

Wolf creeks at Old Fort Supply, near the center of Woodward County. 

Wolf Creek rises in the high table-lands of the Panhandle of Texas 

and flows northeast, in a rather narrow valley bordered by rounded 

bluffs which rarely exceed 100 feet in height. Beaver Creek, Avhich 

has cut a valley averaging 3 miles in width and 200 feet in depth 

throughout its course, rises among volcanic peaks in northeastern 

New Mexico and flows the entire length of Beaver County. The 

principal tributaries, all on the south side, are Coldwater, Palo Duro, 

Clear, and Kiowa creeks. These and other creeks are now dissecting 

the high plateau, but 011 account of_the arid climate and the firm 

sod covering have, at the present time, scarcely more than commenced 

their task (PL V, A). North Canadian Eiver formed by the union 

of Wolf and Beaver creeks, flows in a general southeasterly course 

entirely across the Territory, and its valley is, on the average, 200 

feet higher than the Cimarroii. The hills on either side are usually 

low, often not over 100 feet in height, and in many instances the 

headwaters of streams flowing into the Cimarron approach within 

less than 2 miles of the North Canadian. Sand hills occur practically all along the north slope, and the south bluff is often cut into 

red-beds canyons.

SOUTH CANADIAN VALLEY.

With the exception of Arkansas Eiver the South Canadian is the 

only stream in Oklahoma which takes its rise in the Rocky Momi-
U. S. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. U8 PL. V

A. PRAIRIE STREAM JUST BEGINNING TO CUT.

B. PIT HOLES ALONG PRAIRIE ARROYO.
VALLEYS. 21

tains. In New Mexico and the Panhandle of Texas the drainage 

area is large, but from the western boundary of Oklahoma to its 

mouth in the eastern part of the Indian Territory it will not average 

more than 20 miles in width. In Day and Dewey counties the river 

swings in a series of broad oxbow bends, and flows in a canyon-like 

valley about 200 feet deep and 1 to 5 miles wide. In eastern Dewey 

and Ouster counties it flows across the Gypsum Hills region. Below 

the line of Gypsum Hills it flows in a general southeasterly direction in a valley which averages 4 miles in width and which is bordered by bluffs on either side not exceeding 150 feet in height. In 

many places, however, the slopes north of the river are covered 

with sand hills, but on the south side of the stream steep bluffs are 

common. A few small tributaries, the chief of which are Deer, 

Commission, and Boggy creeks, flow into the South Canadian in 

Oklahoma.

VVASHITA VALLEY.

As has been stated by Mr. Willis," the Washita resembles an eastern more than a western river, having steep mud banks and heavy 

timber along most of its course. In its upper part the narrow valley is continued between bluffs of red sandstone 100 to 300 feet 

high. Where the valley cuts across the Gypsum Hills, in Custer 

and Washita counties, low, white gypsum bluffs are common. Eastward from the southeastern corner of Washita County the river 

flows through wide bottom lands in a valley 2 to 5 miles wide, 

inclosed by hills 100 to 300 feet high. Taken throughout, the 

Washita has more precipitous bluffs and a greater diversity of topography than any other river in Oklahoma, and at the same time sand 

hills are practically wanting. Quartermaster, Cavalry, Rainy Mountain, Cobb, and Sugar creeks are the chief tributaries.

RED RIVER VALLEY.

The main branch of Red River forms the southern boundary of 

Greer and Comanche counties. A number of streams tributary to 

Red River rise either in Oklahoma or the Panhandle of Texas, the 

most important of which are the Salt Fork, Elm Fork, North Fork, 

Cache, and Beaver creeks. North Fork, Salt Fork, and Elm Fork 

rise in the eastern part of the Panhandle of Texas, flow across the 

region of Greer Gypsum Hills through canyons in the gypsumcapped red shale bluffs and then out upon the lower plains, where 

they enter shallow valleys before finally reaching Red River. Cache 

Creek, which rises in the Wichita Mountains, and Beaver Creek, east

0 Willis, Bailey, First Ann. Kept. Reclamation Service, U. S. Geol. Survey, 1903, p. 269.
22 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

of these mountains, flow south across the red beds plain in broad and 

shallow valleys.

CONCLUSION.

All of the larger rivers of Oklahoma rise west of the Gypsum Hills 

region and flow first in broad valleys. In the Gypsum Hills they 

have cut comparatively deep and narrow canyons, and east of this 

range of hills the valleys begin to widen again. These streams, with 

the exception of the Washita, are flanked along the north slope with 

rows of sand hills, usually 2 to 10 miles in width, while the south bank 

is almost invariably cut with canyons carved in the red sandstones 

and shales which make up the greater part of the country rock. In 

other words, the south bank is a red-shale canyon slope, and the north 

bank a sand-hill slope.

GEOLOGY. 

GE^STERAIL, STATEMENT.

The geology of Oklahoma presents certain phases of more than 

usual interest to the student of stratigraphy. As the conditions of 

the water supply depend almost wholly upon the character and position of the rocks, it is necessary to outline the geology of the Territory 

before giving a detailed description of the water supply.

Numerous features of the geology of various parts of Oklahoma 

are as yet but imperfectly understood, and many of the statements 

made in this article therefore are offered only tentatively. It is probable that further investigation may cause decided changes in present 

views of the geology of certain parts of the Territory, especially as to 

the line of separation between the Pennsylvanian and Permian series 

of the Carboniferous rocks in the northeastern part of the Territory, 

the location of certain sanM-hill areas, and the lines of outcrops of 

gypsum deposits in some of the western counties. Certain facts, however, are fairly well established, and it is these, rather than the ones 

not yet understood, that will be given prominence in the following 

pages.

The principal formation in the Territory is a widespread deposit 

of red clay, shale, and sandstone, a large part of which has been 

classed as Permian in age, and is known as the " red beds." To the 

east it is underlain by Pennsylvanian- rocks and to the west covered 

by sands and clays of Tertiary and Quaternary ages. In the northeastern part of the Territory are extensive areas of Pennsylvanian 

rocks, and in the Wichita Mountains rocks of lower Paleozoic age 

appear. The known outcrops of geologic formations in Oklahoma 

are indicated on the map (PL I), and the following table sets forth 

their order and age:
GEOLOGIC FORMATION. 23

hills. 

Tertiary -_.:..._-___...__ .Lava of Black Mesa.

Cretaceous.... ........ ..{Dakota.

IComanche.

Quartermaster. 

Greer.

Permian Woodward.

Carboniferous............ Blaine.

Eriid.

Pennsylyanian. 

Ordovician. ___________ _ Viola limestone.

Cambro-Ordovician _____. Artrackle limestone.

Cambrian________________ Reagan sandstone.

(Granite.

Early Cambrian or older. JGranite-porphry. 

[Gabbro.

RE:LATIONS OF THE PRE-CARBONIFEROUS ROCKS.

The oldest rocks in Oklahoma are in the Wichita Mountains, in 

the southwestern part of the Territory. These mountains are composed chiefly of three classes of igneous rocks, gabbro, granite, and 

granite-porphyry; and three sedimentary formations of lower Paleozoic age, the Reagan sandstone, Arbuckle limestone, and Viola 

limestone. Granite greatly predominates, composing probably ninetenths of all the rocks of the range. In oirler that the reader may 

understand the relations of these various rocks to each other and the 

surrounding " red beds," a short description of the Wichita Mountains is given. The map (PL VI) further illustrates the structure of 

the mountains.

In the Wichita Mountains the rocks do not differ materially from 

similar formations in the Arbuckle Mountains farther east, and for 

that reason it appears to be desirable to give the formations the 

names already used for similar rocks in the Arbuckle region. As 

these rocks have been named and described by Mr. Joseph A. Taff,° 

to whose publication the reader is referred, only a brief mention will 

be made of them in this conection.

The extreme length of the Wichita Mountains, from the Carlton 

mounds on Medicine Bluff Creek near Fort Sill to the last granite 

hill that disappears under the high prairi^ 5 miles west of Headquarters Mountain, at Granite, is 65 miles, iwhile the extreme width 

from Rainy Mountain to the southwestern granite butte on North 

Fork of Red River, 6 miles southeast of Navajoe, is 30 miles. The 

Wichita Mountains are not a continuous range throughout this area,

a Taff, Joseph A., Preliminary report on the geology of the Arbuckle and Wichita 

mountains in Indian Territory and Oklahoma : Prof. Paper No. 31, TJ. S. Geeol. Suryey, 

1904, pp. 50-81.
U.S.GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. 148 PL.VI

SECTION ACROSS THE EASTERN" PART OF THE WICHITA. MOUNTAINS

Approximate vertical scale 

o E.OOO iftooofeet

ft - fsLf>~ -

// LITTLE 

BOW MT.

CVEOLOG-IC

or THE

"WICHITA MOUNTAIN REGION

H Y

JOSEPH A.TAFF AUD C.Ts

PERMIAN i\a"

porphyry, amnUf, and timartotie 

nerattaurm redclay anrl santf

^rbuckle Mmeston.e

'bliitsh and veJlovish limestone and dolomite}

Bandstoiie imestone, green days. sanfisrvneMJui conglomerate.

t ^ ^ cfif totjruv 

~f Dip oi'rocts

hcalo

8 <? 1 8 9____jo milws
24 GEOLOGY AND WATEK RESOtTRCES OF OKLAHOMA.

as they consist chiefly of scattered ranges, peaks, and short chains, 

the bases of which are buried beneath the surrounding and intervening plains.

The Wichita Mountains may be divided into the following three 

general groups: (1) The main range; (2) scattered groups and peaks 

in the western part of the area, and (3) a row of hills which are 

composed chiefly of limestone and which parallel the main range on 

the north and east.

The main range of the Wichita Mountains, the width of which 

averages 10 miles, extends northwest from the vicinity of Fort Sill 

for about 30 miles to the vicinity of Saddle Mountain and Mount 

Baker, just east of the headwaters of East Otter Creek. This part 

of the range is practically continuous throughout and is composed 

chiefly of rugged peaks of granite, the highest of which, Mounts 

Scott and Sheridan, each rise about 1,200 feet above the plain. There 

are two main northwest-southeast ranges, separated by a distinct 

intermontane valley, 1 to 4 miles wide, extending nearly the entire 

length of the ranges. The streams draining this valley flow east 

and south and escape to the plain through gaps in the mountain1?. 

East of this main range are a number of outlying peaks and short 

ranges, some of which attain an altitude of 800 feet or more above 

the surrounding plain.

West of the main range of the Wichitas, which is divided into 

two general ridges, are scattered groups, peaks, and low ridges 

extending a few miles beyond Granite, Greer County, a distance of 

40 miles from Mount Baker. The term " Raggedy Mountains " is 

applied to a group of scattered, roughly outlined ridges and peaks 

lying along the heads of various branches of Otter Creek. Long 

Horn Mountain is near the head of Middle Otter Creek; Dome 

Mountain, Tepee Mountain, Elk Mountain, and others lie near Elk 

Creek; Devils Canyon Mountain, shown in PI. II, B, is 6 miles long 

and lies in a bend of the North Fork of Red River; Navajoe, Quartz,, 

and Headquarters mountains are in Greer County west of the North 

Fork of Red River, which winds in and out among the granite peaks..

Parallel to the Wichitas on the northeast from a point 7 miles; 

north of Fort Sill to Rainy Mountain, a distance of 30 miles to the 

northwest, is a group of limestone hills, which, like the main range 

of the Wichitas, consist of irregular low mountains and scattered 

knobs. The longest range, 16 miles in length, will average 2 miles, 

in width. Near the head of Blue Creek Canyon the range of limestone hills divides into two parts one part running approximately 

N. 70° W. and the other N. 40° W. Both ranges finally end toward 

the northwest in a series of scattered peaks and knobs. These limestone hills, like the granite mountains, are but the tops of buried
IGNEOUS EOCKS. 25

ranges. The rock comprising the plain around and between the 

mountains is much younger than the rocks of the mountains that is, 

it was deposited at a much later period in the earth's history.

IGNEOUS ROCKS.«

GABBRO.

Of the three chief varieties of igneous rocks in the Wichitas the 

gabbro is probably the oldest. This rock is hard, black, and 

crystalline, and sometimes is known to the miners as black granite. 

It frequently has a greenish tint, or again it may be grayish in color, 

and often weathers into rough, lumpy surfaces. It is in places cut by 

dikes, composed of diabase, granite, aplite, etc.

As shown on the map (PL VI) gabbro outcrops in three separate 

localities in the Wichita Mountains, two of which are in the main 

range and the other one west of it. In the main range the most 

extensive exposure, which covers an area about 2 miles wide and 12 

miles long, lies along the north slope of the mountains on both sides 

of Medicine Bluff Creek, and extends northwest and southeast, paralleling- the range from the east end of Mount Scott to the east slope 

of Saddle Mountain. The second gabbro exposure, about 6 miles 

long and 1 mile wide, is in the central part of the intermontane 

valley along the heads of West Cache and Quanah creeks. The 

gabbro in both these localities does not, as a rule, present conspicuous 

relief, but weathers into gentle slopes with occasional low ridges and 

buttes. The third locality in which gabbro is found is in the central 

part of the Raggedy Mountains, west of the main range. This range 

is 15 miles long and extends westward from near Mount Baker to a 

point within 3 miles of North Fork of Red River. Some of the 

peaks rise- to the height of 400 feet above the plain. The average 

width of the range is something like 3 miles, and across it flow the 

various branches of Otter Creek. In the western part of the range 

are numerous dikes and intrusions of other igneous rocks, chiefly 

granite and quartz.

GRANITE-PORPHYRY.

Granite-porphyry occurs in the eastern part of the main range and 

in several localities among the limestone hills. This is a hard, massive rock usually with a grayish groundmass in which are embedded 

numerous large crystals, usually reddish or pinkish, giving a characteristic reddish-gray tint to the rock. The localities in which porphyry occurs are as follows:

In the Fort Sill Military Reservation and between the fort and

0 For classification of the igneous rocks of the Wichita Mountains see Taff, Joseph A., 

op. cit., pp. 59-67.
26 GEOLOGY Attt> WATER RESOURCES OP OKLAHOMA.

Mount Scott the greater part of the rock is granite-porphyry. Signal Mountain, the Carlton mounds, Medicine Bluff, and a number of 

unnamed peaks are composed of this rock. This porphyry weathers 

in small blocks and angular fragments, and the surface of the hills 

composed of this rock are usually grass covered and easily distinguished from granite hills in which the rock weathers out in large 

bowlders and which are covered with trees. In the western part of 

this exposure the porphyry passes gradually into red granite, so that 

in many places it is virtually impossible to tell where one rock stops 

and the other begins.

Near the central part of the main ridge of limestone hills, 6 to 8 

miles' north of Mount Scott, along Blue Creek Canyon, is a second 

exposure of porphyry covering an area of about 8 square miles. 

The rock in this region does not differ materially in character from 

that on the Fort Sill Reservation. On the west the porphyry is cut 

off from the limestone by a fault and on the east, where it is exposed 

along the flanks of a limestone ridge, it lies unconformably below the 

sedimentary rocks.

The third area of porphyritic rocks is in the extreme northern part 

of the Wichita Mountain region, at the northern extension of the 

limestone hills. In this vicinity are twelve or more scattered peaks 

of porphyry. In two instances this porphyry lies unconformably 

below the Reagan sandstone, a formation of Cambrian age.

GRANITE.

With the exception or the gabbro and granite porphyry just discussed and a relatively few dikes, the igneous rocks of the Wichitas 

consist of granite, which varies in color from red to gray with light 

red greatly predominating. It .is cut by several series of joint planes 

and weathers into massive, bowlders (PL II, J., B).

The high peaks of the main range, such as Mounts Scott, Sheridan, 

and Baker, and Saddle Mountain, and others, as well as all the scattered peaks and ranges west of the main range, except the gabbro 

range previously discussed, .are composed of granite. Navajoe, 

Tepee, Devils Canyon, Little Bow, Quartz, Headquarters, and other 

peaks and chains in this western group are all granite mountains.

SEDIMENTARY ROCKS, a

CAMBRIAN ROCKS.

KEAGAN SANDSTONE.

The Reagan sandstone, the oldest sedimentary rock in Oklahoma, 

in its typical development is composed of coarse-grained, angular

0 For a more complete description see Tafl, Joseph A., op. cit., pp. 67 77.
ABBTJCKLE AND VIOLA LIMESTONES. 27

particles derived from the disintegration of porphyry rocks. There 

are local ledges of conglomerate interstratified with shaly members, 

but coarse sandstone makes up the greater part of these rocks. The 

age of this formation, as indicated by trilobites and other fossils, is 

Middle Cambrian.

The Reagan formation is exposed on the granite-porphyry, and it 

is conformably overlain by the Arbuckle limestone at two localities; 

first, in the limestone hills east of Blue Creek Canyon, and second, 

along the side of some limestone peaks in the extreme northern part 

of the mountains. At Blue Creek Canyon the Reagan is exposed 

for a distance of nearly 4 miles, while farther north the line of outcrop is not more than 2 miles long. In both localities the exposure 

is but a few hundred feet wide.

CAMBRO-ORDOVICIAN ROCKS.

ARDUCKLE LIMESTONE.

Conformably above the Keagan sandstone is a limestone formation 

which makes up the greater part of the northern division of the 

Wichita Mountains. This limestone is hard, compact, and massive, 

and is at nearly all places much folded and faulted, so that its beds 

rarely lie level, but have been broken and tilted to various angles, 

usually steep. The thickness of this formation in the Wichita 

Mountains is unknown, but in the Arbuckle Mountains it was estimated by Mr. Taff to be 4,000 to 6,000 feet, and there is no reason 

for supposing that it is less in the Wichitas. In the Arbuckle 

Mountains the lower 700 feet of this limestone contains fossils of 

Upper Cambrian age, while from the upper beds Ordovician forms 

were obtained.

The hills composed chiefly of this limestone extend practically 

uninterrupted northeast from near Fort Sill for 30 miles or more. 

From the region of Blue Creek Canyon there are two ranges, both of 

which finally die out and disappear beneath the plains.

ORDOVICIAN ROCKS.

VIOLA LIMESTONE.

Three small outlying limestone knobs in the vicinity of Rainy 

Mountain Mission consist of Viola limestone, an Ordovician formation, which in the Arbuckle Mountains occurs approximately 2,000 

feet higher in the section than the Arbuckle limestone. In the 

Wichita Mountain region little lithologic distinction can be made 

between the limestone comprising these knobs and the limestone 

which makes up the main range of hills just described. Mr. E. O.
28 GEOLOGY AND WATEB pESOTTBCES OF OKLAHOMA.

Ulrich, however, who studied the fossils from the entire region, finds 

that the paleoiitologic evidence justifies snch distinction, and for 

that reason the rocks composing the three hills near Rainy Mountain 

are classed as Viola.

CARBONIFEROUS ROCKS.

PENNSYLVANIAN SERIES. 

GENERAL RELATIONS.

The oldest rocks on the plains consist of scattered groups of igneous rocks, chiefly granite, forming the hearts of the Ozark, Arbuckle, 

and Wichita mountains. The greater part of the Ozark and Boston 

mountains in Missouri and Arkansas consist of seclimeiitary rocks 

older than the Coal Measures, chiefly limestones and cherts of the 

Mississippian ( u Lower Carboniferous "). Rocks of the same age are 

also found in southeastern Kansas and the eastern part of the Cherokee Nation. Westward the rocks belong to successively younger 

formations.

Resting upon the Mississippian in Indian Territory is a great 

thickness of rocks of Pennsylvania!! age.a These rocks occupy the 

greater part of southern Iowa, western Missouri, eastern Nebraska, 

and the eastern third of Kansas. Large outcrops are also found in 

Arkansas and Texas.

Pennsylvania!! rocks are exposed over a considerable area in eastern 

Oklahoma.. The line of separation between the Pennsylvania!! and 

the Permian, which make up the greater part of the Territory, has 

never been sharply drawn. For reasons to be discussed later this line 

can not be drawn with any degree of accuracy until considerable work 

lias been done in the way of tracing formations in northeastern Oklahoma and until fossils have been collected and identified.6

RELATION OF THE PENNSYLVANIAN TO THE PERMIAN.

The problem of the relation of the Pennsylvanian to the Permian of 

the Great Plains is at best a perplexing one. Perhaps more time 

has been spent in attempting to solve it than has been devoted to 

almost any other phase of western geology, and the results have been 

less satisfactory. In Kansas the rocks of these two epochs have been 

studied for nearly fifty years; and during the past ten years Willis-

" Taff, Joseph A., The southwestern coal fields: Twenty-second Ann. Kept. U. S. Geol. 

Survey, pt. 3, pp. 367-413 ; Geology of the McAlester-Lehigli coal fields, Indian Territory ; 

Nineteenth Ann. Kept. IT. S. Geol. Survey, pt. 3, pp. 423-593, 1899 ; Eastern Choctaw 

coal fields, Indian Territory, Twenty-first Ann. Kept. U. S. Geol. Survey, pt. 2, pp. 255- 

311, 1900; Coalgate Folio, No. 74, 1901, and Atoka Folio, No. 79, 1902. Drake, N. F., A 

geological reconnaissance of the coal fields of the Indian Territory : Proc. Am. Philos. 

Soc., vol. 36, 1898, pp. 326-429.

* See footnote, p. 32.
PENNSYLVANIAN SERIES. 29

ton,a Cragin,& Prosser,0 Hay,*7 Beede,e and others have contributed 

articles which have assisted in the elucidation of this very perplexing 

question. In Kansas, however, the difficulties are not so great as in 

Oklahoma, as in Kansas the Pennsylvania!! rocks which occur in the 

eastern third of the State are in a regular, conformable succession., 

and finally pass conformably into the Permian above. Many of the 

beds have lithologic characteristics, and fossils are abundant. It is 

true that the line of separation between the Pennsylvanian and 

Permian has not been sharply drawn, for such a line depends upon 

paleontologic rather than upon lithologic data, and in certain strata 

there is a commingling of Pennsylvanian and Permian forms, but 

most geologists who have studied the problem have agreed that certain rocks are Pennsylvanian in age and that certain other rocks, 

several hundred feet higher geologically, belong to the Permian.

In parts of Texas where these rocks are well exposed the line of 

division between the two series has been fairly well worked out. 

Certain beds are known to be Pennsylvanian, while certain other 

higher beds are undoubtedly of Permian age.

In Oklahoma, on the other hand, such conditions do not exist. In 

the northeastern part of the Territory particularly the stratigraphy 

is exceedingly perplexing and at the same time fossils are rare. On 

(he geological map (PL I) the author has attempted to outline the 

conditions as they are believed to exist. From this map it will be 

seen that the greater part of the Osage Nation, which is in the northeast corner of Oklahoma, is underlain by rocks of Pennsylvania!! age. 

In this part of the Territory, as in Kansas to the north, the strike is to 

the northeast and southwest, and many of the ledges, notably certain 

limestones, have been traced by Adams f and others from Kansas into 

Oklahoma, some to beyond Arkansas River. The lowest limestone 

ledge that is known in the Osage Nation (although more detailed 

study will probably reveal others still lower) is the Drum limestone 

which has been traced as far south as the vicinity of Bartlesville, in

" Wllliston, S. W., Science, new series, vol. 5, p. 395 ; Kansas Univ. Quar., vol. 6, p. 57 ; 

Jour: Geol., vol. fi, 1898. p. 342.

6 Cragln, F. W., Bull. Washburn Col. Nat. Hist., vol. 1, 1885, p. 86 ; id., vol. 2, 1889, 

pp. 33, 34 ; The Permian system of Kansas : Colorado Col. Studies, vol. 6, 1896, pp. 1-48 ; 

Observations on the Cimarron series : Am. Geologist, vol. 19, pp. 351 363.

f Prosser, Chas. S., The Cimarron series or the Red Beds : Second Ann. Kept. Univ. 

Geol. Survey Kansas, 1897, pp. 75-95 ; The Permian and Upper Carboniferous of southern Kansas : Kansas Univ. Quar., vol. 6, 1897, pp. 149 170 ; Revised classification of the 

upper Paleozoic formations of Kansas : Jour. Geol., Vol. 10, 1902, pp. 703-737.

d Hay, Robt., A geological reconnaissance in southwestern Kansas : Bull. U. S. Geol. 

Survey No. 57. 1890, pp. 20, 27 ; Eighth Bien. Rept. Kansas State Bd. Agric., pt. 2, 1893, 

p. 101.

« Beede, J. W., Jour. Geol., vol. 9, 1901, p. 339 ; Am. Geologist, vol. 28, 1901, pp. 46, 

47 ; Advance Bull. First Bien. Rept. Oklahoma Geol. Survey, April, 1902.

f Adams, Geo. I., Stratigraphy and paleontology of the Upper Carboniferous rocks of 

the Kansas section: Bull. U. S. Geol. Survey No. 211, 1903.
30 GEOLOGY AND WATER RESOURCES OP OKLAHOMA.

the Cherokee Nation, just east of the Oklahoma line. If the direction of the strike of this rock remains constant, however, this ledge 

should touch the Arkansas not far from the mouth of the Cimarron, 

and if so, there are probably several hundred feet of Pennsylvania!! 

rocks in Oklahoma below the level of the Drum limestone.

Another ledge of limestone, the Pawhuska, has been traced by 

Adams from Kansas south through the Osage Nation and across 

Arkansas River to the vicinity of the Cimarron, near Ingalls, Payne 

County, Okla.n The Pawhuska, however, is stratigraphically 600 

feet below the base of the Wreford limestone, which is now considered by Prosser to be the base of the Permian.6 The Drum limestone 

is approximately 950 feet below the Pawhuska, so that in the Osage 

Nation there are at least 1,550 feet of the Pennsylvania!! rocks below 

the base of the Permian.

This part of the problem presents no great difficulty. The point 

which leads to confusion is the failure to identify many of these 

prominent ledges in the region south of Arkansas River. Within a 

belt 50 miles wide on either side of the river the lithologic conditions 

change rapidly. At the Kansas-Oklahoma-Indian Territory line 

there are, between the Drum limestone and the Winfield formation, 

which is the highest prominent limestone ledge in the Permian, no 

fewer than 16 heavy beds of limestone, varying in thickness from 5 

to 40 feet. On passing southward through the western part of the 

Cherokee Nation and the Osage Nation these limestones become thinner and less conspicuous, while at the same time the intervening 

shales become thicker and more prominent, often becoming arenaceous, or, indeed, replaced entirely by sandstone, until by the time 

the Arkansas River is reached the greater part of these limestone 

formations have totally disappeared, while those that remain have 

become much thinner, and the rocks consist entirely of alternating 

layers of sandstone and shale. In the light of our present knowledge 

it is believed that the Pawhuska limestone extends farther south than 

any of the others. This limestone was traced by Mr. Pierce Larkin 

as far south as a point 9 miles south of Chandler, where it seems to 

disappear and its place is taken by shales and sandstones. At the 

same time the shales, which have been of a prevailing drab, bluish, or 

yellowish color, become more and more reddish, until they gradually 

merge into the typical brick-red shales and clays that make up the 

greater part of the Oklahoma red beds.

This condition was first pointed out by Dr. George I. Adams, who

0 Adams, G. I., Bull. IT. S. Geol. Survey No. 211, 1903, pp. 61-65. See also Adams, 

G. I., Carboniferous and Permian age of the red beds of eastern Oklahoma from stratigraphic evidence: Am. Jour. Sci., 4th ser., vol. 12, 1901, p. 383.

& Prosser, Chas. S., Revised classification of the upper Paleozoic formations of Kansas: 

Jour. Geol., vol. 10, 1902, table op. p. 718.
PENNS-YLVANIAN SERIES. 31

has made a special study of these conditions in Kansas, Oklahoma, 

and Texas. In speaking of the problem, Doctor Adams says :a

It appears that rocks in eastern Oklahoma, which have been referred to the 

red beds on lithologic grounds, are in part of Upper Carboniferous or Coal 

Measure age. The sedimentation from the Carboniferous into the Permian 

is an unbroken sequence. From what is known of the Permian limestones of 

Kansas, they will be found, when followed southward, to diminish "in thickness, and this change will be accompanied by a transition to more sandy 

beds. This is in accordance with the observations made by Mr. Gould. The age 

of that portion of the red beds which is iu strike with the Permian of 

Kansas may confidently be expected to be found to be of Permian age. This is 

in accordance with the evidence already furnished by the vertebrate fossils. 

Above the Permian limestone in Kansas occur the Wellington shales, which are 

bluish and greenish gray in color. They are probably represented southwestward by formations which are red. The succeeding formations are typical red 

beds and have thus far yielded only Permian fossils. Upon the accompanying 

map the approximate line of transition in cqlor has been drawn with the purpose of showing that it is diagonal to the strike of the Carboniferous and Permian formations.

Doctor Adams found the conditions in northern Texas very similar 

to those in the Kansas-Oklahoma region. In Young, Archer, Throckmorton, and Baylor counties, Tex., certain beds of limestone of 

Pennsylvania age thin out northerly and their place is taken by shales 

and sandstones, which become distinctly red in color. The line of 

change of color in the rocks cuts diagonally across the strike of the 

beds, very much as in northeastern Oklahoma. Doctor Adams does 

not attempt to draw the line between the Pennsylvanian and the Permian in either Oklahoma or Texas.6

From this it follows that the line of separation between Pennsylvanian and Permian rocks must be drawn far out in the red beds. If 

the Wreford limestone be accepted as the base of the Permian in Kansas, the location of the line of separation is a matter of the location 

of the Wreford in Oklahoma. This ledge is known,to outcrop on 

Beaver Creek in the Kaw Reservation, and has been traced south by 

Mr. Charles A. Long across the western part of the Osage Nation to 

a point in the big bend of the Arkansas, about 10 miles west of Ralston and about 8 miles northeast of the mouth of Red Rock Creek, 

where it is striking southwest. It is probably represented south of 

the river in one of the ledges of limestone which are known to occur 

in the eastern part of Noble County, but until it is definitely located 

the line of separation can only be approximated. For the present, 

then, it will be drawn roughly through eastern Noble, western Payne, 

eastern Logan and Oklahoma, and western Cleveland counties, 

approximately paralleling the Atchison, Topeka and Santa Fe Railroad on the east as far as the vicinity of Oklahoma City, near which

a Adams, Geo. I., Op. cit., pp. 385-386.

6 Adams, Geo. I., Stratigraphic relations of the red beds to the Carboniferous and 

Permian jn .northern Texas; Bull, GeoL Soc, America, vol. 14,'1003, pp. 191-200,
32 GEOLOGY AND WATER RESOURCES OP OKLAHOMA.

place it crosses that line of road and strikes South Canadian River 

in the western part of the Chickasaw country, west of the Arbuckle 

Mountains, and, if carried across Red River, will finally reach the 

region of the western limit of the known Pennsylvanian in Texas."

DESCRIPTION OF PENNSYLVANIAN BOCKS.

If the line of separation between the Pennsylvanian and Permian 

rocks of Oklahoma be drawn at the line above indicated, there 

are in eastern Oklahoma about 5,000 square miles of Pennsylvanian 

rocks. In the southern part of the area these rocks are almost entirely 

red sandstones and clays; in the northern part they consist of alternating layers of clays, sandstones, and limestones of various colors. 

The line of separation between the two kinds of Pennsylvanian-rocks 

can never be sharply drawn, for the reason stated above, that while 

all the rocks are in regular succession they vary in lithologic character along the strike. To express the condition more forcibly, the 

statement may be made that the rocks of the two sections dovetail 

into each other; for in the region along Arkansas River there are red 

shales extending northward into limestone-sandstone regions and 

beds of limestone extending south into the red-clay-shale country. 

As stated by Adams, there is an embayment of red sediments extending 

far to the east among Pennsylvanian strata.

For purposes of description it is proposed to divide the rocks into 

two districts, the names Hominy and Chandler, by which these districts will be known, being used only as convenient working terms.

Hominy district. The Hominy district includes the area of outcrop of all the Carboniferous rocks of the Osage and Kaw reservations which lie below the Wreford limestone. The formations 

exposed in this district include the southern extension into Oklahoma 

of the Pottawatomie, Douglas, Shawnee, Wabaunsee, Cottonwood,6 and 

Neosho 0 formations of the Kansas geologists and have a thickness 

of over 1,500 feet. In the eastern part of the Osage Nation the rocks 

are chiefly sandstones and shales, with some massive beds of fossiliferous limestones, while farther west, along the headwaters of Hominy

* During the summer of 1904, since the above was written, Mr. Charles T. Kirk, working under the direction of the Oklahoma Geological Survey, traced out the line of outcrop of the Wreford limestone south across Oklahoma. Starting on Little Beaver 

Creek, in the Kaw Reservation, he followed the ledge across Arkansas River and found 

that in Payne County the limestone disappeared and its place was taken by a ledge of 

sandstone to which the name Payne sandstone was applied. This ledge was traced 

southwest across Cimarron, Deep Fork, and North Canadian rivers, through western 

Lincoln, eastern Oklahoma, and central Cleveland counties. It crosses South Canadian 

River near Purcell. In southern Oklahoma the ledge lies some 15 to 20 miles east of 

the line of Pennsylvanian-Permian contact indicated on PI. I. For full description see 

Mr. Kirk's paper in Third Bien. Kept. Okla. Geol. and Nat. Hist. Survey, 1904, pp. 5-14.

b Haworth, Erasmus, Univ. Geol. Surv. Kansas, vol. 3, 1898, pp. 91, 94.

c Prosser, Chas. N., Classification of the upper Paleozoic rocks of central Kansas: 

Jour. Geol., vol. 3, 1895, p. 797,
PENNSYLVANIA^ SERIES. 33

Creek and on Salt and Beaver creeks, the sandstones are rare, and 

heavy beds of cherty limestone make up the greater part of the rocks. 

To the south the limestones thin out, and in the vicinity of Arkansas 

River change into red shales.

The name Hominy is from Hominy Creek, in the southern part 

of the Osage country, which flows across practically all formations 

represented in this district.

Chandler district. The Chandler district includes the area of outcrop of all the strata, chiefly shales and sandstones, from the eastern 

boundary of the red beds westward to the base of the Permian, near 

the line of the Atchison, Topeka and Santa Fe Railroad, including 

part of Pawnee, all of Lincoln and Pottawatomie, and the eastern 

parts of Noble, Payne, Logan, Oklahoma, and Cleveland counties. 

It corresponds practically to the southern continuation of the Flint 

Hills of Kansas and the Osage Nation, which disappear about the 

line of Arkansas River. Perhaps it would be more correct to say 

that the rocks of this district are in strike with those of the Flint 

Hills.

In general, the rocks of this district consist of> alternating strata of 

red and whitish sandstone and red-clay shale. Along the streams the 

sandstones outcrop as ledges 20 feet or more thick, sometimes, forming small waterfalls in some of the streams. To the east of the Santa 

Fe Railroad the sandstone beds are most abundant, but they are 

grayish or almost white, though the intervening clay is always red. 

Business blocks at Perry, Orlanclo, Mulhall, Gutjhrie, Edmond, Oklahoma City, Norman, and Noble, along the line of the Santa Fe Railroad, are built of red sandstone. The buildings of the Oklahoma 

Agricultural and Mechanical College, at Stillwater, and many of the 

business blocks at Shawnee are constructed of the lighter-colored 

stone. Practically all of the towns in Lincoln, Payne, and Pottawatomie counties, and those in the eastern parts of Noble, Logan, 

Oklahoma, and Cleveland counties, contain buildings constructed of 

either the red or gray sandstone. Through the entire region it is 

used for the abutments of bridges, for corrals and small buildings, 

and not infrequently for dwellings.

The sandstone is water bearing. Springs are not uncommon, and 

water, which is ordinarily soft and suitable for ajll domestic purposes, 

is usually found in wells at moderate depths. It is the best water 

found anywhere in the red beds below the Quartermaster formation.

The region is well wooded. Trees grow along the streams and in 

many places on the hills. The three eastern counties, especially, 

are covered with a considerable growth of the more hardy forest 

trees, notably oak and hickory. Along the line of the Santa Fe

IEE 148 05 M 3
34 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

Railroad the uplands are level prairie and tlie bottom lands are 

timbered. West of this line the timber becomes less plenti ful.

While fossils are not particularly common in the Chandler district, 

still a number of localities have been found which yield typical 

Pennsylvania!! invertebrates. Near Chandler, the county seat of 

Lincoln County, for which the district is named, the following forms 

were found: Allorisima subciuieata^, Pinna peracuta, Spirifer canieratus, Meekella straticostata^ Productus semireticulatus, and Athyris 

subtilita.

PERMIAN SERIES. 

PERMIAN ROCKS OF KANSAS.

According to the classification of the Kansas geologists, notably 

Prosser, the line of separation between the Carboniferous and Permian in Kansas has been drawn at the base of the Wreford limestone, 

a ledge typically exposed near Junction, Kans., on Kansas River.' 

In southern Kansas this ledge outcrops near the summit of the 

Flint Hills in eastern Cowley County and along Grouse Creek, near 

Dexter, and, as stated above, is found in Oklahoma along Little 

Beaver Creek, in the Kaw Reservation, and in the western part of 

the Osage Nation as far south as Arkansas River. Above the 

Wreford limestone in southern Kansas and eastern Kay County, 

Okla., there are at least three heavy beds of limestone with 

interbedded shales, known as the Florence flint, Fort Riley limestone, 

and the Winfield formation. Above the Winfield formation limestones become less prominent and clays and shales make up the 

greater part of the series. These formations above the limestone 

members constitute the Marion formation of Prosser and the Wellington shales of Cragin.6 In general, both the Marion and Wellington formations consist of gray, blue, drab, and yellowish shales with 

a few ledges of impure limestone. The extensive salt beds in central 

and southern Kansas and the deposits of gypsum in several counties 

of Kansas and in Kay County, Okla., are found in these rocks. 

These two formations, however, appear not to be sharply defined, and, 

inasmuch as both consist of rocks of essentially the same character, 

a definite line of separation will probably not be drawn between 

them, and it is not impossible that as a result of more exact knowledge of the conditions both formations will finally be grouped 

together.

« Prosser, Chas. 8., Revised classification of the upper Paleozoic formations of Kansas: 

.Tour. Geol., vol. 10, 1902, p. 703.

6 See articles by Professor Prosser, Jour. Geol., vol. 8, 1895, pp. 764-796; and by 

Professor Cragin, Colorado Col. Studies, vol. 6, 1896, pp. 8-18.
PERMIAN SERIES. 35

The southern extension of the Marion and [Wellington formations, 

as well as the southern part of the Flint Hi[lls, reach from Kansas 

into Oklahoma. The Flint Hills, as stated above, occupy the western 

part of the Osage Nation, all of the Kaw Reservation, and the eastern 

part of Kay, Noble, and Pawnee counties. The southern extensions 

of the Marion and Wellington occur in western Kay County and pass 

into the Ponca and Otoe reservations, occupying a triangular area 

between the Flint Hills and the red beds. A glance at the map (PL 

I) will reveal the fact that these formations narrow rapidly in northern Oklahoma and their place is taken by the red beds. Perhaps 

it is more correct to state that the color of the shales changes to the 

south, becoming red, while at the same time more of the red sandstone comes in, so that finally the formation changes to typical red 

beds. On the State line the distance from the Winfield formation, the 

upper conspicuous limestone member, to the eastern outcrop of the 

red beds is perhaps 30 miles; on the southerii line of Kay County,

Okla., it is not more than 15 miles, while

of separation can not be determined, for thq reason that the limestone disappears and its place is taken by re 

In southern Kansas there are three distinct 

First, the heavy limestones in eastern Co^ 

Walnut River; second, the bluish and gray 

Marion and Wellington formations from ^ 

Sumner County; and third, the typical rec

:1 shales and sandstones.

dnds of Permian rocks: 

'ley County and along 

Clays and shales of the 

alnut River to western 

beds consisting of red

sandstones and clays extending from this point nearly to the west 

line of the State. In eastern Oklahoma, on the other hand, only 

the red beds appear.

Thus it is seen that the red beds extend fi 

than in Kansas, and that the eastern limit 

coincide with the line of separation between 

Permian. In other words, the red color of t]

thought characteristic of only the Permian

transgresses far into the region of the Pen n^ylvanian rocks. This

means, 'of course, that the line of separation between the rocks of these

two epochs must finally be drawn far out in t

writer has attempted to do.tt

GENEBAL RELATIONS OF PERMIAN BOCKS

Permian rocks, usually known as the " red 

part of Oklahoma. This series of rocks is b; 

in the Territory, inasmuch as it is not only 

the soils, but it also supplies most of the

farther south the line

lather east in Oklahoma 

f the red beds does not 

the Pennsylvania!! and 

e rocks, which has been 

of the region, in fact

red beds, and this the

Il|« OKLAHOMA.

beds," occupy the greater 

far the most important 

the origin of nearly all 

Gilding stone, gypsum,

See footnote, p. 32,
36 GEOLOGY AND WATER EESOUECES OF OKLAHOMA.

salt, and other economic products, and at the same time furnishes 

the water supply for the greater part of the Territory. These rocks 

have been studied for a number of years both in Kansas and Texas, 

and considerable literature has accumulated upon the subject,0 but no 

attempt has ever been made to write a description of the red beds as a 

whole, nor is such a task contemplated here. All that is attempted 

is, first, to give only such references as will enable the reader to understand former classification, and afterwards to present a classification, 

based upon the results of several years field work, that is believed to 

embody such conditions as exist in Oklahoma.

The geological age of the red beds has long been an open question. 

The reason for this uncertainty has always been a lack of fossils, 

for until within the past few years organic remains had been found 

in but one or two localities in the Oklahoma red beds, and in Kansas 

none at all. Recently, however, fossils, both vertebrates and invertebrates, all of Permian age, have been discovered in at least five 

general localities in the red beds of Oklahoma. It seems reasonably 

certain, however, as shown by Adams,** that a large part of the 

typical red beds rocks in eastern Oklahoma are really Pennsylvanian 

in age, and, on the other hand, since fossils are not at the present 

time known to exist in the higher members of the series, the age of 

that part of the red beds is still open to doubt. And, moreover, until 

the correlation with the Texas red beds has been more fully worked 

out and fossils collected and identified throughout the entire region 

the matter can not be considered as settled. Instead of using any 

strictly geologic term in speaking of the rocks of the series the 

writer will employ the name of " red beds," by which the rocks are 

generally known, to include the rocks of both the Pennsylvanian 

and Permian ages, it being understood that the rocks above the lower 

part of the Enid formation are regarded as Permian in age and 

those below this point as Pennsylvanian.

The red beds area of the southern part of the Great Plains extends 

for 600 miles or more across Kansas, Oklahoma, Indian Territory, 

Texas, and New Mexico. The most northern exposure of the beds, 

so far as known to the writer, is near Arlington, a few miles south 

of Hutchiiison, Reiio County, Kans. To the southwest they pass 

under the Tertiary of the High Plains, or Llano Estacado, and 

appear in the valleys of the Pecos and Rio Grande in New Mexico.

The eastern border of the outcrop of the red beds in Kansas and 

Oklahoma is a crescent-shaped line running southeast from near 

Hutcliinson and east of Kiiigman, Kans., crossing the KansasOklahoma line at Caldwell, then trending southeast near Nardin,

a See under " Classification." 6 Loc. cit.
PERMIAN SERIES. 37

Tonkawa, and Red Rock, cutting diagonally across the strike of 

Pennsylvania!! limestones and shales through the eastern parts of 

Payne and Lincoln counties to the western part of the Creek and 

Seminole nations. Here the line swings to the southwest and continues through the Chickasaw Nation to the vicinity of Da vis, Ind. T., 

passes around the western end of the Arbuckle Mountains, crossing 

Red River 35 miles west of Gainesville, Tex., and, as stated by Adams,. 

cuts diagonally across the strike of Pennsylvania!! rocks in Archer, 

Young, and Throckmorton counties, Tex.a Wherever exposed, the 

rocks of this series along their eastern border merge into the Pennsylvanian limestones and shales.

The western limit of the red beds in Oklahoma and Kansas is much 

more irregular. In all instances, so far as observed, the upper line 

is one of unconformity. The superjacent itocks range from the 

Lower Cretaceous to those of the latest geologic formations, but by 

far the greater part of the overlying deposits are of the later Tertiary 

age. In places the Tertiary deposits extend east along some divide 

nearly across the red beds area. In other localities they have been 

almost removed by erosion and the red beds are exposed far to the 

west of the main body. Along the valleys of the larger streams the 

red rocks reach many miles westward, although the level uplands are 

covered by the Tertiary beds. The South Canadian, for instance, 

has cut through the Tertiary deposits for practically its entire course 

across the plains, and red beds are everywhere exposed. Other 

streams, including the Salt Fork, CimarrOn, North Canadian, 

Washita, and Red rise in the Tertiary deposits west of the red beds 

and flow southeast across these beds and pass into the Pennsylvania!! 

area to the east. It is along the course of these rivers that some of 

the finest exposures of the red beds may be seen.

CLASSIFICATION.

The red beds in Texas were described by Professor Cummins b in 

1891. He divided the series into the Wichita beds, the Clear Fork 

beds, and the Double Mountain beds. In 1902 Professor Hill proposed the term " Brazos series " to apply to the red beds as a whole c 

Professor Cragin has published two papers on the red beds of Kansas 

and Oklahoma. In his first paper, published in 1896,* the red beds 

were designated the Ciniarron series in contradistinction to the Big

" Op. cit., p. 196.

6 Cummins, A. W., Second Ann. Kept. Geol. Survey Tex^s, 1891, pp. 394-424.

a Hill, Robert T., Geology and geography of the Black and Grand prairies, Texas: 

Twenty-first Ann. Rept. U. S. Geol. Survey, pt. 7, 1901, p. 160.

d Cragin, F. W., The Permian system in Kansas: Colorado Col. Studies, vol. 6, 1896, 

p. 3.
38 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

Blue series or lower Permian, and the Permian rocks were divided as 

follows:

Cimarron series.--

Kiger division.

Big Blue series.

Big Basin sandstone. 

Hackberry shales. 

Day Creek dolomite. 

Red Bluff sandstone. 

Dog Creek shales. 

Cave Creek gypsums. 

Flowerpot shales. 

Cedar Hills sandstones. 

Salt Plain measures. 

Harper sandstone.

Sumner division...... /Wellington shales.

IGeuda salt measures. 

(Chase limestones (Prosser). 

lNe.osho shales (Prosser).

Salt Fork division.

Flint Hills division.

Professor Cragin afterwards adopted Prosser's name, Marion, 

instead of Geuda salt measures. In a subsequent paper Professor 

Cragin modified his classification of the Cimarron as follows: a

f Taloga . __-_.__-_._-_-.__ Quite variable with locality. 

Kiger _.____<Day Creek. ................None.

iRed Bluff __.____..--___-. .None determined.

Dog Creek (Stony Hills) _ /Chapman dolomite.

lAmphitheater dolomite.

r Shinier gypsum. 

Cave Creek. ..............A Jenkins clay.

I Medicine Lodge gypsum.

Glass Mountain ._____.

Salt Fork __

Kingfisher

- \Cedar Hills sandstone.

f Salt Plain. 

IHarper.

The writer has spent four seasons in studying the red beds of Oklahoma and finds that there are local conditions which make it desirable 

to propose a somewhat different classification from any previously 

suggested. The writer has used the earlier classifications as far as 

they can be applied, and he has adopted the names which are equivalent to those that he recognizes, but where new classification has 

become necessary he has given new names to avoid confusion of terms.

The following table shows the relation of Professor Cragin's 

revised classification to the one used in this report :6

0 Cragin. F. W., Observations on the Cimarron series : Am. Geologist, vol. 19, 1897, 

pp. 851-363.

* See article by the writer in Second Bien. Kept. Oklahoma Geol. and Nat. Hist. Survey, 

1902, pp. 42 et seq.
PEEMIAN SERIES. 

Relation* of classifications of Perm tali rocks.

39

Cragin's classification. Classification used in this report.

Taloga

Quartermaster formation.

Mangum dolomite member. 

Collingsworth gypsum member. 

Cedartop gypsum member. 

Haystack gypsum member. 

Kiser gypsum member. 

Chaney gypsum member.

Greer formation...

Day Creek _.......-__-.

Bed Bluff ..............

Dog Creek (Stony Hills)

Cave Creek. ____________

Glass Mountain 

Kingfisher _____

I Woodward formaI tion_____________

Blaine formation _ _

WEnid formation.

Day Creek dolomite member. 

Whitehorse sandstone member. 

Dog Creek shales member.

Shimer gypsum member. 

Medicine Lodge gypsum member. 

Ferguson gypsum member.

The term " formation " is here used in a general sense to designate a 

larger or smaller sequence of strata, which in one instance corresponds 

to a formation having a simple and uniform lithologic character, or 

in another, to a group of such formations. The classification is 

intentionally elastic, since the precise stratigraphic relations, which 

could be determined only with accurate base maps and detailed 

surveys, have not yet been ascertained. The generalized section 

shown in fig. 2 represents graphically the classification used in this 

report.

ENID FORMATION.

The Enid formation includes all the rocks of the red beds from 

tjie base of the Permian to the lowermost of the gypsum ledges on 

the eastern slope of the Gypsum Hills. The top of this formation, 

however, is not a plane, since the gypsum beds, which mark its uppermost limits, are found to be more or less lenticular when traced for 

long distances. The Enid comprises all of the Harper, Salt Plain, 

and Cedar Hills members and the greater part of the Flowerpot member of Cragin's first paper and the Kingfisher and Glass Mountain 

formations of his second paper. It is named from the county seat of 

Garfield County.
40 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

Tertiary

Quartermaster 300 <

Greer 275 ,

Woodward 425'«

Coarse sandstone and

Delhi fdolomite) 

Collingswortb (gypsum) C 

Cedar Top (gypsum) 

Haystack ( gypsum) 

Kiser (gypsum) 

Cbaney (gypsum)

Day Creek (dolomite)

Red Bluff (sandstone)

Dog Creek shales

f Shimer (gypsum)

Blame 100' < Medicine Lodge .»

CFerguson ' i_>

Enid 1500'

FIG. 2. Generalized section of the Oklahoma Permian red beds. In the above legend 

" Delhi " should read Mangum and " Red Bluff " Whitehorse.
PERMIAN SERIES. 41

The Ehid outcrops over a larger area than any other formation 

of the Permian in Oklahoma and is exposed extensively in adjoining 

States. In Kansas it outcrops over parts of Sumner, Kingman, 

Reno, Barber, and Comanche counties and all of Harper County. In 

Oklahoma it is found in the western parts of Kay, Noble, Payne, 

Logan, Oklahoma, and Cleveland, parts of Woods, Woodward, 

Blaine, and Canadian, and all of Kingfisher, Garfield, and Grant 

counties. It also extends into the Chickasaw Nation.

The Enid formation consists chiefly of brick-red clay shales, with 

some interbedded ledges of red and .whitish sandstone. It occurs in 

two general areas, which may be distinguished on lithological grounds 

as follows: An eastern area, in which there are a few inconspicuous 

ledges of sandstone, and a western area, in which the sandstones are 

mostly wanting. In the present state of knowledge it is impossible 

to draw an accurate line of separation between these two areas, and 

for this reason the strata in them are not defined as separate members.

The eastern area of the Enid formation is triangular and occupies 

several counties in the central part of the Territory, in which there is 

little hard rock of any kind. Its eastern boundary is approximately 

along a line from Blackwell to Norman and its western limit is along 

a line from Alva to El Eeno. It includes eastern Blaine, Canadian, 

and Woods counties, all of Grant, Garfield, and Kingfisher, and the 

western parts of Kay, Noble, Logan, Oklahoma, and Cleveland 

counties.

Throughout this area the soil is red, except where later deposits 

cover the uplands or among the sand hills north of some of the 

streams. Eed clays and occasional ledges of thin sandstone outcrop 

along the bluffs of a few streams. These sandstone ledges, however, 

are of comparatively little economic value, being generally too soft for 

building purposes. Quarries occur near Nardin, Kingfisher, Hennessey, and Luella. In the general absence of building stone, foundations for houses are usually made of brick, and artificial stone may 

come into use extensively.

The rocks of the western area of the Enid consist chiefly of red 

clay shale, some inconspicuous ledges of soft sandstone, and occasional 

bands of whitish or greenish shales, which vary from 1 inch to several feet in thickness. The upper strata are in places highly gypsiferous, and at some localities brine springs issue from them. No 

attempt is made to separate the eastern and western areas of the Enid 

formation, except to state that they are sometimes separable locally a 

few miles east of the base of the Gypsum Hills.

The Enid formation is in most places strongly impregnated with 

mineral salts, particularly common salt and gypsum. In many localities the water from the wells is unfit for drinking, and the people are 

obliged to use cistern water.
42 GEOLOGY AND WATER RESOURCES OP OKLAHOMA.

In the western area, along the base of the Gypsum Hills, salt measures are prominent. The Little Salt Plain, in northern Woodward 

County, near the Kansas line, and Big Salt Plain, in the northeastern part of the same county, are both located in the Cimarron channel, while the Salt Creek Plain, in north-central Blaine County, is 

on a tributary of the same river. At the Salt Creek Plain some 

of the most typical saline springs in the Territory may be seen. In 

several canyons at the head of Salt Creek are exposures of a grayishred, mottled, saliferous sandstone. This sandstone is often distinctly 

cross-bedded, and appears to have been tilted; from it issue numerous springs of strong brine. So far as known, this sandstone is not 

found elsewhere in the region, and it seems to be a local phase of the 

clay-shale formation. It is possible, however, that these sandstones 

are not themselves salt bearing, but are merely porous strata through 

which brines from some deep-seated source reach the surface. The 

water from the springs issuing from the various canyons forms 

rills, which, in turn, unite to form the headwaters of Salt Creek;

Above the level of the Salt Plains and below the gypsum ledges 

there intervene 150 or 200 feet of red clay shale, which is interspersed 

with bands of whitish, greenish, and bluish clay and local thin ledges 

of gypsum.

The following analyses of shales from the slope of the Gypsum 

Hills indicate their chemical constitution:

Analysis of clay from Stucks Canyon, at the head of Salt Creek, 4 miles west of 

Ferguson, Blaine County, 'Olcla.

Per cent. 

Silica ___-________________________._______________ 64.17

Calcium oxide___________________________________ 1. 34

Iron oxide_______________________'__________________ 8.10

Aluminum oxide_ ___ ___ _ ________ _ _ _ _i___ ___ ___ 14. 80

Magnesium sulphate _________________________________-, 5. 57

Magnesium carbonate _ _ - _ ___ _ ___ _ _______________ . 27

Water ___________________________________________ 6. 54

Total________________________________________ 100.79

Analysis of so-called copper ore from Henquenets Canyon, an Stilt Creek, 4 miles 

east of Ferguson, Blaine County, Okla.

Per cent. 

Silica and insoluble silicates___________________ __ 67i 43

Iron oxide_______________________________________ 16. 95 

Calcium carbonate_________________-_______________ 1. 85

Magnesium carbonate________________________________ 5. 41

Sodium chloride ____________________________________ 4. 99 

Water __________________________________-______, 3. 40

Total_________________._______________________ 100.03

The material analyzed was a concretion-like piece of green clay or 

shale. It is thought by some to be copper ore, on account of its color,
U. 8. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. 148 PL. VII

A. TYPICAL RED-BEDS EROSION.

J5. RED-BEDS SLOPE BELOW MASSIVE GYPSUM.
PERMIAN SERIES. 48

but it contains no copper, and the green color is due to some form 

of iron, probably a mixture of ferrous and ferric oxides.

Analysis of ffi/psiferous yreen clay from slope of the Gypsum Hills, near Mount 

Reman, eastern Woodward County, Okla.

Per cent.

Calcium sulphate ___________________________________ 58. 00 

Calcium carbonate _________________________________ 5. 35

Magnesium carbonate ______ ______ __________________ 3. 49

Water._________ _______________ _________________ 15. 38

Oxides of* iron and aluminum______________!______________ 3.27

Silica and insoluble residue.____________________________1 13.58

Total________________.________________________ 99.13

The very soft material of which this shale is composed renders it 

particularly susceptible to the action of weathering and the entire 

thickness is characterized by such marked erosion forms as are shown 

on PL VII, B. Wherever the cap of gypsum has been removed over 

any considerable area, or for any great length of time, these shales 

have been worn away. Perhaps the most common erosion form is 

that of cones of red clay cut by deep and uneven gullies regular 

badlands structure. Not infrequently rows of these cones are 

arranged palisade-like along the summit of a fast-disappearing ridge 

into which gullies are eating their way (PI. VII, A.} In the Glass 

Mountains, for instance, the slope of the bluffs below the gypsum 

ledges is much cut by erosion. The action of the water has produced a great variety of unusual forms; small buttes and buttresses, 

cones and minarets, pinnacles and peaks, shoulders and ridges, 

domes, towers, chimneys, gullies, ravines, and all sorts of fantastic 

shapes have been carved by erosion from the blood-red shales along 

the slope of the bluffs.

The face of the bluffs is frequently covered with fragments of gypsum, either in the form of plates of transparent selenite (PI. VIII, 

B] or in the form of concretionary masses (PI. VIII, A}. The 

selenite is usually found in seams running diagonally through the 

clay, and the crystals weather out and reflect the sun from thousands 

of points, making the slopes appear to be covered with glass, whence 

the name Glass Mountains.

An analysis of two specimens of the transparent selenite and one 

of the concretionary masses is given below.

Analysis of a. tliin ledge of satin spar from the canyon 4 wiles west of Ferguson,

Blaine Comity, OJcla.

Per cent.

Calcium sulphate __________________________________ 78. 87 

Water___________________________________________ 20.94 

[nsoluble residue-__________________________ _ . 18

Total__________________________________________ 99.99
44 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

Analysis of selenite flakes from Mount Hemau, eastern Woodward County,

Okla.

Per cent. 

Calcium sulphate_____________________________ 76. 76

Magnesium carbonate__________________________________ . 84 

Water__________________________________________ 19.80 

Iron and aluminum oxides_______________________________ 1.45 

Insoluble residue_________________________ _________ . 95

Total_________________________________________ 99.80

Analysis of crystalline i/ypxum concretions from Henquenets Canyon, If miles

west of Ferguson, Okla.

Per cent. 

Calcium sulphate_________________________________ 75. 20

Magnesium carbonate____________.______________________ 1. 58

Water___________________________________________ 17.32

Oxides of iron and aluminum____________________________ 2. 52 

Insoluble residue________________________________ 4. 54

Total_________________._____-_______________ 100.89

The thickness of the Enid formation is unknown, but it is probably 

not less than 1,200 feet, and may reach 1,500 feet. The well at Fort 

Eeno, a section of which is shown in PL XXII, was started at about 

the same level as the top of this formation and reached a depth of 

1,370 feet, the drill stopping in red clay. It is possible, however, 

that this well passed through the Permian rocks into red beds of 

Pennsylvanian age beneath. At Spencer, 12 miles east of Oklahoma City, a well passed out of the red beds at a depth of 1,550 feet. 

The greater part of this thickness, however, was in Pennsylvanian 

rocks.

BLAINE FORMATION.

The Blaine formation consists of red shales with interbedded strata 

of gypsum and thin ledges of dolomite. It includes the portion of 

Professor Cragin's Flowerpot formation above the base of the Ferguson gypsum and all of his Cave Creek formation. It is named 

from Blaine County, Okla., where it is typically developed.

The characteristic which justifies its recognition as a formation is 

the abundance of gypsum contained in it, and its extent and limits 

are defined accordingly. The bottom of the lowest massive gypsum 

bed the Ferguson gypsum member is the base of the formation 

throughout its occurrence northwest from Darlington, Canadian 

County. Where it disappears the shales of the Enid continue up to 

the base of the Medicine Lodge gypsum member, which necessarily 

becomes the basal member* of the formation. The top is the Shinier 

gypsum member. Where the gypsum members run out, as they all 

do north of Darlington, the Blaine can not be distinguished readily
U. S. GEOLOGICAL SURVEY

WATER-SUPPLY PAPER NO. 1+8 PL. VIII

A. GYPSUM CONCRETIONS COVERING THE SLOPES OF RED CLAY, GLASS

MOUNTAINS.

B. SELENITE AND SATIN SPAR IN RED CLAY.
PERMIAN SERIES. 45

from the Enid below and the Woodward above, and this local division of the red beds can not well be traced. The Blame formation 

gives rise to an escarpment known as the Gypsum Hills, extending 

from Darlington northwestward between North Canadian and Cimarron rivers, through the corner of Kingfisher County, across Blaine 

County into Woods County. At the Glass Mountains the escarpment approaches closely the Cimarron, which it parallels northwesterly to the Kansas boundary. Beyond Cimarron Kiver the gypsum 

beds are exposed in the northwestern corner of Woods and pass into 

Barber County, Kans., where they trend north and northwest and 

finally disappear under the Tertiary sands north of Medicine River, 

30 miles northwest of Medicine Lodge.

From the east the Gypsum Hills appear as a wall crowned with a

Massive white gypsum 

Sandy dolomite

Bed clay shale

Massive white selenitic gypsum

Eed clay shale with bands and 

concretions

Massive greenish to white gypsum

Bed clay shale with gypsum 

concretions and thin ledges

Medicine Lodge

Perguson

Fio. 3. Section 2 miles east of Altona, Okla.

white band, but the sky line is not continuous, as numerous breaks 

occur where.the gypsum ledge has been dissolved by water and carried away. The general appearance is rather that of an uneven row 

of flat-topped buttes or mesas of various sizes than a single hill with 

a continuous escarpment. To these buttes the name " Mansard 

Mounds " has been given by one writer, in fancied resemblance t :> a 

mansard roof.® Not infrequently a few bold points stand out at a 

distance east of the main range, and these outliers being more conspicuous have sometimes received distinct names, as Glass Mountains, 

Mount Heman, Cedar Hill, and Henquenets Butte, Particular 

names have been given to certain parts of the range, as Stony Hills, 

in Blaine County, east of Watonga, and Chatauqua Mountains for

"Hay, Robert, Bull. U. S. Geol. Survey No. 57, 1890, p. 22.
46 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

the same range farther north, extending to the Glass Mountains. The 

name Marcy Range has been proposed for the entire section of hills. 

These names, however, probably will never supersede the much-used 

term, " Gyp Hills/'

The Blaine formation consists of three ledges of massive gypsum 

interstratified with red shale and an occasional local ledge of more or 

less arenaceous and argillaceous dolomite, which usually occur at the 

base of the heavy gypsum. Only the gypsum members will be 

described in this report. The shales which make up the greater 

part of the red beds have not been differentiated and the dolomites

Massive white gypsum 

Gray sandy dolomite

Ked clay with conspicuous green bands 41' 

near the top

Massive white gypsum 

Grayish sandy dolomite 

Bed clay

Massive white gypsum

Shhner

Medicine Lodge

Eed clay shale with green gypsiferous 54' , =:=^-=s^^^=^====^=* =?^Sbands and thin ledges of gypsiferous gr~ ^~ ~^H=--_^1 == =2

Ferguson

sandstone

FIG. 4. Section near Watonga, Okla., in sec. 32, T. 16 N., R. 10 W.

are too local to deserve formation rank. The gypsum members of the 

Blaine are briefly described below.

Ferguson gypsum member. The Ferguson gypsum member is the 

lowermost of the thick gypsum beds in the red beds of this region. 

It varies in color from almost pure white to a dirty brown, accordingto the purity of the mineral. It outcrops usually a little more than 

half way up the slope of the escarpment formed by the formation* 

but is rarely conspicuous. In Canadian, Kingfisher, and southern 

Blaine counties it is the thickest of the three gypsum members, but 

it thins out to the north and disappears in the region of the Glass 

Mountains, north of which only the two upper gypsum ledges appear. 

The name is derived from the town of Ferguson, Blaine County, in
PERMIAN SERIES. 47

the hills southwest of which the ledge is typically exposed. The 

following is an analysis of this ledge:

Analysis of gypsum from 4 miles west of Ferguson, OJcla.

Per cent.

Calcium sulphate_________ ________________________________ _ - 80. 09

Water ___________________________________________ 19. 82

Insoluble residue______________ __-_ _-- __-_ _-- . 65

Total ___________ __ ___ ____ - _____________ - 100. 56

On PL IX, A, the Ferguson is the lowermost of the gypsum members, scarcely distinguishable as a white line halfway up .the slope. 

Its relation to the other gypsum members is shown in fig. 5.

Massive white gypsum 

Fossiliferous, sandy dolomite

Red clay with seleuite bands

Massive white gypsum 3' 

TCed clay with seams of seleuite 17'

Massive, pinkish to white, gypsum 5'

Shimer

e Lodge

Ferguson

Red clay with layers of concretions 77 , =H -= _- ~ =-==L

FIG. 5. Cedar Hill section in SW. J sec. 18, T. 16 N., R. 10 W.

Medicine Lodge gypsum member. The Medicine Lodge gypsum is 

the most conspicuous gypsum deposit in the red beds. It extends 

uninterruptedly from near the head of Medicine River, in Kansas, 

lo Canadiaii County, Okla., and is in most places the ledge which 

forms the cap of the Gypsum Hills. Perhaps no better description 

of this ledge can be given than that of Professor Cragin, who first 

described it in Kansas, as follows: a

In minor parts, the Medicine Lodge gypsum is nearly pure white: in others 

it is suffused with leaden-gray or dusky-brown shades; most commonly it is

" Cragin, F. W., The Permian system in Kansas : Colorado Col. Studies, vol. 6, 1896, 

p. 32.
48 GEOLOGY AND WATEE EESOUECES OP OKLAHOMA.

grayish white mottled with feebly denned dark spots. The latter are generally the expression of a tendency that existed in the gypsum to form crystals 

under the original conditions of a precipitation, as is shown by the occurrence of 

spots in every gradation from ill-defined spot-like segregations to well-formed 

crystals of selenite. Some of the crystals are of the common rhomboidal pattern, others are of the stellar type.

In the region around the head of Salt Creek and its tributary, 

Bitter Creek, in Blaine County, Okla.. the Medicine Lodge gypsum,

Massive white gypsum 

Gray dolomitie- sandstone

Red clay

Shimer

Massive white gypsum 12' 

Gray dolomitic sandstone 2'

17' Red clay shales 

Massiye white gypsum

Red clay shales with 90 

thin bands of gypsum

3'

Medicine Lodge

JFerguson

PIG. 6. Hitchcock section 4 miles south of Hitchcock, Okla., along Rock Island Railroad.

the middle of the three ledges, has a peculiar form. The middle part of 

the ledge, usually 8 to 10 feet thick, is much harder than the rest of the 

bed or any other ledge of gypsum known in the Territory. As seen 

from below, this part of the ledge is pure white, as shown on PL IX, B. 

It breaks with an even fracture, so that it may often be distinguished 

a mile away. On closer examination it is found to be very hard and 

very fine grained, usually pure white, but with an occasional bluish
U. S. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. 148 Pi.. IX

A. CEDAR HILL, EAST OF WATONGA, OKLA. 

Showing Ferguson gypsum on the slope and Medicine Lodge gypsum as a cap.

B. ANHYDRITE MEMBER OF THE MEDICINE LODGE GYPSUM. 

Salt plain in foreground.
PEKMIAN SERIES. 49

or reddish tint. It takes a good polish and has the general appearance of marble, and is known locally as the Salt Creek marble. And 

sometimes it is difficult to persuade farmers who own a part of the 

ledge that the rock is not valuable for building stone or for ornamental purposes. A chemical analysis reveals the fact that the rock 

approaches an anhydrite that is, it has a very small per cent of 

water of crystallization. Ordinary gypsum contains from 20 to 21 

per cent of water, while in the rock from this ledge the amount of 

water is sometimes as low as 2 per cent.

The area covered by the anhydrite is about 10 miles long and 1 

mile or more wide. No adequate explanation of this peculiarity of 

structure has ever been forthcoming. It is probably because of this 

relatively harder ledge, which resists erosion, that the marked 

topographic forms mentioned above are due.

The following analyses show the relatively small amount of water 

in this rock:

Analyses of " marble" gypsum from the middle part of the Medicine Lodge

member.

Per cent. Per cent.

Calcium sulphate _______________________________ 94.83 92.73

Magnesium sulphate_______ T __________________ 1.93 _

Magnesium carbonate ____ ________________________ 3.15

Water ___________________________________ 2.74 3.15

Insoluble residue___________________________ . 33

Total _______________________.________ 99.50 99.36

Analysis of "red marble" gypsum from the middle part of the Medicine Lodge

member.

Per cent. 

Calcium sulphate. __ _______________________ ______ __ 84. 00

Calcium carbonate_________________________________ 3. 41

Magnesium carbonate______________________________ 2.13

Water ________________________________________________ 5. 38

Oxides of iron and aluminum.___________________________ .78

Insoluble residue__ ________________________ __ 1. 69

Total_________________________________________ 97.39

The analyses given below indicate the composition of the gypsum 

from the lower, middle, and upper parts of the Medicine Lodge:

Analyses of gypsums from the lower (J), and middle (2 and, 3) parts of the 

middle ledge of the Medicine Lodge member.

Per cent. Per cent. Per cent.

Calcium sulphate _____________________ 79.66 94.94 ' 80.82 

Water ____________________________ 20.22 4.95 20.89

Insoluble residue______ _____ _ ______ .46 .67 .35

Total _________________________ 100.34 102. 06
50 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

No. 1 is very hard, being almost an anhydrite, and is left in large 

bowlders when the softer parts are worn away. No. 2 is softer and 

sometimes fills the place usually occupied by No. 1.

Analyses of gypsums from the upper part of tlie Medicine Lodge member.

1. 3.

Per cent. Per cent. Per ceat.

Calcium sulphate____________________ 78.41

Magnesium carbonate____ ___________ 2.03

Oxides of iron and alumium________________ 1. 38

Water __________________________ 18.23

Insoluble residue________-____________ .41

Total ____________________________ 100.46

78.23

.98

20.75

.34

100.30

89.30

1.44

9.33 

.16

100.23

Massive white gypsum 

Gray sandstone

Bed gypsiferons clays 32f < T=

Massive white gypsum \j[

Bed clay

Pinkish to white massive

Shimer

Bed clay antl shale slope

Medicine Lodge

Ferguson

PIG. 7. Bitter Creek section, 6 miles southwest of Ferguson, Okla., on West Branch of

Bitter Creek.

Nos. 1 and 2 are the rocks that make up the greater part of the 

ledge and are used for plaster. No. 3 is harder material, approaching 

anhydrite, sometimes found in lumps or masses, and is not used for 

plaster. K
PERMIAN SERIES. 51

The name Medicine Lodge is that of the county seat of Barber 

County, Kans., and was proposed by Professor Cragin in 1896.

Shimer gypsum member. A third gypsum ledge, to which Professor Cragin gave the name Shimer gypsum, from a township in 

Barber County, Kans., where the rock was first studied, is the uppermost member of the Blaine formation. It is typically exposed either 

as the highest gypsum outcrop somewhat back from the brow of the 

hills, or as the cap rock of occasional bluffs and buttes overlooking

Red clay

Bed clay

Dolomite 

Red clay

Massive white gypsum 

Soft saudy dolomite

Red gypsiferous clay

Massive white gypsum

Red clay, bands of seleuite 

Pinkish mottled gypsum

Shimer

Red gypsiferous clay

with greeu and white selenite bands

Medicine Lodge

Ferguson

FIG. 8. The Rubey section, in South Canyon, head of 'Salt Creek, at the Rubey stuccoplaster mill, Ferguson, Okla.

the slopes below. It is the upper white ledge shown in Pis. IX, #, 

and XXI, A. The description of the Medicine Lodge gypsum 

quoted above from Professor Cragin will in most places apply equally 

well to the Shinier, but the thickness of the upper ledge is not so 

great as that of the Medicine Lodge. Its areal extent and physical 

characters are about the same, except that so far as known there is 

no anhydrite in the Shimer.

The following analyses, made from specimens obtained from the
52 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

Shimer member of the Blaine formation in the canyons 4 miles west 

of Ferguson, indicate the constituents of this rock:

Analyses of gypsum from the lower (1), middle (2), and upper (3) parts of the

Shimer member.

1. 2. 3.

Per cent. Per cent. Per cent.

Calcium sulphate ____________________ 78.22 80.16 79.07

Water ___________________________ 21.22 20.00 21.00

Insoluble residue.___________________ .87 .86 .39

Total _______________________ 100.31 101.02 100.46 

In some localities the shale member which separates the Medicine 

Lodge from the Shimer thins out and the two massive gypsum ledges 

are practically continuous. Caves are not uncommon below the 

various ledges. A generalized section of one of these caves is shown 

in fig. 9.

FIG. 9. Section of gypsum cave.

The thickness of the Blaine formation varies considerably with the 

locality, but it averages about 75 feet.

WOODWARD FORMATION.

Above the Blaine is approximately 300 feet of rocks, consisting 

chiefly of shales, sandstones, and dolomites, and distinguished from 

the formations above and below by the prominence' of dolomites and 

the absence of gypsum. The formation includes all the rocks between 

the two conspicuous gypsum horizons, the Blaine and the Greer, and 

in general it may be divided into three members the Dog Creek, 

the Whitehorse and the Day Creek which were all recognized and 

named by Professor Cragin from localities in Kansas, except that his 

term Eed Bluff was preoccupied, and for it the name Whitehorse has 

been substituted. For the formation as a whole, from the top of 

the Shimer gypsum to the base of the Chaney gypsum, the name 

Woodward is proposed, from the county in Oklahoma where the 

&trata are well represented.

Creek shales member-, The Dog Creek member is composed
PERMIAN SERIES.

mainly of clays, containing occasional thin ledges of magnesian limestone, which in places grade into a fair quality of dolomite.

The ledges, however, are usually thin and rarely sufficiently conspicuous to be worthy of more than passing notice. Professor Cragin's original description of this member is as follows:"

The Dog Creek * * * consists of some 30 feet, or locally of a less or 

greater thickness, of dull-red argillaceous shales, with laminae in the basal

Massive white

gypsum

Dolomite

Red clay

Massive white 

gypsum

Soft sandy dolomite

Red clayThin ledge of soft 

selenite aiid sandy 

red clay

Shimer

] Medicine,Lodge

Red clay with gree 

bands and gypsum 

concretions

PIG. 10. Roscoe section, 1 mile south and 1J miles west of Roscoe, Okla.

part and one or two ledges of unevenly lithified dolomite in the upper. The 

color of these shales resembles that which prevails in most of the divisions 

below rather than of the terranes above the Dog Creek.

In his second paper he modifies his description in this way:

In central Oklahoma it is a great dolomite formation, laminated dolomite 

occupying a considerable part of the thickness.**

0 Op. cit., p. 39.

6 Cragin, F. W., Observations on the Cimarron series: Am. Geologist, vol. 19, 1897, 

p. 358.
54 GEOLOGY AND WATER RESOURCES OP OKLAHOMA.

t

In his second paper he suggests that the name Dog Creek be 

changed to Stony Hills. The writer agrees that the name Dog 

Creek is, perhaps, not the best that could be used, but in view of the 

fact that the dolomites which make up the Stony Hills in eastern 

Blaine county belong to the Blame formation and do not belong to 

the Dog Creek, there seems to be no good reason for using the name 

Stony Hills to designate this member.

Shimer

\ Medicine Lodge

PIG. 11. Glass Mountain section, on northwest side of the mountain.

Studies made during the last three years have demonstrated that 

in many parts of Oklahoma the thickness of the Dog Creek is much 

greater than that given by Professor Cragin. Near Quinlan, in 

eastern Woodward County, the aneroid readings indicate 225 feet 

as the thickness of these beds, measured from the top of the underlying gypsums of the Blaine formation to the sandstones of the next
PERMIAN SERIES. 55

higher formation of this member, the Whitehorse, and in a number, of 

localities 150 and 175 feet were recorded. Exposures are common 

along the top of the Gypsum Hills from Canadian County to the 

Kansas line and beyond.

Whitehorse sandstone member. The Wllitehorse sandstone was also 

described (under the name Reel Bluff sandstone) by Professor Cragin 

in his first paper, as follows: a

This formation consists of some 175 or 200 feet of light-red sandstones and 

shales. * * * Viewed as a whole it is very irregularly stratified, being in

Massive white gypsum 

Fosailiferous dolomite 

Bed clay

Massive white gypsum 

'Sandy gypsiferous rock

Shimer

I Medicine Lodge

Red clay, with bauds of 

gypsum concretions, satin spar

FIG. 12. Granton section ; gypsum-capped butte 1 mile east of Granton, Okla.

some cases considerably inclined, in others curved, and this -oblique and 

irregular bedding, being on a much larger seal 3 than that of the ordinary 

cross beddings, at first glance gives the impression of dips, anticlines, synclines, 

etc., that have been produced by lateral pressure, the dips, however, being in 

various directions. * * * The Red Bluff beds exhibit the most intense 

coloration of any of the rocks of the series. When the outcrops are wet with 

recent rains their vividness of color is still greater, and the contrasts of their 

almost vermilion redness with other colors of the landscape is most striking.

0 Cragin, JF. W., The Permian system in Kansas: Colorado Col. Studies, vol. 6, 1896, 

p. 40.
00 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

Spots and streaks of bluish or greenish gray sometimes occur in these rocks, 

but not to nearly so great an extent as in the lower beds. The sandstones of 

the Red Bluffs are generally too friable for building stone, but in some instances selected portions have proved hard enough for such use and are fairly 

durable.

In Oklahoma the Whitehorse member often weathers into conspicuous buttes and mesas. For instance, in eastern Woodward and

Massive white gypsom, somewhat

selenitic

Gray dolomite, honeycombed

Red clay shale

Shimer

10' !!== 

Massive greenish to whitish gypsum 18'

Bed clay with harder ledges

FIG. 13. Section of hill west of the mouth of Greaver Creek.

western Woods counties a row of these buttes, which rise 100 to 200 

feet above the surrounding country, extends from the vicinity of 

Whitehorse Springs, whence the name, southwest across the Cimarron, 

to the high divides beyond. To some of these buttes characteristic 

names have been given, as Lone Butte, Potato Hill, Watersign Hill, 

Wild Cat Butte, and the like. The noted Ked Hill, between Watonga 

and Geary in southern Blaine County, is composed chiefly of the 

Whitehorse formation. South of South Canadian River this sand-
U. S. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. 148 PL. X

A. EROSION FORMS IN CADDO COUNTY BUTTES.

B. DAKOTA SANDSTONE HILLS.
PERMIAN SERIES. 57

stone thickens and on weathering often forms conspicuous bluffs, such 

as the famous Caddo County Buttes, southwest of Bridgeport, shown 

on PL X, A. The Whitehorse sandstone is exposed along the Washita 

from near Chickasha, Ind. T., westward, and in the vicinity of Anadarko it forms bold bluffs both north and south of the river, and 

extends as far west as Mountain View. Ledges which probably 

belong to the same general horizon outcrop north of the Wichita 

Mountains in the vicinity of Hobart and Harrison, and it is not 

impossible that further studies may demonstrate that the same beds 

extend under the upper gypsums across Greer County.

Day Creek dolomite. Resting upon the upper part of the Whitehorse sandstone in Kansas and Oklahoma is a conspicuous ledge of 

hard, white dolomite, first described by Professor Cragin from exposures in southern Kansas, as follows: a

Upon the latest of the Red Bluff rests a persistent stratum of dolomite varying in thickness from less than a foot to 5 feet or more. * * * It is a true 

dolomite, containing with the carbonate of lime an equal or even greater percentage of carbonate of magnesia. * * * Though not of great thickness, it 

is an important member of the upper Permian of southern Kansas and northern 

Oklahoma, owing to its persistence, which makes it a convenient horizon of 

reference. * * * The stone is nearly white in .fresh fracture, weathering 

gray, and often has streaked and gnarly grain resembling that of fossil wood. 

* * * Its cherty hardness and fracture are not due to the presence of silica, 

as one is tempted to infer, but are characters belonging to it as a dolomite. It 

is a durable building stone.

In his second paper on the Permian rocks, in describing a typical 

Oklahoma locality Professor Cragin says:

The brow of the Red Hills near Watonga, Okla., is capped with the Day Creek 

dolomite, which here presents itself as a compact stratum of gray, somewhat 

pinkish or reddish tinged cherty-hard rock, little different from the typical ledge 

that skirts the flanks of Mount Lookout in Clark County, Kans. The stratum 

here has a thickness of 3 feet.

The line of outcrop of the Day Creek in Oklahoma is not continuous ; nevertheless, it is found in numerous localities, and on account 

of its distinctive lithological appearance it is always easily recognized. It is displayed on many of the hills of Woodward County, not 

only north of the Cimarron, but also between the Cimarron and the 

North Canadian and south of the latter stream. In Blaine County 

it forms the caps of a number of the prominent hills, notably the Eed 

Hills betweeen Geary and Watonga. South of South Canadian River 

in Caddo County the dolomite covers the Whitehorse buttes southwest

0 Op. cit., p. 44.
58 GEOLOGY AND WATER RESOURCES OP OKLAHOMA.

of Bridgeport and outcrops southwestward as far as the headwaters 

of Cobb Creek and on the west side of that creek past Colony. In 

the vicinity of Mountain View, in the valley of Washita River, a 

ledge of dolomite appears at the same general level as that occupied

Massive white 3o'< 

gypsum

Red clay

Massive white 23' 

gypsum

Honeycombed 

dolomite

Shimer

Medicine Lodge

Eed clay 140 ^-^r^=r^^E^^^^

FIG. 14. Section on Main Creek one-half mile northeast of Bat Cave.

by Day Creek, and another dolomite ledge in the hills north of Harrison may provisionally be referred to this horizon.

The composition of this material in Oklahoma may be understood 

by reference to the following analysis:
PEEMIAN SERIES'. 59

Analysis of dolomite from the summit of the Red Hills 6 miles northwest of

Qeary, Okla. Per cent 

Calcium carbonate_____________________________ 42. 17

Magnesium carbonate _______ _____ _ ______________ 52.86

Water _______________________________________________ 1. 82

Oxides of iron and aluminum__________________________ 1.35

Silica and insoluble residue__________________________ 1.82

Total _______________________________________ 99. 88

GREEK FORMATION.

Above the Woodward formation are red clays, shales, and sandstones, and intercalated beds of gypsum and magnesium limestone or 

dolomite 150 to 300 feet thick. Gypsum is the characteristic deposit 

of this formation, as it is of the Blaine. This formation, for which 

the name Greer is proposed, from the county in southwestern Oklahoma, in which it is well exhibited, is exposed over a very irregular 

area. For the purposes of discussion it may be grouped according to 

two general areas, an eastern and a western. The eastern area extends 

from the southern part of Woodward County southeast through 

Dewey, Ouster, Washita, Caddo, and Comanche counties into the 

Chickasaw Nation. The western area extends over Washita County, 

touches the extreme southeastern part of Roger Mills County, and 

crosses Greer County to Collingsworth, Tex. The rocks of these 

two areas are overlain by the same formation.

The rocks of the eastern area of the Greer formation strike northwest and southeast just west of the outcrops of the Woodward formation. They are chiefly red clay shale, interstratifiecl at several horizons with red sandstone and gypsums, which are, however, very 

irregularly bedded and can rarely be traced as continuous or definite 

ledges. Nevertheless, the thickest ledges of gypsum known in the red 

beds are found in this area. Thus 5 miles northwest of Weatherford 

a ledge 60 feet thick was measured, as shown in fig. 18; in the vicinity 

of Cloud Chief beds 50 feet thick are not uncommon (see fig. 19) ; 

and in a well near Seger, Washita County, a ledge 115 feet thick is 

reported. But these beds are not constant, thickening rapidly or disappearing without apparent regularity. Along a single bluff one 

may see the beds change from gypsum to sandstone within a distance 

of a few rods, and a quarter of a mile farther the sandstone again 

merges into gypsum. So variable is the stratification of all the rocks 

of the Greer formation in this region that no attempt is made to 

divide it into members. A section would usually not answer for a 

point half a mile away.

The most northern outcrop of this formation, so far as known, is
60 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

in the southeastern part of Woodward County, Okla., a few miles 

south of Richmond. It is possible that these strata represent the

'

Massive white, 

gypscim 22'

FIG. 15. Section on Sand Creek, 5 miles northwest of Quinlan, Okla.

southern continuance of Professor Cragin's Hackberry shales and 

Big Basin sandstone, but further study in the field is necessary to
PERMIAN SERIES. 61

.substantiate this point. A few miles south of Richmond, Wogdward 

County, on the divide between the North Canadian and South .Canadian, a thin bed of gypsum appears, interstratified between shales 

and sandstones. This ledge, which is 1 to 3 feet thick, continues 

south, appears as a cap to the high bluffs along the South Canadian

Soft red sandstone

Red clay 110' , ^S=^=HEI Dog Creek

Massive white gypsum

Bed clay

Massive white gypsum

Shimer

Medicine Lodge

Bed clay

FIG. 16. Section on butte at mouth of Doe Creek, Woodward County, Okla. In the 

above legend " Bed Bluff" should read Whitehorse.

north and west of Taloga, and outcrops on both sides of this river as 

far as the vicinity of Stone, Day County. The ledge thickens to the 

south, and at Weatherford, Custer County, one of the beds is more 

than 60 feet thick. PI. XI shows the entrance to a cave at this 

place, and fig. 18 a section of the hill, The various exposures,
62 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

averaging perhaps 10 feet in thickness, appear along the various 

branches of Barnitz Creek and the Washita Eiver in Ouster County 

and as far west as Eoger Mills County. In eastern Washita County, 

in the vicinity of Seger, in the region between Cloud Chief and 

Weatherford, the gypsum members seem to find their extreme development, there being several heavy ledges, and one, as stated above, 

that has a reported thickness of 115 feet. Fig. 19 gives section of 

a butte on the Washita Eiver near Cloud Chief.

Massive white gypsam 15'

Red clay

Massive white gypsam

Red clay, bands of gelenite

PIG. 17. Section of high bluff at southeast corner of the Salt Plain.

Following the strike to the southeast outcrops of gypsum occur on 

the hills north of Washita Eiver, between that river and Cobb Creek, 

almost to Fort Cobb. South of that river the gypsum forms the top 

of conspicuous bluffs opposite Fort Cobb, and on the hills to the south 

and east. Exposures of gypsum continue on the divide between 

the waters of the Washita and those of Eed Eiver as far as the 

vicinity of the Keechi Hills in southwestern Caddo County,.along 

Little Washita Eiver (see fig. 20), and between these hills and 

Apache. The same beds probably extend to the region of Marlow, 

Ind. T.
U. 8. GEOLOGICAL SURVEY

WATER-SUPPLY PAPER NO. 148 PL. XI

ENTRANCE TO GYPSUM CAVE NEAR WEATHERFORD, OKLA.
PERMIAN SERIES. 63

The character of the gypsuni in the eastern part of the outcrop of 

the Greer formation may be better understood by the following 

analyses of material taken from this region, No. I being from the 

cave 5 miles northwest of Weatherford, No. 2 from ledge 4 miles west

C

Massive white gypsum 50'

Red clay shale

White dolomite

30'

Red sandstone 75

Fro. 18. Section of bluff 5 miles northwest of Weatherford, Okla.

of Weatherford, No. 3 from 5 miles west of Weatherford (near ledge 

of sandstone), and No. 4 from 5 miles southwest of Cement, Okla.:

Analyses of gypsum, from near Weatherford and Cement, Okla.

l.

Calcium sulphate______________ 75. 57 

Calcium carbonate_______________ 1. u 

Magnesium sulphate_____________ 

Magnesium carbonate__________ __ .49 

Water ______________ 20. 22 

Oxides of iron and aluminum________ . 45 

Silica and insoluble residue_________ 1. 66

3. 4.

Per cent. Per cent. Per cent. Per cent. 

77.38 27.25 74.45 

46. 73 4. 25 

.83 ____ _____

-__ 1.42 

17.36

Total ________ 99.4!

20.78

.67

.41

100.07

.84

18.61

8. 30 . 61

1. 22 1. 02

102. 28 99. 78
64 GEOLOGY AND WATEE BESOUBCES OF OKLAHOMA.

In the western area of the Greer formation the rocks differ in 

several particulars from those in the' eastern area just described. 

Instead of being unevenly stratified the rocks are deposited in regular 

layers. Sandstones are practically absent, or at least inconspicuous, 

and the sequence consists of layers of gypsum and magiiesian limestone or dolomite interstratified among gypsiferous clays.

The rocks of this area appear to connect with those of the eastern 

area in southwestern Washita County, although throughout the region 

between Cloud Chief and the southwestern part of the county across 

the valleys of the various branches of Elk Creek, the gypsums ordiMassive white gypsum

Sandstone and red clay

Massive white gypsum

Soft, red gypsiferous sandstone 75 < 

F[G. 19. Section of butte 5 miles southwest of Cloud Chief, Okla.

narily do not appear. However, at several points along the line of 

strike, ledges 10 feet or more in thickness may be seen in canyons or 

along stream beds. Just before reaching the North Fork oi Eed 

River, and just north of the corner of Roger Mills, Washita, and 

Kiowa counties, regular ledges appear, and along the north side of 

the North Fork for 10 miles or more they form an escarpment 125 to 

175 feet high, as shown in PL III, #, and fig. 21. This is, perhaps, 

the finest exposure in Oklahoma, the gypsum members, here appearing in four separate ledges, having a thickness of 75 feet. The 

river cuts through the formation west of these bluffs, and the gypsums 

again appear at Haystack Butte in Greer County about 20 miles
PEKMIAN SEKIES. 65

northwest of Granite. The rocks of the Greer form conspicuous 

bluffs on both sides of Haystack Creek and on Elm Fork of Red River 

and its tributaries as far as Collingsworth County, Tex. The gypsums which occur in such abundance in southern Greer County in the 

vicinity of Duke and Eldorado also belong to the Greer formation.

The rocks of the western area of the Greer consist of red clay 

shales, heavy gypsum members, and a ledge of dolomite or magnesiaii 

limestone. At the base of the formation is an unknown thickness 

of red gypsiferous and saliferous shales and sandstones. These 

shales contain occasional local ledges of gypsum a foot or two thick,

Bed clay shale

Soft rock gypsum, white, pinkish 15

Soft red sandstone

Bed clay shale

Bed sandstone

FIG. 20. Little Washita River section, taken west of Frisco Railroad crossing.

and beds of white and greenish shales are not uncommon. In the 

region of the heavy gypsum formations there are several salt plains 

fed by springs that issue from below the gypsums, or in one instance, 

from shales between the gypsums. These shales between the gypsimi beds do not differ materially from those at the base of the 

formation, nor from those between the gypsum ledges of the Blaine 

formation. Immediately beneath the heavy gypsum beds there is 

often a foot or two of bluish or greenish clay or shales. Figs. 22, 23, 

and 2i show characteristic sections taken in this region. 

IKB 148 05 M 5
66 GEOLOGY AND WATER EESOUECES OF OKLAHOMA.

There are five prominent ledges of the Greer formation outcropping in this region, the three upper ones being thickest and most 

conspicuous. In general, neither of the two lower members is more 

than 4 feet thick, and because of their position near the foot of the 

bluff they are frequently inconspicuous. The various members are 

described below.

Chaney gypsum member. This gypsum is well exposed along'the 

south side of Elm Fork from Mangum northwest to the Texas line.

Weathered sandy dolomite 

Red and greeu shale

Massive white gypsum

Red and greeu shale 

Massive white gypsum

Bed aiid greeu clay shale

Massive white gypsum, 

occasional thin ledges sandstone

Reddish and green shale 24', =1=-^^=-=-=^=^=-=

Greenish gypsum, gypsiferous shale 5'

Ked and greeu clay shale

PIG. 21. Section of bluff at the Salt Plain, on North Pork of Bed River, 5 miles south

of Carter, Okla.

It is also seen on Haystack Creek, but on North Fork, in Roger Mills 

County, it loses its characteristic structure and becomes simply a 

gypsiferous band in the red clay. On Elm Fork at the mouth of 

Hackberry Creek and also at the Kiser and Chaney salt plains near 

the Texas line, it is a hard massive stratum 3 to 5 feet thick, usually 

\\hite, but sometimes gray or bluish. It is often distinctly stratified 

or apparently cross-bedded, or it may be that the lines of stratification 

are wanting. The formation derives its name from the Chaney Salt 

Plain on Elm Fork of Red River, 4 miles east of the Texas line.
PERMIAN SERIES. 67

Kiser gypsum member. This member is exposed throughout the 

western area of the Greer formation. It is rarely white and in this

Red clay 100'<

Bed clay 50" :^^=^=r^-=-

Hard sandy rock 4'

Red aud green 20 

clay

Massive white 

gypsum

Red and green 8' 

clay

Massive white 

gypsum

Red and green 20' 

clay

Bluish and drab 4' 

gypsum

Red clay

Gypsum and 5 

hard rock

FIG. 22. Haystack section, 6 miles south of Delhi, Okla. In above legend " Delhi "

should read Mangum.

regard differs from all other ledges of the Greer. It varies from a 

decidedly bluish or greenish tint to drab or gray. On the North
68 GEOLOGY AND WATER RESOURCES OP OKLAHOMA.

$^S^:l"f;v:K:^l??^K Collingsworth

Fork it is composed of greenish gypsum and gypsiferous shales, becoming hard locally, and on Haystack Creek of bluish and drab 

gypsum, grading into gypsiferous rock and clay. On Elm Fork, at 

both the Kiser and Chaney salt plains, it is composed of soft, bluish 

to greenish, selenitic gypsum, and at the mouth of Hackberry, 10 miles 

down Elm Fork, it is a bluish stratified gypsum. These occurrences

Dolomite, honeycombed

Ked clay

Massive white gypsum 

Eed and blue clay .

Massive white gypsum

White and green and red clay 6

Massive white gypsum

Eed and greenish clay

Greenish selenitic gypsum 

Eed clay

Hard stratified gypsum 

Bluish and red clay 

Hard gypsum

Cedar Top

Haystack

Bed and bluish shale, banded 75

Kiser

FIG. 23. Section at Salton, Greer County, Okla. In above legend " Delhi " should read

Manguin.

show that while the general character is fairly constant, the stratum 

varies considerably in local sections. The softness of the rock renders 

it particularly susceptible to weathering, and it is frequently inconspicuous. Its thickness varies from 1 to 3 feet. The name is from 

the Kiser Salt Plain on Elm Fork, Greer County, where the ledge is 

well exposed.
PERMIAN SERIES. 69

Haystack gypsum member. The upper part of the Greer formation consists of three layers of massive gypsum and one of dolomite, 

interstratified between beds of red clay shale. The lowermost of the 

three thicker layers, the third gypsum member from the bottom of 

the formation, consists of the typically massive gypsum, almost pure 

white or occasionally grayish in places, with a few thin bands of 

gypsiferous sandstone. This ledge is often cut by joints which separate the rocks into rectangular blocks. These blocks frequently 

weather out and roll down the'slope and in places render it conspicuously white for miles. The Haystack varies locally from 18 to 25

Hard dolomite

Eed clay

Massive white gypsum

Red and blue clay

"Massive white gypsum

Eed and blue clay

"Massive white gypsum thin ledges, 

hard rook

Eed and blue clay

Bluish stratified gypsum,folded

Eed and blue clay

White and bluish gypsum 

Eed and blue clay

Delhi

gsworth

Cedar Top

Haystack

Chaney

PIG. 24. Section at mouth of Hackberry Creek, Greer County, Okla. In above legend 

" Delhi " should read Mangum.

feet in thickness, and so far as known is the thickest gypsum member 

in the western area of Greer. It is exposed along all the bluffs on 

North Fork and Elm Fork and is particularly conspicuous on Haystack Creek and in the vicinity of Haystack Butte, whence the name. 

Cedartop gypsum member. The Cedartop is a massive white 

gypsum, very similar in appearance to the Haystack. It has a constant thickness of 18 to 20 feet throughout the region of outcrop. It 

is very conspicuous on North Fork, Haystack, and Elm Fork, and 

forms the caps of a number of buttes and bluffs throughout the region. 

It is called u Cedartop, 1 ' from a prominent butte on the North Fork of 

Red River, in the extreme southeastern corner of Roger Mills County.
70 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

This rock forms the upper ledge of this butte, and may be seen from 

a great distance up and down the river and even from Headquarters 

Mountain at Granite, 15 miles away. It is shown in PI. Ill, B.

Dolomite, hard rock 

Red and blue clay

Massive white gypsum 8

Red clay with ledges 24' 

of gypsum

Massive white gypsum 12

Red and blue clay 15 . =^^r-=_ ~^~ -

Soft shaly rork 

and gypsum

Red and blue clay 22 J S^^^^:

Bluish gypsiferous rock 10'

Red and blue clay

Massive white gypsum 3'

Red clay

FIG. 25. Section 10 miles south of Mangum, Okla., in bluffs between Salt Fork and Horse

Branch.

Collingsworth gypsum member. This is the upper gypsum ledge 

of the Greer formation, and it does not differ materially in lithological appearance from the Haystack or Cedartop. Like them, it is 

massive and white throughout, and like them, also, it is cut by a 

series of master joints into rectangular blocks. Where exposed, the
PEEMIAN SEEIES. 71

thickness varies from 18 to 20 feet, being approximately that of the 

Cedartop and not so great as the Haystack. As it is the upper 

gypsum member it has often been eroded, and for that reason does 

not always appear in a section. Near the heads of the various creeks, 

however, it is the prominent ledge, and it is also exposed on a num- 

.ber of the conspicuous bluffs, as along North Fork. It is named 

from Collingsworth County, Tex., just west of Greer County, Okla., 

where the gypsum is well exposed.

Mangum dolomite member. Above the Collingsworth and sepa rated from it by about 20 feet of red clay shale is a very persistent 

o-foot bed of more or less dolomitic limestone. In places it is true 

dolomite; while at others it contains only a small per cent of magnesia and is a magnesian limestone. The character of the rock

Massive dolomite

Ked and green shale and clay

Massive white gypsum

Ked clayClay and hard rock

Massive white gypsum

Bed and bine clay

Hard and massive gypsum in the creek bed 15'

FIG. 26. Section on Boggy Creek, 9 miles northeast of Eldorado, Okla.

varies considerably. In places it is arenaceous and soft, in other 

localities cavernous or honeycombed. Often, however, it is firm and 

solid and forms an excellent building stone. Its color is white, drab, 

or sometimes yellowish. The underlying clays have often been 

eroded and the rock frequently covers slopes at a considerable distance below its original position. While the thickness averages 3 

feet, it varies from 1 foot to 5 feet. This member is exposed on the 

hills north of North Fork, in Boger Mills County, and on practically 

all the divides of Elm Fork and Haystack, Bull, and Fish creeks in 

Greer County. The name of Magnum is that of the county seat of 

Greer County, near which the dolomite is well exposed.

Figs. 21 to 26, inclusive, showing sections taken in Boger Mills and 

Greer counties, indicate the stratification in that region.
72, GEOLOGY AND WATER RESOURCES OP OKLAHOMA.

QUABTEBMASTEB FOBMATION.

Above the Greer are 300 feet or more of soft, red sandstones, and 

arenaceous clays and shales, to which the name Quartermaster has 

been applied. So far as known this is the highest formation of the 

red beds in Oklahoma.

In the lower part of the formation the rocks are chiefly shales, 

typically red, but sometimes containing greenish bands and layers. 

The shales become more arenaceous above, and in places form a 

strong, consolidated sandstone, which is rather thin bedded and prone 

to break into small rectangular blocks, and weather queeiiy into 

long and narrow buttresses or rounded, conical, or nipple-shaped 

mounds from 10 to 50 feet or more high. These mounds may be solitary, but in some areas hundreds of them occur in a single quartersection. The sandstone is further characterized by the marked and 

very peculiar dip of the rocks in certain directions. The strata often 

dip at angles of from 20° to 40° to all points of the compass, even 

in a small area. These dips often produce escarpments that have 

the appearance of those formed by regularly bedded dipping strata. 

The most plausible explanation of this phenomenon is that the erratic 

dipping is caused by the undermining of deep-seated rocks, probably 

some of the various gypsum members of the Greer.

In this sandstone, particularly in its upper part, there are many 

springs of soft water, which usually issue as seeps at the head of 

deep canyons or beneath bluffs of red sandstone. While few of 

them have large flows, many are large enough to supply farmhouses, 

or, in some cases, to furnish stock water for ranches. Wells in these 

sandstones frequently yield good water at moderate depths. In fact, 

with the exception of the eastern area of the Enid, the Quartermaster is the only red-beds formation in which any large amount of 

good water is found.

Except where covered by younger rocks, the Quartermaster outcrops over practically all of Day and Roger Mills counties, and is 

also extensively developed in the western part of Dewey, Ouster, and 

Washita counties. To the south and east it is underlain by the 

Greer, while to the west and north it disappears beneath the sands 

of the Tertiary. Streams tributary to the South Canadian, Washita, 

and the North Fork of Red River in the region form canyons in this 

rock and are fed by springs issuing from it. The name is from 

Quartermaster Creek, which flows from Day County through the 

extreme northwestern corner of Roger Mills County and empties into 

Washita River in Washita County. Along this creek both the lower 

shales and the sandstones higher up in the formation are well 

exposed. The peculiarities of structure and weathering are also 

well exemplified along this stream. In the present state of our
PERMIAN SERIES. 73

knowledge it is not deemed advisable to attempt to subdivide the 

Quartermaster formation.

i BED ^EDS OF UNCERTAIN RELATIONSHIP.

There are in Oklahoma two areas of red beds which are not certainly known to belong to any of the five formations heretofore 

described. In this report the names Lawton and Laverne will be 

used to designate these two areas, the term being used in a geographic 

sense.

Lawton area. One of the areas referred to includes the country 

surrounding the Wichita Mountains on all sides, occupying practically all of Comanche and Kiowa counties, besides eastern Greer, 

southern Washita, and southwestern Caddo counties. The deposits 

of the Greer formation surround the Wichita Mountains, at a distance of from 20 to 30 miles, on all sides except on the south. (See 

PI. I.) It is between these Greer outcrops and the mountains that the 

rocks referred to occur. They consist chiefly of red clay shales, with 

a few ledges of sandstone and dolomite, and in that regard correspond 

to the Woodward. Like the Woodward, also, these beds appear to 

underlie the Greer. Until the correlation of the rocks with the 

Texas beds south of Eed Eiver has been worked out, however, the 

exact relation of the red beds of this area must remain a matter of 

doubt.

Laverne area. The second area in Oklahoma in which the relations of the red beds are still obscure is a narrow strip along the 

south side of Beaver Creek in Woodward and Beaver counties. The 

beds are composed chiefly of shale, with an occasional ledge of sandstone or gypsum. These beds are in strike with the outcrops of the 

eastern area of the Greer formation farther south in the Territory, 

the intervening country being covered with Tertiary deposits. (See 

PL I.) In lithologic character the rocks are also very similar to the 

Greer formation. Until the stratigraphy of the region is thoroughly 

worked out, however, the question of their correlation must remain 

open.*

Conglomerate. At the bases of all of the Wichita Mountains, 

whether composed of igneous rock or limestone, are considerable 

deposits of conglomerate, evidently derived from the rocks of which 

the mountains are composed that is, at the base of the limestone 

hills the conglomerate is made up of limestone bowlders, at the foot of 

porphyry knobs the conglomerate is made up of porphyry, while

n There are also exposures of red beds below Dakota and Tertiary rocks on the 

upper Cimarron River, in the northwestern corner of Beaver County, and extending up 

that stream into New Mexico. These beds may or may not be the same in age as those 

along the south side of Beaver Creek in the eastern part of the county. It is in these 

red beds near Kenton that the copper mines, which at various times have been worked 

with more or less success, are located.
74 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

granite or gabbro peaks produce granite or gabbro conglomerate. 

Near the base of the mountains this conglomerate is composed of 

rather large stones, sometimes as large as a peck measure. On leaving 

the mountains the stones become smaller and more rare, and at the 

same time the shales in which they are embedded become more reddish 

in color until at a distance of a few miles from the mountains the conglomerate has changed into typical red beds. In some places red 

shales approach the very base of the peaks and may occasionally 

be seen lying unconformably on granite, porphyry, or limestone 

rocks. Eegarding the age of this conglomerate Mr. Joseph A. Tali' 

wrote me under date of January 23, 1904, as follows:

It is my interpretation that the conglomerates at the base of the Wichita 

Mountains are composed of near-shore deposits of the red beds and therefore are 

of the same age, supposedly Permian. Of course, you understand that there are 

considerable surfacial deposits of gravel and sand, especially in the south 

side of the mountains, along the valleys of West Cache Creek, wLich would be 

classed as Recent.

GYPSUM IN THE BED BEDS.

In 1902 the Oklahoma Geological Survey made an estimate of the 

amount of available gypsum in the Territory. The following method 

was employed: A ledge of gypsum a foot thick and a mile square was 

used as a basis, the specific gravity of the gypsum was estimated at 

2.32, and the weight of a cubic foot of water at 62.5 pounds. From 

this it was estimated that a ledge of gypsum of the thickness given 

above would weigh 2,021,184 tons.

In estimating the amount care has been taken to include only available material. Throughout a large portion of the region the deposits 

are often covered to considerable depths by overlying shales and clays, 

which make up the greater part of the hill. The ledges, however, 

outcrop again on the other side of the hill, perhaps a mile distant. 

In other regions the ledges outcrop along an escarpment .and disappear entirely beneath the higher hill to the west. In still other localities the ledges do not appear on the surface, but their presence is 

attested by numerous sink holes and by ledges encountered in shallow 

wells, while, on the other hand, in many places the ledges are exposed 

over considerable areas, and not infrequently a ledge 20 to 50 feet 

thick will be uncovered for half a mile or more, so that the entire 

thickness might be removed without being compelled to strip any 

material from above the ledge.

West of this region of gypsum outcrops this rock occurs beneath 

the surface, being encountered in deep wells at various depths, increasing to the west. In a well at Childress, Tex.,. about 20 miles from the 

southwest corner of Oklahoma, gypsum beds were found at a depth of 

more than 1,000 feet, and there seems to be no doubt that the ledges 

which outcrop in the various localities in Oklahoma extend westward
PERMIAN SERIES. 75

for considerable distances, passing deeper and deeper beneath th^ 

surface. It is entirely useless even to conjecture upon the extent of 

these deposits, for nothing but an extended system of deep borings 

will ever solve the problem. These deep-seated ledges have not been 

taken into account in making up the results. No deposits have been 

considered in these calculations that are more than 100 fpet beneath 

the surface, and in general the ledges discussed are less t in 50 feet 

deep, with the greater part exposed upon the surface.

In arriving at results the plan has been to estimate the wmmber of 

square miles occupied by gypsum and the approximate combined 

thickness of the ledges. In both calculations care was constantly 

taken to make conservative estimates. The number of square miles 

was multiplied by the thickness in feet and this by 2,000,000. This 

product is considered the number of tons of gypsum in a given area.

Classified by counties the approximate amount of gypsum in Oklahoma is as follows:

	Tons.

Canadian County_____________________________ 50,000, 000

Kingfisher County _____________L ______________________ 50,000, 000

Blaine County _______________________________ 2, 500, 000, 000

Woods County ______ _ _______________________ 14, 000, 000, 000

Woodward County ____________________________ 24,000,000,000

Cornancbe County_____________________________ 200, 000, 000

Caddo County _______________________________ 3, 000, 000, 000

Washita County______ _ _________________.______ 20, 000, 000,000

Custer County _______________________________ 6, 000, 000,000

Dewey County_______________________________ 1, 000, 000,000

Day County _________________________________ 500,000, 000

Roger Mills County ____________________________ 1,000,000,000

Greer County_________________________________ 53,000, 000, 000

Total_______________________________ _ _ 125, 300, 000, 000

At the present there are eight mills in Oklahoma where gypsum 

is manufactured into plaster.

PALEONTOLOGY OF THE BED BEDS.

The scarcity of fossils in the Kansas-Oklahoma red beds has been a 

matter of comment ever since these rocks have been studied. In Kansas, particularly, Hay, Cragin, Prosser, Beede, Williston, and others 

have at various times searched carefully over the counties in which 

these rocks are exposed, but without avail. So far as known not a 

single fossil has ever been found in the Kansas red beds.

In Oklahoma, fortunately, the results have been more satisfactory. 

Not that fossils are abundant, for they are in fact very rare, yet 

enough forms have been found at various horizons to assist the geologist in the classification of the rocks. Four years ago the geologic 

age of the red beds was not certainly known, for at that time fossils
76 GEOLOGY AND WATER RESOURCES OP OKLAHOMA.

had been found in but one locality, and these for the purpose of correlation were far from satisfactory. Of the five localities west of 

the provisional base of the Permian from which fossils have been obtained in Oklahoma two only have yielded invertebrates, in two 

other localities vertebrates alone have been found, and from the fifth 

locality vertebrates, invertebrates, and plants have been secured. A 

brief description of these localities and the fossils obtained from each 

will be given.

On the farm of W. T. McCann, 5 miles southeast of Nardin, Kay 

County, a number of fossils were found in a ledge of sandstone which 

lies just at the base of the red beds. A vertebrate, identified as 

Eryops megacephalus by Dr. S. W. Williston, a small crustacean, 

Estheria minuta, and some fossil leaves comprise the collection.

Dr. E. G. Gase has identified the following forms obtained near 

Orlando, Logan County: a

PISCES.

Diacranoclus (Pleuraeanthus) arnpressus (?) Cope. 

Sagenodus (?) sp.

BATBACHIA.

Diplocaulus magnicornis (?) Cope.

limbatus (?) Cope.

salamandroides Cope. 

Trimerorhachis sp. Cope.

leptorhynchus sp. nov. 

Crieotus sp. Cope.

Crieotillus brachydens g. et sp. nov. 

Eryops megaeephalus Cope. 

Crossotelos annulatus g. et sp. nov.

REPTILIA.

Noasaurus sp. Cope. 

Ernbolophorus (?) sp. Cope. 

Pariotichus ordinatus Cope.

sp. Cope. 

Pleuristion braehyeoelous g. et sp. nov.

A number of vertebrates have recently been discovered 5 miles east 

of Pond Creek, Grant County. These bones have not been identified, 

but from superficial examination they appear very similar to the 

specimens from Nardin or Orlando.

In a ledge of soft, sandy dolomite which underlies the Medicine 

Lodge gypsum near Ferguson, Okla., a number of invertebrates have 

been found, among which Dr. J. W. Beede finds the following forms:

Pleurophorus subeuneatus Meek. 

Schizodus (?) like S. Wheeleri.

" Case, E. C.. On some vertebrate fossils from the Permian of Oklahoma : Second 

Biennial Kept. Oklahoma Geol. Surv., 1902, pp. 62, 68.
CRETACEOUS ROCKS. 77

Near Whitehorse Spring, 16 miles west of Alva, a considerable 

number of invertebrates were obtained. Doctor Beede identified the 

following genera:" Naticopsis, Pleurotomaria, Pleurophorus, Lima, 

Sedgwickia, Avicidopecten, Bakewelia, Gonocardium, and Dielasma. 

The last four genera are represented by new species.

AGE OF THE RED BEDS.

Eegarding the age of the red beds, Doctor Williston identifies 

Eryops inegacephalus, from Narclin, as a Permian amphibian, 

described by Cope, from Texas. Of the Orlando fossils he says: fi 

" Altogether these fossils unmistakably point to the Permian." Doctor Case points out the close resemblance of these fossils to similar 

forms from the Permian of northern Texas, Ireland, and Bohemia.0

Doctor Beede, in the paper referred to, in speaking of the Whitehorse invertebrates, says:

On the whole, these fossils show an advance over the fossils of the Permian 

below. Some of the species still persist, as we should expect from the fact that 

there is no unconformity between these various formations. On the other 

hand, there is a new species of Dielasma belonging to a group new to the 

American Permian. * * * Taking all this into consideration, there can be 

little doubt that the age of these beds is Permian.

Of these localities Orlando, Nardin, and Pond Creek are in the 

Enid formation; Gypsum Hills locality in the Blaine, and the 

Whitehorse locality in the Whitehorse sandstone, the middle member 

of the Woodward formation. So far as known no fossils have 

been found in the Greer and Quartermaster formations of Oklahoma, 

but there is no reason for supposing that these beds differ greatly in 

age from those immediately subjacent/

CRETACEOUS ROCKS.

Wherever the red beds are covered by other rocks there is always 

a distinct line of unconformity, showing that erosion has taken place 

before the later rocks were deposited. As far as known there is no 

evidence of Triassic or Jurassic rocks in Oklahoma and the formations next higher than the red beds in the geological scale are Cretaceous rocks, which are exposed in many parts of western Oklahoma, 

but almost invariably in local and scattered areas. The Cretaceous 

rocks belong to either the Comanche or the Dakota series.

0 Beede, J. W-. Advance Bulletin of the Second Annual Report of the Oklahoma Geological Survey, April, 1902.

" Letter of November 24, 1900.

c Op. cit., p. 62.

d Since the above was written fossils found in the Quartermaster sandstone In Collingworth County, Tex., have been identified by Doctor Beede, who finds that they are 

very similar to tbose from Whitehorse and of Permian age.
78 GEOLOGY AND WATER RESOURCES OF OKLAHOMA. 

COMANCHE SERIES (LOWER CRETACEOUS).

In general the Comanche or Lower Cretaceous rocks in Oklahoma 

consist of limestone and shales. In many of the western counties 

these deposits are found on hillsides and are known locally as " shell 

rock," because they are composed largely of fossil shells belonging 

chiefly to some member of the oyster family. '

Outcrops of the Comanche series are known to occur in the following counties: Woodward, Dewey, Custer, Day, Washita, Roger Mills, 

and Beaver. In every instance these rocks lie on the eroded surface 

of the old red beds floor, and in many instances apparently upon the 

flank of a former pre-Cretaceous red beds hill.

The most eastern point to which the Comanche deposits formerly 

reached can not be ascertained, because these deposits have been 

largely eroded since they were laid down. It seems probable, however, that the same deposits are but the remnant of a much larger 

area of the Comanche beds.

The Oklahoma Cretaceous beds form a connecting link between 

larger aVeas of Comanche series in Texas and Kansas. In the former 

State the Lower Cretaceous beds occur in large areas. In Kansas 

there are extensive outcrops of Comanche deposits near Belvidere, 

Kiowa County, and in Clarke, Comanche, and other counties, the 

thickness in places reaching 200 feet or more. Near Salina, in the 

central part of the State, the Mentor beds are also of Lower Cretaceous age. It is not the intention of the writer to discuss the age of 

these beds further than to say that it seems probable that they belong 

to the Washita or upper member, of the Lower Cretaceous.. This 

statement is substantiated by the fact that in the extreme northwestern part of Beaver County a series of clays containing typical 

Cretaceous fossils, Gryphcea, Ex,ogyra^ Ammonites, etc., are found 

lying conformably below the Dakota sandstone.

UPPER CRETACEOUS. 

DAKOTA SANDSTONE.

As far as known the outcrops of the Dakota in Oklahoma occur 

only in the extreme western part of the Territory, along canyons cut 

by the Cimarron and the headwaters of Beaver Creek. Typical 

exposures occur near Ken ton, Okla., within a few miles of the New 

Mexico line, and for 60 miles farther up the Cimarron, as far as the 

vicinity of Folsom, N. Mex. The section shown in fig. 28 was made 

on the Black Mesa, 2 miles north of Cimarron River, at Kenton, Okla. 

The Dakota in that region consists of alternating ledges of shale and 

sandstones, a form of structure which is characteristic of the Dakota
TERTIARY ROCKS. 79

in central Kansas and Nebraska, where it is typically exposed. 

Typical Dakota hills in Oklahoma are shown in Pis. IV, A, B; X, B; 

and XVII, J., B. A few imperfectly preserved dicotyledons belonging to the genera Populus, $«7Ar, Ficus, and Platanus were found in 

the sandstone rocks near Mineral, Okla. These genera are common 

forms in central Kansas, where dicotyledon leaves are abundant. The 

writer does not desire to express an opinion as to whether or not the 

Morrison may be found in the region of Kenton.

TERTIARY ROCKS.a

Lying unconformably upon the surface of the red beds and Cretaceous over a large part of western Oklahoma is an extensive deposit 

of Tertiary rocks, the exact age of which has never been determined 

with accuracy. Paleontological evidence is rare, but, following the 

usual classification of beds of apparently the same age in western 

Kansas and Nebraska, there seems no valid reason for not considering 

them Miocene or Pliocene. In Nebraska Darton distinguishes the 

Arikaree and Ogallala formations, the former being Miocene and 

the latter doubtfully Pliocene in age.6 In Kansas the geologists 

have not differentiated the strata, and in the light of our present 

knowledge it seems impossible to do so in Oklahoma, and for this 

reason this formation will be referred to as Miocene or simply as 

Tertiary.

With the exceptions of the alluvium and sand hills the Tertiary 

is the uppermost formation in Oklahoma. The red beds underlie it, 

except that between the red beds and the Tertiary occur sometimes 

Comanche Cretaceous members, but in nearly every instance the latter 

are but inconspicuous beds sandwiched in between the other formations.

In general the later Tertiary occupies the uplands of the western 

half of Oklahoma, almost always occurring on the high divides be0 For discussions of Tertiary deposits for various parts of the Great Plains the 

reader is referred to the following publications :

Hay, Robert, Water resources of a portion of the Great Plains: Sixteenth Ann. Kept. 

U. S. Geol. Survey, pt. 2, 1895, pp. 535 et seq.

Gilbert, G. K., The underground waters of the Arkansas Valley in eastern Colorado: 

Seventeenth Ann. Kept. U. S. Geol. Survey, pt. 2, 1896, pp. 557 et seq.

Haworth, B., Physical properties of the Tertiary : Univ. Geol. Survey Kansas, vol. 2, 

1897, pp. 247-284. Underground waters of southwestern Kansas : Water Sup. and Irr. 

Paper No. 6, 1897.

Johnson, Willard D., The high plains and their utilization: Twenty-first Ann. Kept. 

U. S. Geol. Survey, pt. 4, 1901, pp. 601-741. Continued in Twenty-second Ann. Rept. U. S. 

Geol. Survey, pt. 4, 1902, pp. 631-669.

Darton, Nelson Horatio, A preliminary report of the geology and water resources of 

Nebraska west of the one hundred and third meridian : Nineteenth Ann. Rept. U. S. 

Geol. Survey, pt. 4, 1899, pp. 719-785. Preliminary report on the geology and underground water resources of the central Great Plains: Prof. Paper U. S. Geol. Survey 

No. 32, 1905.

B Op. cit., pp. 732 et seq.
80 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

tween the streams. It comprises mostly all of Beaver County, and 

in Day and Woodward counties it occupies the extensive level prairies 

between Cimarron and South Canadian rivers. The high divide 

between the North Fork of Red Eiver and the Washita in western 

Roger Mills County is Tertiary also. In the central part of the Territory Tertiary deposits occupy the greater part of the uplands, and in 

places are known to extend nearly as far as the eastern tier of counties. 

Pis. V and XIII exhibit characteristic Tertiary topography.

Physical properties.® The Tertiary consists for the most Dart of 

clay, sand, and gokvel. These materials are in no regular stratigraphic succession, as shown in fig. 27. In places the entire thickness of the formation is clay; again sand and gravel predominate, 

and often deposits of different character will be interbedded.

The clay is usually white or pinkish, and sometimes forms steep 

banks or cliffs along the bluffs or around the heads of canyons. To 

the harder ledges the name " mortar beds'" has been applied by the

FIG. 27. Tertiary structure, showing formation of mortar beds.

Kansas geologists. Outcrops of this formation are shown in Pis. 

XII, XIII, and XIV, B.

The sand is of various degrees of fineness, and is composed for the 

most part of quartz, although other minerals are present. The grains, 

when examined under the microscope, are usually rounded, indicating 

the action of water.

" Tertiary pebbles " is the term usually applied by geologists to the 

smooth, rounded, waterwom pebbles scattered abundantly over the 

slopes and points throughout western Oklahoma and Kansas. These 

pebbles have been washed out of the Tertiary deposits, of which they 

often constitute a moderately large proportion. They are frequently 

cemented together and form a hard conglomerate rock known as Tertiary grit, which on exposure forms conspicuous ledges. (See PL 

XIV, A.) A good example may be seen near the head of Bents 

Canyon, on the trail from Woodward to the Big Salt Plain.

The pebbles are of all sizes, from coarse sand to stones several 

inches in diameter. Quartz is the principal mineral, granite, feldspar, and other minerals also being present.

0 See article by E. Haworth, Second Ann. Kept. Kansas Univ. Geol. Survey, pp.. 247-284.
U. S. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. 148 PL. XII

CROSS-BEDDING IN MORTAR BEDS.
U. S. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. US PL. XIII

MORTAR-BED TOPOGRAPHY.
U. S. GEOLOGICAL SURVEY

. TERTIARY PEBBLES IN PLACE.

£. MORTAR-BED STRUCTURE.
TERTIARY ROCKS. 81

In the grits and conglomerates the cementing material usually is 

calcium carbonate. A drop of acid placed upon almost any of the 

material taken from a depth of a few feet below the surface will cause 

it to effervesce rapidly. In addition to the materials named above 

there are also in the Tertiary rocks small amounts of other substances, 

of which the most important are silt, black sand, and volcanic ash, 

but they need not be discussed in this connection.

Origin. The Tertiary is not only the latest important deposit in 

point of time, but it is also the only fresh water formation in Oklahoma (except, perhaps, some Pleistocene). The Pennsylvania!!, Permian, and Cretaceous are sea deposits and contain marine fossils, 

but the fossils of the Tertiary are chiefly bones of land animals, mastodons, rhinoceroses, camels, etc., and fresh-water shells. There has 

been considerable difference of opinion among geologists regarding 

the mode of deposition of the Tertiary, but there has never been any 

doubt as to the fact that the Rocky Mountains alone could have supplied the vast amount of material that has been spread out over the 

western part of the plains.

Extent and thickness. It is probable that the Tertiary deposits at 

one time covered the entire western part of Oklahoma. The valleys 

of the present streams have been carved in these deposits, and in many 

parts of the Territory all traces of the Tertiary are gone, except 

scattered quartz pebbles.

The thickness of the formation varies with the locality, being 

greatest on the high divides. Throughout a large part of western 

Oklahoma its thickness averages 100 feet or more, while in a few 

ocalities distant from the streams it may reach as much as 300 feet. 

()n the other hand, in a great many places there is but a thin blanket 

c f the deposit over the red beds.

LAVA OF BLACK MESA.

Black Mesa extends from Colorado and New Mexico into the extreme northwest corner of Oklahoma (see fig. 28). The height of 

the table-land above the valley of Cimarron River is approximately 

500 feet, the upper 125 of which is conposed of a black, firm, basaltic 

lava, which lies unconformably upon beds of typical Tertiary, both 

the pebbles and marl being exposed along the slope of the mesa. 

The Tertiary in turn lies unconformably on the Dakota sandstone. 

The area in Oklahoma covered by this lava is 6 square miles The 

age of the lava flow is not ascertained beyond the fact that it was 

later than the Tertiary deposits, but doubtless the flow occurred when 

the many volcanic peaks in northeastern New Mexico were formed. 

IBB 1-48 05 M 6
82 GEOLOGY AND WATER RESOURCES OP OKLAHOMA. 

QUATERNARY SYSTEM.

SAND HILLS.

In Oklahoma there are two general regions in which sand hills

'MalpaiaTbasaltic lavaioo'- =

Tertiary pebbles and 20') S-grg-^ 

mortar beds

Heavy, massive sandstone, cross bedded

Clay shale, yellowish , n' 

black

Massive cross bedded CQ' 

sandstone, small rounded < 

concretions

Shale, yellow and black.,,, ' ~~ 

talus slope / luu 1 ^^

Sandstoue, gray and 

 eddish

Red clay

FIG. 28. Section of Black Mesa, 2 miles north of Kenton, Okla.

occur the first being located in the eastern tier of counties and the 

second in the central and western part of the Territory. The sand
QUATERNARY SYSTEM. 83

hills of the two regions differ somewhat in origin, but all are due to 

the wind.

In the eastern region the sand hills are extensively developed in 

parts of Pottawatomie, Lincoln, and Payne counties, as well as in 

the eastern part of the counties immediately adjacent on the west. 

The greater part of this region is underlain by Pennsylvania!! rocks 

of the Chandler district, which consists largely of ledges of soft sand 

rock interbedded between arenaceous shales. It is to this sand rock 

that we must look for the origin of the sand hills. The agents of 

weathering rain, frost, temperature, wind, etc. break down the 

sand rock, leaving loose unconsolidated sand grains. The modifying force is the wind. Inasmuch, however, as this is mainly a timbered country, wind action is made much less violent than in localities 

farther west, and so the sand hills are usually not so pronounced as in 

other parts of the Territory.

The sand hills of the western region are mainly the resultant of 

two factors gravity and wind. Practically all of the sand is derived from the Tertiary deposits, which, as has been stated, probably 

once covered nearly the entire central and western part of Oklahoma. 

Along the streams, particularly along the southern slopes, this blanket 

of Tertiary beds has been largely removed by erosion; but on the 

divides, and on the north slopes of the streams as well, it has remained 

in many places. As the Tertiary deposits consist largely of clay, 

sand, and pebbles, and the clay is washed away more rapidly than the 

coarser materials, much unconsolidated sand remains in many areas. 

Some of this sand finds its way to the various streams and eventually 

chokes their channels. During times of drought strong south winds 

blow this sand out of the channel onto the flood plain to the north. 

Some persons believe that all sand hills along the streams are composed of sand blown from the stream, but the facts observed do not 

justify so sweeping an assumption. In many parts of the Territory 

there are sand-hill regions 15 or more miles wide, extending north 

from the stream, and on top of some of these sand hills pebbles as 

large as a walnut, weighing several ounces, have been found. The 

writer is not yet ready to admit that the wind can carry a pebble of 

this size and deposit it on a sand hill.

The theory of river sand being untenable in many cases, another 

origin must be sought. To the writer it appears most probable that 

the sand which forms the greater part of these sand hills is obtained 

directly.in place from the disintegration of Tertiary rocks and that 

the wind is but the modifying factor. The sand hills are mainly 

north of the streams, and the force of gravity is also constantly at 

\vork, producing a slow but constant creeping of the sand streamward; but, on the other hand, the prevailing winds being from the
84 GEOLOGY AND WATEE EESOUECES OF OKLAHOMA.

south tend to counteract the creeping motion, and so it may be 

assumed that the material composing the hills remains practically 

stationary.

Another interesting feature is the zonal arrangement of the sand 

hills. Every stream in the Territory, except Washita River, which 

is unlike all other streams of the Plains, has a row of sand hills along 

its north bank. Salt Fork, Cimarron, North Canadian, South Canadian, and Red rivers are all bordered with sand hills on the north 

side, while the south bank of these streams is usually a canyon-cut 

slope composed of the red clays and shales of the red beds. This 

subject will be discussed on pages 121, 122.

ALLUVIUM.

The flood plain, or " bottom land," of the rivers of Oklahoma is 

made up largely of alluvium, or, as it is often-known, valley wash, 

derived largely from the uplands. For the most part this alluvium 

is composed of material derived from the disintegration of two kinds 

of rocks, red beds clays, and Tertiary sands and clays. In places 

the bottom lands have the bright vermilion hue of a red beds slope, 

or, again, the flood plain is made up almost entirely of white sand; 

but in the majority of cases the alluvium is a dark-colored chocolate 

loam and forms an extremely fertile soil. The extent of the alluvial 

deposits varies greatly along different streams. Their width is from 

2 to 4 miles along such rivers as Salt Fork, Cimarron, North Canadian, South Canadian, Washita, and Red, and perhaps less than a 

mile along the secondary streams. The depth of the material as 

shown in wells varies from 2 to 30 feet.

WATER SUPPLY.

GENERAL CONDITIONS.

The water of Oklahoma varies from the purest of spring water 

from granite rocks or sand hills to water so thoroughly impregnated 

with mineral salts as to be totally unfit for domestic use. The quantity of the water is in most localities ample for all ordinary purposes, 

there being few sections in the Territory in which a supply may not 

be obtained in wells of moderate depth.

In order to study intelligently the problem of water supply in a 

region with so many and varied kinds of water as Oklahoma it 

becomes necessary to subdivide the Territory into districts, each of 

which furnishes water of a certain more or less uniform quality. In 

Oklahoma it has been found that no better general system of classification may be adopted than the one already given under the heading
WATEE SUPPLY. 85

" Topography," for the topographic features and character of water 

both depend primarily on the rocks. The topographic divisions are 

as follows: Wichita Mountain region, Flint-Sandstone Hills region, 

Low Plains region, Gypsum Hills region, High Plains region, and 

Dakota Sandstone region. The general outline of these various 

regions is given on pages 13-18, and illustrated on fig. 1 (p. 14).

Another factor which should be mentioned before taking up the 

various regions in detail is the kinds of rocks in which water occurs. 

Leaving out of account the Wichita Mountain region and the Osage 

nation, practically all the water in Oklahoma conies from either red 

beds or Tertiary deposits. In the Tertiary areas the water is almost 

uniformly sweet, pure, and wholesome; in the red beds, on the other 

hand, it is often unfit for use. The red beds are practically everywhere present at the surface, except in the western part of the 

Territory, where they are covered by Tertiary deposits. It will be 

remembered that Tertiary rocks cover nearly all of Beaver County, as 

well as large areas in other western counties, and occur as rows of 

sand hills covering the red beds along the north side of practically all 

the large streams nearly to the eastern part of the Territory. The 

water in these Tertiary sand hills is good; it follows that well-defined 

zones or belts of good water extend far east into the general area of 

red beds.

The water in the alluvial deposits along the. streams is usually both 

abundant and of good quality. As the alluvium is composed largely 

of sand, clay, and loam derived from red beds and Tertiary rocks, and 

the amount of sand usually is sufficient to make it porous, the entire 

flood plain of nearly all the streams is saturated with water. Even in 

those areas of the red beds where good water can not be obtained from 

the red clays of the uplands, it is not unusual to find an abundant 

supply of pure water along the river bottoms, and not infrequently 

a small creek or even a prairie sand draw will contain a deposit of 

alluvium from which a considerable supply of water may be obtained.

I Medford, Enid, and Weatherford may be cited as examples of cities

' that obtain water under such conditions.

WICHITA MOUNTAIN REGION.

In the Wichita Mountains numerous springs issue from granite 

and porphyry rocks and furnish an abundant supply of water of 

good quality. Such creeks as Medicine Bluff, Blue Beaver, West 

Cache, Oak, Otter, and Rainy Mountain are fed at least in part by 

springs from igneous rocks.

In the limestone hills north of the main range springs issue from 

the Arbuckle limestone, and Blue, Chaiiler, East Cache, Eainy Mountain, and other creeks are fed in part by them. Few wells have been
86 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

put down as far as either igneous, or limestone rocks, but in many 

mining shafts water is encountered in such quantities as to interfere 

seriously with the progress of the work, indicating the presence of 

considerable quantities of ground water.

In the red beds country surrounding the mountains, water is 

usually found, but in many places neither the quantity nor the quality 

is satisfactory.

FLINT-SANDSTONE HILLS REGION.

This region includes the Osage and Kaw reservations north of 

Arkansas River, all the counties along the eastern boundary of the 

Territory and the eastern part of Kay, Noble, Logan, Oklahoma, and 

Cleveland counties. In other words, it comprises practically all 

the territory east of the main line of the Atchison, Topeka and Santa 

Fe Railway. It is 150 miles long, north and south, with an average 

width of 50 miles, and has an area of approximately 7,500 square 

miles.

This region corresponds closely to the outcrop of the Pennsylvanian series as represented in eastern Oklahoma. In the western 

part of the Osage Nation is the southern end of the Flint Hills, the 

rocks of which consist chiefly of limestones and shales, while farther 

east in the same reservations sandstones and shales predominate. 

South of Arkansas River limestones are rare, sandstones and shales 

predominating. In this part of the region, particularly in parts of 

Lincoln and Pottawatomie counties, there are considerable areas of 

sand hills, the material of which is disintegrated sand derived from 

the rocks in place.

In general, this district is the best-watered part of the Territory. 

There are several reasons for this condition: First, the rainfall is 

from 35 to 40 inches, being greater than in the regions farther west; 

second, the rocks consist largely of porous sandstone which is an 

excellent water carrier; third, there is a smaller amount of mineral 

salts in the rocks of this region than in those farther west. Springs 

are not uncommon. In the Osage Nation, as well as in the counties 

south of Arkansas River, a number of springs issue from above the 

shale beds, beneath either limestone or sandstone ledges. Wells have 

been put down on practically every quarter section and the greater 

part of them furnish good water at moderate depths.

LOW PLAINS REGION.

This region has been outlined on page 16. It extends practically 

from the main line of the Atchison, Topeka and Santa Fe 

Railway west to the Gypsum Hills. Geologically it includes the 

Enicl division of the red beds, the rocks consisting chiefly of red
WATER SUPPLY.

clays and shales, with a few thin interbedded beds of red sandstone. 

North of each of the rivers which cross this region Salt Fork, 

Cimarron, and North and South Canadian is a strip of sandhills 

country from 2 to 15 or more miles wide.

Water from the red beds usually contains mineral salts, which in 

many places render it unsatisfactory for use. In Oklahoma water 

that is unpleasant to the taste is often called " gyp water." As the 

popular phrase has it, " Gyp water tastes sleek and greasy and leaves 

an aftertaste in the mouth." Much of the water, however, does not 

contain any great percentage of calcium sulphate. The most common 

salts are sodium chloride, sodium sulphate, calcium carbonate, magnesium sulphate, sodium carbonate, magnesium carbonate, calcium 

chloride, and sodium borate, in the order named. Sometimes nearly 

all these salts are found in the water of a single well, while in other 

instances but one or two may appear.

In this part of Oklahoma springs are rather rare in the red beds, 

and the greater part of the water for domestic use is obtained from 

wells. Often a farmer is obliged to sink half a dozen wells in 

order to find one in which the water is both sufficient in quantity and 

suitable in quality for general use. In certain parts of the region, 

notably part of Woods County, the water is often so salty as to be 

unfit for drinking.

Among the sandhills north of the rivers the conditions are different. Here water is both abundant and pure. Springs which issue 

along bluffs and wells obtain a good supply of excellent water at moderate depths.

GYPSUM HILLS REGION.

The Gypsum Hills region includes parts of Woods, Blaine, Caddo, 

and Comanche counties, and all counties west of these except Beaver 

and parts of Woodward and Roger Mills. The rocks consist of the 

Woodward formation, the Greer gypsum, and the Quartermaster 

formation. It will be remembered that the Whitehorse, the middle 

member of the Woodward formation, and the Quartermaster are both 

composed of sandstone. With these, exceptions the remainder of the 

rocks here consist of beds of gypsum interstratified between red 

shales. It is the gypsum that gives the mineral character to the 

water. In both the Blaine and Greer gypsum hills the water of 

many springs is so strongly impregnated with calcium sulphate as 

to be undrinkable. Salt springs are not uncommon, six of the seven 

known salt plains in Oklahoma being at the base of the Gypsum 

Hills.

In wells in the Gypsum Hills water is usually reached at a moderate 

depth, ranging all the way from 10 to 150 feet. It usually resembles
88 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

the water from the springs in the same region and contains relatively 

large amounts of gypsum.

Water from the Whitehorse sandstone is usually pure and wholesome. Springs are not uncommon in this member and wells usually 

obtain a good supply at reasonable depths.

In the Quartermaster formation where the water is usually good 

the rocks consist largely of fine-grained red shaly sandstone. A 

very peculiar class of springs, best described by the term " seep 

springs," is found here, and that character is due to the nature of the 

rock. Usually these seep springs issue from the head of small canyons carved in the red sandstone, and bold springs are rarely found in 

this region. Seeps, however, are common and one not infrequently 

comes upon a basin which has been hollowed out in the soft sandstone and is kept full by this kind of flow. Wells in the Quartermaster usually obtain a sufficient supply of water at moderate depths. 

Among the sand hills areas north of the various streams springs and 

wells are common.

HIGH PLAINS REGION.

The Tertiary plains of Beaver, Woodward, Day, and Rogers Mills 

counties only are included here, although in fact the sand hills north 

of the various streams in the Territory belong to this division both by 

reason of the quality of the water and the character of the rock. In 

the High Plains good water is obtained almost uniformly. The Tertiary rock consists chiefly of sand, clay, and gravel, and as the sand 

and gravel beds almost invariably contain water, wells sunk to these 

beds usually secure an abundant supply. In the counties mentioned 

above the wells are usually deep, often as much as 300 feet or more, 

and windmills are used almost exclusively to bring water to the surface, but the supply is certain. In PL XV are shown typical High 

Plains windmills.

In many places where a stream has cut through the Tertiary into 

the subjacent red beds exposing an unconformity, a spring issues, the 

water of which is sweet and pure like the well water on the high 

plains. Some of the best water in Oklahoma comes from the Tertiary springs. Many a ranch and farmhouse and even some towns, 

as for instance Cleo and Grand, have been located with reference to 

some Tertiary spring.

DAKOTA SANDSTONE REGION.

In Kansas and Nebraska the Dakota sandstone is famous for its 

springs, but in the Dakota sandstone of western Beaver County 

springs are scarce, and so far as noticed by the writer the conditions 

in other parts of Oklahoma and New Mexico where these rocks are
U. S. GEOLOGICAL SURVEV WATER-SUPPLY PAPER NO. 148 PL. XV

HIGH PLAINS WINDMILLS.
WATER SUPPLY. 89

exposed are similar to those in Beaver County. However, springs in 

the Dakota beds are not unknown and the water that is found is of 

good quality. Few wells have been put down in that region and 

consequently data for wells in the Dakota in Oklahoma are not 

available.

STREAMS.

None of the important rivers of Oklahoma rise in the Territory. 

Two out of the seven the Arkansas and South Canadian rise in 

the Eocky Mountains, and the others have their headwaters on the 

High Plains of Texas, New Mexico, Colorado, or Kansas, and flow 

across Oklahoma in a general southeast course. The Salt Fork and 

Ciniarron empty into the Arkansas in northeastern Oklahoma; the 

North and South Canadian unite before joining the Arkansas in the 

eastern part of Indian Territory, and the Washita joins the Red 

River at the southern line of the Indian Territory. The map (PI. 

XVI) shows the drainage areas of the rivers which flow across 

Oklahoma.

ARKANSAS RIVER.

Arkansas River flows southeast across the northeast corner of 

Oklahoma, separating the Kaw and Osage nations from the remainder 

of the Territory. For almost its entire course in Oklahoma it winds 

through a rather deep and narrow valley among the Flint Hills, 

where it is characterized by sweeping curves and bends. In many 

places it flows at the foot of steep limestone bluffs, while the whole 

region is cut into a series of hills and hollows by a number of small 

creeks tributary to it. It is estimated that during the past few years 

the supply of water in the Arkansas has decreased, owing to the 

fact that so much is taken out for irrigation purposes near the head 

of the river. In central Kansas there seems little doubt that the 

visible supply is less than in former years. Much of the water in 

this stream in Oklahoma comes from tributaries, such as Little Arkansas, Ninnescah, Walnut, and Grouse, that empty below Hutchinson, 

Kans. In Kansas, where the river flows in a broad valley in the 

prairie, it has a considerable underflow, but in crossing the Flint Hills 

this underflow is forced to the surface, arid for that reason the channel 

rarely runs dry. Analyses Nos. Ill, 112, 113, and 114 are from' 

waters of the Arkansas or the smaller tributaries.

SALT FORK.

Salt Fork of the Arkansas rises in southern Comanche County, 

Kans., west of the line of Gypsum Hills, enters Oklahoma in northwestern Woods County, and flows through southern Grant and Kay
90 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

counties before joining Arkansas Eiver. Its total length is approximately 150 miles, 115 miles of this distance being in Oklahoma.

Salt Fork receives a number of tributaries, most of which are fed 

by springs from the Tertiary. The greater part of these enter from 

the north, and two of them Medicine and Chikaskia rivers carry 

as much water as does the Salt Fork above the mouth of the Medicine. Besides the two large tributaries just mentioned the following 

creeks enter from the north: Mule, Sand, Crooked, Roundpond, Cottonwood, and Bois d'Arc, and from the south Coldwater, Clay, and 

Sand creeks. These creeks are for the most part typical prairie 

streams, with shallow valleys, low banks, and sand-filled channels, 

and for a part of the year at least they are dry.

In eastern Woods County the Salt Fork flows across the northern 

end of the Great Salt Plain, which has an area of approximately 60 

square miles. It is 10 miles long and 6 miles wide, irregularly oval 

in shape, level as a floor, and, except after a rain, as white as a snow 

field. The water of the river mingles with the saline water of the 

plain and takes on a distinctly salty taste; so much so that at certain 

times of the year stock will not drink it.

Analysis No. 86 is of water taken above the Woods County Salt 

Plain; Nos. 87 and &8 from below the plain, and Nos. 89 and 90 

from small streams tributary to the Salt Fork.

CIMARRON RIVER.

The Cimarron rises among the volcanic peaks of northeastern New 

Mexico and carries a small volume of water into Oklahoma. In 

New Mexico and'for 30 miles into Oklahoma the river flows in a 

canyon cut through Dakota sandstone rocks into the subjacent red 

beds. From the sandstone issue springs which supply a number of 

intermittent creeks, Travessier, Carriso, Carrisoso, Tequesquite, and 

others which flow for at least part of the ye'ar. The channel of the 

Cimarron in this part of its course is not more than 20 feet wide and 

is confined often by mud banks. In flowing out of the canyon onto 

the Tertiary plain, 30 miles east of the New Mexico line, the character 

of the stream begins to change; the channel widens and fills with 

sand, the banks become low, and from this point to-its mouth at 

'ordinary stages of the river the water wanders about over sandy beds.

At irregular intervals along this river water sinks in the sand 

and passes beneath the surface for a number of miles. For instance, 

from the old post-office of Metcalf, Okla., to Point of Ro'cks, Kans., 

a distance of 25 miles, the channel of the Cimarron is often dry, but 

at Point of Rocks the water conies to the surface at Wagon Bed 

Springs, a famous camp on the old Santa Fe trail, and the channel 

is usually full for a number of miles. It gradually sinks again,
U. 3. GlOLOGiCAL WATER-SUPPLY PAPER NO. 1+8 PL. XVI

L._._.il ._.!_._ 5a i >R . iicale ~ T l^ T lo ^[///////M

Eed Eiver

MAP SHOWING DRAINAGE AREAS OF STREAMS CROSSING OKLAHOMA.
WATER SUPPLY. 91

however, before reaching Oklahoma the second time, so that above 

the mouth of Crooked Creek the channel is often dry. This creek, 

however, is perennial, and below its mouth the river carries water 

for many miles.

Until it flows across the Salt Plains in northern Woodward 

County the water of the Cimarron is pure and sweet, being derived 

largely from Tertiary springs, but from this point it contains so 

much salt that stock will scarcely drink it. Salt springs flowing 

from the base of the Gypsum Hills give rise to the Little Salt Plains 

near the Kansas line and the Great Salt Plains, shown in PI. XX, 

10 miles farther downstream.

The drainage basin of the Cimarron is more regular in outline than 

that of any other Oklahoma stream, averaging 40 miles or more in 

width across the Territory, and the stream flows approximately equidistant from either divide. The valley is from 100 to 300 feet 

lower than the valley of North Canadian River, which parallels the 

Cimarron on the south. Excluding a number of short streams in the 

Gypsum Hills, the principal creeks that enter the Cimarron from the 

north are Eaglechief, Indian, Turkey, and Skeleton, and those from 

the south are Salt, Kingfisher, and Cottonwood. These creeks, which 

will average 30 or more miles in length, enter the river at an acute 

angle, have a well-developed radiate drainage, and are in every way 

normal tributary streams, a fact rather unusual among the smaller 

creeks of Oklahoma.

In central Oklahoma the channel of the Cimarron is from a quarter 

to a half mile wide, with low sandy banks and a relatively small 

amount of water. For a part of each year the river runs dry, but, 

like all other streams of the plains, it is subject to sudden and rapid 

rises, at which times the river will often remain bank-full for several 

days. The sand partakes of the nature of quicksand, and after a rise 

it is unsafe to attempt to cross the river. Farther east the river 

enters the sandstone-bluff country and the channel is often narrowed, 

but the characteristic sandy condition prevails to its mouth. Water 

analyses Nos. 91 and 92 are from the Cimarron above the Salt Plains, 

Nos. 93, 94, 95, 96, 97, 98, and 99 from below the Salt Plains, and Nos. 

100, 101, 102, 103, 104, 105, 106, 107, 108, 109, and 110 are from tributaries of the Cimarron.

NORTH CANADIAN RIVER.

Beaver Creek and Wolf Creek unite at old Fort Supply, in central 

Woodward County, to form the North Canadian. Wolf Creek rises 

in the northern part of the Panhandle of Texas and flows northeast 

into Oklahoma, while Beaver Creek heads in northeastern New Mexico 

and flows east the entire length of Beaver County before reaching
92 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

Woodward. Both these creeks are fed largely by Tertiary springs, 

and for that reason are practically perennial streams, and both are 

subject to rapid rises occasioned by local storms. The, North Canadian has no large tributaries. With the exception &f Indian and 

Persimmon creeks, in Woodward County, neither of which exceed 20 

miles in length, there are few tributaries more than 10 miles long.

Throughout its entire course, a distance of approximately 200 miles, 

the width of the drainage basin of the river does not average more 

than 15 miles, and in places the distance from the bed of the North 

Canadian across the divide to the waters of the Cimarron is not more 

than a mile. This is the case at Oklahoma City and a few miles east 

of Elreno.

The North Canadian has perhaps the best water of any of the 

larger streams in Oklahoma, owing chiefly to two causes first, the 

river is fed largely by Tertiary springs; and, second, it does not flow 

through regions of salt springs. The waters of Salt Fork, Cimarron, 

and Red rivers are salty, and the South Canadian and Washita waters 

are derived largely from the red beds, and consequently contain both 

gypsum and salt. The water of the North Canadian, on the other 

hand, is usually soft and of a good quality. There is more timber 

along the banks of this stream, the flood plain is more uniform, and 

in general it appears more like an eastern river than any of the others 

just mentioned, except the Washita. Water analyses Nos. 115, 116, 

117, 118, 119, 120, and 121 are of water from the North Canadian, 

and Nos. 122, 123,124,125, 126, 127, 128, and 129 from its tributaries.

SOUTH CANADIAN RIVER.

The headwaters of the, South Canadian flow from the snow-covered 

peaks of the high ranges of the Rocky Mountains in northern New 

Mexico. A characteristic view along its upper course is shown in 

PL XVIII, B. In that territory the South Canadian drains approximately 30,000 square miles, having a drainage area of 150 by 

200 miles in the northeastern part of the Territory; but in the Panhandle of Texas this basin narrows, funnel shaped, until by the time 

the river flows into Oklahoma, in Day County, the distance between 

the divides north and south of the river does not exceed 25 miles. 

From the Texas line to the mouth of the river, a distance of about 

300 miles, the width of the drainage basin does not average more than 

20 miles, while in places it is less than 10 miles. The channel of the 

river is sand choked, and throughout Oklahoma averages half a mile 

in width, the banks being low and sandy. Its channel is constantly 

shifting, and oxbow bends and cut-offs are common.

The South Canadian is the most uncertain and treacherous of all 

Oklahoma streams, and, with the exception of Arkansas River, the
U. S. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. 148 PL. XVII

A. BLUFF OF DAKOTA SANDSTONE.

B. RED BEDS DAKOTA UNCONFORMITY.
U. S. GEOLOGICAL SURVEY

A. DAM SITE AT QUARTZ MOUNTAIN.

B. SCENE ALONG THE UPPER COURSE OF SOUTH CANADIAN RIVER.
WATER SUPPLY. 93

largest. Its water supply is derived from several sources partly 

from rainfall and springs in the mountains, partly from small tributary streams fed by Tertiary springs, and partly, of course, from local 

storms. This river, perhaps more than any other on the plains, is 

subject to sudden and rapid rises. The channel may be dry from 

bank to bank, when suddenly, without warning, a wall of foaming 

water several feet high, carrying all sorts of debris, will rush downward at great speed, filling the channel bank-full. For several days 

it will be full, when the water will gradually recede and the channel 

be dry again. The possible explanation of the phenomenon may be 

found in the fact that there is a large drainage area at the head of 

the river, but that it narrows rapidly downstream. A heavy storm 

on almost any one of the head tributaries of the river would cause it 

to rise, and the water flowing into the main channel, the sand of which 

is already saturated, would cause a sudden rise all along the river. 

It must be admitted that this explanation is at best far from satisfactory, and until the data from a number of gaging stations along 

this river have been obtained and the results studied it is improbable 

that we shall be able to determine all the causes that lead to this very 

interesting phenomenon.

Water analyses Nos. 130, 131, 132, and 133 show the character of 

the water from various points of South Canadian Eiver.

WASHITA RIVER.

The Washita is an anomaly among streams of the plains. It alone 

has steep mud banks, comparatively little sand in the channel, and 

heavy timber on the bottom lands. To account for these facts it is 

necessary to consider briefly the nature of the region drained by the 

Washita. It alone of all the rivers of Oklahoma flows for practically 

its entire course through red beds rocks. In its upper part only does 

the river drain other formations, notably areas of Tertiary.

Rising in the eastern part of the Panhandle of Texas it flows across 

Roger Mills, Ouster, Washita, and Caddo counties before entering 

Indian Territory. These counties are included in the Gypsum Hills 

region, and consequently the water of the Washita contains an appreciable percentage of mineral salts. The red clays and shales along 

the river bank are easily disintegrated, making the Washita the muddiest stream of Oklahoma. It enters Indian Territory and, after 

flowing for more than 100 miles across the red beds, passes through 

a gorge which it has cut through the lower Paleozoic rocks of the 

Arbuckle Mountains.

RED RIVER.

Red River, which forms the extreme southern boundary of Oklahoma, resembles the Cimarron or South Canadian in having a broad
94 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

and sandy channel and an intermittent flow. The name of the river 

is derived from the color of the water, and the red color is derived 

from the red beds across which the river runs.

In Oklahoma there are several northern tributaries to the Red, 

the chief of which are Salt Fork, North Fork, and Cache Creek. 

Of these North Fork and Salt Fork take their rise on the high plains 

among Tertiary rocks and flow southeast across the Gypsum Hills 

before joining the Red. Elm Creek, which is tributary to the North 

Fork, drains a region of salt springs. This combination of salt, gypsum, and other mineral salts makes the water rather impure. The 

valley of the North Fork is shown in PL III, B.

Red River is subject to sudden and rapid rises, as are the Cimarron and South Canadian. The stockmen living near the river speak 

of a " 7-foot rise " and a u 10-foot rise " as a not uncommon occurrence. This river, however, rarely runs dry, as do those farther north. 

Besides the Arkansas the Red is the only Oklahoma stream that 

empties directly into the Mississippi.

STREAM MEASUREMENTS.

There are few data regarding the discharge of Oklahoma streams, 

for only within the past two years have gaging stations been established in Oklahoma. During the year 1903 stations were maintained 

on the following streams: Salt Fork, at Alva and Tonkawa; Cimarron, at Waynoka; North Canadian, at Elreno and Woodward; 

Washita, at Anadarko and Chickasha, Ind, T.; North Fork of Red 

River, at Granite; and Otter Creek, at Mountain Park. These stations, with two exceptions, were established in 1903, and as yet the 

records are in an incomplete state, but they will be found in Progress Report of Stream Measurements for the year 1903.a

SPRINGS.

Springs can best be classified with regard to the character of the 

water. Following this plan the springs of Oklahoma naturally are 

divided into three groups fresh-water springs, salt springs, and 

sulphur springs. Under the first are grouped all the springs of the 

Territory except those in which the water is either noticeably salty or 

contains an appreciable amount of sulphur. The term u fresh water," 

as used in this connection, does not necessarily imply the absence of 

mineral salts, for the water from many of the springs described is 

hard, containing often a large percentage of lime, gypsum, or other 

mineral salt. These fresh-water springs are found in all parts of 

Oklahoma and form a great proportion of the whole number. Salt

0 Water-Sup, and Irr. Paper No. 99, U. S. Geol. Survey, 1904, pp. 244 et seq.
SPRINGS. 95

springs, on the other hand, are found in but few localities and usually 

under peculiar stratigraphic conditions. Sulphur springs are even 

more rare, occurring only in the Wichita Mountain region.

FRESH-WATER SPRINGS.

In the Wichita Mountains there are two principal kinds of 

springs those from the crystalline rocks and those from the limestone. In eastern Oklahoma there are limestone springs and sandstone springs, and in the low plains there are red beds springs. 

Besides these there are gypsum springs, Tertiary springs, and river 

terrace, or alluvial springs. These will be discussed in the order 

given. PL I gives the location of such springs in Oklahoma as are at 

the present time known to exist.

WICHITA MOUNTAIN SPRINGS.

The Wichita Mountain region, as a whole, is well watered. A 

number of bold springs flow either directly from fissures in the porphyry or granite or issue along dikes, or, perhaps, at the point of 

contact between igneous and sedimentary rocks. Blue Beaver 

Springs, Talahina Springs at Cutthroat Gap, springs near Saddle 

Mountain, Mount Scott, and Mount Sheridan that feed Medicine 

Bluff Creek, and numerous springs that supply Otter, Cache, and 

other creeks that flow south through the mountains are of this character. In addition to these there are great numbers of relatively 

weak springs that issue from small fissures in granite or gabbro rocks 

and flow during wet weather.

The water from these springs from the crystalline rocks is notably 

fresh and pure, in the main the purest water of the Territory, chemical analysis revealing a very small percentage of solid residue.

LIMESTONE SPRINGS.

Under this heading will be described not only the springs issuing 

from the Arbuckle limestone hills in the Wichita Mountains, but 

also those that flow from the conglomerate that surrounds these 

hills, and the limestone springs in eastern Oklahoma, chiefly north of 

Arkansas River.

The springs flowing from the conglomerate hills "north of the 

main range of the Wichita Mountains are probably the largest of 

any in the whole region. The distribution of the conglomerate is 

very irregular; it fills the old valleys and in some places extends 

beyond, covering tracts of country several miles in area to a depth 

of sometimes as much as 00 feet. The formation is very porous and 

most of the rain which falls on it is absorbed, so that the supply of
96 GEOLOGY AND WATEE BESOTIKCES OF OKLAHOMA.

underground water during wet seasons is large, and springs often 

flow as much as a cubic foot of water a second. The areal extent of 

the formation is so limited, however, that after a few months of 

drought the flow from the springs either decreases materially or may 

even cease entirely. None of the springs are badly choked with 

sand, so their flow is not retarded in this way.

Most of the limestone springs of the region do not differ greatly 

in this respect from the conglomerate springs. They are often as 

strong as the former, and like them they usually go dry or run very 

low during dry seasons, particularly in the later summer months. 

The hills from which these springs get their supply of water consist of tilted ledges standing almost on edge, which naturally form 

a good reservoir, but these hills are so limited in size that where the 

water is free to escape it soon leaves the rock dry. Where banks of 

sand and alluvium surround the base of these hills the water is retarded in its escape, and under this condition there is a constant flow 

without much fluctuation. Next to the alluvial springs, which will 

be discussed below (p. 99), the limestone springs are more widely 

distributed throughout the region than any others.

The water from both conglomerate and limestone springs contains 

a certain amount of mineral salts, chiefly calcium carbonate, but none 

in quantities that render it objectionable. These springs are among 

the most important in the Territory.

Limestone springs in eastern Oklahoma are confined to the Osage 

Nation and Kay and Pawnee counties, where they occur along many 

of the creeks. They usually come from a ledge of limestone which 

immediately overlies a stratum of clay or shale, although sometimes 

they may be found flowing from a porous rock lying above a more 

impervious limestone, the largest springs of the region appearing 

under the latter conditions. The springs of this part of the Territory are neither large nor very numerous, the flow being limited by 

the impervious character of the rock as well as by the fact that the 

water-bearing beds are not of sufficient extent to supply a strong 

stream of water.

The springs which flow from the harder ledges of limestone generally are unimportant, being mere seeps, often too weak to be utilized 

even for watering stock. Farmers owning such seeps sometimes dig 

cisterns in the clay just under the point where the water appears, 

and by so doing manage to secure a supply of water for domestic 

purposes. Some of the ledges of limestone are more porous than 

others, and these porous or shattered ledges furnish an abundance of 

spring water where the overlying strata permit percolation. A condition of this kind in eastern Kay County yields several good springs, 

one particularly on Deer Creek, northeast of Newkirk, which issues
SPEINGS. 97

just over a ledge of compact limestone. This is the largest spring of 

this character known, and its flow averages about 0.5 second-foot.

SANDSTONE SPRINGS.

In eastern Oklahoma the whole region from Payne County southward is crossed by a number of alternating ledges of sandstone and 

clay, ana in many places where a draw or creek cuts one of these 

strata a spring is found. In the northern counties the flow is usually 

free and uninterrupted, but farther to the south there is often a 

superficial covering of sand, derived from disintegration of rocks in 

place, through which the water flows, and eventually reaches the 

underflow in the sand-choked bed of some stream without appearing 

at the surface. In the southern counties, where this condition often 

occurs, there are fewest springs, but to offset this plenty of well 

water can be obtained at a short distance beneath the surface. 

In wet Weather springs often appear for a few weeks in places 

where this blanket of sand 011 a hillside is not deep enough' to 

carry off the flow of the buried spring in addition to the extra rain 

water which is moving down the slope, but the stream supplied by 

such a spring usually sinks before it goes far. The flow from most of 

the springs of this region is very limited. This is due to probably 

two principal reasons: First, the country is so cut up by small 

streams that the area of water tables is limited; and second, the rate 

of flow through sandstone is so slow that no large quantities of water 

can be delivered at the spring under the slight hydrostatic pressure 

in such small areas. Many small hills often have a half-dozen 

springs on their slopes. The upper ledge of sandstone usually furnishes the main flow, although a hill which contains a number of 

alternating strata often has seeps coming from all the sandstone 

formations. Few, if any, of the springs of this country will flow 

over 0.5 second-foot; but as a whole the region is well watered.

RED BEDS SPRINGS.

Most of the red rocks of the Low Plains region belong to the Enid 

formation and consist of shales and clays, with occasional ledges of 

sandstone. While springs occur in all the rocks, they are by no moans, 

abundant, the unbroken topography not being suitable for their development and the rock not being sufficiently. permeable. The clay, 

however, is often a kind of joint clay and the water passes through 

its seams to a limited extent in veins. Where springs occur in the 

shale and clay of this part of the red beds they often are large. Two 

causes may be assigned for this. In the first place, the water beds, 

although with a small capacity for holding water, are of wide extent.

IBB 148 05 M 7
98 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

In the second place, the clay of the region yields readily to the action 

of running water, and when once a small vein is cut it soon becomes 

enlarged and joins with others in its vicinity, thus producing a bold 

spring.

The quality of the water of these springs is variable, some of them 

yielding soft and palatable water, while others are heavily charged 

with sulphur and gypsum. The conditions which bring about these 

different characteristics are local. Bois d'Arc Springs, in Kay County, 

are charged with gypsum, while not far from these are Willow 

Springs, the water of which is almost soft. Timberlake Springs, in 

Woods County, on the western border of the plains, flow soft water, 

while a number of springs not far east of them contain gypsum. The 

springs flowing from the sandstone of the region resemble those coming from the same kind of formations in the eastern part of the 

Territory, except that they are never choked with sand.

GYPSUM SPRINGS.

In the Gypsum Hills region, in the western part of the Territory, 

are numbers of springs in which the water is strongly impregnated 

with calcium sulphate, which are consequently known as u gypsum 

springs,"1 or more popularly as "gyp springs." The greater part of the 

springs of this kind issue from directly beneath heavy ledges of gypsum, and in many cases are due to underground streams. The Gypsum Hills country is full of sink holes and caves, most of which 

contain underground streams. Such caves and sink holes as are 

shown in PI. XI and fig. 9 are abundant.

Gypsum springs such as those just described are particularly common in Blaine, Woodward, AVashita, and Greer counties, where the 

Gypsum Hills have their most conspicuous development. Some of 

them are strong, flowing as much as 5 second-feet.

TERTIARY SPRINGS.

Springs occur in the sand hills north of the rivers from the western 

line of the Territory as far east as the eastern limit of the Low Plains, 

as well as in the High Plains region of Beaver, Woodward, and Day 

counties. In the western part of the High Plains region they flow out 

near the rivers on both sides of the stream, but farther eastward they 

appear chiefly along the divides of the rivers. Before reaching the 

Gypsum Hills, the Sand Hills formation, from which they flow, disappears along the south sides of the rivers, but continues, usually in 

the form of a heavy row of wind-blown sand hills, on the north sides. 

These hills, as well as the springs flowing from them, extend eastward 

across the Low Plains country and gradually grow smaller, finally 

disappearing in the eastern part of the Territory.
U. S. GEOLOGICAL SURVEY NO. 148 PL. XIX

TERTIARY SPRINGS AND CONTIGUOUS TOPOGRAPHY.
SPEIFGS. 99

The springs in these hills as far west as the High Plains almost 

always issue along the lines of unconformities between the Tertiary 

deposit above and the reel beds beneath, usually where a creek has 

cut through the sand into the red clay and shale below, thus exposing 

the water plane, as shown in fig. 29. In some places the water flows 

out along a bank for a distance of several hundred yards, as in the 

case of Cleo Springs in Woods County; in other cases it issues as a 

single bold stream for instance, in Bents Canyon in northern Woodward County. In many cases these springs boil up from the sand, 

and are often called boiling springs. Springs of this kind are, in 

fact, artesian in character, and will often raise the water to a height 

of several feet if confined. In PI. XIX Tertiary springs and characteristic contiguous topography are shown.

FIG. 29. Ideal section of Tertiary springs. A, D, Tertiary springs ; C, F, wells in red

beds : E, well in Tertiary.

It can be said almost without exception that all Tertiary springs 

yield relatively strong flows. The material from which -the water 

conies and through which it circulates is so coarse that the flow is 

less impeded than in the case of any other class of springs of the Territory, unless, indeed, it be the springs flowing from the conglomerate 

in the Wichita Mountains. An immense amount of water is allowed 

to go to waste every year by not utilizing these springs. In some 

instances the owners are using them for irrigation purposes, but as 

a general rule little attention is paid to their economic value. The 

city of Alva uses water from a Tertiary spring. It is carried by 

gravity through pipes a distance of 2 miles to a cistern and is then 

distributed to the different pipe lines of the city by pumps. The supply is more than adequate. None of the Tertiary springs have been 

known to go dry during the droughts which are common to the region 

in which they occur. They sometimes diminish in flow, but this is 

rarely ever the case. The water of the Tertiary springs is almost 

without exception soft and palatable.

ALLUVIAL SPBINGS.

Springs of this kind occur along the rivers in all parts of the 

Territory, but are most common in the Wichita Mountains and 

along Arkansas Eiver. The alluvial springs of the Wichita Mountains are found along the banks of every stream of the region,
100 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

issuing just above the surface of the water or flowing out onto the 

low bottom lands. Nearly every piece of low land has at least one 

spring flowing from it. They are rarely strong. The flow usually 

comes from the base of the deposit and trickles out for several rods 

along the bank, or else it issues from a single outlet. These springs 

furnish a large amount of water to the creeks, and altogether they 

probably do more than their share toward supplying the running 

water of the region. On account of their number and distribution 

they are probably of more economic value than the other springs of 

the mountains, but at the same time are less conspicuous.

Along Arkansas River in Oklahoma these springs from terrace 

deposits usually are large, although in many cases they do not flow 

out in a bold stream, but hundreds of small seeps come out along a 

bank for several hundred yards and the aggregate is a large stream 

of water. In the Wichita Mountain region these springs appear near 

the present creek beds, but along Arkansas River they usually flow 

from terrace deposits which are now many feet above the river 

channel. These deposits are rarely over half a mile wide and seldom 

more than 30 feet deep. The springs flowing from them seldom go 

dry and are rarely ever affected by drought.

SALT SPRINGS AND PLAINS.

Wells and springs, the water of which contains an appreciable 

amount of common salt (sodium chloride), are found not only 

throughout the red beds, but also in the Pennsylvania!! rocks, and in 

certain regions the water from the springs is of such noteworthy 

salinity as to warrant the popular phrase kw salt spring " or kk salt 

plain."1 Leaving out of account the regions in eastern Oklahoma in 

which the w^ater is but slightly salty, it is proposed to describe the 

localities, particularly in the western part of the Territory, in which 

salt springs and salt plains are common.

There are two salt plains in Woodward and Greer counties and 

one each in Woods, Blame, and Roger Mills counties. These plains 

have a wide geographical distribution and vary greatly both in size 

and amount of flow. While all the salt springs come from Permian 

red beds, they do not issue from the same geologic horizon. The 

Woods County plain is located a little more than halfway up the 

Enid formation of the red beds, the Woodward and Blaine county 

plains are supplied by springs that issue near the top of the Enid, 

not far below heavy gypsum members of the Blaine formation, and 

the Roger Mills and Greer county plains are found either near the 

base of the Greer formation, or, in some instances, springs are known 

to issue between gypsum ledges which are members of the Greer.
U. S. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. 148 PL, XX

SALT PLAINS ON THE CIMARRON.
SPBINGS. 101 

WOODS COUNTY PLAIN.

This is the largest of all the Oklahoma Salt Plains and also the 

only one that contains 110 large salt springs. It is located just south 

of the Salt Fork of the Arkansas in the eastern part of Woods County, 

about 35 miles from the nearest point of the gypsum hills, and 

includes an area of approximately GO square miles, extending about 

10 miles north and south and 6 miles east and west. The plain is as 

level as a floor, and on ordinary occasions as white as a snow field, 

from the incrustation of salt crystals which cover it. It is absolutely 

barren of vegetation, with only here and there a scattered bit of driftwood to break the monotony.

The origin of the salt on this plain is somewhat obscure. About the 

margin of the plain are a few weak salt springs, but they rarely furnish sufficient water to form a running stream. On digging a hole 

a few feet deep in any part of the plain, however, salt water begins 

to run in, and in ten minutes the hole will fill up to a point within 6 

inches of the top. The plain is composed of loose reddish-brown 

sand and clay, which is apparently everywhere saturated with salt 

water. The surface evaporation of this water gives rise to the white 

salt incrustations which render the surface of the plain white, except 

after a rain which has dissolved the salt crystals. To the writer the 

only plausible explanation of the origin of the salt water is to suppose 

that it comes from a large number of small springs which issue from 

 the red beds at the bottom of the plain. There is no way of estimating the amount of flow from this plain, but total volume of water 

is many second-feet.

WOODWARD COUNTY PLAINS.

In Woodward County there are two salt plains, both located in the 

valley 'of the Cimarron and fed by springs which issue from red shales 

50 to 100 feet below the Medicine Lodge gypsum. Locally these 

plains are known as Big Salt Plain* and Little Salt Plain, the latter 

being just south of the Kansas line, where the Cimarron Kiver first 

breaks through the line of gypsum hills.

The Big Salt Plain is located 12 to 20 miles farther down the 

Cimarron, extending for 8 miles or more along the river. In width 

it varies from half a mile to 2 miles. On the south bank the bluffs 

of red shale and sandstone capped with gypsum rise directly from the 

edge of the plain to a height of 100 feet or more, as saown in PI. XX. 

North of the plain these hills are not so steep and are at a distance 

of half a mile or more from the plain, but even here the sinuous white 

line of gypsum may be traced along the tops of the bluffs as far as the 

eye can reach. In other words, the plain lies in a broad canyon of
102 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

the Cimarron, inclosed on both sides by gypsum-capped red shale 

hills.

The plain is flat, except for a few meandering channels which in 

wet weather contain small streams of water, but are ordinarily dry. 

After a rain sometimes a stream of considerable volume flows down 

the channel across the plain, but during the summer months nearly 

all the water either evaporates or sinks into the sand. In places 

where a small stream still runs down the channel the water is often 

so salty that a thin crust of crystal white salt, resembling a sheet of 

ice, forms on the surface of the stream. The entire plain is covered 

with a thin incrustation of snow-white crystals, which in most places 

does not exceed an eighth of an inch in thickness, but which reflects 

the sunlight like a snow field.

In a large cove among the gypsum-covered red hills on the south 

side of the plains proper are a number of salt springs, which boil up 

from the flat surface of the plain. The water is crystal clear, and it 

sometimes requires more than ocular proof to convince one that it contains nearly 50 per cent of salt. There are scores, perhaps hundreds, 

of these springs on an area of but a few acres, some of which flow 

streams as large as a man's arm; others are much weaker. In all 

cases the presence of a spring is marked by a conspicuous white 

incrustation of salt, which forms around the spring and along the 

sides of the little stream that flows from it. Particles of grass or 

weeds blown into these springs or streams soon become covered with 

white salt crystals, forming strings of them which are often an inch* 

or more in diameter and look like rock candy. In places the incrustations around the springs are so thick that the salt may be scraped up 

and hauled away. Beds of rock salt are reported from this plain, 

but have* never been seen by the writer. The combined flow of the 

various springs which feed the plain will approximate perhaps 2 or 3 

second-feet.

BLAINE COUNTY PLAIN. *

Besides the two plains of the Cimarron, just described, the Salt 

Creek plain, in northern Blaine County, is also fed by springs which 

issue from below the gypsum ledges, and, like the others, it is located 

in a canyon at the foot of the Blaine Gypsum Hills. This plain is 

much smaller than the Big Salt Plain just described; its width 

is not more than a quarter of a mile in the widest place, and for the 

greater part of its course is not more than 100 yards, with a length 

of perhaps 3 miles.

The. region of Salt Creek is one of the most picturesque spots in 

Oklahoma. The upland is covered with jack oak and the capping of 

Tertiary sands breaks off abruptly into precipitous cliffs and canyons
U. S. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. 148 PL. XXI

A SALT SPRING ISSUING FROM BENEATH GYPSUM LEDGE.

B. LOG AND EARTH DAM ON UPPER CIMARRON RIVER.
SPRINGS. 103

200 or more feet deep, the slopes of which are composed of the brickred shales of the upper part of the Eiiid formation, capped by massive white gypsum ledges of the Blame formation. (See Pis. VII, B, 

and IX.) Numerous narrow canyons with cedar-covered slopes radiate outward from the head of Salt Creek, a tributary of the Cimarron. 

In the head of the main Salt Creek canyon are the springs which 

supply the plains. A ledge of reel and blue mottled cross-bedded 

sandstone outcrops along the heads of several branches of the main 

canyon, and from it issue the springs, the waters of which form a 

small creek. Along the bottom of the canyon salt incrustations, 

formed by evaporation, cover a narrow strip of 100 yards or more of 

the sandy level. A 'mile below the springs the canyon widens, the 

creek leaves the wall of hills and enters the flat country, the salt plain 

spreads out to become in one place as much as a quarter of a mile 

wide. A mile or so farther downstream it is joined by creeks which 

do not carry salt water, and it soon loses its individuality.

From the standpoint of economic importance the Salt Creek plain 

bids fair to exceed all others in the Territory, as it is nearer to the coal 

fields of the Indian Territory, as well as near to market. A number 

of primitive salt plants have at times been located along the edge of 

the plain. The methods employed in securing the salt are extremely 

simple. A well is dug in the sand of the plain and the water pumped 

by hand into vats and evaporated by boiling. Fuel, chiefly cedar and 

oak, was formerly obtained from the canyons near by. It is stated 

that three buckets of brine will make one bucket of salt. The 

capacity of one of these plants is approximately 2,000 pounds per clay. 

The salt is hauled in wagons to supply local trade, and the demand 

is said to have exceeded the supply for a number of years.

The Oklahoma Salt Company has erected a plant with a capacity 

of 450 barrels per twenty-four hours at Fergiison, Okla., the nearest 

railroad point to the plain. The brine is obtained from open and 

drilled wells and is carried 2-J miles in a 2^-inch wrought-iron pipe. 

Steam will be employed to operate rakes, elevators, conveyors, etc. 

Pans are of cement 12 by 150 feet and 20 inches deep.

ROGER MILLS COUNTY PLAIN.

In the extreme southern part of Roger Mills County, on sees. 10, 

11, 14, and 15, T. 8 N., K. 22 W., is a salt plain occupying an area of 

about 40 acres. This plain, which is about half a mile distant from 

the North Fork of Red River, is located near the base of the Greer 

Gypsum Hills, which in this region are well exposed. In places 

springs of salt water issue directly from beneath gypsum ledges, as 

shown in PL XXI, A, while in other instances the water boils up in 

the form of bold springs from the level surface of the plain. There
104 GEOLOGY AND WATER RESOURCES OE OKLAHOMA.

are in all 20 or more springs, the waters of which unite to form a 

stream estimated to flow at least 1 second-foot, although, in view of 

the fact that a great part of the water sinks into the sand, it is probable that this amount represents but a part of the actual flow. Salt 

lias been manufactured at this plain for many years. The water is 

said to contain a considerable proportion of gypsum, but not so much 

as to render it unfit for use.

GREEK COUNTY SALT PLAINS.

The two Greer County salt plains are located in small canyons 

which have been carved in Gypsum Hills, south of Elm Fork of Red 

River, about 5 miles east of the Texas line. From the names of the 

owners these plants are known locally as the Chaney Salt Plain and 

the Kiser Salt Plain. Neither covers an area of more than an acre or 

two. Both -are fed by springs that issue from the red shales below 

heavy ledges of Greer gypsum. Springs boil up from the level sand 

floor, and the water flows out of the canyon to mingle with the water 

of the river. A flourishing local industry has been carried on at these 

plains for twenty years or more, and some years as much as 600,000 

pounds of salt have been manufactured at each one. Since the timber, 

which formerly grew in the canyons, has been exhausted solar evaporation has been largely employed to produce salt. The average combined flow from the springs is estimated at 1 second-foot from each 

plain. In a number of canyons emptying into Elm Fork in this 

region there are salt springs, but no others have sufficient strength of 

flow to warrant the establishment of salt plants.

Salt has been manufactured at various times on all of the salt 

plains of Oklahoma except the large plain in Woods County, which, 

as stated above, contains no springs of any size. Until the present 

time, however, primitive methods only have been employed, and no 

considerable amount of capital has been invested. It goes without 

saying that salt springs of this character will ultimately develop 

into properties of much value. Ten or more second-feet of saturated 

brine will not always remain unutilized.

SULPHUR SPRINGS.

All the springs in Oklahoma which may be denominated sulphur 

spring's are located in the vicinity of the Wichita Mountains. In all 

there are a score or more, the greater part of which are mere seeps, 

located usually among the limestone hills which lie north of the 

granite peaks of the Wichitas. The three which are hereafter described are probably the strongest of the lot.
DEEP WELLS. 105 

GRANITE SULPHUR SPRING.

This spring is located in the northwest part of the town of Granite, 

Greer County, Okla., in a cove south of Headquarters Mountain, the 

westernmost of the high peaks of the Wichita Range. The water 

issues from deposits of clay and gravel close to the granite rocks at 

the foot of the mountain. The water is comparatively pure'except 

for a small quantity of sulphides. The spring has quite a reputation and its water is used for medicinal purposes.

RAINY MOUNTAIN SULPHUR SPRING.

Standing out on the plain in the eastern part of Kiowa County 

are three limestone knobs, the extreme northwestern outliers of the 

range of limestone hills referred to above. From a small ravine at 

the base of one of these hills there issues a sulphur spring which from 

its location near Rainy Mountain is known as the Rainy Mountain 

Sulphur Spring. It is situated in sec. 33, T. 7 N., R. 15 W. Not 

only sulphur, but salt as well is found in the water of this spring.

APACHE SULPHUR SPRING.

This spring is about 10 miles southwest of Apache, Comanche 

County, Okla., in sec. 32, T. 5 N., R. 12 W., near the foot of one of the 

limestone hills that make up the range lying north of the Wichitas. 

The flow of the spring is small; the source of the water is probably 

in the limestone rock.

DEEP WELLS.

GENERAL CONDITIONS. \

Within the past few years a number of deep wells have been put 

down in various parts of Oklahoma. These wells have been bored 

for water, gas, oil, and other products.

Because of the fact that shallow wells do not always furnish a sufficient amount of water, efforts have been made in various places to 

find deep-seated waters, and in many instances they have been successful. So far it has been found .that if a depth of 400 feet is 

reached without securing the desired amount and quality of water 

there is little use in going farther. The reason for this is that the 

greater part of Oklahoma is underlaid with red shales, which usually 

contain a large percentage of salt, gypsum, or other mineral salts. 

So far as known, except along the eastern edge of the outcrops of the 

formation, the drill has never penetrated to the base of these red 

shales, and so their thickness is unknown.
106 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

In this discussion only those wells that have reached a depth of 400 

feet or more will be considered. Any classification of deep wells that 

might be made must be largely an arbitrary one, but perhaps the 

classification based upon the purpose for which the well was drilled 

will more fully meet the conditions in Oklahoma than any other, and 

for this reason the deep wells of the Territory will be described under 

the two heads " Water wells " and " Oil and gas wells."

WATER WELLS.

Fort Reno well. In. 1893 a well 1,370 feet deep was drilled at Fort 

Reno, Canadian County, for the purpose of securing a supply of 

water for the post. The well, however, failed to secure enough good 

water for the purpose intended and was abandoned. A small amount 

of salt water was encountered at about 400 feet and fresh water tvt 

441 feet. This is the only well in the Territory in which fresh water 

is found below 400 feet. The rock passed through consisted mainly 

of red shale. The section is given in PI. XXII, A.

Kingfisher well. At Kingfisher an attempt was made to secure 

deep-seated water, and at a depth of GOO feet a great flow of strong 

salt water was encountered, the water rising to within 8 feet of 

the top.

Optima 'well. At Optima, in north-central Beaver County, a well 

was drilled to a depth of 498 feet without obtaining water, a rather 

rare occurrence on the high plains. The strata passed through seem 

to be all Tertiary deposits, and the depth indicates the thickness 

which these deposits attain. The log given in PI. XXII, B, shows the 

rocks passed through.

Cllildress^ Tex., -well. The Fort Worth and Denver Railroad 

Company had a well put down at Cllildress, Tex., 15 miles southwest 

of the southwest corner of Oklahoma, in an effort to secure water for 

engines and shops. The water found was impregnated with salt and 

gypsum, and therefore unfit for use. The rocks passed through were 

red shale, clays, thin sandstones, and gypsum and salt beds. These 

formations being soft caved badly, and the well was abandoned. The 

log of the Childress well is given in PI. XXII, G,

OIL AND GAS WELLS.

Wells in the Omge Nation. Along the eastern line of the Osage 

Nation, from the Creek country to Kansas, a number of wells have 

been sunk for the purpose of securing oil. In a number of these both 

oil and gas have been found, the former product running as high 

as 200 barrels per day and the latter product several million cubic 

feet per day. The wells pass through shales, limestones, and sandstones of Pennsylvanian age. Salt water is frequently encountered at
U. S. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. 148 PL. XXII

I

20 

24

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179

2!B 

258

3!

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464

664 

687

704 

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937

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102 

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132 

139 

144

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303

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18 LIMESTONE 

17 RED CLAY

7 LIMESTONE moa 

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1118 

53 RED CLAY 

1138 

1148 

10 LIMESTONE 1183 

25 RED CLAY 1173

10 SAND t-,, 

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10 RED CLAY ,n1s 5 SAND l*lo

24 RED CLAY 1238 

5 LIMESTONE 1253 

10 SHALE | 263

41 LIMESTONE

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5 LIMESTONE 

8 LIGHT SHALE

25 LIMESTONE 

16 SHALE g" 

43 LIMESTONE

10 SHALE 

19 LIMESTONE 25

40 LIGHT SHALE 4B 

60

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130 SHALE 14j 

163

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302

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567

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612

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40 RED SHALE

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15 RED SHALE

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105 SHALE

95 SKALE

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155 SHALE

37 LIMESTONE 

16 SHALE

38 LIMESTONE 

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4 SHALE

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55 LIMESTONE 

58 SHALE

137 LIMESTONE

40 SHALE 

37 LIMESTONE

48 SHALE 

150 LIMESTONE

95 SHALE 

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M 400 feet

WELL SECTIONS.
OIL AND GAS WELLS. 107

a depth of 1,400 feet. A log of one of these wells, near Bartlesville, is given in PL XXII, D.

Cleveland well. At Cleveland, Pawnee County, a well was drilled 

to a depth of 520 feet through comparatively thin ledges of red and 

blue shales and sandstone with two limestone members. Salt water 

was found at 220 feet and rose to within 40 feet of the surface.

Newkirk well. At Newkirk, Kay County, in the. northern part of 

the Territory, several wells have been drilled for oil and gas. These 

wells start 011 top of the Flint Hills, and consequently pass through 

a larger amount of limestone than any other wells in Oklahoma. A 

small amount of oil was encountered in all the wells, but not enough 

to pay for the cost of drilling. Salt water was found at various 

depths, in one instance rising to within a few feet of the mouth of the 

well. The log is given in PI. XXII, E.

Shawnee well. The log of the Shawnee well, given in PI. XXII, 

FI illustrates the conditions along the eastern edge of the red beds, 

where alternating strata of shales and sandstones make up the entire 

formation. If the well had been continued a few hundred feet 

deeper, there is no doubt that the drill would have passed through 

the red bedg into the subjacent members.

Jet well. The Saline Oil and Mining Company has put a well 

down 975 feet at Jet, Woods County, in the hopes of securing oil 

and gas from the red beds. The well passed through red and blue 

shales all the way,'with the exception of about 8 feet of sand at 280 

feet, which are reported to have yielded one to three barrels a day. 

Soft water was reported at 180 feet. The log is shown in PL 

XXII, G.

Anthony, Kans., well. This well was drilled 12 miles north of the 

Oklahoma line. A study of the log (PI. XXII, H) will assist in understanding the conditions in the northern part of the Territory. At 

this point the red beds are 551 feet thick, below which are 395 feet 

of blue shales and 404 feet of salt beds. Limestone, notably that of 

the Flint Hills, was encountered at 1,350 feet,"

CONCLUSIONS.

From the above facts and known conditions the following conclusions regarding the underground conditions in Oklahoma may be 

drawn: (1) In general, water may be obtained in fair quantities 

between the depths of 200 and 400 feet, but such water often contains 

a high percentage of soluble salts, which sometimes render the water 

unfit for use. (2) Water below 400 feet is almost invariably too

" Since the above was written a well at Spencer, 12 miles east of Oklahoma City, has 

been put down to a depth of 2,050 feet. The red beds were penetrated at 1,550 feet, 

below which gray to brown shales and sandstones were encountered.
108 GEOLOGY AND WATEE EESOUECES OF OKLAHOMA.

salty for any purposes except for the manufacture of salt. (3) Drilling wells to any considerable depth in the red beds is difficult, because 

of the unstable and treacherous character of the formations.

ARTESIAN WATER.

There is little hope for artesian water in Oklahoma. The Dakota 

sandstone, the great artesian water-bearing formation of the plains, 

outcrops only in the extreme western part of the Territory. Tertiary rocks carry large quantities of water, but, so far as known, the 

structural conditions are not suitable for an artesian flow. The red 

beds are water bearing, but in the main sparingly so, and, besides, 

they all dip westward or toward the higher lands.

Flows of artesian water depend upon several conditions, among 

which the two most important are (1) a porous stratum of rock 

contained between impervious strata; and (2) an exposure of this 

porous stratum at the surface at a higher elevation than the mouth 

of the well. It has been thought that in Oklahoma these conditions 

might be furnished by the red beds, which extend westward far up 

the flanks of the Rocky Mountains, but the rocks have not been found 

to yield flows. As to prospects in the subjacent rocks, the difficulty 

is that the drill has rarely penetrated the red beds in Oklahoma. 

In one or two instances wells which started in the red beds have 

leached the blue and gray clays and shales below, but in these instances the wells were located near the eastern margin of the red 

beds. Salt water only was found in these wells and in no instance 

did it reach the surface. The relations and capabilities of the 

formations underlying the red beds in central and western Oklahoma remain to be settled.

There are a few local instances of flowing wells in Oklahoma, but 

none of economic importance. At Guthrie a well in the red beds 

flows over the surface. Near Beaver City an artesian well is reported 

from the Tertiary.

In many parts of Oklahoma are wells that are semiartesian in 

character; that is, the water rises in the well often nearly to the top, 

but does not flow out. At Newkirk, in a well which was drilled 1,680 

feet for gas or oil, salt water was encountered which rose practically 

to the surface. In the vicinity of Norman there is a water-bearing 

stratum at a depth of about 250 feet below the surface, and in a number of wells which have reached this stratum the water rises from 

150 to 175 feet, standing within 75 to 100 feet of the surface. This 

fact may be readily explained by remembering that the rocks at 

Norman dip west 10 to 20 feet per mile, while the surface slopes to 

the east. The sandstone in which the water is found at a depth of 

250 feet comes to the surface some miles east of Norman, and at a
WATER CONDITIONS IN OSAGE NATION. 109

level lower than the mouth of the well. Under this condition the 

water rises to the level of the intake area, which is 75 to 100 feet 

below the level of the mouth of the well.

WATER CONDITIONS, BY COUNTIES.

In the following pages will be discussed briefly the general conditions of water supply in each of the 27 counties (counting the Osage 

Nation as one). The order is as follows: First, a brief mention of 

the rocks and the principal drainage features; second, a statement of 

the character of the wells and springs; and third (pp. 156, 173), a list 

of 10 wells from the county. These well records, more than 250 in 

all, have been selected froin about 3,000 records now on file in the 

office, and are believed to represent fairly well the water conditions of 

the various counties.

OSAGE NATION..

Rocks and drainage. The Osage Nation, which includes all of 

Oklahoma lying north and east of Arkansas River, is approximately 50 miles square. Tributary to the Arkansas in the Osage 

Nation are Beaver, Salt, and Gray Horse creeks. The greater part 

of the Nation is drained by Verdigris River, through Hominy, Bird, 

Buck, and Sand creeks. In the eastern part of the reservation the 

rocks are chiefly shales and sandstones, with an occasional ledge of 

massive limestones, while farther west to the Arkansas River the 

limestone ledges are more frequent. In this reservation the Flint 

Hills reach their highest development in Oklahoma, although they 

are here not so conspicuous as in Kansas. South of the river the limestone ledges begin to thin out and disappear.

Water supply. In general, this area is not yet extensively under 

cultivation and consequently comparatively few wells have been put 

down. The Osage Indians are the most primitive of all the tribes in 

Oklahoma. Many yet retain their tribal customs and manners of dress, 

and are usually known as " blanket Indians." During the last few 

years, however, many of the Osages have taken allotments, and the 

greater part of the land along the various streams has been leased to 

enterprising white men who are cultivating farms, often of considerable size. This is particularly the case along the valleys of Arkansas 

River and such minor streams as Beaver, Salt, Hominy, and Sand 

creeks. Except in rare instances, however, the uplands a*re not cultivated, and for that reason no comprehensive statements may be made 

regarding wells on them; but in such wells as have been put down 

near farmhouses and on ranches in the valleys an abundant supply of 

water has usually been found. There is no reason to doubt that on 

the uplands a satisfactory supply of water can be obtained. As is
110 GEOLOGY AND WATEE EESOUEGES OF OKLAHOMA.

usual in a limestone country, the water often is hard, but usually is 

not unfit for use. In the eastern part of the Osage country, as stated 

above, the rocks are chiefly sandstone and shales,' and in this region 

the wells furnish a good supply of soft water.

Throughout the greater part of the Osage Nation are many springs 

of considerable size. In the eastern part of the reservation these 

springs flow out from under sandstone ledges, usually above shale 

rocks, and the water of such springs is soft. Many Indian cabins 

and even many farms and ranches of considerable size have been 

located with reference to some spring. The water in Buck, Sand, 

Bird, and Hominy creeks, which rise in the Flint Hills and flow east 

across the reservation, emptying into Verdigris River, usually conies 

from springs that are for the most part perennial. In the western 

part of the Osage Nation are also many large springs, usually issuing 

from under limestone ledges, and the water is consequently hard. 

Such creeks as Little Beaver, Big Beaver, Salt, Gray Horse, and 

others are fed by springs from the Flint Hills. Some of these 

springs are of considerable size 'for instance, Big Spring, on Little 

Beaver Greek, 6 miles south of Maple City, Kans., has long been 

known as a camping place and resort. On the hill above this spring 

are located the famous Timbered Mounds, which are, in fact, nothing 

but ancient flint quarries from which Indians obtained the material 

for their implements.

But few wells have been reported from the Osage Nation, and because of the insufficient data no records are given.

KAY COUNTY.

Rocks and drainage. This is the northeastern county of Oklahoma. 

It is limited on the east by Arkansas Eiver and on the north by the 

Kansas boundary. The county is approximately 30 miles square, and 

is one of the most fertile in the Territory. With the exception of the 

portion along Arkansas River in the eastern part of the county, the 

topography is in general very even.

The Salt Fork of the Arkansas flows through the southern tier of 

townships and empties into Arkansas River in the Ponca Reservation 

a few miles south of the Kay County line. Tributary to the Salt 

Fork in Kay County are Chikaskia River, Bois d'Arc Creek, and 

Deer Creek^ and tributary to the Chikaskia are Duck and Gypsum 

creeks. All of these streams have carved shallow channels in the 

level upland, rendering the surface in many places slightly rolling, 

but in only few localities are there bluffs of any considerable height.

In the eastern part of the county from the Kansas line south to 

Ponca City are the limestone rocks, which form the southern part of
WATER CONDITIONS IN KAY COUNTY. Ill

the Flint Hills. From the level of the river to the top of the hill 

near Newkirk there, are 6 or 8 heavy ledges of limestone varying in 

thickness from 5 to 30 feet.

West of the limestone country there is an area comprising the 

greater part of the county, in which the rocks consist of grayish or 

bluish shales with a few ledges of thin limestone. This area, which 

i-xtends about as far southwest as Deer Creek, is the southern extension of the Marion and Wellington formations of Kansas, which in 

that State outcrop over several counties and extend from the top of 

the Flint Hills westward to the line of the red beds or Cretaceous 

rocks. In Oklahoma, however, these formations have but a limited 

areal extent, being confined to Kay County. In both Kansas and 

Oklahoma the shales contain extensive deposits of gypsum and salt, 

and one of the Oklahoma gypsum mills is located in this county.

In the southwestern part of the county, including the township 

west of Deer Creek and most of the regions south of the Salt Fork 

of Arkansas River, are typical red shales and sandstones of the red 

beds. Along several of the streams, particularly along the north 

slope of the Salt Fork, there are areas covered with Quaternary sand 

hills.

Water supply. Wells have been sunk on nearly every quarter section in Kay County, with depths varying from 20 to ,80 feet, and 

usually yield an abundant supply of water. In central and northern 

Kay County, in the gypsum region west of the limestone hills, the 

supply of water is abundant, but rather inferior in quality, being 

usually too hard for domestic use. In the red beds region, in the 

southwestern part of the county, the water usually contains more 

or less gypsum, although there are a number of wells which obtain 

water from a bed of sandstone. In these wells the water is almost 

uniformly soft. The best water in Kay County is found in the sand 

hills region, north of the Salt Fork, where the wells are usually shallow, not exceeding 20 to 30 feet in depth. In the bluffs along 

Arkansas River in the eastern part of the county are numerous 

springs, and, as is usual in a limestone region, the water from these 

springs is hard, though in most places not sufficiently so to render it 

unfit for use. There are also a number of springs of good soft water 

among the sand hills, particularly along the north bank of Salt Fork 

west of Tonkawa. Analyses Nos. 41, 42, and 43 are of water from 

wells, and Nos. 138 and 139 are of water from springs in Kay County.

Well records. Of 104 wells reported from Kay County, 35 furnish soft water, 55 hard water, and 14 salty water. The average 

depth of the 104 wells reported was 61 feet. The list on page 162 

includes records of 10 wells taken from various parts of the county, 

jind is believed to be representative of the water conditions.
112 GEOLOGY AND WATER RESOURCES OP OKLAHOMA.

NOBLE COUNTY.

Rocks and drainage. Noble County lies directly south of Kay 

County. In describing this county there will be included the Otoe 

and the southern half of the Ponca reservations. Arkansas River 

flows for 20 miles or more along the northeastern boundary of the 

county, forming a double oxbow bend. Across the county from west 

to east flow Red Rock and Black Bear creeks, both of which rise in 

Garfield County and empty into Arkansas River.

The rocks in the northeastern part of Noble County are largely 

shales and limestones, but in this region many of the ledges of limestone, which form the main part of the Flint Hills in the Osage 

country, finally disappear and give place to shales and. sandstones. 

The greater part of the rocks of this county, however, particularly in 

the vicinity of Perry and westward, consist of typical red beds clays 

and sandstones. It would perhaps be correct to say that the transition from the Flint Hills and the Pennsylvania!! rocks to the typical 

red beds takes place largely in this county. The sandstones throughout the greater part of Noble County are normally gray or brown, 

while the shales are almost always brick red. Along the western line, 

however, even the sandstones become red, and so continue to the western part of the Territory.

Water supply. The water in the eastern part of Noble County, 

particularly in the region now occupied by the Otoe and Ponca reservations, is not particularly abundant. Wherever wells have been 

put down, however, a sufficient supply of water for domestic and 

stock use has usually been obtained. In the southern part of the 

county sandstone beds are abundant, and in most localities wells yield 

plenty of good water. In the western part the water often contains 

mineral salts, chiefly gypsum or salt, but there are comparatively few 

wells in which water is not suitable for house use. There are also 

springs of considerable importance in Noble County, and a number of 

the small creeks which are fed by them flow the year round. Analyses Nos. 52, 53, 54, 55, and 56 are of water from wells in Noble County.

Well records. Of 29 wells reported from Noble County, 16 contained soft water, 9 hard water, and 4 salty water. The average 

depth was 52 feet. A list of wells from all parts of the county is 

given on page 166.

PAWNEE COUNTY.

Rocks and drainage. The shape of Pawnee County, which lies 

immediately east of Noble, is that of a right angle triangle, of which 

Arkansas River on the northeastern side is the hypotenuse. The 

eastern end of the county extends farther east than any other part 

of Oklahoma except the Osage Nation. Cimarron River empties into
WATER CONDITIONS IN PAWNEE AND PAYNE COUNTIES. 113

the Arkansas in the extreme southeastern part of the county. Black 

Bear Creek enters from Noble County and flows southeast to join 

Arkansas River. A number of small creeks tributary to the Arkansas, Cimarron, and Black Bear have cut the surface into a series of 

valleys and ridges, and in parts of the county the surface is uneven, 

high hills and steep slopes being common.

The rocks are mostly shales, sandstones, and limestones and do 

not differ materially from those of Osage Nation, just across the river. 

In Pawnee and Noble counties the Flint Hills finally lose their 

identity and become merged with the red beds and heavy ledges of 

sandstone.

Water supply. As would be expected in a region with the geologic structure of Pawnee County, water is abundant and there is 

no part of the county where it is not good. Wells which usually 

obtain a permanent supply at moderate depths are found on practically every quarter section. In a few instances the water from the 

wells is salty, but such cases are rare.

Springs which usually issue from beneath ledges of limestone 

are common in Pawnee County, and from under several of these ledges 

there is almost constant seep for a distance for sometimes several 

miles. In other localities bold springs are common. Analyses Nos. 

64, 65, 66, 67, 68, and 69 are of water from wells and No. 142 is of 

water from a spring in Pawnee County.

Well records. Of 151 wells reported from Pawnee County, 94 

furnish soft water, 50 hard water, 6 salty water, and 1 sulphur 

water. The average depth is 57 feet. The records on page 166 were 

taken from all parts of the county.

PAYNE COUNTY.

Rocks and drainage. The Cimarron flows through the southern 

part of Payne County and across the northwest corner of the Creek 

country before joining Arkansas River. The largest tributary of 

the Cimarron in Payne County is Stillwater Creek. The smaller 

creeks cutting across sandstone ledges have produced the rough 

surface characteristic of so much of eastern Oklahoma.

The rocks of Payne County are chiefly shales and sandstones, with 

a few interbedded limestone layers which have persisted from the 

Flint Hills region. The color of the rocks in the western part of the 

county is normally red, although some of the sandstones are brown or 

gray. Farther east they are all of a lighter color, but the shales 

continue to be red nearly to the eastern line of the county.

Water supply. The general conditions of water supply in Payne 

County do not differ materially from those in Pawnee and Noble

IBB 148 05 M 8
GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

counties. Wells are numerous and furnish plenty of water, usually 

of good quality. In the western part of the county, however, where 

the rocks are typical red beds a considerable amount of hard water 

is encountered, and some wells even contain salt water. Springs are 

found in practically all parts of the county. Most of them, however, are nothing but small seeps, which issue from under limestone 

or sandstone ledges. Analyses 70, 71, 72, 73, 74, and 75 are of water 

from wells in Payne County.

Well records. Of 140 wells reported from Payne County, 78 furnish soft water, 56 hard water, and 6 salty water. The average depth 

of the 140 wells reported is 55 feet. Records 202-211, on page 166, are 

from this county.

LINCOLN COUNTY.

Rocks and drainage. Deep Fork of the Canadian flows east across 

the center of Lincoln County. The north line of the county 

approaches nearly to the Cimniaron, while part of the south boundary 

is North Canadian River. This stream arrangement causes two eastwest divides, which pass across the county, and small tributary creeks 

flowing into the Cimarron, Deep Fork, or North Canadian have cut 

into these divides and increased by erosion the asperity of surface features. The rocks of Lincoln County are largely sandstones and shales; 

the shales are usually red, the beds of sandstones being often brown 

or gray.

Water supply. Wells in this county obtain abundant supplies oi 

water at depths ranging from 25 to 150 feet. Sandstone is the 

source of the water in the greater part of them, and most of them 

supply soft water. The springs of Lincoln County do not diffei 

from those in counties farther north, where similar rocks are found, 

From under sandstone ledges numerous seep springs issue and ir 

certain localities bold perennial springs are common. Over a considerable part of the county the soil is loose and sandy, and mucl] 

water which under other conditions might come to the surface in tht 

form of springs escapes in underflow. In many places where a spring 

reaches the surface the water soon again sinks into the sand. Analy 

sis No. 140 is of water from a spring in Lincoln County.

Well records. Of 58 wells reported from Lincoln County, 40 fur 

nish soft water, 16 hard water, 1 salty water, and 1 sulphur water 

The average depth of the 58 wells is 84 feet. The 10 well record: 

on page 164 indicate the water conditions in this county.

POTTAWATOMIE COUNTY.

Rocks and drainage. This is the southeastern county of the Terri 

tory. The North Canadian flows through the northern part, th< 

South Canadian forms its southern boundary, and Little Rive
WATER CONDITIONS IN CLEVELAND COUNTY. 115

flows from west to east across the central part of the county. Numerous small tributaries to these larger streams have cut into the upland, 

forming low, rolling hills.

The rocks are similar to those in counties north, being chiefly sandstones and shales, normally red in color. The sandstone is loosely 

consolidated, and the cementing material, chiefly calcium carbonate, 

having been dissolved, the sand grains fall apart and form loose sand, 

which is blown by the wind into sand hills. This county, as well as 

Lincoln and Payne, lies entirely within the Sandstone Hills region of 

Oklahoma.

Water supply. Wells have been put down in all parts of this 

county, and the water obtained from them is usually of a good quality, 

although in certain sections it contains gypsum and other mineral 

salts. In this county springs occur chiefly under three conditions 

in creek bottoms, where water removes the sand down to the underlying shale; on hillsides, where the covering sand mantle is too thin to 

carry all the water that flows down the hill, and as seep springs, 

which in wet weather occur in shale beds. Analyses Nos. 76, 77, and 

78 are of water from wells in Pottawatomie County.

Weir records. Of 76 wells reported from Pottawatomie County. 

37 furnish soft water, 37 hard water, and 2 salty water. The average 

depth is 70 feet. On page IBS is the record of 10 representative wells, 

selected from practically all parts of the county.

CLEVELAND COUNTY.

Rocks and drainage. South Canadian River bounds this county 

on the south and west; Little River, a tributary of the latter stream, 

rises in the county and flows east into Pottawatomie County. The 

eastern part of the county lies in the Sandstone Hills region and the 

northwestern part in the Low Plains region. The eastern part of 

the county is somewhat broken, as the streams that flow into Little 

River and South Canadian have cut rather deep valleys into the 

sandstones that comprise the greater part of the rocks. The divide 

between Little River and Canadian is generally level.

The rocks consist for the most part of red beds in which sandstone 

members are common in the eastern part of the county, although even 

here red shales make up a great part of the rocks. West of the Atchison, Topeka and Santa Fe Railway there is relatively little sandstone, and red shale makes up the greater part of the rocks. Along 

the north slope of the South Canadian there are areas of sand hills, 

probably composed of remnants of Tertiary sands.

Water supply. In the eastern part of Cleveland County much 

of the water is found in sandstone, and is consequently soft. On the 

level divide between the rivers the water is, in general, not so good,
116 GEOLOGY AND WATER RESOURCES OP OKLAHOMA.

being impregnated in many places with mineral salts, although even 

here many of the red beds wells furnish pure, soft water. In the 

sand-hills region north of the South Canadian the water is always 

good. Springs are not abundant in this county; in the eastern part 

there are a few springs issuing from under ledges of sandstone, in 

which the flow, while never very strong, is constant. In the sandhills region are a number of springs that flow the year round. Analyses Nos. 7, 8, 9, 10, 11, 12, 13, 14, 15, 16, 17, 18, 19, 20, 21, 22, 23, and 

24 are of water from wells in Cleveland County.

Well records. Of 82 wells reported from this county, 40 furnish 

soft water, 33 hard water, 7 salty water, and 2 iron water. The average depth of the 82 wells was 88 feet. Kecords of wells in Cleveland County are given on page 158.

OKLAHOMA COUNTY.

Rocks and drainage. The drainage of Oklahoma County is rather 

complex. North Canadian River flows east through it, making a 

large bend to the north in the eastern part of the county, but its drainage area is limited, and the four corners of the county drain into four 

different streams. Deep Fork of the Canadian drains the northeast 

part and Little Eiver the southeast corner. South Canadian drains 

the southwest corner, and Chisholm Creek, a tributary of the Cimarron, heads in the northwest corner.

Oklahoma County, like Cleveland County, lies partly in the Sandstone Hills region and partly in the Low Plains region; consequently, the rocks of the eastern part of the county consist largely of 

red sandstones, while farther west sandstones become less abundant, 

and shales and clays make up practically all the rocks. The eastern 

part of the county is more broken than the western. The headwaters 

of Deep Fork have cut canyons into the sandstones, giving to the 

country the dissected surface so characteristic of eastern Oklahoma, 

while farther west there are comparatively few forms of relief.

Water supply. Wells in this county find water at reasonable 

depths. In the Sandstone Hills region the water is often soft, but 

farther west hard water predominates. Along the North Canadian, 

wells in the alluvial flood plain have good water. Oklahoma County 

has comparatively few springs. Of these the greater part flow from 

the sandstone beds in the eastern part of the county, generally near 

one of the divides, and issuing at the head of a canyon which has been 

cut through the sandstone into the clay and shale below. Especially 

is this condition true along the canyons which empty into Deep Fork. 

Red beds springs occur, however, along both Chisholm and Cottoiiwood creeks. So far as known, there are 110 Tertiary springs in this
WATER CONDITIONS IN LOGA.N COUNTY. 117

county. Analyses Nos. 57, 58, 59, 60, 61, 62, and 63 are of water obtained from wells in Oklahoma Comity.

Well records. Of 36 wells reported from Oklahoma County, 25 

furnish soft water, 10 hard water, and 1 salty water. The average 

depth is 60 feet. The 10 well records given on page 166 are believed 

to represent typical conditions in this county.

LOGAN COUNTY.

Rocks and drainage. With the exception of the southeastern part 

of the county, the water of which flows into Deep Fork, all of Logan 

County is drained by the Cimarron, which flows east across the county. 

Skeleton Creek from the north and Cottonwood Creek from the south 

are the chief tributaries of this river. The surface is rather broken, 

particularly in the southern and eastern parts of the county.

Sandstone beds interstratined with red shales make up the greater 

part of the rocks of Logan County; but, as in the counties north and 

south of Logan, the sandstone members become thinner as the western 

part of the county is reached. North of the Cimarron there are belts 

of sand hills.

Water supply, The wells of Logan County are in a general way 

similar to those in Payne and Oklahoma counties. In the sandstone 

country the wells produce soft water, while farther west the rocks 

contain more mineral salts. At Guthrie there is an artesian well 

which probably is supplied from a local head. There is no reason 

for supposing that other wells of this character will be encountered.

Springs are scattered quite generally over Logan County, but are 

most numerous in the sandstone region in the eastern and northeastern parts. Many of the streams which flow into Deep Fork from 

the southeastern part of the county are fed by springs, and they are 

also abundant near Mulhall, in the northeastern part. Tertiary 

springs are reported from Sandy Creek, in the southwestern part of 

the county, and from the sand hill region north of the Cimarron. 

Analyses Nos. 49, 50, and 51 were from wells, No. 141 from a spring, 

and No. 154 from a pond in Logan County.

Well records. Of 35 wells reported from Logan County, 16 furnish soft water* 19 hard water, and the average depth is 78 feet. On 

page 164 are given the records of wells in various parts of Logan 

County.

CANADIAN COUNTY.

Rocks and drainage. Both North Canadian and South Canadian 

rivers flow southeast across Canadian County, and into both of these 

rivers empty a number of short tributary creeks. The southwestern 

part of the county drains into the Washita, and the northeastern
118 GEOLOGY AKTD WATER RESOURCES OF OKLAHOMA.

part into the Cimarron. Nearly all the county lies in the low plains 

region of Oklahoma.

The rocks are chiefly red shales and clays, with occasional thinbedded sandstones. They belong to the Permian red beds. In the 

northwestern part of the county occur the southern end of the Blaine 

Gypsum Hills in Oklahoma. In Canadian County, however, the beds 

of gypsum are not massive, rarely being more than 3 feet thick. 

North of both rivers there are deposits of Tertiary sands, these deposits being more abundant in the northwestern part of the county, 

north of North Canadian River and west of the Chicago, Rock 

Island and Pacific Kailroad.

Water supply. Water is obtained at moderate depths in practically 

all parts of Canadian County, and, as would be expected in a region 

composed largely of red shales, the water is often hard, containing a 

large percentage of mineral salts. Among the sand hills north of the 

larger streams and in the alluvial flood plain along the rivers, however, the water is usually soft, and pure.

There are springs of both hard and soft water in most parts of 

Canadian County, particularly in the Gypsum Hills region. Softwater springs come from under sandstone beds in the eastern part of 

the county and from Tertiary sand hills north of the streams. Caddo 

Spring, at the Cheyenne Indian school, 4 miles north of Darlington, 

is the most noted Tertiary spring in Canadian County.

Well records. Of 21 wells reported from Canadian County, 11 

furnish soft water, 9 hard water, and 1 salty water. The average 

depth is 61 feet. The water conditions of the county are set forth 

in the list of wells on page 158.

KINGFISHER COUNTY.

Rocks and drainage. The entire drainage of Kingfisher County is 

into the Cimarron, which, flows from its northwest to its southeast 

corner. Turkey Creek from the north and Salt, Copper, Kingfisher, 

and Walnut creeks from the south rise in other counties and cross 

Kingfisher before emptying into the Cimarron.

The rocks are typical red beds. Few sandstones are found, and the 

rocks consist largely of soft red shales. In the extreme southwestern 

part of the county are the Blaine Gypsum Hills, composed of masses 

of white gypsum. North of and parallel to Cimarron Kiver is a 

row of Tertiary sand hills from 3 to 10 miles wide. The county is 

all in the Low Plains region of Oklahoma.

Wafer supply. The greater part of the water of Kingfisher County 

comes from the red beds and contains a considerable percentage of 

mineral salts, chiefly calcium sulphate. Wells are found in all parts 

of the county, and it is rare that an abundant supply of water is not
WATEE CONDITIONS IN GAIIFIELD COUNTY. 119

found at a reasonable depth. Among the sand hills north of the 

Cimarron wells are usually shallow and yield soft water.

The best springs of Kingfisher County are found in the sand hills 

region north of the Cimarron. These springs are larger than those 

in Logan, the next county east, and being sand springs, consequently 

furnish soft water. Both in the flat region south of the Cimarron 

and among the Gypsum Hills in the extreme southwestern part of 

the county there are a few hard-water springs. Analyses Nos. 44, 

45, 46, and 47 are of water from wells in Kingfisher County.

Well records. Of 38 wells reported from Kingfisher County, 23 

furnish soft water, 13 hard water, and 2 salty water, and the average 

depth is 36 feet. The 10 well records given on page 162 represent the 

conditions in Kingfisher County.

GARFIELD COUNTY.

Rocks and drainage. Garfield County drains in three directions 

south into the Cimarron, north into Salt Fork, and east into the Red 

Rock and Black Bear creeks, tributaries of the Arkansas. It has no 

large river. The surface of the greater part of the county is flat, 

monotonous prairie, while along the large creeks the bluffs are low 

and inconspicuous.

Red beds make up the greater part of the rocks of the county, and 

of the red beds red shales and clays constitute the greater proportion. 

A few beds of sandstone, however, outcrop in the eastern part of the 

county, but they are so infrequent as to give scarcely noteworthy 

relief. The southwestern fourth of the county contains more or less 

conspicuous deposits of sand, approaching, in localities, sand-hill 

conditions. Most of the shallow creek bottoms, and some portions of 

the uplands, are covered with a blanket of Tertiary sand.

Water supply. Water in the red beds of Garfield County is 

abundant; it varies from that which is pure and soft to water so 

full of gypsum and other salts as to be unfit for use. Wells are found 

everywhere, and water is encountered at reasonable depths. In the 

sand-hills region good water is abundant, and in many parts of the 

county upland wells or those along prairie streams yield soft water.

Springs, which are most abundant in the sand-hills region in the 

central and southwestern parts of the county, supply good water, 

usually in considerable quantities. The water from many of these 

springs, however, soon sinks again into the sand, and in some 

instances reappears farther downstream as another spring. In the 

red beds region springs are found, but in general these springs 

rarely furnish sufficient water for domestic use. Strong red beds 

springs are, however, not unknown, and in some of them the water is 

of good quality. Water analysis No. 38 is from a well in Garfield 

County.
120 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

Well records. Of 104 wells reported from Garfield County, 41 

furnish soft water, 46 hard water, 15 salty water, 1 sulphur water, 

and 1 iron water. The average depth is 42 feet. Typical water 

conditions are shown by the well records on page 160.

GRANT COUNTY.

Rocks and drainage. This county lies west of Kay, its north line 

touching Kansas, and is entirely within the Low Plains region of 

Oklahoma. The drainage is all into the Salt Fork of the Arkansas, 

which flows east across the southern part of the county. The chief 

tributaries in the county are Deer, Cottonwood, Pond, and Sand 

creeks, all of which enter Salt Fork froin the north. The surface is 

smooth or rolling, very few conspicuous relief forms being found.

The rocks consist chiefly of red beds and Tertiary deposits. The 

red beds, which belong to the Enid formation and constitute the 

bed rock throughout the county, consist largely of sandstones and 

clays, of which the latter form the major part. Few ledges of 

sandstone hard enough for building purposes are found in Grant 

County. Sand hills are found along the Salt Fork, principally on 

the north side of the streams, in an east-west belt from 5 to 15 miles 

in width. A considerable portion of the upland is covered also with 

sand and loam of Tertiary or Quaternary age.

Water supply. Wells may be found on nearly every quarter section in Grant County, and in most cases the water is both abundant 

and wholesome. Among the sand hills this is almost universally 

true. In a number of cases where the rocks are chiefly red beds, wells 

put down in the sand and gravel deposits along some prairie creek 

have plenty of good water. As an example of this fact may be given 

the city well at Medford. After trying in vain to secure good water 

in the red beds under the city a well was dug in the bed of a small 

stream a mile distant and an abundant supply was obtained. There 

are wells in which the water contains gypsum, salt, soda, magnesia, 

or some other such substance, but in the majority of them such is 

not the case.

Springs, which are abundant in most parts of the county, issue 

usually from sand deposits, and almost without exception furnish 

soft water. The streams north of the Salt Fork are fed in a large 

part by bold, perennial Tertiary springs. There are also springs in 

the red beds-in Grant County, but like those of this formation in 

adjoining counties, they are usually unimportant. Analyses Nos. 39 

and 40 are of water from wells and 152 and 153 of water from ponds 

in Grant County.

Well records. Of 54 wells reported from this county, 27 furnish 

soft water, 18 hard water, and 9 salty water. The average depth of
WATER CONDITIONS IN WOODS COUNTY. 121

the wells recorded is 33 feet. The well records on page 162 show the 

characteristic water conditions in the county.

WOODS COUNTY.

Rocks and drainage. With the exception of the southwestern and 

northwestern parts, which are included in the Gypsum Hills region, 

Woods County lies within the Low Plains region of Oklahoma. Three 

of the larger streams of the Territory flow across the county the 

Salt Fork, which flows across the northern part; the Cimarron, 

which crosses the county south of the center, and the North Canadian, 

which touches the extreme southwest corner. Sand, Mule, and Medicine creeks from the north and Clay Creek from the south are the 

chief tributaries of the Salt Fork, which receives the drainage of 

perhaps one-third of the county. Of the smaller streams emptying 

into the Cimarron, Eagle Chief and Indian flow from the north, and 

Cottonwood, Skull, Barney; Greaver, Main, and West creeks, all of 

which take their rise among the Gypsum Hills, from the south. 

The Cimarron and its tributaries drain more than half of Woods 

County. North Canadian Eiver, in the southwestern part, receives 

the drainage of but a small area, perhaps not to exceed two townships in all, no creeks emptying into it in this county.

The rocks of the county consist largely of red beds clays and 

Tertiary sand. The Blaine Gypsum Hills, which it will be remembered are a part of the Permian red beds, extend parallel to and 

south of the Cimarron across the southwestern part of the county, 

v and appear again in the northwestern part, near the Kansas line. 

In the Gypsum Hills the rocks consist chiefly of red shales with 

interbedded deposits of massive white gypsum and dolomite. With 

the exception of the formations in the Gypsum Hills, the rocks of 

the red beds do not differ materially from those farther east, being 

composed chiefly of red shales, with a few inconspicuous sandstone 

members. The sand hills, also, are like those already discussed, the 

only difference being that toward the western part of the Territory 

the Tertiary deposits are more pronounced and the sand-hills districts 

more conspicuous.

The alternation of surface deposits of sand hills and red beds gives 

rise to a peculiar zonal distribution of formations noticeable in many 

parts of western Oklahoma, but nowhere better exemplified than in 

Woods County. It may be illustrated as follows: In passing from 

the Kansas line to the southwestern part of the county one will cross 

successively a number of these various lithologic zones. On the 

Kansas line is found the typical red shales; a few miles south, north 

of the Salt Fork, one enters the sand-hills region, a strip of country 

here about 10 miles wide, that continues south to the river. South
122 GEOLOGY AND WATEE RESOURCES OF OKLAHOMA.

of the Salt Fork the red beds again appear and continue for 20 miles 

or more across the divide between the waters of the Salt Fork and the 

Cimarron, until finally the sand hills north of the latter stream begin 

to appear. This belt of sand hills is 10 to 15 miles across. Then 

comes the red beds slope south of the Cimarron, including the Gypsum 

Hills, while on top of these hills and still farther southwest lie the 

sand hills on the north slope of the North Canadian.

Water supply. The water conditions follow closely the lithologic 

conditions in this as in other Oklahoma counties. In red beds areas 

the water is abundant, but often hard; in the sand hills it is both 

abundant and soft, and in the region around the Great Salt Plain, in 

the eastern part of the county, water from wells is often salty, while 

among the Gypsum Hills and in some other parts of the county gypPIG 30. Section at Cleo Springs, Okla. A-B, red beds-Tertiary unconformity; R, 

spring; C, bed of Eagle Chief Creek.

sum water is found, often of such a character as to render it unfit for 

use. The water is about equally divided between hard and soft.

Woods County has an abundance of springs, most of which are 

located in regions of Tertiary rocks. North of the Salt Fork there 

are scores, perhaps hundreds, of strong perennial springs, and among 

thp sand hills north of the Cimarron they are equally abundant. Cleo 

Springs (see fig. 30), near the mouth of Eagle Chief Creek, and Elm 

Springs, from which the city of Alva obtains its water supply, may be 

cited as examples of Tertiary springs. There are springs in the red 

beds in Woods County, and some of them have a considerable reputation. In the vicinity of the Salt Plains there are a number of salt 

springs, although none of them are of size comparable with the salt 

springs in Woodward, Blame, or Greer counties. Clay Creek is fed 

largely by springs, Timberlake Springs were famous long before 

the country was open to settlement, Whitehorse Springs supply the
WATER CONDITIONS IN BLAINE COUNTY. 123

whole township with water, and among the Gypsum Hills are a 

number of perennial springs. Analyses Nos. 79, 80, 81, 82, 83, and 

84 are of water from wells, and Nos. 143, 144, 145, 146, 147, 148, and 

149 are of water from springs in Woods County.

Well records. Of 304 wells reported from Woods County, 148 furnish soft water, 138 hard water, 15 salty water, and 3 sulphur water. 

The average depth of the 304 wells reported is 46 feet. The well 

records on page 170 show the water conditions in various parts of this 

county.

BLAINE COUNTY.

X

Rocks and drainage. Cimarron, North Canadian, and South 

Canadian rivers flow southeast across Blaine County. The Cimarron 

touches the northeast corner, the South Canadian flows for 15 miles 

through the southwest corner, while" the North Canadian enters at 

the northwest corner and flows diagonally across to the southeast 

corner. While the Cimarron flows but such a short distance through 

the county, it receives nearly half of the drainage. This is due to 

the fact that the valley of the Cimarron in Oklahoma is from 200 to 

300 feet lower than the valley of the North Canadian. Several creeks 

of considerable size, of which Salt Creek is the largest, rise among the 

Gypsum Hills and flow northeast into the Cimarron. The North 

Canadian receives a few short tributary creeks, most of which enter 

from the south, and drains a strip of country about 20 miles wide. 

An area of perhaps 150 square miles in the southwestern part of the 

county is drained by the South Canadian.

The rocks of Blaine County consist of Permian red beds and Tertiary and Pleistocene sands and alluvium. The northeastern part of 

the county is included in the Low Plains region, and the remainder 

of the county in the Gypsum Hills region. The Blaine Gypsum Hills, 

which are parallel to and 10 to 15 miles south of the North Canadian, 

rise like a wall 200 to 300 feet above the level prairie to the east. 

Red shales make up not only this flat prairie country, but also the 

greater part of the slope of the Gypsum Hills, while on top of these 

hills and between the bluffs and the North Canadian lie extensive 

sand hills. Southwest of this river red beds again appear, the 

rocks consisting largely of the Whitehorse and Day Creek members 

of the Woodward formation. On Red Hill, 8 miles northwest of 

Geary, is one of the best exposures of Day Creek dolomite in the 

Territory. Sand hills occur again along the north slope of the South 

Canadian, and beyond that stream red beds are again found.

Water supply. The water of Blaine County varies with "the locality. In the sand-hills region it is good. East of the Gypsum Hills, 

in the red shale country, the water from wellsc ontains a comparatively
124 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

large percentage of mineral salts, chiefly gypsum. South of the North 

Canadian, also, the water is often not suitable for use. North of both 

Canadian rivers, in the sand-hills country, wells usually encounter 

good soft water at moderate depths.

Springs are common among the Gypsum Hills, issuing generally 

from above shales and beneath gypsum ledges, but in such a case the 

water is often so strongly impregnated with gypsum as to be unfit 

for use. In the bottom of one of the deep canyons among these hills, 

4 miles west of Ferguson, are a number of springs of strong salt 

water. The waters of these springs unite and form a plain, which 

extends for several miles along Salt Creek. There is enough salt 

water going to waste in this region alone to make sufficient salt to 

supply several States. The best soft-water springs in Blaine County 

are found among the sand hills north of the streams, and these springs 

as in other counties in which sand hills are found, are generally 

strong and flow the year round. As an example of the use to which 

a Tertiary sand-hills spring may be put may be cited the case of the 

Rubey Stucco-Plaster Company, at Ferguson, Okla. The cement mill 

is located in a canyon at the base of the Gypsum Hills and good 

water was not available. A pipe was laid from a spring located on 

a hill at an elevation of 200 feet above the plant and 2£ miles distant, 

and an ample supply of water was obtained for boiler and domestic 

use. Analyses Nos. 3, 4, and 5 are of water from wells in the red 

beds at Geary, Blaine County, and Nos. 150 and 151 are of water 

from salt springs at the head of Salt Creek, 4 miles west of Ferguson, 

Blaine County.

Well records. Of 108 wells reported from Blaine County, 63 

furnish soft water, 39 hard water, 6 salty water, and the average 

depth is 60 feet. The 10 records on page 156 were taken from all parts 

of the county and represent the general water conditions.

CADDO COUNTY.

Rocks and drainage. Washita River flows east across the central 

part of this county, while the South Canadian touches the northeast 

corner, and Cache Creek, a tributary of the Red River, drains several townships in the southern part. The chief tributaries to the 

Washita in this county are Sugar and Cobb creeks, both of which 

enter from the north.

Red beds constitute the greater part of the rocks of Caddo County, 

and, as in other parts of the Territory, sandstones and clay shales 

make up the greater part of the red beds. In Caddo County, however, the sandstone greatly predominates. The Whitehorse member 

of the Woodward formation thickens in this region, giving rise to a 

series of fine-grained red or grayish sandstones, often weathering
WATER CONDITIONS IN COMANCHE COUNTY. 125

into conspicuous buttes, which are typically exposed on the high 

divide between the Washita and South Canadian southwest of Bridgeport. (See PI. X, A.) In the southern and western parts of the 

county the deposits of Greer gypsum outcrop in conspicuous ledges on 

hilltops. So far as known there are no extensive deposits of Tertiary sand in Caddo County. It is true that there are sand hills, but 

they are composed largely of sand of disintegration from the Whitehorse. In the southwestern part of the county there are hills composed of Arbuckle limestone, the northern extension of the Wichita 

uplift.

Water supply. The water in Caddo County is generally good. 

Wells in the sandstone usually secure soft water, although in certain 

parts of the county, notably on the divide between the Canadian 

and the Washita, the depth to water is often as much as 200 feet, but 

the water when found is almost uniformly pure and wholesome. In 

the gypsum region hard water predominates. Springs are not uncommon in Caddo County, although over considerable areas strong 

springs are rare. The water which percolates through the finegrained sandstone conies out as seeps along the side of a hill or in 

the head of a narrow canyon. In the limestone hills are a number 

of strong springs which issue from limestone rocks. Analysis No. 6 

is of water from a well at the Anadarko brickyard.

Well records. Of 75 wells reported from Caddo County, 62 furnish soft water and 13 hard water. The average depth is 88 feet. 

The 10 well records on page 156 show the character of the water in the 

various parts of the county.

COMANCHE COUNTY.

Rocks and drainage.- With the exception of small areas in the 

northwestern and northeastern corner, which drain into the Washita, 

Comanche County is drained by Red River. Beaver, Cache, Deep 

Red, and other creeks are the principal tributaries.

The main range of the Wichita Mountains lies in the northwestern 

part of Comanche County. These mountains consist largely of 

igneous rocks gabbro, porphyry, and granite. North of the main 

range is a row of limestone hills containing rocks of Cambrian and 

Ordovician age. The rocks over the remaining portion of the county 

are chiefly red bed and shales, except along the north bank of Red 

River, where there is a district covered with sand hills.

Water supply. Comanche County is well watered. Wells which 

have been put down in the red beds encounter water, usually of good 

quality, at moderate depths. Springs are found in most parts of the 

county. Those in the red beds are usually weak and uncertain, 

often being nothing but seep springs. Among the granite and lime-
126 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

stone mountains, however, springs are abundant, and the perennial 

streams issuing from these mountains are fed by the springs. The 

springs among the limestone rocks contain a considerable amount of 

calcium carbonate, while the granite springs yield very pure water. 

Analyses Nos. 25, 26, 27, 28, 29, 30, 31, 32, 33*, 34, 35, and 36 are of 

water from wells; Nos. 136 and 137 of water from springs, and Nos. 

134 and 135 are of water from creeks in Comanche County.

Well records. Of 25 wells reported from Comanche County 18 

furnish soft water, 7 hard water, and the average depth is 32 feet. 

Typical water conditions are given in the 10 well records on page 158.

KIOWA COUNTY.

Rocks and drainage. The North Fork of Eed River forms the 

western line of Kiowa County, and the Washita flows through the 

northeast corner. The drainage of the greater part of the county is 

carried by Elk and Otter creeks, which flow south into North Fork, 

and Rainy Mountain Creek, which flows northeast into the Washita. 

The rocks consist chiefly of red beds and granite, the latter rock 

forming the western extension of the Wichita Mountains. The red 

beds consist largely of typical red clay shale, which, in localities near 

the mountains, grades off into conglomerate. In the northern part of 

the county are a few ledges of dolomite and sandstone, and along 

North Fork are localities in which sand hills are found.

Water supply. Water is obtained from wells in practically all 

parts of the county. Its quality varies, being usually better south 

of the mountains than north. Springs are found among the mountains, and the water there obtained is pure and sweet; Otter Creek is 

fed largely by springs of this kind. Red beds springs are also 

known, but as a rule the amount of flow from springs of this kind 

is not great. Analysis No. 48 is of water from a well at Snyder.

Well records. Of 35 wells reported from Kiowa County, 21 furnish soft water, 12 hard water, and 2 salty water. The average 

depth is 29 feet. The water conditions in various parts of the 

county are shown by well records on page 164.

GREEK COUNTY.

Rocks and drainage. Greer, the southwestern county in Oklahoma, lies southwest of the North Fork of Red River, and all the 

drainage is into one of the four branches of the Reel North Fork, 

Elm Fork, Salt Fork, or South Fork. The surface is generally 

level with the-exception of canyons in the Gypsum Hills along parts 

of Elm Fork and Salt Fork, The extreme western extension of the 

Wichita Mountains lies west of North Fork of Red River, in the 

northeastern part of the county,
WATER CONDITIONS IN WASHITA COUNTY. 127

The rocks are mostly red beds, with red shale predominating. A 

very considerable part of the county is underlain with gypsum, which 

in places outcrops along the sides of various streams. Sand hills 

occur along, some parts of both the North Fork and the South Fork.

Water supply. As Greer County has more gypsum than any 

other two counties in the Territory, one would expect to find hard 

water. Wells frequently encounter beds of gypsum at depths ranging from 20 to 100 feet, and in such cases the water often found just 

beneath the gypsum partakes of the quality of that mineral. The 

springs of Greer County issue usually from beneath gypsum ledges 

along bluffs, although prairie springs are not unknown. In the 

western part of the county, within 5 miles of the Texas line, there are 

two salt plains, each formed from salt springs which issue from 

the bottoms of canyons carved into the Gypsum Hills south of Elm 

Fork. For a number of years salt has been manufactured on both 

these plains. Sand-hills springs are found near some of the streams 

and at Granite there is a sulphur spring. In general, the water of 

Greer County is abundant in quantity but rather undesirable in 

quality.

Well records. Of 152 wells reported from Greer County, 26 furnish soft water, 109 hard water, and 16 salty water. The average 

depth is TO feet. The well records on page 162 show the varying character of the water of this county.

WASHITA COUNTY.

Rocks and drainage. Washita River flows southeast through the 

eastern part of the county and receives more than three-fourths of its 

drainage. The southwestern corner is drained by Elk Creek, a 

northern tributary of North Fork of Red River. v In the eastern part 

on both sides of the Washita there are considerable ledges of gypsum, 

while farther west sandstone of the Quartermaster formation prevails. On the divide between Elk Creek and the Washita, in the 

western part of the county, there are sand hills. Red beds constitute practically all the rocks of the county.

Water supply. In the eastern part of Washita County wells often 

pass through gypsum and obtain a supply of hard water directly 

beneath a bed of it. One such deposit, penetrated in a well near 

Seger, is reported to be 115 feet thick, the thickest so far known in the 

Territory. In the western- part of the county good water is obtained 

from the Quartermaster, although the supply is sometimes limited.

Springs in Washita County are principally of two kinds gypsum 

springs and sandstone springs. In the eastern part of the county the 

water from gypsum springs is not always good; water from the 

sandstone springs in almost every instance is soft and wholesome,
128 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

although occasionally limited in amount. Many of the gypsum 

springs issue as bold streams from beneath heavy ledges, while the 

sandstone springs usually occur as seeps from the fine-grained sandstone along the heads of prairie canyons.

Well records. Of 60 wells reported from Washita County, 43 furnish soft water, 13 hard water, and 4 salty water. The average 

depth is 66 feet. The well records on page 168 show the water conditions in this county.

CUSTER COUNTY.

Rocks and drainage. The greater part of the drainage of Custer 

County enters Washita River, which flows southeast across the 

county. South Canadian River, however, crosses the northeast corner and Deer Creek, a tributary of that stream, drains the eastern 

part. Beaver, Barnitz, Turkey, Quartermaster, and other creeks are 

tributary to the Washita. The surface is rolling, the streams having 

cut rather deep valleys into the upland.

The rocks are- chiefly of red-beds shales and clays. In the western 

part of the county the Quartermaster formation is well developed, 

and in the eastern and central parts are considerable deposits of 

gypsum. Small areas of Comanche Cretaceous rocks are found in 

Custer County, but are of no importance as far as the water supply is 

concerned. Sand hills are rare in Custer County.

Water supply. The character of the water is such as would be 

expected in a region of red-beds shales and gypsums, generally containing mineral salts in greater or less amounts. Wells usually 

obtain an abundance of water, however, and there is very little of it 

that may not be used. Springs are also found, but not in large 

numbers. In the Quartermaster sandstone, in the western part of the 

county, springs typical of that formation occur weak seep springs 

which issue usually from the head of a small canyon that has been 

cut into the soft sandstone. The water from these springs is uniformly good.

Well records. Of 125 wells reported from Custer County 44 furnish soft water, 80 hard water, and 1 salty water. The average 

depth is 74 feet. Typical conditions are shown by the well records 

given on page 158.

DEWEY COUNTY.

Rocks and drainage. The South Canadian flows east through this 

county in a series of oxbow bends, while the North Canadian crosses 

the northeast corner. Perhaps three-fourths of the drainage empties 

into the South Canadian, although the creeks tributary to this stream 

are usually short and unimportant.

The rocks are largely red beds. Sand hills occur north of the
WATER CONDITIONS IN ROGER MILLS COUNTY. 129

South Canadian. Among the red beds sandstone is rare, the greater 

part of the rock consisting of red shales interspersed with beds of 

white gypsum.

Water supply. Wells are common in Dewey County, and the 

water, which varies much in quality, is usually plentiful. Springs 

are found chiefly among the sand hills, where the water is both 

abundant and pure, although red beds springs which furnish hard 

water are not unknown. Analysis No. 37 is of water from a well 

in Dewey County.

Well records. Of 123 wells reported from Dewey County, 21 furnish soft water and 102 hard water. The average depth is 93 feet. 

The 10 records on page 160 indicate the varying conditions of the 

water of this county.

ROGER MILLS COUNTY.

Rocks and drainage. The North Fork of Red Eiver forms the 

southern boundary of this county, and the Wasllita flows across its 

northeastern corner. A number of short creeks emptying into these 

rivers drain the entire county. Except a part of the divide between 

the Washita and North Canadian rivers, in the western part 

of the county where Tertiary sand hills are found, the rocks 

consist largely of red beds which cover practically the entire county. 

The greater part of these belong to the upper Quartermaster formation of the Permian and consist of fine-grained sandstone and 

shales. In the extreme southern part of the county, along the North 

Fork of Eed Eiver, gypsum ledges are exposed along a bluff nearly 

200 feet high and 10 miles long, one of the finest exposures known in 

the Territory.

Water suppty. With the exception of the southeastern part of the 

county, in which gypsum water is found, soft water predominates 

throughout Eoger Mills County. Wells in the Quartermaster formation usually secure good water, although in limited amounts, while 

in the sand hills water is both abundant and wholesome. Springs 

which occur in the Quartermaster are usually rather weak seep 

springs, but often furnish sufficient water to supply a farm with 

domestic and stock wrater. In the southern part of the county are 

a number of salt springs, while in the western part Tertiary springs 

are not unknown, and some of them furnish large amounts of water.

Well records. Of 47 wells reported from Eoger Mills Comity, 27 

furnish soft water and 20 hard water. The average depth is 60 feet. 

Characteristic water conditions are shown in the 10 records on 

page 168.

IBB 148 05 M 9
130 GEOLOGY AND WATEE RESOURCES OF OKLAHOMA.

DAY COUNTY.

RocJfs and drainage. The South Canadian has cut a broad canyon 

through this county, swinging from north to south in a series of oxbow bends, and across the southwestern corner flows the Washita, 

here but a small creek. The drainage is into these two rivers.

Red clay and sandstones of Permian age, which form the bed rock, 

and considerable deposits of Tertiary sand and clays on the uplands, 

particularly in the region north of South Canadian River, constitute 

the rocks of Day County. The valley of the South Canadian has 

cut its way through this upper sand and clay formation into the 

red-beds clays and sandstones below. North of the Canadian, as 

well as in the region between this river and the Washita, in the southwestern part of the county, are large areas of sand hills, while in 

the southeastern part there are extensive deposits of gypsum among 

the red beds.

Water supply. In the sand hills soft water is found in all the wells, 

and as the area covered by these hills is larger than that occupied 

by the red beds, it follows that in this county the water is usually 

good. Springs are found in both the sand-hills and the red-beds 

areas, the former being usually strong and furnishing good water, 

while the red beds springs are usually weak and the character of the 

water often unsatisfactory.

Well records. Of 28 wells reported from Day County 21 furnish 

soft water and 7 hard water. The average depth is 84 feet. Typical 

records of the wells of this county are given on page 160.

WOODWARD COUNTY.

Rocks and drainage. Woodward County is drained by Cimarron 

and North Canadian rivers. The former stream enters the northwest 

corner from Beaver County, flows southeast for 10 miles, passes into 

Kansas, and after flowing a distance of 25 miles in that State, again 

flows into Woodward County and continues in a southeast course for 

 10 miles or more before reaching Woods County. North Canadian 

River is formed by the junction of Beaver and Wolf creeks, which 

unite at old Fort Supply, near the center of the county, Beaver 

Creek flowing southeast and Wolf Creek northeast to form this 

junction. The chief streams flowing into the Cimarron in Woodward 

County are Doe, Chimney, Sand, Long, Traders, and Buffalo creeks 

from the south, and Anderson, Indian, Whitehorse, and Redhorse 

creeks from the north, all of which rise in the Gypsum Hills. Neither 

North Canadian River nor Beaver Creek have any tributaries of 

importance emptying from the north in Woodward County for the 

reason that the north slope of these streams is covered with sand 

hills; Kiowa, Otter, Clear, Indian, and Persimmon creeks are south-
WATER CONDITIONS IN BEAVEE COUNTY. 131

ern tributaries to these streams, while Wolf Creek has a number of 

smaller creeks emptying from both north and south.

In Woodward County red beds are exposed along the streams, 

while Tertiary sand covers the uplands. Along the Cimarron and 

its tributary creeks beds of gypsum outcrop, and the entire valley in 

Woodward County is but a broad canyon cut into the Gypsum Hills. 

Along the North Canadian and Beaver Creek red beds are exposed, 

especially on the south side of the stream, but on Wolf Creek the red 

beds are mostly hidden and only Tertiary rocks are found. All the 

divides in Woodward County, as well as the north slope of the North 

Canadian and Beaver Creek, are covered with sand hills or consist of 

level upland capped by Tertiary rocks.

Water supply. Along the Cimarron and south of North Canadian 

JRiver the water is usually obtained from red beds, and in consequence 

is usually not good. The water from the red clay is sometimes good, 

but more frequently it carries so much mineral salts as to be unsuitable for house use, but on the uplands and the north slope of the 

North Canadian wells put down in the Tertiary formations secure an 

abundance of good water. On some of the uplands the wells are 

200 feet deep or more, but the average depth of the wells of this kind 

is perhaps not more than 75 feet.

Springs occur both in the red beds and Tertiary formations. 

Among the Gypsum Hills along the Cimarron springs issue sometimes from beneath heavy ledges of gypsum in which the water contains large amounts of calcium sulphate in solution. In the northern 

part of the county there are two regions of salt springs, the largest of 

which includes a plain 8 miles long and 2 miles wide, from which 

flows a stream carrying approximately 2 second feet. The Tertiary 

springs of Woodward County are among the finest in the Territory. 

The Moscow Springs on the North Canadian have long been famous, 

and the Bent Canyon Springs, 20 miles north of Woodward, form a 

veritable oasis. Old Fort Supply was supplied with water carried 

in pipes from a Tertiary spring 3 miles distant, and Woodward, the 

county seat, obtains its water supply from Tertiary rocks. Analysis 

No. 85 is of water from a well in Woodward County.

Well records. Of 53 wells reported from Woodward County, 37 

furnish soft water, 15 hard water, and 1 salt water. The average 

depth is 56 feet. The well records on page 170 show the typical 

water conditions in this county.

BEAVER COUNTY.

Rocks and drainage. Beaver County (formerly known as " No 

Man's Land " or the " Neutral Strip ") extends from the one hundredth to the one hundred and third meridian, a distance of 1C5
132 GEOLOGY AND WATEK BESOURCES OP OKLAHOMA.

miles west of the main part of Oklahoma. Its width is 35 miles. 

It is a typical part of the high plains, apparently flat and level as a 

floor, but in reality sloping from an altitude of over 4,500 feet at the 

New Mexico line to about 2,000 feet in the eastern part of the 

county.

Across this county Cimarroii River and Beaver Creek flow from 

west to east. The Cimarroii flows across the northwestern part of 

the county for 50 miles, then goes on a long excursion through Colorado and Kansas and returns to Beaver County 25 miles west of 

the eastern line of the county. Except for a distance of 15 miles 

where the stream bends south into the Panhandle of Texas, Beaver 

Creek flows across Beaver County from end to end. Both of the 

streams have carved valleys averaging 150 feet in depth and 3 miles 

in width, and tributary creeks are now at work dissecting the high 

table, but at the present time have scarcely more than commenced 

their task. Such creeks as Duckpond, Clear, Palo Duro, Coldwater, and others emptying into Beaver Creek from the south have 

their rise in Tertiary springs and are practically perennial streams.

With the exception of small areas of reel beds along the south bank 

of the larger streams and some outcrops of Cretaceous rocks, particularly in.the extreme western part of the county, practically all the 

surface rocks of Beaver County consist of formations of Tertiary 

age, which form a deposit sometimes as much as 400 feet thick above 

the subjacent red betls. Along the streams these Tertiary rocks have 

been weathered away and form sand hills, but on the uplands the 

surface is hard and firm.

Water supply. Beaver County has good water. Wells on the 

upland rarely fail to obtain an ample supply of pure, wholesome 

water, although the depth of the well, often from 100 to 250 feet, 

renders the water difficult to draw; accordingly windmills are in 

almost universal use, both on ranches and near farm houses. There 

are a few places along the south side of Beaver and Cimarron where 

water is obtained in the red beds, but this is uncommon.

Springs are found in Beaver County usually issuing from Tertiary 

rocks, and as is the usual case the water from these springs is always 

good. Beaver Creek and its tributaries, perennial streams, are fed 

by springs from the Tertiary.

In the Dakota sandstone region, in the western part of the county, 

there are both wells and springs which furnish soft water, although 

the Dakota in this region does not supply as much water as in Kansas and Nebraska. Analyses Nos. 1 and 2 are of water from wells 

in Beaver County.

Weft records. Of 29 wells reported from Beaver County 19 furnish 

soft water and 10 hard water. The average depth is 110 feet. The
IRRIGATION FROM RIVERS. 133

varying character of the water conditions is shown by the 10 well 

records on page 15G.

IRRIGATION.

GENERAL STATEMENT.

Irrigation in Oklahoma has met with considerable indifference, or 

even open opposition, on the part of many of the people. The western 

part of the Territory, in which irrigation is most needed, has been 

settled mainly during the last five years, and in that time the rainfall 

has been greater than the average, and the crops have been abundant. 

There is a general impression that an acknowledgment that irrigation is needed will be detrimental to the interests of the Territory, and 

for this reason in many places the matter has usually met with a cold 

reception. During the last few months, however, public opinion has 

in a large measure undergone a change, and communities that formerly scouted the idea are now asking how such operations may be 

brought about.

In Oklahoma water for irrigation may be obtained from rivers, 

from reservoirs, from springs, and from wells. These various sources 

will be discussed in the order named.

IRRIGATION FROM RIVERS.

As has been stated in another part of this report, seven rivers flow 

southeast across Oklahoma, but for the greater part of the year many 

of these streams carry comparatively little water. Most of them also 

have sandy banks, and for that reason ditches leading across the bottom lands would lose much of their water by seepage or would soon 

become sand choked. In a number of places where dams have been 

thrown across small streams and the channel diverted into ditches it 

is necessary to remove the silt from the ditch every few months or to 

construct a new one, but in other cases where there is no sand to 

obstruct the ditch it remains open from year to year.

It must be remembered also that while the normal flow of Oklahoma streams is not great, they are all subject to sudden and rapid 

rises. The South Canadian, Red, and Cimarron rivers, in particular, 

often rise 10 feet or more in an hour and remain bank-full for several 

days, when the water gradually subsides and the channel may be practically dry for weeks. These sudden rises are often sufficient to tear 

out any dams such as have heretofore been constructed. On account 

of the broad and shallow valleys, the depth to bed rock, and the scarcity of building material, masonry dams are practically unknown, 

and those constructed have been of piling, plank, logs, loose rock, 

earth, brush, etc. (See PI. XXI, B.)

Along Cimarron River and Beaver Creek, both of which are sand-
134 GEOLOGY AND WATER RESOURCES OP OKLAHOMA.

filled, and often sand-choked, irrigation has been carried on for a 

number of years. These streams have both been carved out of the 

level Tertiary upland, and both have in many places cut entirely 

through this surface formation into the subjacent red beds. Along 

Beaver Creek the red beds occur almost continuously on the south 

bank of the stream as far west as the mouth of Palo Duro Creek, 

while on the north side of the creek there are sand hills which extend 

5 to 10 miles from the river. In other words, iu eastern Beaver 

County are exhibited the phenomena so often observed along the 

rivers farther east, viz, a strip of sand hills north of the stream 

and a row of red beds canyons south of it. The amount of water 

in Beaver Creek varies greatly at different points and at different 

times of the year, so that any estimates as to amount of flow, unless 

based on data collected through a series of years, would be misleading. Such tributaries as Kiowa, Coldwater, and Palo Duro carry 

nearly as much water as the main stream afe the point where they 

join Beaver Creek.

There are numerous small irrigation plants all along the streams 

of Beaver County, where rude dams of logs, earth, or loose rock 

have been built across the creeks and the water diverted from the 

channel and carried out over the bottoms to irrigate small fields and 

gardens. In times of flood these frail structures are washed out 

and often not rebuilt for several months. One of the better class 

of stone dams was washed out during the flood in May, 1903, and 

had not been rebuilt the following August. It is safe to estimate 

that at least one dam is present every 5 miles along Beaver and its 

larger tributaries as far west as Guymon. It is the universal testimony of persons living along the stream that the water taken out 

for irrigation does not sensibly diminish the flow, and the explanation given is that springs come in all along the bed of the stream. 

It is very probable, however, that this is due largely to the fact 

that much of the water seeps back into the channel and the stream 

is thereby replenished.

The character of Cimarron River in Beaver County does not differ 

from that of Beaver Creek. Both these streams have cut channels 

into Tertiary rocks, and in places into the red beds below, and both 

are fed at least in part by Tertiary springs.

The most successful irrigation plant in this region is just across 

the Kansas line near Englewood, Clark County, Kans., but the water 

comes from the Cimarron, in Oklahoma. The following description of this plant is taken from the report of Mr. W. G. Russell: °

The principal irrigation development in this part of the country has been 

carried on by C. D. Perry, of Englewood, Kans. About fourteen years ago he 

constructed a ditch from the Cimarron River to irrigate his lands in Kansas.

« Russell, W. G., First Ann. Rept. Reel. Service, U. S. Geol. Survey, 1903, p. 271.
IRRIGATION FROM RIVERS AND RESERVOIRS. 135

He built a sheet pile dani across the channel, consisting of 2-inch piling driven 

to a depth of about 12 feet in the sand. The tops were held in line by two 

walings fastened with three-eighth inch bolts through the piling and both strips. 

This ditch was 8i miles long and had a capacity of about 14 second-feet. It 

was not well built and was difficult to maintain. The total cost was nearly 

$10,000. The floods tore out a considerable portion of the dam, filled the channel with sand, and made a new channel, passing around the remains of the 

dam.

A new ditch was built by Mr. Perry, with head-gates lower down the stream. 

Instead of a dam for diverting the water, he constructed a wooden stave pipe, 

30 inches in diameter, sunk in the sand, extending from the headworks diagonally upstream. This was 900 feet long and was planned to extend a mile or 

more. The underside of the pipe had perforations through galvanized sheet 

iron, intended to admit the water. The pipe was partly washed out before it 

was tested and the remaining portion filled with sand. Water was obtained, 

however, through a ditch heading at a brush dam below the pipe. The ditch 

now in operation is 7 miles long and cost nearly $3,000, including the wooden 

stave pipe. It is successful and discharges at the lower end into the old ditch. 

Experiments for obtaining the so-called " underflow " could probably be made at 

this locality with good chances for success.

Between Englewood, Kans., and Kenton, Okla., are a numbewiof 

small plants where water is taken from the river by means of dams 

of stone, earth, or logs, and west of Kenton practically all the water 

is taken from the Cimarron and its tributary creeks and used for 

irrigation. PL XXI, Z?, shows a log-and-earth dam'on the upper 

Cimarron.

Along Wolf Creek, in Woodward County, and certain branches of 

Washita" and Red rivers small irrigation plants have been erected 

from time to time, but the same conditions exist as in Beaver County, 

and the temporary dams are usually washed out by every flood, and 

no great importance can be attached to these irrigation systems.

One fact regarding irrigation from Oklahoma rivers remains to be 

mentioned, namely, the character of the water. Cimarron, Salt Fork, 

and North Fork of Red River drain regions of salt springs which 

render the water too salty to be of any use for irrigating purposes. 

Salt Fork crosses the Great Salt Plain in eastern Woods County, 

and below that point its waters contain a considerable percentage of 

salt. Cimarron River flows through two salt plains in northern 

Woodward County and receives the drainage of the Blaine County 

salt plain. The salt plains of Roger Mills and Greer counties are 

drained by North Fork of Red River, and the water of that stream 

below the mouth of Elm Fork is very salty. Besides the cases mentioned, the water of the other Oklahoma streams is suitable for 

irrigation.

IRRIGATION FROM RESERVOIRS.

The greatest difficulty in the construction of large reservoirs in 

Oklahoma is that so few available sites exist. All of the larger
136 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

streams of the Territory flow for practically all their course through 

broad and shallow sand-filled channels. There are a comparatively 

few localities where streams flow through narrow gorges and masonry 

dams might be constructed. Of these localities the most satisfactory that have so far been examined are located in the Wichita Mountains. In October, 1903, the writer, in company with Mr. Bailey 

Willis, of the United States Geological Survey, visited the most 

available of the sites in these mountains. The following descriptions 

are from Mr. Willis's report:

MEDICINE BLUFF SITE.*1

In sec. 7, T. 3 N., R. 12 W., the valley of Medicine Bluff Creek is an extensive 

bottom land, approximately from 1 to 1* miles wide GO feet above the stream 

level. The stream itself has moderate fall. Near the south line of the section 

the valley narrows to a canyon 75 feet deep and 400 feet wide between steep 

walls. Beneath the wider valley the rock is rather impervious red shale and 

sandstone; in the canyon it is granite, more or less jointed, but forming a fairly 

solid mass, suitable for the foundations of the dam. The stream in the canyon 

runs on bed rock.

The drainage area tributary t'o this site is estimated from the map at about 

90 square miles. The waters from the reservoir might be conveyed a distance of 10 miles down the valley to Fort Sill and thence over the prairie lands 

in the vicinity of Lawton. The height of the dam site above Lawton is 200 

feet, and the water would be available upon the highest prairies of the neighborhood.

The value of this reservoir site is limited by the small area tributary to it. 

Medicine Bluff has the reputation of being a comparatively constant stream 

for the region; but from field observation, without measurement, it would 

appear probable that the greater part of its flow throughout the year could be 

stored without utilizing the entire capacity of the reservoir site.

The waters from Medicine Bluff Creek flow largely from granite slopes and 

so far as they are derived from other rocks are not contaminated by gypsum 

or alkali.

LOWER NARROWS OF OTTER CREEK.6

In sec. 9, T. 3 N., R. 17 W., several branches of Otter Creek assemble in a 

usually flat valley, and the combined stream enters a canyon about 200 feet 

wide and approximately 100 feet deep, with nearly vertical walls. The conditions are the same as those already described on Medicine Bluff, except that 

the valley above the canyon is much broader and shallower and the canyon 

is narrower. It is estimated from the map that the drainage area of Otter 

Creek tributary to this reservoir site is about 125 square miles. Surveys have 

been made by the Otter Creek Irrigation Company on the basis of a dam 60 

feet in height, constructed to throw the water over the lowest point into the 

divide on the southeast, and according to Mr. Mark Roberts, the originator of 

the plan, the area included within the contour at a level of the top of the 60- 

foot dam is 6,000 acres, and the average depth of water in the reservoir would 

be about 20 feet. Aneroid readings appear to agree fairly well with Mr.

« First Ann. Rept. Reel. Service, U. S. Geol. Survey, 1903, p. 267. 

"Op. cit., p. 268.
IRRIGATION FROM RESERVOIRS. 137

Roberts's statements of the position of the outline of the reservoir, at least 

along the route by which it was crossed.

The area to be irrigated by the water which may be thus stored lies south of 

Mountain Park, on the lower course of Otter Creek and along Red River. The 

area of agricultural lands available is probably more than can be supplied by 

the drainage basin, which it is proposed to utilize, and the capacity of the 

reservoir also is probably sufficient to hold the water that can be stored from 

that basin.

. The waters of Otter Creek flow in part from hills of igneous rock, but in 

greater part from areas of red beds. They do not, however, contain any notable 

quantity of gypsuru or alkali.

QUARTZ MOUNTAIN SITE."

North Fork of Red River is .joined in T. 5 N., R. 20 W., by a very considerable 

stream known as " Elm Fork," the waters of which contain a large amount of 

gypsum and probably of other salts. Any irrigation plan contemplating the 

use of the waters of North Fork of Red River should exclude those of Elm Fork 

on this account. Above its junction with Elm Fork, North Fork of Red River 

flows from a valley in the red beds across a small area of granite in the east 

end of Quartz Mountain. The narrowest point of the short canyon which is thus 

formed in the eastern part of .sec. 22, T. 5 N., R. 20 W., and the wider valley 

above the canyon occupies sections 14 and 15. The canyon has a minimum 

width at water level of 500 feet. The depth to granite in the bottom land is 

indeterminate. Fence posts are sunk in red and green clays of the red beds 

just below the narrowest part, and it may be inferred that the granite is not 

near the surface, even at the dam site; but the shales and sandstones of the 

red beds would probably afford an equally substantial foundation. It was stated 

that even when the river bed is otherwise dry there is always a pool of water 

next to the granite at the dam site, and this would seem to indicate that the 

underflow was brought to the surface by ledges of rock. About 200 yards 

west of the canyon there is a depression in the granite ridge 80 feet above the 

river, and this would limit the depth of the reservoir unless a supplementary 

dani were placed in that gap. The gap is narrow and could be easily controlled 

by closing it with the dam or by utilizing it as waste way. A dam 80 feet high 

would back the water up the valley of Red River for many miles, and would 

constitute a reservoir of very large proportions. The foundations and walls at 

the dam site appear to be adequate for any such construction.

The drainage basin of Red River tributary to this site is roughly estimated 

at 3,000 square miles. The quality of water, even in the autumn season, is good, 

although slightly saline to the taste. The water from this site could most 

easily be conducted across Elm Fork and southwestward into Greer County. 

The Otter Creek Irrigation Company proposes, however, to divert at least the 

flood waters to a canal extending east from the above-described dam site to 

Tepee Creek, and thence across to Elk Creek, by a deep cut in the divide, to 

the basin of Otter Creek. Surveys for this purpose were contemplated late in 

October. 6

«0p. cit, p. 268.

6 Since the above was written Mr. Gerard H. Matthes and other engineers of the 

Reclamation Service have pursued extensive Investigations on the Wlchita Mouatain 

reservoir sites. The results of their work will be found in Second Ann. Kept. Reel. 

Service, U. S. Geol. Survey, 1904, pp. 412, 423.
138 . GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

PL XVIII, JL, shows the location of the dam site at Quartz Mountain. .

CIMAKKON RIVER SITE.

On the Cimarron River, in northeastern Beayer County, Mr. W. G. 

Russell describes a reservoir site as follows: a

A suggested opportunity for construction of storage works has been pointed 

out in sec. 32, T. 5 N., R. 6 E. of the Cimarron meridian. The river at this 

point passes a bluff 30 feet or more high. To the south the overflowed bottom 

is about one-half mile wide, and to the north the ground rises gradually for 

a quarter of a mile before gaining the height of the south bluff. A dam 30 

feet above the river would measure about one-half mile in length, and onelourth mile additional would be required to complete it on the north slope. 

The bottom lands increase in width above the dam site, and the fall of the 

rfver being approximately 8 feet to the mile, it is estimated that a reservoir 

could be created about 3.5 miles long by 1 mile wide, having a capacity in 

round numbers of 35,000 acre-feet. A survey has not been made, but these 

figures are given from inspection of the ground. It is believed that the flow of 

the Cimarron River is sufficient to fill this reservoir. Below it are lands 

bituated on both sides of the river. It is claimed that there is an impervious 

clay lying only a few feet below the bed of the river upon which a dam could 

be formed. A structure placed at this point must be built presumably of 

earth, as there is little rock in sight. On the tops of the bluffs, about 300 feet 

above the river, are fragments of a porous limestone, which may be used in 

concrete or for revetment on the slopes.

The construction of a dani across the Cimarron, in Beaver County, is a 

difficult undertaking, and one which must be given careful consideration. 

Little can be known without expensive surveys and borings to ascertain the 

character of the foundations and the proper material to be used in the structure.

UTILIZATION OF STORM WATERS.

In addition to the sites mentioned, all of which are located on rivers, 

there are in western Oklahoma hundreds of places where small dams 

might be thrown across small watercourses, draws, or arroyos, forming a reservoir for the storing of storm waters. In many instances, 

such reservoirs could be so located as to irrigate many acres of fertile 

land now too dry to yield satisfactory crops.

Some of the difficulties are, first, relatively small amounts of rainfall ; second, the great evaporation, and third, sandy character of the 

soil. The rainfall of Beaver County varies from 20 inches in the 

eastern part to less than 10 inches near the New Mexico line. The 

greater part of this precipitation usually falls during a few neavy 

downpours, amounting often to cloud-bursts, while for months at a 

times almost no rain will fall. A difficulty, of course, is that after a 

heavy rain, any but the most strongly constructed dams will be washed 

out.

There are few data available as to the amount of evaporation in tho

"Op. cit., p. 271.
IREIGATIOK FROM SPRING^. 189

region under discussion, but it amounts to at least 6 feet per year in 

the western portion of the Territory. As stated by Johnson and 

others, there are large areas where there is practically no run-off, the 

drainage flowing down shallow draws into playa lakes. Areas of 

many square miles are as flat and level as a floor, and the water that 

falls remains on the surface of the ground until it is evaporated.

In a region of this kind, with high summer temperature and almost 

constant wind, it would be expected that a large proportion of water 

collected in reservoirs would soon be evaporated. Lakes on the Plains 

usually go dry during the summer, and the same conditions obtain 

in artificial reservoirs, except that these can be made of sufficient 

depth to provide a surplus of water beyond the evaporation.

Much of the soil in this region is sandy, particularly along the 

streams where reservoirs must usually be constructed. In the sandhill districts there is practically no run-off; the water is either 

evaporated or soaks into the soil, and it goes without saying that it 

is useless to locate a reservoir in such a locality.

Notwithstanding the objections cited in the preceding paragraphs, 

however, there are plenty of places in central and western Oklahoma 

where a reservoir a few acres in extent might be profitably constructed which would afford useful water storage. The writer does 

not venture an opinion as to whether such projects would be profitable. The problem is one, however, that should be carefully investigated.

IRRIGATION FROM SPRINGS.

At best, irrigation from springs can be but local, on account of the 

relatively small amount of water supplied from even the strongest. 

Of the various classes of springs in Oklahoma, the water from red 

beds and Tertiary springs only is used for purposes of irrigation'; 

in by far the greater number of instances a Tertiary spring is so 

used. As has been stated in another part of this report, the supply 

from these springs is practically inexhaustible, the amount from a 

single one often approximating several second-feet. The quality 

of the water leaves little to be desired, being usually pure, sweet, and 

free from mineral salts. The chief difficulties in the way of irrigation from these springs are those of location. Tertiary springs 

issue almost invaribly along the line of unconformity between the 

red beds below and the Tertiary above, as shown in figs. 29 and 30, 

and usually in a canyon or along a bluff where the country below is 

so rough and broken that in most cases the water can not be utilized. 

In a number of instances, however, the water from one of these 

springs is led out over a garden or orchard. The table given herewith (p. 140) sets forth the location of areas irrigated from springs 

so far as ascertained by the writer.
140 GEOLOGY AND WATER RESOURCES OP OKLAHOMA.

Water from Tertiary springs is utilized in another way, namely, 

as a source of city supply. At Alva the water from Elm Spring, 

3 miles away, is carried in a pipe by gravity to the north part of the 

city, and then forced by a pump into the water mains and carried to 

all sections of the city. Old Fort Supply obtains its water from a 

Tertiary spring 3 miles away across Beaver Creek, the water being 

carried in a 6-inch main. Woodward, Grand, Beaver, and other 

county seats in the western part of the Territory are supplied either 

from Tertiary wells or Tertiary springs.

Irrigation from springs in Oklahoma.

Name of owner.

W.E. Miller.. . ..........

Jacob Eckart... --------

S. A. Pollock.-. .........

J.E.Fitzlin .............

L.F.LaBrue ...........

M. L. Bodenheimer

F.M.Matthews.........

M.L.GKtffey ........_...

C.N.Jett.. .... 

Do.........

Township.

35

24

22

23

23

28

28

27

27

25

22

27

27

17

25

25

Range.

1W.

16W.

21 W.

21 W

21 W

14 W.

14 W.

9 W.

8 W.

10W. 

10W.

9W.

Q W

4W.

9W.

10W.

Section.

13

2

4

14

4

8

35

9

20

9 

15

33

6

36

Irrigation 

section.

SW.

NE.

NE.

NE.

SW.

NW.

SW.

SE.

NE.

NE.

<sw

NE.

NW.

NE.

Kind.

..._.do_...

_ .do_.__

__._.do_._.

_....do....

___..do_.._

.....do. 

____.do____

.. ...do -

Red bed. _

.....do--..

__.__do_.__

Red bed..

.....do....

.....do---.

Acres.

3

5

10

3

12

1

3

12

9

6

12

Crops irrigated.

Garden.

Orchard.

IRRIGATION FROM WELLS.

In a great part of western Oklahoma there is sufficient underground 

water, if it were brought to the surface, to irrigate considerable areas. 

The difficulty here is that no cheap method has yet been devised 

whereby sufficient underground water may be elevated from considerable depths to be of practicable importance. Windmills seem to furnish the simplest solution of the problem, and considerable literature 

has already accumulated on the subject.0 PL XV gives types of 

Oklahoma windmills.

In western Oklahoma a great part of the water lies at depths of 100

" For a discussion of the relation of windmills to water supply the reader is referred 

to the following numbers of the Water-Supply and Irrigation Papers of the U. S. Geological Survey :

No. 1. P.umping water for irrigation, Herbert M. Wilson, 1896.

No. 8. Windmills for irrigation, C. E. Murphy, 1897.

No. 14. New tests of certain pumps and water lifts used in irrigation, O. P. Hood, 1898.

No. 20. Experiments with windmills, T. O. Perry, 1899.

 No. 29. Wells and windmills in Nebraska, E. H. Barbour, 1899.

Nos. 41 and 42. The windmill, its efficiency acid economic use, E. C. Murphy, 1901.
CLIMATE. 141

to 400 feet, and windmills have so far proved inadequate to the task 

of lifting sufficient quantities of water for irrigation purposes. 

Farms and ranches are supplied by windmills, and in certain parts of 

Oklahoma to-day lone windmills are the only signs of civilization, 

but in most cases all efforts to secure a greater supply of water than 

is necessary for stock and domestic purposes has proved a failure. 

The problem is one that deserves attention and which may in Jame 

yield practical results.

CLIMATE.

Eastern Oklahoma lies in the humid, western Oklahoma in" the 

semiarid, and extreme western Beaver County in the arid belt of the

FIG. 31. Map showing the arid, semiarid, and humid regions of the United States.

United States, as these belts are usually demarked (see fig. 31). In 

the Osage Nation and the eastern tier of counties the annual precipitation for the last ten years has averaged about 35 inches. In central 

Oklahoma during the same time the average Has been 30 inches, along 

the western line, exclusive of Beaver County, 25 inches, and in the 

western part of this county the annual rainfall has not exceeded 15 

inches (see fig. 32).

In the eastern part of the Territory the rainfall is not only more 

abundant, but it is also more evenly distributed. As a general thing 

rain falls during every month, but on the average there are more than 

]T5 clear days in the year, while days with 0.1 inch precipitation will 

not average more than 70 each year. On the high plains the precipitation is neither regular nor abundant. For months at a time 

there may be practically no rainfall, when, again, during a heavy
142 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

storm, often amounting to a cloud-burst, a level plain will be covered with several inches of water.

FIG. 32. Map showing the mean annual rainfall of the United States.

The mean annual temperature for ten years has been 59°, varying 

from 55° in Beaver County to 62° in Comanche. The winters are 

mild and the heat of the summers tempered by almost constant 

breezes.

WATER ANALYSES.

METHOD.

The calcium oxide, magnesium oxide, sulphuric anhydride, chlorine, and solid residue are determined in the usual way, using Cheever 

and Smith, Sutton, Cairns, and Mason as guides. The carbon dioxide 

is not estimated, but is calculated by differences.

In general, in this report, the metals in their combination with the 

acids are taken in the following order: Calcium, magnesium, sodium.

In their combination with the metals the acids are taken in order 

as follows: Sulphuric acid, hydrochloric acid, carbonic acid.

These combinations are only hypothetical, yet they can not fail to 

give a better idea of the constituents of the water, and it is merely 

for this purpose that such combinations have been made.

DEFINITION OF TERMS.

That the general reader may more readily understand the analyses 

given below, the following definitions and explanations of terms are 

given:

Grains per gallon. The number of grains per United States gallon 

are determined from the parts per million on the basis that " 1 United
COMPARISON OP RED-BEDS WELLS. 143

States gallon of pure water at 60° F., weighed in air at 60° F. at 

atmospheric pressure of 30 inches of mercury, weighs 58,334.946 

grams." °

Commo-n names. Calcium sulphate is gypsum, and in its dried 

form is commonly known as plaster of Paris; calcium carbonate is 

limestone; magnesium sulphate is Epsom salt; sodium sulphate is 

Glauber's salt; sodium chloride is common salt; sodium bicarbonate 

is common baking soda. All the remaining salts occurring in the 

analyses have no common names.

' COMPARISON OP RED-BEDS WELLS.

To show the great variations in the supply and quality of waters 

from the red beds, even in the same locality, eight wells within a 

radius of two blocks in the city of Norman, Okla., have been taken 

as an example.

Comparative table showing variation of red-beds waters. 

[Parts per million.]

Sample 

No.

8-..---.

9.......

10-..___.

11, _____

12.......

13.......

14

How put 

down.

Dug ....

_.._do_.-

Drilled..

_.__do.._

Dug ....

,-._do __.

....do ...

--,_do ...

Kind of rock.

Bed beds _

.____do ....

____.do __._

_.__-do ....

...__do ....

.....do ....

_____do ....

-.-..do ....

Total 

depth.

Feet.

28

30

50

20

23

25

23

24

Depth 

to 

water.

Feet. 

12

25

14

16

14*

21

21

21

Depth 

of 

water

Feet. 

16

5

36

4

8*

4

2

3

Variation of 

water depth at 

different times 

of year.

None ....,-.

None _____ .

.....do ..---.

___._do .....

.....do ---_--

Amount of water.

lowered 

Do.

Do.

lowered.

lowered. 

Do.

Quite easily

lowered. 

Do.

Sample No.

8__. .... ...

9 .. ......... 

10..--..... --

11 ............

12

13 ............

14_____. ______

Calcium 

oxide.

115.0

122.0

242.0 

152. 0

53.0

174.0

137.0

137. 0

Magnesium 

oxide.

9.'0

60.0

220.0 

139.0

43.0

96.0

96.0

63.0

Sulphuric 

anhydride.

271.0

256.0

1,129.0 

709.0

68.0

236.0

58.0

50.0

Chlorine.

160.0

60.5

1,185.0 

750.0

33.0

104.0

89.5

54.5

Total residue.

945.0

621.0

4, 365. 0 

2, 980. 0

572.0

1,099.0

856.0

641.0

Normal 

hardness.

58.5

53.3

1.3 

. 3.9

9.6

14.3

11.7

14.3

Carbon 

dioxide.

146.0

121.8

147.0

124. 0

146.0

170. 0

130.0

Mason's Examination of Water, 2d ed., 1901, p. 93.
144 GEOLOGY AND WATER EESOTJRCES OP OKLAHOMA.

The wells selected are Nos. 7 to 14, inclusive, in the general report 

of analyses.

Sample No. 7 is a dug well, 28 feet in depth. In this the depth of 

water is 1C feet. No. 8, less than a block from No. T, is 30 feet in 

depth and has but 5 feet of water. The supply of water in both is 

practically constant the year around and is. not easily lowered by 

excessive use. In calcium oxide, sulphuric anhydride, normal hardness, and carbon dioxide Nos. 7 and 8 differ but slightly. However, 

in magnesium oxide No. 7 is very low and No. 8 is comparatively 

high, while No. T greatly exceeds No. 8 in chlorine and total solid 

residue. These differences are remarkable because the geologic and 

sanitary surroundings of the wells are apparently the same.

Nos. 10 and 11 also make an interesting comparison. No. 10 is 20 

feet deep, varies but slightly in water depth at different times of the 

year and is easily lowered by excessive use. No. 11, distant from No. 

10 by but a little more than the width of a street, is 23 feet deep, 

contains 8^ feet of water, varies considerably in water depth at different times of the year, and is not easily lowered by excessive use. 

With a difference of but 3 feet in depth, and so close together, the 

difference in the amount of water constituents is worthy of notice. 

In No. 10 the calcium oxide, magnesium oxide, and solid residue are 

about five times that of No. 11, while the sulphuric anhydride is 

about ten times and the chlorine twenty-five times as much. The 

normal hardness of each is small, but that of No. 11 is more than 

twice that of No. 10, which has no carbon dioxide as carbonates, 

while No. 11 has a fairly large amount. It might be noted here that 

No. 11 runs lower in nearly all the tests than any other water taken 

for comparison.

In the same block with No. 11 are wells Nos. 12, 13, and 14, occurring in the order given. The width of the two lots separates wells 

No. 11 and No. 12. The depths of these wells are practically the same, 

yet in No. 12 the solid constituents greatly exceed in amount those of 

No. 11, running especially high, comparatively, in calcium oxide, 

sulphuric anhydride, chlorine, and solid residue. Wells Nos. 12 

and 13 are separated by about the width of one lot and differ by but 

2 feet in depth. In No. 13 the calcium oxide, chlorine, solid residue, 

and normal hardness are but slightly less than in No. 12; the magnesium oxide is the same in both; the carbon dioxide in No. 13 is 

higher than in No. 12; but the most noticeable difference is that of 

the sulphuric anhydride, which in No. ] 3 is but about one-fourth of 

that in No. 12. No. 14 differs but little from Nos. 11 and 13.

All of the wells so far compared have been between 20 and 30 feet 

in depth. It may therefore be of interest to include one deeper well. 

For this comparison No. 9 will answer the purpose. Both No. 9 and
COMPARISON OF BED-BEDS WELLS. 145

No. 10 are on the same lot, about 40 feet apart. No. 9 is a drilled 

well 50 feet in depth and contains 36 feet of water. It might be well 

to note in this connection that good water was struck at 14 feet and 

at a depth of 40 feet salt water was encountered. This lower stream 

of water has rendered the well altogether unsuitable for drinking 

purposes. In this water the calcium and magnesium oxides are considerably higher than in any other of the waters taken for comparison, while the sulphuric anhydride, chlorine, and solid residue are 

excessively high.

All other deep-well waters from this section of the country which 

have been analyzed have, like No. 9, run exceedingly high in sulphuric anhydride, chlorine, and solid residue. These deep-well 

waters also vary greatly, although perhaps not so noticeably as the 

waters from the shallower wells.

The wells used in the above comparison may be considered as 

typical of all the wells having their origin in the red beds. For general domestic purposes the shallow wells are the'more satisfactory, although few of these contain water which can be classed as really 

good. In short, the red beds make a poor and unreliable source of 

water supply.

IEE 148 05 M 10
If- 3> 

Norman

addition.... lot Elmwood 10,

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addition. .... lot Elmwood 4,

addition Elmwood lot6,

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in head south acanyon, Ferguson, 

..............._-........ of Salt Creek 

Caddo County: 

of ........ south Anadarko, brickyard 

Cleveland County: 

LarslTs lotblock addi- 8, 10,Norman, 

?

Number. | 1 i- s 

Beaver County: 

106. ....... block ........ lot Beaver, 14,

............... on square Guyman, city

Blaine County: 

at Elevator Mill and Geary,eary 

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Location.

(CaO). oxide Calcium 

oxide Magnesium 

(MgO).

anhydride Sulphuric 

). 3 (S0

(CD. Chlorine 

residue. solid Total 

(CO»). dioxide Carbon 

sulphate Calcium 

). 4 (CaSO

chloride Calcium 

). a <CaCl

carbon- Calcium 

). 3 (CaCO ate 

- 1 u s Magnesium 

). 4 (MgSO phate 

chlo- Magnesium 

(MgClo). ride 

- r a c Magnesium 

). 3 (MgCO bonate 

sulphate Sodium 

>. 4 (Na»SO

chloride Sodium 

(NaCl).

carbonate Sodium 

). 3 CNa»CO

bicarbon- Sodium 

(.NaHCOg). ate 

combination ofconstituents. Supposed 

9tl QJSCV saoaaosaa
16

17 

18 

19

20

21 

23 

23

24

25 

26

27 

28

29

30 

31 

32

33 

34 

35 

36

37

38

39

40

41 

42 

43

Norman, SE. i sec. 32, T. 9 N., B. 3 W. 

Norman, old city well.... ..............

Norman, at oil mill............ .........

Norman, SE. J sec. 19, T. 9 N., B. 2 W.

Norman, SW. t sec. 24, T. 9 N., B'. 3 W.

Norman, NW. J sec. 31, T. 9 N., B. 3 W. 

Norman, on university campus .-_....

Box, NE. J- sec. 25, T. 6 N., B. 1 E ..... 

Noble, lot 9, block 39 ...................

Comanche County: 

Madden, sec. 20, T. 2 S., B. 19 W.......

Madden, sec. 19, T. 3 S., B. 19 W.......

Madden, sec. 20, T. 2S., B. 19 W. ......

Lawton, SW. i sec. 29, T. 2 N., B. 11 W.

Lawton, NW. J sec. 29, T. 2 N., B. 11 

W., Indian school ...... ..............

Lawton, SW. i sec. 20, T. 2 N., B. 11 W_ 

Fort Sill, at Bock Island depot . .

Lawton, N. i sec. 14, T. 2 N., R. 12 W_.

Lawton, lot 3, block 5, Beal addition .. 

Lawton, lot 3, block 6 ............

Lawton, lot 16, block 4 .__.......,......

Lawton, lot 1, block 13 .........

Dewey County :

Taloga, 13 miles east and 1 mile south.

Garfield County : 

Enid, test well for city supply........

Grant County : 

Pond Creek, 1 mile east................

Pond Creek, at Bock Island depot. . . . .

Kay County: 

Newkirk, lot 19, block 4................

Newkirk, block 50.... ..................

Newkirk, NE. i sec. 6, T. 28 N., R. 2 E.

2 7 

1.7 

3.9

5.3

4.8 

4.0 

.3 

6.2

23.4 

60.9 

14.1 

7.6

6.1

4.2 

9.0 

3.2

5.8 

8.0 

4.4 

5.2

6.3

6. 7

6.5 

6.0

10.0 

5.3 

10.9

1.8 

1.5 

4.3 

3.3

3.1

3.4

2.7 

1.1 

4.2

3. 7 

8.9 

3.9

O K

1 3

1.7 

1.6 

1. 7

2.0 

. 7 

.9 

2.6

.4

2.6

5.6 

3.97

3.6 

3.3 

3.7

9.7 

54.5 

93.7 

28 0

96.4

81.1 

89.2 

3.0 

3.6

18.3 

65.6 

7.0 

5.6

3. 7

4.9 

9.98 

8.9

3.3 

3.0 

3.5 

5.6

.1

2.8

4.0 

12.4

4.2 

3.7 

14.6

5.4 

3.4

8.8 

12.6

2.5

4.7 

3.3 

.6 

3.7

37.2 

94.5 

15.3 

.9

1.6 

3. 7 

1.3 

21 2

1.1 

3.4 

8.8 

5.9

1.3

3 2

34.7 

25.7

13.3 

3.2 

.4

31.5 

114.2 

183.3 

71.0

173.0

149.4 

161.7 

6.8 

30.97

158.3 

338.3 

73.4 

33.9

33.4 

33.4 

30.3 

54.5

26.4 

'.27.1

<0 « 43.7 

40.3

17.96

24.4

88.1 

89.5

41.6

27.4 

47.3

3.5

29.6 

2.96 

2.8

.0

.0 

.0 

.9 

9.3

11.6 

20.4 

11.3 

6.2

12.1 

9.6 

5.7 

2.5

9.8 

8.3 

11.8 

11.3

4.9

7.3

8.3 

6.8

10.2 

7.3 

6.4

« Not determined.

4.0

9.5

6.8

12.9

11.8

9.8

6.1

31.1

111.6

11.9

9.5

6.3

8.3

16.95

7.7

5.7

5.1

5. 95

9.5

11 2

4.8

7.1

6.2

24.9
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sec. .. NE. T.23 $ N.,B.2E Bedrock, 25,1 21sec. T. BW.NW.± N., Perry,22, 

Oklahoma County: 

Choctaw ltblock 28.-.-..---.. City, 8,

SW. 23,T.12 N.,B.1E. Jsec. Sweeney, 

sec. T. 12Oklahoma NE.i4,N., City, E.4W ................................ ||

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O5

^

j. g I 

CO IB i i M i i ii i 

OS CO OS 

to If CO 

CO OS Mi i 1 = 

If-

-i

to

GO 

Q5

GC

GC

CO

M co co to 

O OS OS OS 

Gc to en 1 i 

CO If. CO KJ 

OS ' h- f. 

jf- e» T-T CO ^i 

CD CO -^ in ' l 

M ' h- *-» CO 

O 05 -1 CO 

to

1 h- 

; ; ; ; 

Number.

Location.

(CaO). oxide Calcium 

oxide Magnesium 

(MgO).

anhydride Sulphuric 

). 3 (SO

(CD. Chlorine 

residue. solid Total 

). 2 (CO dioxide Carbon 

sulphate Calcium 

(CaSO<).

chloride Calcium 

(CaClo).

carbon- Calcium 

). 3 (CaCO ate 

sul- Magnesium 

). 4 (MgSO phate 

chlo- Magnesium 

(MgCL). ride 

- r a c Magnesium 

). 3 (MgCO bonate 

sulphate Sodium 

). 4 (NaoSO

chloride Sodium 

(NaCl).

carbonate Sodium 

). 3 CO 8 (Na

bicarbon- Sodiitm 

). 3 (NaHCO ate 

of combination constituents. Supposed 

 waters ivellContinued. Oklahoma Analyses of

ADOT:oao OJSLV saoaaosaa £0 VWOHVIMO 
ANALYSES OF WELL WATERS. 149

co ot 1 

oo o» c

m 9.

8 r91

S

CO >O CO 

i-i ' LC5 C§ OC

co I-H o;

IO 00 ~

CD IO CO

91 O5 1-

CC rH *

CO 91 -d

>O -* o:

91 o:

91 91 -*

00 rH CC

£ *$. OS

CO CO

IO CO 1 

CO 1 CC

Do_.... ........................-_ ... City,sec.33,T.12N.,R.3W. Oklahoma 

no ___________. ___ 

5 rH 91 CO 

CO CO CC

i i i

: i i

rH CO 00 t- tf) OC

rH ri 91 t-^ *# iCO O CO free 91 jj CC

1 CO | CS 

i CD i OC

CO rH i 00 '

CO CO ' 91 '

CD CD 

CD

91 91 '

M ^ i

 * 00 ' CO ' 

-* 01 ; 91 ;

1 1 Q_ ' Oi L 

i-i r-i 1 rH to

to CO

Oi Oi Oi »O CC fli IO

t in CO C- 91 CO i 

 * i-H i-H

t- 91 91 CO CO O OC

>O to rH C- 91 CO

-# CD 1- -* >0 CO C

rH rH Q O OS IO 00 91 91 Si t- 91 CO 95

I- 91 CO rH 91 OS 1 

s

CD IO 00 IO CO 91 1-

-* CO CO CO rH 00 CO CD i i

O O! rH 00 CO 00 O

CO 91 rH "O i-H 91

91 CO CD I- CO CO *

CD * rH O CO 00 CD

Countr'. Pawnee 

31 EBlackburn, 1,T.N.,R 6 sec. ...... W. T.EBlackburn, N 30,3. R 7Jsec.N.,R.7E..... Blackburn, 10,23 T.sec. ._ E. SE.Pawnee, 36,R. 4isec............. iniles Jennings, Hwest. ................ N., Valley, NE. T.6E 31 R.14, isec. . 

County: Payne

Cushimr. N..T\TW. seo.5T. IfiR5E__ 4-_

*g >O CO t- 00 O5 O

i X'

; 51

rH 53

5i

^ CH

CJ t--

« s

rH t 

1 i S8O2

i C

t.

» 00

^ "*

' I- i-H

i C- i 

i IO -*

: S

C- 91 91

91 CD CO

CO »O CO

! CO to i-H 

91 JU rH

»O »O I-

-1 s

IO t- 91

IO

rH IO CO

rH 00

1- CD *

91 C5 CO

Stillwater,! mile north.......... ._ Perkins, NE..,14 T7 R.3Eisec. .

I-H 9! CO

t-

;

iC ai 

CO

91

o:

91

CO

S

9

O

C5

91

91

j 

1

S

, i 91 00 Oi

;| & 8

t ir- CO »O ii

rH rH rH 91 | ]

1Q CO -* CO 

i-i r-i t- CO

CO 00 00 1 

o CD c:

91 I CC

I i CC

j

o co 0.0.

CO rH 91 00

rH CO "O

9! rH 1C

00 rH <r_

CO r-i T.

t- * 91 CO CO t- 91

1 -^ O ^J CO iC

-tn to cS rH -n jj co

 « ^ rt 5 S *

i-H »__ i-H »O CD CC Ci

CO 00 »O 3^ 00 O C*" CO i-H i-H t- IO 95 91 91

IO L- Ci 00 »O 91 t91 -* 91 CC

CO CO 91 to 1 91 i-H

 * 91 00 1 00 to CC

 * O O CO 00 i-H i 

" - ?i §. K

CO CO 91 91 CS CR rCO CC * 91 CO OC

NW.Jsec.8,T. N.,R.E. Stillwater, 30 

Pottawatomie County: 

Tecumseh, 12,block lot33 .............. T. 9N.,R3E NW.Pink, 17isec. .... Tecumseh,NW.isec.l8,T.8N.,R.4E. 

Woods County: 

16. Alva, lots and14,3 block ........... lot I, Ament's addition Alva, block ._

»O CD t- 00 Oi O rj i

IO Jj V

1 1 

>o oo c

CC i-i 91

CO i IT

91 | cr

CO ' trH r-

| ^

3D 1 tl-H | CO

CO -!H C

rH rH CC

'. C5

! 05

i

1- CO

10 in CD

»O CO T 

 * rH CO 

CO 91 1C

91 00 CO

O: »O rH

91 r91 00 i 

i-H 1C

CC CD CO

CD 1- t-

'° -------------- ' "" 

and milesCleo, 6inorth___ 9eastwell----....... Cleo, town ...-.-.......-

91 CO *

'00 00 00

1

05

CO 1-H

91

CD

i

1

rH

^

S

CC

IO

-*

s

O5

00 1-H

IO

CCi 

91

tco

co

iS

County: Wooiward 

Wood war.............................

iO 

00
Analyses of Oklahoma stream iva

[Grains per United States gallon.]

1.

EJ

fc

86

87 

88

89 

90 

91

92 

93

94 

95 

96 

97 

98

99 

100

101

Stream.

Salt Fort, above 

Salt Plains.

1 Salt Fork, below 

1 Salt Plains.

Tributaries 

(

of 

Salt Fork.

Cimarron 

I

River, 

above Woodward County 

Salt Plains.

Cimarron Eiver, 

below Woodward County 

Salt Plains.

i

[Tributaries of 

f Cimarron.

Location.

jPond Creek, i mile east .-...

"|At ford south of Ponca 

I School.

Chikaskia 

I

River, west of 

Ponca City. 

Deer Creek, west of Tonkawa.

1 At head of Col. C. D. Perry's 

I ditch.

Waynoka, 4 miles southwest.

Kingfisher, 8 miles north . . .

Per kins, 2£ miles southeast .

Perkins, at crossing south 

of town.

Cleo, at ford south of town .

f Cotton wood Creek, north of 

I Guthrie.

Istillwater Creek, * mile 

1 south of Stillwater.

Calcium oxide(CaO).

33.3

7.9 

17.4

4.8 

6.7 

7.0

7.6 

8.9

24.0 

14.3 

18.1 

14.33 

8.3

16.4 

13.4

8.2

Magnesium, oxide 

(MgO).

5.1

3.3

3.8

1.8

HI. i

3.4

4.3 

1.1

9.7 

5.6 

6.7 

4.9 

1.2

3 7 

5.1

4.5

Sulphuric anhydride 

(SO3).

35.7

34.96 

32 3

4.0 

5.3 

10.1

36.5 

13.4

34.2

31. 7 

13.8 

17.7

7.5

34.4 

17.4

8.6

Chlorine (CD.

6.5

178.5 

286.7

1.8 

9.6 

43.8

3.97 

232.8

355.9 

205.3 

245.7 

316.9 

34.7

236.3 

3.4

4.2

Total solidresidue.

95.3

347.8 

516.2

211.5 

33.7 

103.6

97.7 

420.6

664.5 

385.6 

463.1 

397.3

74. 7

435.9 

61.6

55.1

Carbon dioxide (CO2).

2.1

.6 

3.7 

.9

7.7 

15.9

3.6 

3.5 

3.0 

3.9 

1.9

2.3 

14.3

9.4

Calcisulp

5

1

3

1

1

2

6

3

2

3

1

3

2

1
102

103

104

105

106

107

108

109

110

111

112

113

114

115

UK

117

118

119

120

121

122

Tributaries of 

Cimarron.

Arkansas River 

and tributaries.

North Canadian

and tributaries.

Boomer Creek, £ mile east

of Stillwater.

Council Creek, 8£ miles

northwest of Ingalls.

Little Stillwater Creek, 6

miles east of Stillwater.

Salt Creek, 10 miles northeast of Ingalls.

Wild Horse Creek, 11 miles 

southwest of Stillwater.

Stillwater Creek, i mile

south of Stillwater.

Dog Creek, Way noka .......

Salt Creek, £ mile below

Salt Spring, Ferguson.

Cottonwood Creek, * mile

north of Guthrie.

Ponca City, 2 miles east.....

Black Bear Creek, 2 miles

northwest of Stillwater. 

Bed Rock Creek, at Otoe

School.

Black Bear Creek, north of

Stillwater.

/Beaver Creek, sec. 9, T. 4

N., R. 32 E.

Paladuro Creek, NE. J sec.

23, T. 1, R. 18.

Cold Water Creek, Hardesty, Okla.

North Canadian, at Cantonment.

North Canadian, 4 miles

northwest of Wa tonga.

North Canadian, 2 miles

north of El Reno.

North Canadian, at Sweeney

Branch of Deer Creek, NE.

isec 4, T.12N., R. 4 W.

7.9

1.9

3.9

3.2

3.97

1.5

7.2

198.5

3.1

6.5

6.5

3.5

6.1

7.2

6.5

7.5

7.5

5.5

6.9

6.2

16.5

2.97

1.8

1.6

2.3

3.6

0.9

3.6

87.3

1.2

0.4

3.0

0.9

1.6

5.6

1.0

1.9

2.3

3 Q . tj

4.6

3.2

4.3

3.5

.2

.0

0.0

0.0

1.1

7.5

192.3

3.5

3 2

2.1

1.2

0.6

13.3

8.3

12. ti

9.6

10.3

11.8

3.9

30.2

1.1

. 7

.8

0.8

1.8

0.2

2.1

7,930.0

2.5

7.6

3.2

1.5

1.4 "

38.7 '

10.4

8.6

19.5

19.5

14.0

6.3

" 1.4

35.6

13.9

23 2

15.1

3"! ?!

10.0

35.9

17.4

29.8

34.8 

14 6

29.1

99.3

42.0

50.3

65.2

67 7'

58.0

36.3 

83.4

3.5

6.1

5.3

6.9

1.8

5.5

2 7

3.9

6.4 

2.98

5.5

7.3

5.8

4.9

4.1

2.8

3.3

5.8 

5.5

Hot determined.
Analyses of Oklahoma stream waters 

a

<4

1?.3

134

125

126

1^7

128

129

130

131

1 Qg

133

134

135

Stream.

and tributaries.

South Canadian

Wichita Mountain streams.

Location.

south of Oklahoma City.

Clear Creek, S. i sec. 24, T.

25 N., R. 35 W.

of Whitehead.

Kiowa Creek.

ward.

south of El Reno.

South Canadian, at 100th 

meridian.

E., ^ mile 8. of Taloga.

miles above Port Sill.

Cache Creek, SE. i sec. 39,

T. S N., R. 11 W.

sD

s

M

O

PS

J3

10.2

4.1

6.7

6.7

6.5

7.6

6.3

17.5

9.0

4.8

6.3

6.9

 d

o

2%

ss

d

cS

^

3.8

0.0

3.4

0.5

1.3

0.8

2.9

5.3

8.0

1.98

2.8

1.1

1.6

m 

13

!-i 

l>>

08 -o

0

.2?

3

"is

02

9.7

4.1

3.1

4.0

4.1

13.6

9.5

33.3

14.5

6

05

a

_o

^

10.5

(fl)

3.9

1.7

28.9

14.9

4.9

11.0

4.4

9.3 4.6

25 12

5.1 1.5

5

S

*

-S

 

0

O

o 

 d

' M

.2 

 d

d

0

cs

a

48.3 4.8

(f'l

23.8

21 r

82.7

53.0

76.0

64.3

31.0

24.6

4.4

6.5

6.0

3 ''

6.4

3.7

2.0

12.0

9 9

O Q

6.S

a Not determined.
Analyses of Oklahoma, spring w

[Grains per United States gallon

No.

136

137

138

139

140

141

143

144

145

146

147

148

149

150

151

Kind of 

spring.

Limestone...

Sandstone ...

isalt ..........

Location.

Island right of way.

Lawton, Dunbar Springs, NW. i

sec. 16, T. 2 N., R. 12 W.

Newkirk, NE. J sec. 15, T. 28 N.,

R. 3E.

Uncas, SE. J sec. 13, T. 27 N., R. 4 E_

Baker, SE. i sec. 14, T. 16 N., R. 5 E.

Guthrie, lots 11 and 12, block 11 ....

Pawnee, NE. i sec. 12, T. 21 N.,

R. 5E.

NW. i sec. 21, T. 27 N., R. 16 W.

Whitehorse, SE. i sec. 7, T. 27 N.,

R. 16 W.

....do................................

....do................................

1 head of Salt Creek.

I Plain.

O03 O

5

o

a.pi

'G

03

4.7

6.5

7. 1

7.8

3.2

13.4

6.4

6.1

5.2

3.1

6.9

6.1

18.6

3.7

210.8

195.2

5

8

So 

Zg

05 S.

a

60

^

0.7

1.4

2.3

2 2

1.4

6.6

2.3

3.3

2 4

1.98

2.6

3.1

9.9

1.2

97.8

78.5

 S

a

ii

«O2

ft

pi

OQ

3.7

5.0

1.2

rj

.4

4.4

1.0

4.1

9.4

.9

2 7

2.3

35.3

1.2

164.3

198.7

3

|

,4

0

0.8

1.6

1.3

.5

.6

12.9

.9

1.2

1.9

.5

3.1

2.9

63.9

.9

9,065.3

7,697.3

s

<D

M

5

o

OJ

"§

^

25.4

18.2

20.2

23.0

11.7

66.7

19.7

26.6

26.4

10.9

20.3

19.6

173.3

14.6

( Of )

0

o

O

dioxid

u

9.1

3.5

7.4

7.8

3.7

14.9

7.1

_8.9

3.7

4.1

5.3

5.6

5.4

3.2

a Not determined.
Analyses of Oklahoma pond w

[Grains per United States gallon

No.

152 

153

154

Location.

Grant County: 

Lament, 1 mile east and $ mile north ..-..

Logan County:

_:

O

s

0>

 d 

1

a

13

o

1.2

.7

1.5

!°

'S

o 

a

c3

a

0.2 

.3

2

Sulphuric anhydride 

(S03).

0.0 

.0

.0

Chlorine (Clj.

0.3

1.2

.3

<D 

S

'o

IB 

0

13.5 

19.9

70

Carbon dioxide (CO2>.

0.4 

1.2

1.8 ... - .

Calcium sulphate (CaSO4).

<")

® 

 d

|

'3

a

« Traces of calcium and magnesium si
WELL EE COEDS. 155

WELL RECORDS.

On the following pages are given descriptive notes of 10 wells 

from each of the 26 counties in Oklahoma. These data were obtained 

by a complete canvass of all available sources of information, mainly 

by schedules sent by mail. Returns from over 5,000 wells were received from all parts of the Territory, probably representing -all 

classes of wells. In the selection of data presented in the table care 

was taken to include only those which were most typical for each 

general locality and which represented ordinary conditions. It is 

believed that these records show the typical hydrologic conditions 

for the Territory, although in some cases there are local conditions 

which may differ more or less widely from those indicated.

In several instances there has been considerable difficulty in ascertaining the geological horizon of the water-bearing stratum, and for 

that reason the statements given in the column headed " Geological 

horizon " are to be accepted only tentatively. Where the term "red 

beds " is used, it is to be understood in the sense of the Pennsylvanian 

red beds. When the well is located in the undoubted Permian, that 

word is used. It will be observed that in general wells in the Tertiary and the (Pennsylvanian) red beds contain soft water, while 

those in the Permian yield hard water, but in a few localities the 

conditions are exceptional in that respect.

The height of the water level in the wells as given in the table 

is in some cases only approximate, for usually there has been no 

means for accurately measuring it. Moreover, there is often more 

or less variation in the level from year to year, and the present level 

may be different from the one found at the time of observation.
PiDOOOO 2OOOOO 2 OOOOOOOO) O

! '.'.'.'. '.'.'.'.'. :::!!;: i

. ..... .......

fci3tdt""t obot>- o td t"* <i ! ^ Osn^^jO^tdO s HHH'iuiM Hit-Hi i i

:::::§ : : 7 P : p » : P : : g g

J-1 | H 'B H P » «H > P 1 -3 JH .8 1 | g ^ g t S &* ^ P * 

:°'::^ h^S': p .°^: |r ^ ^' : ?* : : ^ P" T1

i 1 ! ! i * £ i i i p ! i : § ! i i i * i i

* 

.

O 

i

D

2 

< 

i

,-s Q 

COh-i tOC7»<£>,S C"CntO Oi«3Cn W CO tO ht-00 £* £* O C7» >*» C

^ - a

-JMCOOCO^CO^tOOOCOtO^ OOtMh-'tOtOMtO h-

-

J

t^- 05 t>0 h- ^ CO tOh-» tO I 1 tOtwtO tCi CO MO

CO tO CT> CJi ^O i^f. OtOCT> - 1 I C7> h^ O^ Oi OOCO OO 1 CJi CO I 

liillllllllll lilillli s

to

rf*. Oll~J ^ I 1 -OS ht*^>f*CT

0000 OJOO1 OJ OJOJOJ OJOJOO O> tO M 00 Ol Oi Oi O 00 00 O

rf^M I 'tO I tO CnOiCO COCJil ' CJ tO M OOtO CC> tO tO ^ CO 0

co«3 ojoo -i oocn ojoj^ o -i o COM oo -j ^ en o o

g g 8 £ g 5 i § 8 8 g K 6 8-&SSSSSfe S i 

1 hL llll hL' hJ 111 1111111 j

COtOtO L-1 Oll 'tOtOOOOrf* tO tO^C/JI 'COtOh-'rf-- tO*

oo ooo o ooo ooo o o o oo o o o o o o
WELL EECOEDS. 157

well records.

How obtained at 

surface.

Mill and

pump. 

.....do......

Mill and

pump. , 

Pump ......

Mill and 

pump.

.....do......

pump. 

.....do......

Steam pump 

Mill and

pump. 

.....do......

Bucket .....

Mill and 

pump.

.....do......

Mill and

pump. 

Bucket ..... 

.....do......

.....do......

Pump ......

Bucket .....

Mill and

pump. 

Steam pump

Pump ......

Bucket .....

Mill and 

pump.

.....do..... 

.....do......

Quality.

....do...

Soft ....

Soft .... 

....do...

....do... 

....do...

....do...

....do...

Gypsif . . 

Soft.....

....do... 

Gypsif . .

Soft. ....

Salty...

Soft..... 

....do...

....do...

....do...

....do...

Hard ...

Soft..... 

....do...

....do... 

....do...

....do...

 soft.

Supply 

per 

minute.

Gals.

0.5

10.0 

10.0 

.5

4.0 

.08

4.8 

1.25

2.77

.88

4.16

6.0

10.0

.06 

.02

.4

.02

.15

60.0 

.06

1.66 

.22

5.3

Increase or 

decrease of 

supply.

Neither. ......

.....do........

.....do........

.....do........ 

.....do........

.....do........ 

.....do........

.....do........

.....do........ 

.....do........

.....do........ 

.....do........

.....do........ 

.....do........

.....do........ 

.....do........

.....do........

.....do........

.....do........ 

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........ 

.....do........

.....Ao. ....... 

.....do........

.....do........ 

.....do........

Effect of 

pumping on 

level of 

water.

lower. 

.....do.......

.....do....... 

.....do.......

.....do.......

lower.

Easy to lower 

with the 

pumpinuse.

lower. 

Easy to lower

Not easy to 

lower.

.....do.......

Not easily 

lowered.

lower.

with the 

steam pump 

used in testing flow.

lower. 

.....do.......

lower. 

.....do.......

lower. 

.....do.......

.....do.......

.....do.......

.....do.......

.... do....... 

.....do.......

Geological 

horizon of 

well mouth.

.....do......

.....do......

.....do...... 

.....do......

.....do...... 

.....do......

.....do......

Dakota Cretaceous.

.....do...... 

.....do......

.....do...... 

.....do......

Permian red 

beds.

.....do......

.....do......

.....do...... 

.....do......

.....do......

.....do......

.....do......

.....do......

.....do...... 

.....do......

.....do...... 

.....do......

.....do...... 

.....do......

Geological horizons of waterbearing strata.

.....do............

.....do............

.....do............ 

.....do............

.....do............ 

.....do............

.....do...........

Dakota Cretaceous

.....do............ 

.....do............

.....do............ 

.....do............

.....do............ 

.....do............

.....do............

.....do............

.....do............ 

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............ 

.....do............

.....do............ 

.....do............

.....do............ 

.....do............

No.

*1

*2

3

4

5 

6

7 

8

*9

10 

11

12 

13

14 

15

16 

17

*18

19

20

91

72

23

 >4

9,5

26

27

28 

29

30

jfc M
g £

p, p,

o :

| I

O O

>5' S 

* : g

« : F

B o ; ;

<* ^ So

g H g* 

& w <j

<rt- TA '

M M

*- Cn

M M 

CO tO

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CO OS

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en o

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* * *

cr. cs cs os en en en ep 

co to MO to GO -j os

o S" So ooo o

|| fi ||| \

ro ?! . B TO !

I i i g r i

3 : o : : "

(k. tO C7* 50 tO M tt- (O

 i M )-i M tO 

f>.en COCO *- CO CO O

CM tO M tO tO M

5 GO O S S 1C tO O

35 CO OS OS O OS OS S

 ^1 CO Orf^ M M M en

,n o in Cn CO Go QD o

COSO P CO MMM 01 

InO Cn G M C7> OS O

II '1 III

|0 tO CO tO MM JOO OO OOO O

* * * * *** * * *

: i | : : : : : : : 3

3 OO3§ OOOO OOO 3 2 £.

, :JL.:.. : : : B 

: : S : : : : : : : o-

? li^i |»o|g^i| | i i 

§fK f f § f %l! ! s ^ ?

^ : : :° : S1 T : : i ? T p| :

MIC ht-MMM'T? MMMM M 

X CeCnCfcZ OO^GO OOO O tO O

coco, _ ,to COMM co to co

S tOGOOtO ^^3-^ ^^^ ^ ^ ^

M icOtOM M^^tO t-1 *-1 ^ CO M

3 to M to to toococo Stoco to co S

M OS

to to to co 1-1 to to

tO OSQSMCn O5O5-<IH^ OS tO CO CD OD l-i 

M OOtOM lOtO-JO CnotO CO to IO

M cntfc-MCO CnenOSCO tOMlC 00 M O 

CO tOOOto OCOtOCn ~j-j~j CO en O

1 1 1 1 1 1 1 III 1 M M 1-1 tO M 

M ht-COMCO bSQCOCO 1 'MM tC CO M 

O rf-OOM 5Jio~JO OOtO CO to NJ

o oooo oooo ooo o en o

*

hU 

O 

0 

Eda ..........

I ^

M 

CO 

en 

-i 

to 

o 

to 

GO 

rf- C

en 

0 

1 

rf*- 

o 
WELL RECOBDS. 159

records Continued.

How obtained at 

surface.

pump.

Mill aud

pump. 

.....do......

.....do......

Mill aud

pump. 

Bucket .....

pump.> 

Steam pump

.....do......

Bucket ..... 

.....do......

Mill aud

pump.

.....do...... 

Bucket .....

pump. 

Bucket .....

Pump ......

.....do......

.....do...... 

Mill aud

pump. .

.....do......

Bucket .....

Mill aud 

pump.

Bucket .....

Mill aud 

pump.

Bucket ..... 

.....do.... .

Quality.

Soft.....

Slightly

hard. 

Salty . . .

Soft.....

....do...

Soft ....

....do...

....do...

Hard ...

Soft ....

Hard . . . 

Soft .... 

....do...

....do... 

....do...

Alkali . .

Soft ....

Hard . . .

Soft ....

Soft ....

Soft ....

Hard . . .

Soft.....

....do... 

Gypsif . .

Hard . . .

Soft.....

Gypsif . . 

....do...

Supply 

per 

minute.

Gals.

044

.2

2 V7

11.69 

.55

1.7 

.11

.044

.44 

04

.55- 

2.66

1.0

2° 5

3.33

1.16 

.22

.08 

.22

Increase or 

decrease of 

supply.

Neither.......

supply.

.....do........

supply.

.....do........

.....do........ 

.....do........

.....do........ 

.....do........ 

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........ 

.....do........

.....do........

.....do........

"NToit'hov

.....do........

.....do........

.....do........ 

.....do........

.....do........ 

.....do........

.....do........ 

.....do........

Effect of 

pumpiug ou 

level of 

water.

day aud 

uight.

lower.

lower.

lowered.

lower. 

.....do.......

.....do.......

.....do....... 

.....do.......

.....do....... 

.....do....... 

.....do.......

.....do....... 

.....do.......

.....do.......

.....do.......

.....do.......

.....do.......

lower. 

.....do....... 

.....do.......

.....do.......

lower. 

.....do....... 

.....do.......

.....do....... 

.....do.......

.....do....... 

.....do.......

Geological 

horizou of 

well mouth.

.....do......

.....do......

.....do......

.....do......

.....do......

.....do......

.....do......

.....do......

.....do...... 

.....do......

.....do...... 

.....do...... 

.....do......

.....do...... 

.....do......

.....do......

.....do......

.....do...... 

.....do......

.....do......

.....do...... 

.....do......

.....do......

.....do......

.....do......

.....do...... 

.....do......

.....do...... 

.....do......

.....do......

.....do......

Geological horizous of waterbeariug strata.

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............ 

.....do............

.....do............ 

.....do............ 

.....do............

.....do............ 

.....do...".........

.....do............

.....do............

Permiau ..........

.....do............ 

.....do............

.....do............

.....do............ 

.....do............

.....do............

.....do............

.....do............

.....do............ 

.....do............

.....do...... ...... 

.....do............

.....do............

.....do............

No.

*3?

33

*34

*35

*36

37

*3S

39

*40

*41

*42 

*43

*44 

*45 

*46

*47 

*4H

*49

*50

51

52

53

54

55

*,Tfi

57

*58

*F>9

60 

61

62 

63

64 

65
*

00 ~J O3 :

PI PJ Sj 

OOO

.. Billings...... .. Waukomis... 

. Carrier ......

i? O p

C. Rosencrants.. 

las. Thain....... hn Pope ........

to to to

*» M CO

00 ~J 00

M tO M ~3 00

00 00 00 

CO CO ^O 

03 Si &

ZO l£*. If*. 

O5 00 00

l-i -J CO 

O CO o

>-i ~J tO

o to 01

: i i

05 to 

00 O C7i

o o 'o

1

p. oo

e-i Bn>

to

CO

005i

O5

CO1-1

to

001 go

COi

SOo

White..........

to0

05

CO

00£

O3

»|M

131

to 

too

CO;

& oQ

Si

m. Walker ......

CO

Jto ~I

00 

CO 

CO

O3 88

1 80

8

0, o

... Waukomis...

Pd

H 1

to

O3 8

£ 8

00BK

000

CO CO 00 

t- 0 «0

o :

3s a, b, 

<L o o

... Deltis........ 

... Webb........ 

. Glenella .

o n o

;o. W. Harris.... enry Schultz L. Bushwisel...

00 <I -Jf

00 00 CO

co to to

00 CO CO

O5 O5 O5

4- ' ^

o to o

S

O * 

O O

1 1 1 

g 1 8

OOO

£

p- o

Roseland .g

tr1 e

05

O5

ots

05

isMI o

00 00 00 00 QO OO

OOO O O O

W |3 ! IT* ^ ^ 

Big- 1 E T

OH P

P P : . : :

p. ; ; ; ; ;

3 > > bd > 3

O w o ^ i 

g <? S ^ j1 y

& n> g H5 ^ o

ts « tj ts ot ot

S ti S S K K

CO tO l-i l-i tO 

Oi Oi CO t-i CO <I

O O l-i O O H*

00 O5 O5 O5 O5 O5

4- tO ~3 CO 00 to

Oi 00 M 00 O5 O

to o i oo S o

' ' M ' L ' 

if* 00 O £t 01 ^

to o o oo oo o

OOO O O O

£%s 33 Sla

o : : : ; : : 

n> . 1 ! . 

^oo oo ooo

I o r Sg s f 

ny.t O ..i

r : i : T i : 

W M^ ^» .^^ 

» ^ tc W g ^ -f 

5: ._fl' ^' f^

^2 P- 

5££ S£ S£

l-i tO tO tO tO IO to 

CO 1 i IO 1 ! 

tOOCO OM O5MI

tOh"tO I-J'M tO tO 

00 00 tO O500 tOOO

COOirf- O3O1 00 tO 

tOOlO C5O1 OOtO

CO^[O5 if- it- OCO

111 ' ' M M 

tocno oocn osto

COO1O3 rf^CO OCOC

OOO OO OOO
WELL RECOBDS. 161

records Continued.

How obtained at 

surface.

Mill and 

pump.

Bucket .....

Mill and 

pump.

.....do......

Bucket .....

Mill and 

pump.

.....do......

.....do...... 

Bucket .....

.Mill and 

pump.

Bucket .....

Mill and 

pump.

Pump ...... 

Bucket..... 

.....do......

Mill and 

pump.

Bucket .....

Mill and 

pump.

.....do......

Bucket ..... 

.....do......

Mill and 

pump.

Pump ...... 

Bucket .....

Mill and 

pump.

.....do......

Mill and 

pump.

Bucket.....

Pump ......

Mill and 

pump.

IKK 1-J

Quality.

Soft.....

Gypsif.. 

Hard . . .

Gypsif..

Hard . . .

Soft.....

Hard . . .

Soft..... 

....do... 

....do...

....do... 

....do...

....do... 

....do...

Hard, a 

little 

salty.

Soft..... 

Hard . . .

....do...

Alkaline

....do...

Soft..... 

Hard . . . 

....do...

Soft..... 

Hard...

Slightly 

salty.

Soft.....

Hard . . .

Soft.....

18 05 SiSupply 

per 

minute.

1

Gals. 

.44

.08 

.44

.111

.111

4

5.5 

.5 

1.116

.06 

20.0

3.0 

.133 

.66

.44 

2.0

.26

.5 

.04

.44

.22 

.44

2.22

.333

.5

-11

Increase or 

decrease of 

supply.

.....do........ 

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........ 

.....do........ 

.....do........

.....do........ 

.....do........

.....do........ 

.....do........ 

.....do........

.....do........ 

.....do........ 

.....do........

Increased..... 

.....do........

Increased ....

.....do........

.....do........ 

.....do........

.....do........

.....do........

.....do........

Effect of 

pumping on 

level of 

water.

Not easy to 

lower.

Easy to lower

Not easy to 

lower.

Easy to lower

lower. 

.....do.......

.....do.......

.....do.......

.....do....... 

Easy to lower

Not easy to 

lower.

Easy to lower

Not easy to 

lower.'

.....do....... 

.....do....... 

Easy to lower

.....do.......

Not easy to 

lower."

.....do.......

Easy to lower 

.....do.......

Not easy to 

lower.

.....do.......

.....do....... 

.....do.......

Not easily 

lowered.

Can't pump 

out water.

Runs in as 

fast as 

pumped 

out.

Not easy to 

lower.

Easy to lower 

Lowers level.

Geological 

horizon of 

well mouth.

.....do......

.....do......

.....do......

.....do......

.....do...... 

.....do...... 

.....do......

.....do...... 

.....do......

.....do...... 

.....do... .. 

Permian....

Tertiary .... 

.....do......

Permian .... 

.....do......

.....do......

.....do......

.....do......

.....do...... 

.....do...... 

.....do......

.....do...... 

.....do......

.....do...... 

.....do......

.....do...... 

.....do...... 

.....do......

Geological horizons of waterbearing strata.

.....do............

.....do............

.....do............

.....do............

Tertiary ..........

Tertiary(?) ....... 

.....do............

.....do............ 

.....do............

.....do............ 

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............ 

.....do............ 

.....do............

.....do............ 

.....do............

.....do............ 

.....do............

.....do............ 

.....do............ 

.....do............

No.

69

70

71

72

73

74

*75

*76

*77 

78

*81

82

83

84

85

86

87

90

*91

92

*93

94

*95

96

97

*98
***** * 

*

*3 CO CO CO CO tO tO tO tO tO 

l*fc W tO h- ' O SO OO <! 73 Ol

: : B : . : : :

.0 o a ooooo 3 o

*!_(«« b'fccliJSri W i-9 

CD<^B^ *"* o ^ 5! ^ f^

B 

O H * ? ^ £- ' M i_i £ B a p gf u jj # * fl 

B

M M M 1C tO tO tO tO tO tO

-J -J 00 ^M^H^ ^ 5|

OO <! OO O tO SO SO SO Ol SO

oosooo oooogooso oo oo

| o, o, °° ~ ~~T~ ^ ~~

CLO CO t-* ^.CO^^CfD ^ M 

**Cnt>O -^OOOOO 00 tO

WW O3 fc£ W CO M M t-1 

bOCOOD OiCiOOOOO hP* M

ill 1 1 I 1 1 1

tOtO COtOtOMlO M

0001*- t-*aiooooo it* oo

ooo ooooo o o

*

to

& odg

. L. Bevore......

to

CO

oo 

oo§

If*

~3

If*1 £o

* *

ci £

b.^

q ;

'"d 1^

1"

0 Q

ty. .............. acar Taylor......

to to

O5 00

to to

H H

to 8

it- H"

to o

CT l§

& fe

1 1

to co

CO O>

0 0

B g E

p. p. pooo

|!I

M CH CB

irling Soloman. 

A. Kinjkendall aac C. Stewart .

« en £

8 8 8

Oi CO -<i

§11

to to os

rf* CO Oi 

rfk -<i -J

fe g S

1 1 

52 SS fe

000

*

OO <I O3 Ol *- CO

PL PL PL PL PL PL 

oooooo

lillll

i % I \ f \

3 OB 3 CH Q r

^ 5 s1 if :M ^

« 3 1 § § 2

r s £ w P. .4

i FPJ £1 . . . . ««( .

tO tO CO tO ^B M

8 8 8 g 3 8

,^

E co t- gt 3 5

"

M 00 fcO O tO H*

^ ?o

CJS 00 OS -^1 tO OS

M M 

§l_i to 5D CO O 

O 0 3s 0 c^i

§ s a g § se

1 1 II

CO O5 OO CO SO

o oo o -q o -J

oooooo

k-» 1 1 

tO M

. Medfor 

. Martin

. S. Robertson... hn Brim .......

§ S

Oi Oi

CO tO

i 1

O3 OO

CO Cu

0 05

1 1

CO *.

0 0

* * *

I-" O O 

O SO 00

p- O. PL 

0 00

M M CH 

?o m *

§ 2 1

: : ?

O O d

T. James ...... W. Foetisch... P. Moffett.....

g g 8

CO if. OI

oo oo oc

CO CO <!

OO O". I-*

to so co

OO CO Ol

to oo co

OO en Oi

! 1 1

CO 1 

oo en oo

0 0 .0
WELL RECORDS. 163

records Continued.

How obtained at 

surface.

Mill and

pump. 

Bucket .....

.....do...... 

.....do......

Mill and

pump.

Windmill...

.....do......

Mill and

pump. 

.....do......

.....do...... 

.....do......

.....do......

Bucket .....

Mill and 

pump.

Bucket ..... 

.....do......

Mill and

pump. 

Steam pump 

Mill and

pump. 

.....do......

Mill and 

pump.

.....do...... 

.....do...... 

Pump ......

.....do......

Mill and 

pump.

.....do......

.....do ...>.. 

.....do......

Quality.

Hard ...

Soft.....

Soft..... 

Hard . . .

....do...

Soft.....

Hard . . .

....do...

Soft......

....do...

Salt.....

Gypsif . .

Salty . . .

Soft .... 

Hard . . .

Gypsif

Hard . . . 

....do...

Gypsif..

Gypsif . .

Soft .... 

....do...

....do...

Hard

and 

salty.

Hard ...

....do... 

....do... 

Alkaline

Soft .... 

....do...

....do... 

....do...

Supply 

per 

minute.

Gate. 

.66

3.33

30.0 

.66

2.66 

.22

1.37 

.11

.08

11.8

.42

.083

3.33 

.056

7.0 

4.0

4.0

.133

5.0 *

Increase or 

decrease of 

supply.

Neither.......

.....do........

.....do........

.....do........ 

.....do........

.....do........

the season.

same. 

Constant......

same.

.....do........

.....do........

.....do........

.....do........ 

.....do........

.....do........

.....do........ 

.....do........

.....do........ 

.....do........

.....do........

.....do........ 

.....do........

.....do........

.....do........

.....do........

.....do........ 

.....do........ 

.....do........

.....do........ 

.....do........

.....do........

.....do........ 

.....do........

Effect of 

pumping on 

level of 

water.

lowered.

lower.

Constant ....

ered.

To lower

Lowered

Not affected.

dry.

ered.

lower. 

.....do.......

.....do....... 

.....do.......

.....do.......

.....do....... 

.....do.......

.....do.......

lower. 

.....do.......

and night.

lower.

ered.

Not easy to 

lower.

.....do....... 

.....do.......

Can not lower

Not easy to 

lower.

.....do.......

.....do....... 

.....do.......

Geological 

horizon of 

well mouth.

Tertiary ....

Tertiary ....

.....do......

.....do......

.....do...... 

.....do......

.....do......

.....do......

.....do......

.....do......

.....do...... 

.....do......

.....do......

.....do...... 

.....do......

.....do...... 

.....do......

.....do......

.....do...... 

.....do......

.....do......

.....do......

.....do......

.....do...... 

.....do..!... 

.....do......

.....do...... 

.....do......

.....do......

.....do...... 

.....do......

Geological horizons of waterbearing strata.

Tertiary ..........

Tertiary ..........

.....do............

Tertiary..........

.....do............

.....do............ 

.....do............

.....do............

.....do............

.....do............

.....do............

..... do. ...........

.....do............

.....do............

.....do............ 

.....do............

.....do............ 

.....do............

.....do...... .---.

....do............ 

.....do............

.....do............

.....do............

.....do............

.....do............ 

.....do............ 

.....do............

.....do........;...

.....do............ 

.....do............

.....do............ 

.....do............

No.

*99

100

*101

*102 

*103

*104

*105

*106

*107

*108 

*109

*110

111

112

113

114 

115

116

*117 

118

119 

120

121

*122 

*123

*124

*125

*126

*127 

*128 

*1?,9

*130 

*131

132

133 

134
3:

b o

. Crescent .....

A. CRingold....

-41

CO

g

'?

. Langston ....

. Freeman Wallace S

ts

to

to

b o

.. Mulhall .....

SH W

CD" 

*<S

00

CO

' O

£

§ 

.. McKinley ...

. D. KCampbell .

01

ts

to

§5

§ 1

STp

CO

frf00

ts

COo

Oq . 

B 0

.. Clifton ...... .. McKinley ...

. I. C.Boulsoii..... 

. David Swank

Ol tO

ts *.

£ SS

§0

.. Perkins......

. Jose Hert........ M

COg

b0

.. Wellston ....

. G. W. Blakeley...

Ol

to£

s00

§"

.. Clifton ......

. Farmers' Gin*Co .

to

tsg

S3 g

p, a

0 0

! i

.. Riddle....... 

.....do.......

. C. ASherwin, s. 

. C. ASherwin, jr.

to to

H tS

£ g

C7I &1

. Joe Dufralne..... £

to Hg

&

b o

CH

W W

Ol H

00

S

§ B

0 15H

00

SroO

CD 

V)

. Wm. Bedford

Ol

CO

tsg

( < O CD CC -4

O O O O O

2 ' "* '

H B 1> ^ B

I pg S|

B | p | |

tc w

t2j 0-, 2; ^ <i

M MM M

M CO

fe£

0 0

0 o,

1 l-h

^ > 

si CD S' 

H B

M en

Cn CO

CO

i

: 

o 

0 

1 

5 

C

IO 

C

*

00 

CD 

CO§

1C

00-1

too

1

engg1

rf- oo

1

oo

Oi

to

CO1 0

000gg1 0o00 

CD

00§Es1 oo

GO g 

CO CO

00 OS

CO Oi 

OO M

<DO rf^ 

OS Oi

1 1

M CC

o o

1

013

CJ 

001 so

e?

-4&

g;i

to

CD0

I

to o§

CO

O51

M 

OSO

CO 00 

I-1 HCO

gg

gg1 '

O I 1

rf*- M

o o

1

010%1 o

1

Ol o

Jg81

00

a.

COs

01£gi

a.

1£1igw

I 1 1 1 :

<7i W O O t-i

^5 1^ 1 I MM

O^ GO GO CO 4

bd W M M CO

1 1 ! 1

i_k to K- > K-> 

os to Oi o

0 00 0

i I

cc o

M M £> M

g S

i i i 1 ( »

to p

0 0

 

' 

' 

f

e

M 

to 

V-

o 

1 

M 

O 

o 
WELL RECOKDS. 165

records Continued.

How obtained at 

surface.

Mill and

pump. 

Pump ......

.....do......

.....do...... 

Bucket .....

Bucket .....

Pump ......

Bucket ..... 

.....do......

.....do......

Bucket .....

.....do......

.....do.......

Bucket .....

.....do......

.....do......

.....do......

Bucket .....

Bucket .....

pump. 

.....do......

Bucket .....

Mill and

pump. 

Pump ......

Quality.

Hard,

nearly 

soft.

Soft.....

Hard . . .

Soft..... 

....do...

....do...

Salty ...

Gypsif . .

Soft.....

....do... 

Salty . . .

Soft.....

Soft.....

....do...

....do...

soda. 

Soft.....

....do...

....do...

....do...

Soft.....

....do...

Medium 

soft. 

Hard . . .

....do... 

....do...

....do...

Soft ....

....do...

....do...

Supply 

per 

minute

Gals. 

40.0

10.0

........

.04

.02 

.04

3.0

3.33

1.66

.83

.14

.087

.27

Increase or 

decrease of 

supply.

.....do........

.....do........

.....do........ 

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........ 

.....do........

.....do........

.....do......... 

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........ 

.....do........

.....do........ 

.....do........

.....do........

.....do........ 

.....do........

.....do........

Increase ......

Effect of 

pumping on 

level of 

water.

lower. 

.....do.......

.....do.......

.....do....... 

.....do.......

.....do.......

.....do.......

Not easy to 

lower.

Easy to lower 

.....do.......

lower.

lower.

Not very easy 

to lower.

lower.

ered to 23 

feet.

lower.

lowered.

lower. 

.....do.......

lower. 

.....do.......

.....do.......

.....do.......

ered.

er.

Iseasily lowered.

lower.

ered.

Can be 

§um p e d 

ry 111 4 

hours.

Geological 

horizon of 

well mouth.

.....do......

.....do......

.....do.... . 

.....do......

.....do......

.....do......

.....do...... 

.....do......

.....do......

.....do......

.....do......

.....do......

.....do...... 

.....do......

.....do......

.....do......

.....do......

.....do......

.....do......

.....do......

.....do...... 

.....do......

.....do......

.....do......

.....do...... 

.....do......

.....do......

.....do......

Geological horizons of waterbearing strata.

.....do............

.....do............

.....do............ 

.....do ............

.....do............

.....do............

.....do............ 

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............ 

.....do............

.....do............

.....do............

.....do............

.....do............

.....do. ...........

.....do............

.....do............ 

.....do............

.....do............

.....do............

.....do............ 

.....do............

.....do............

.....do............

No.

135

136

137

138 

139

140

141

143

143

144 

145

146

147

148

149

160 

*151

*15fl

*153

*154

*155

*156

*157

*1P8

*159 

*160

*161 

*162

*163

*164 

*165

*166

167
1

hi p

CD

CD ~ m

t-" :

. Hiram B. Allnutt * Seenotes a endof

E to

gj- 1^&S1

000

*1o

Ralsto p

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CD" &H

to

00 

CD

to

to

fig

CD

Ol

* *

O CD 

O CD

Pi Pi

O O

; ;

a i-1*

II

CD ;

. FredStrobal..... 

. L. PBotts.......

to to 

to co

H H

p*» 00

g s -J SO

8 g

*. CO

1 1 S

CO 

to

o c

,*

CD 

000p

CD

.| Louis Demieville.

E3H

01i

<,

fesi

to

COo

*

pi o

g gP1 B

. J. SStritch...... §Hg1g

to

001

C3O

1

pi o

hi 

to

CD

. E.G. Wheeler.... S

sfS

00

O3 igi

CJ

330

*0

pi 0

.) B. FHarmon.... gK

toS

00

to

00

to1 o

* * 1 1 t *

o o

g ®

S CD"

y 5 5 2

B *

. S. Vandment..... 

. W. CLegrande..

Be

& M

s s

>£* O1

O3 O

00 ~7

to -a

-a -a

1 1

CO O3

o o

* *

hi :

g o1 

1 I

g 0

: T1

. C. HMcLung . 

. Lone Chief.......

E3 K

H ^

00 CO

00 CD

O3 O^

to co

to co

00 00

to to 

-a oo

o o

io

Luthe Qt-S

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CD" 

ftKMg

00oago0

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^ 

.^

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CO3ssCO

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. Homer Britton .

COHg1

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00

Pi O

o p

CDQ

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. C. AChandler ...

to

ft

toI

Ol Ki1

CD0

g

PI 0

p. 0

. Carrie Miller.....

i i

to3

to

COis

IB

ESI 0

00 

Ol i0

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. J.A.Kennedy...

toH81S

-3&iO

*

00

Itpi oW3-BWCD 

P 

i-i n

CO3

CO H" io1M

O OO

*%

CD

. Lee Dalrymple .

i i

COM£I

C3 £

fe

1 

feO

3

00

tooE

O D4

S"

. JohnQuim...... G3g1

OS £

SJ1

COo

001

Pi o

,'I

. Henry Koelzer.. £Mg§

ftS

Ol

to1 o

oo;

a Si'

. Jay K.Graves ....g

COE1

C3 si1

 73 0

3 3 <r -J

CD 00

O O

0 C

at

P 

. J.E.Writt........ . Hull Bros........

to to

M 3

5 <!

CO M

5 ft

is

I l

§ P

o o

3 

*3 

0 

o 

P 

O 

O 

8 

w 

CD 

| 

gg

^ 

Ol 

00 

Oi 

00 

g

0 

to 

00 

ti 

O 
WELL KECOKDS. 167

records Continued.

How obtained at 

surface.

.....do......

Mill and

pump.

Mill and

pump. 

.....do......

Mill and

pump.

1 Mill and 

pump.

.....do......

Mill and

pump. 

.....do......

Bucket.....

.....do......

Bucket .....

.....do...... 

.....do......

Pump ......

Bucket .....

pump. 

Bucket..... 

Pump ...... 

Bucket .....

.....do......

Mill and

pump. 

Bucket.....

Quality.

Soft ....

Soft ....

....do...

Hard ...

....do...

....do...

....do...

Salty ...

Soft ....

....do...

....do...

....do... 

....do...

salty. 

Hard . . .

Soft ....

....do...

....do... 

....do...

....do...

Soft .... 

Salty . . .

Soft ....

....do...

....do...

Hard . . . 

....do...

Soft. ....

....do... 

....do...

....do...

Supply 

per 

minute.

Gals. 

.135

10.4

.13

14.0

1.33

4.16

.266

2.0

10.0

4.16

3.33 

4.0

2.5

1.3

.13 

.03

.03 

6.6

Increase or 

decrease of 

supply.

.....do........

Incrsjisc

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........ 

.....do........

.....do........

.....do........

.....do........

.....do........

Neither

.....do........ 

.....do........

.....do........

.....do........

.....do........

.....do........ 

.....do........ 

.....do........

.....do........ 

.....do........

.....do........

Effect of 

pumping on 

level of 

water.

ered.

lower. 

.....do.......

lowered.

.....do.......

lowered. 

.....do.......

Easily lowered.

ered.

lower. 

.....do.......

ered.

Not easy to 

lower.

Not easy to 

lower.

.....do.......

.....do.......

lower. 

.....do....... 

.....do.......

.....do.......

lower. 

Easv to lower

Geological 

horizon of 

well mouth.

.....do......

.....do......

.....do......

.....do......

.....do......

.....do......

.....do......

.....do......

.....do.. ...

.....do......

.....do......

.....do......

.....do......

... .do......

.....do......

.....do......

....do.......

.....do......

.....do......

.....do...... 

.....do......

.....do......

Pennsylvanian.

.....do......

.....do......

.....do......

.....do......

.....do...... 

.....do...... 

.....do......

.....do...... 

.....do......

Red beds...

Geological horizons of waterbearing strata.

.....do............

.....do............

.....do............

.....do:... ........

.....do............

.....do............

.....do............

.....do...........

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............ 

.....do............

.....do............

Pennsylvanian . . . 

.....do............

.....do............

.....do............

.....do............

.....do............ 

.....do............ 

.....do............

... ..do. ...... ....: 

.....do............

Red beds .........

No.

*168

*169

*170

*171

172

173

174

*175

*176

*177

*178

*179

*180

181 

*182

*I83

*184

*185

186

*187

*188

*189 

190

*191

*192 

*193

*194

*195

*19fi

*197 

*198 

*199

*200 

*201

*202
to to tc to to to to to to

OSCOCOCO CO OS COCOCO 

OO-JOSCT tU OS tO MO

: : : : : : ^ : :

OOOO 0 0 5-00

wtdpso GO td o :n B S O P O u & O T | ;

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: : : : : : : :

flODiV^ p JH ^.M ^ 

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f : | ! i r : 1

tOtOOOO M O tOtOM

MMMM M M MtotO 

tO pf- <I 00 OS to Pi- Pi- O

tO tO CO M M tOCOM

ootctooo GO to tptpoo 

oo 8 to to oo o OMOO

PS*. os <r os

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t-l M tO

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00 CO *. M O CT OS OS -J

MO to co ce P&. ososto

-4 O 00 O O *- O O PfcI'll 1 1 II

M to IO to OS if- 01 to 

* O 00 OS O O O~JCC

OOOO O O OOO

to to to to tc to to to to to to

tO tO tO ro tO IO tO tO tO tO M

tO CO <I OS 071 if- OS IO M O tO

: : : : : : : w : :

b, b, b. b, b, b, b, 1 b, p, b,

OO OOO OO*! O 5 O

tdO WO'ij O d b > td 

pS fSff ^ ; ^ | D 1

: : : : ; : : : :

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tOM tO tO 00 CO-O --J M hto to to to to to to to S £; £;

^.4*. co 4~ i i tOMto ra P3 P3

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&3 <!& to^i 1 CT'CO UT CO fctk.

1 1 111 111 1 1 1

Os<I OiOS 01 W 05 Cs OS OS

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to to to to M os co p^ -~i p&~ <i

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to to to to to to to 

OO^IOSO1P£*-CO tC 

:::::: _ 

oooooo § 

:::::: g. 

^Ilgitd g 

p^ : : 3 : £ S 

1 ? ? P ? | & 

cD' 1 ' 1 ^. 

, . , . . . 

:::::: 

a M ^ SB y ^ -w 

! i : i : ! P" 

M MM 

O <I J -^ M l l «-7 

COCOCO ^** CO 

i_i i_i M M tO 

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bobobooococo co 

COOOCOCOtOCO tO 

Osososososos » 

COpUCTOOOOCO 03 

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OSp^pJ^QO<rcO tO 

OPl-OOMO --7 

1 1 1 i ^ 1 

OSOSM-<IO5O P^- 

<y os ai o sn ~j o 

OOOOOO O 
WELL EECORD8. 169

records Continued.

How obtained at 

surface.

.....do......

Mill and

pump. 

.....do......

Mill and

pump. 

Bucket .....

.....do......

.....do......

.....do......

.....do......

.....do......

.....do......

.....do......

.....do...... 

.....do......

.....do......

Mill and

pump. 

Bucket ..... 

.....do......

Bucket .....

.....do......

Pump ......

Mill and

pump. 

.....do......

.....do......

.....do......

Quality.

Hard . . .

....do...

Soft..... 

....do...

....do...

....do...

....do...

Hard . . .

Soft.....

....do...

....do...

....do...

....do...

Soft.....

Hard . . .

Soft. .... 

Hard . . .

....do...

....do...

Gypsif . . 

Soft.....

....do...

....do...

...do....

...do.... 

...do....

Soft ....

Hard,

salty. 

Hard ...

Soft ....

...do....

...do....

Supply 

per 

minute.

Gals. 

.02

.11

.166

.55

.1

1.0

.05

1.33

1.66

.08

.016

.04

21.3 

.08

8.0

10.0

.5 

8.3

.088

.04

Increase or 

decrease of 

supply.

.....do........

.....do........ 

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........ 

.....do........

.....do........

.....do........

.....do........ 

.....do........

.....do........

.....do........

.....do........

.....do........ 

.....do........

.....do........

.....do........

.....do........

.....do........ 

.....do.....*...

.....do........

Decreased ....

Effect of 

pumping on 

level of 

water.

lower. 

.....do.......

.....do....... 

.....do.......

.....do.......

lower.

lower. 

.....do.......

.....do.......

.....do.......

ered.

lowered. 

.....do.......

Easily lowered.

.....do.......

lower.

lower.

lower. 

.....do.......

lower.

ered very 

little.

lower. 

.....do....... 

.....do.......

.....do.......

Easvto lower

Geological 

horizon of 

well mouth.

.....do......

.....do...... 

.....do......

.....do......

.....do......

.....do......

.....do......

.....do......

.....do......

.....do......

.....do......

.....do......

.....do......

.....do......

.....do......

.....do......

..... do ......

.....do......

.....do...... 

.....do......

.....do......

.....do......

.....do......

.....do...... 

.....do......

.....do......

.....do......

.....do......

.....do...... 

.....do......

.....do......

.....do......

Geological horizons of waterbearing strata.

.....do............

.....do ............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............ 

.....do............

.....do............

.....do............

.....do............

.....do............ 

.....do............

.....do............

.....do............

.....do............

.....do............ 

.....do............

.....do............

.....do............

No.

*203

*204

*205

*206

*207

*208

*209

*210

*211

212

213

214

215

*216 

217

*218

*219

*220

*221

223

224

22)

22f>

227

228

229

230

231

232

233

234

235

236

237

238
S

P- o

Detroit ......

O. ANickerson ..s8y

1

p. 0i

Wm. Martindale .B

00£

to

p- 0

Shattuek ....

H 

(tp

Vj 3a3

g&

P. 0;

Laverne .....

o k&

to

Os

B, 8

8 g 

<1 OS

0 O '

Oleta ........ Speermore...

1

1 Martha N. Smith. Aaron Hartfield .

10 to

g 8

to

OS M

to0

Waynoka....

J.J.Russell ......8

-*S

go

Belva........

fed o

o 

ffi gMM

S

& o

Speermore

| E. Strohmeier .

fe

OT§

ti3p

re" po

5"2

CD &

tow

' I-1

too

Concord .

re O

o°3

re

I-! 80M

3a\o

Chester .

Prank Foward.8

OS

00

£ E CO CO

o o

I Aubnru . Byron ....

^ P

a f?

o ^ 

^ "

3 ?

S S

o to

(0 M

j 

, 

1

to

00

. 1

000

I-0

I 1 

tc

I 1 o

I 1 s0

00 

00

to

OS

OT

W 

OT@O

tooMwwI §050 00

OS ti

*<l M

CC 06

S Eo

1 1

Or M 

Or 1C

0 O

8

OC

OSE1 0

§S

to1 0

8

feg

to

If*1

to0

OS

050£

1 8O

1

COM

?e 

Si1 c

1oeg

i s0

so ce

to o

8 2

S fe

1 1

0 0
WELL RECORDS. 171

records Continued.

How obtained at 

surface.

.....do...... 

Mill and

pump.

Mill and 

pump.

.....do......

Mill and

pump. 

.....do......

.'....do......

.....do......

.....do......

.....do......

.....do......

.....do......

.....do......

.....do......

Mill and

pump.

Quality.

Soft.....

Hard . . . 

....do...

....do...

....do...

....do...

....do... 

....do...

Gypsif . .

Soft.....

....do...

....do...

....do...

....do...

....do...

Salt.....

Soft.....

....do...

....do...

Supply 

per 

minute.

Gals.

.83

5.0

2.2

2.22 

.22

.4

.3

.22

6.6'

.22

.03

06

AO

.17

69 -14

.05

no

Increase or 

decrease of 

supply.

.....do........ 

.....do........

.....do........

Neither.......

.....do........ 

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

.....do........

Effect of 

pumping on 

level of 

water.

lower. 

.....do.......

lower.

lower " 

.....do.......

.....do.......

.....do.......

lower. 

.....do.......

.....do.......

lowered. .

lowered.

lower.

lowered.

with sand 

pump.

lowered.

Geological 

horizon of 

well mouth.

.....do...... 

.....do......

.....do......

.....do...... 

.....do......

.....do......

.....do......

.....do.....:

.....do......

.....do......

.....do......

.....do......

.....do......

Tertiarv

Geological horizons of waterbearing strata.

.....do............ 

.....do...........

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

.....do............

No.

240 

?41

 >4o

<?43

<>44

245 

?4fi

*'?47

?4i>

?4fl

25(1

?,M

row

?53

354

flM

?5h

?57

?5S

?5q

?6fl

tffil
172 GEOLOGY AND WATER RESOURCES OF OKLAHOMA.

NOTES ON WELLS OF OKLAHOMA.

No. 1. Flows an inch stream nearly all the time.

No. 2. Tertiary sands are mixed with the Permian to some extent.

No. 9. The water from this well is hauled for miles by the settlers, many of whom 

have no other water near. The location is given from the Cimarron meridian (103°). 

Water analysis No. 2. *

No. 18. This is a test well. Pump was removed.

No. 31. Water in sand and gravel.

No. 32. Water in gravel.

No. 34. Water in red sand.

No. 35. Water in shale.

No. 36. Water in shelly sand rock.

No. 38. Water in sand.

No. 40. Water in sandy gravel.

No. 41. Water in sand.

No. 42. Water in sandstone. Water contains iron, Glauber's salt, chlorine, and 

perhaps other elements. Water analysis No. 22.

Nos. 43 and 44. Water in sand.

No. 45. Water in clay.

No. 46. Water in coarse sandstone.

No. 47. Water in gravel.

No. 48. Water in sandstone.

No. 49. Water in sand.

No. 50. Surface water in clay at 25 feet, main supply in sand rock.

No. 56. Used to irrigate garden.

No. 58. The well is in Oklahoma.

No. 59. Temporary watering station.

No. 75. Well is in Day County. Post-office in Woodward County.

No. 76. The owner says the amount is inexhaustible.

No. 77. The well is in Day County. Post-office in Woodward County. The above 

flow is about all it will yield. (I visited the well in person. Long.)

No. 81. The well is not far southeast from the Canadian River and is dug in a 

sandy loam with water in quicksand.

No. 91. Water in gravel.

No. 93. Water in sand.

No. 95. Abundance of water in quicksand.

No. 98. An abundance of water in sand. Used for irrigation.

No. 99. Water in sand rock. Is used for irrigation.

No. 101. Water was found in a clay formation.

No. 102. Water was found in gravel.

No. 103. Water found hi red gravel.

No. 104. Water found just under a hard cap rock in sand.

No. 105. Water in gravel.

Nos. 106 and 107. Water was struck in rock.

No. 108. Water found in sand.

No. 109. Water in red kiel.

No. 110. Water was struck in rock.

No. 117. The well is in Oklahoma.

No. 122. Water in gravel.

No. 123. Water in gravel. It is used to irrigate garden.

No. 124. Water in gravel.

No. 125. Water in slate.

No. 126. Water in sand.

No. 127. Water in soapstone.
' NOTES ON WELLS. 173

No. 128. Water in blue soapstone.

No. 129. Water in gray gypsum rock.

No. 130. Water in sand.

No. 131. Water in sand and gravel.

No. 151. Water analysis No. 48.

No. 152. Water in sandstone.

No. 153. This is a test well put down by a railroad company. Water found in 

sandstone.

No. 154. Water under sandrock. A strong flow.

No. 155. Water in sand.

No. 156. Water in iron-sandstone.

No. 157. Water in sandrock.

No. 158. Water in sand.

No. 159. Water in clay.

No. 160. Water in shelly sandstone. (Well in -Lincoln, post-office in Payne 

County.)

No. 161. Water in gravel.

Nos. 162, 163, and 164. Water in sandstone.

No. 165. Water in sand.

No. 166. Water in clay.

No. 168. Water in soft sandstone.

No. 169. Water in gravel.

No. 170. Water in gravelly clay.

No. 171. Water in cla^v.

No. 175. The owner says it is like putting a pump into a river to try to pump it dry.

No. 176. Analysis No. 52.

No. 177. Water in soft red sandstone.

No. 178. Water in clay.

No. 179. Water in white sandstone.

No. 180. Water in clay.

No. 182. Water in clay and sand.

No. 183. Water in sandrock.

No. 184. Water in white sandstone.

No. 185. Water in sandrock.

Nos. 187, 188, 189, and 191. Water in sandstone.

Nos. 192 and 193. Water in sand.

Nos. 194 and 195. Water in sandrock.

No. 196. Water in white sand.

No. 197. Water in sand and gravel. The well will fill up in 30 minutes.

No. 198. Water in limestone.

No. 199. Water in flint.

No. 200. Water in blue clay.

No. 201. Water found in fine gravel.

No. 202. Water in sandstone. A fair supply.

No. 203. Water between gravel and soapstone.

No. 204. Water in clay.

No. 205. Water found in sandstone.

Nos. 206 and 207. Water in sandrock.

No. 208. Water in limestone.

No. 209. Water in sandrock; supply abundant, but no record of the flow.

Nos. 210 and 211. Water in gravel.

No. 216. Water contains traces of soda.

No. 218. Water in white sandstone.

Nos. 219 and 220. Water in sandstone.

No. 221. Water in sandrock.

No. 247. The well has since gone dry.
INDEX.

A.

Adams, G. I., on Kansas physiography .... 14

on Oklahoma geology.................. 30-31

Allorisima subcuneata, occurrence of...... 34

Alluvium, occurrence and origin of ....... 84

springs from .......................... 99-100

water of ................................ 85

Altona, section near, diagram showing.... 45

Alva, water supply of..................... 99-140

Ammonites, occurrence of................. 78

Analyses of water .................... 143,146-154

Anthony, Kans., well at................... 107

Apache, sulphur spring at, character of... 105 

Arbuckle limestone, occurrence and character of......................... 27

water in............................. 85,95-96

Arbuckle Mountains, location of........... 15

Area of Oklahoma ......................... 11

Arkansas River, location and character of 18-19,89 

Arkansas River, Salt Pork of, gaging station on......................... 94

location and character of ........... 19,89-90

Athyris subtilita, occurrence of............ 34

Aviculopecten, occurrence of.............. 77

B.

Bakewelia, occurrence of .................. 77

Bat cave, section near, diagram showing.. 58 

Batrachia, occurrence of................... 76

Beaver County, rocks and water of ...... 131-133

Beaver Creek, _irrigation from............ 133-134

Beede, J. W., fossils identified by .......... 77

Big Salt Plain, location of.................. 101

section on, diagrams showing.......... 62,66

Bitter Creek, section along, diagram showing ............................. 50

Black Mesa, location of.................... 81

section of, diagram showing........... 82

Blaine County, rocks and water of....... 123-124

salt plain of, location and description

of............................. 102-103

Blaine formation, equivalents of .......... 39,44

occurrence and character of ........... 44-52

Bine Creek Canyon, rocks in............... 26

Boggy Creek, section at, diagram showing. 71

C.

Caddo County, buttes of, erosion forms of, 

' view of......................... 56

rocks and water of ................... 124-125

Cambrian rocks, occurrence and character

of............................... 26-27

Cambro-Ordovician rocks, occurrence and

character of.................... 27

Canadian County, rocks and water of.... 117-118

Page.

Carboniferous rocks, occurrence and character of......................... 28-77

Carter, section near, diagram showing..... 66

Case, E.G., fossils identified by ............ 76

Cedar Hills, rocks of, view of .............. 48

section through, diagram showing..... 47

Cedartop gypsum member, occurrence and

character of.................... 69-70

Cement, gypsum from, analyses of......... 63

Chandler district, rocks of ................. 33-34

Chaney gypsum member, occurrence and

character of.................... 66

Chemical constituents, common names of . 143 

Childress, Tex., well at..................... 106

Cimarron River, dam on, view of.......... 102

gaging station on....................... 91

irrigation from ....................... 133-134

location and character of ........ 19-20,90-91

reservoir site on, description of ........ 138

Cleo Springs, section at, diagram showing.. 122 

Cleveland, well at.......................... 107

Cleveland County, rocks and water of ... 115-116 

Climate, character of..................... 141-142

Cloud Chief, section near, diagram showing ............................. 64

Collingworth gypsum member, occurrence

and character of ............... 70-71

Comanche County, rocks and water of... 125-126 

Comanche series, occurrence and character of........................... 78

Conglomerate, occurrence of............... 73

springs from............................ 95-96

Conocardium, occurrence of ............... 77

Contour line system, explanation of ....... 13

Cragin, F. W., on red beds ..... 37-39,47-48,53-57

Cretaceous rocks, occurrence and character

of...................... ........ 77-79

Cricotillus brachydens, occurrence of...... 76

Cricotus sp., occurrence of ................. 76

Crossotelos annulatus, occurrence of....... 76

Cummins, A. W., on Texas red beds........ 37

Ouster County, rocks and water of......... 128

D.

Dakota sandstone, bluff of, view of ........ 92

erosion of, view of...................... 18

hills of, view of......................... 56

occurrence and character of......... 18,78-79

water in................................ 88-89

Dakota sandstone region, topography of ... 18 

water in ................................ 88-89

Day County, rocks and water of........;... 130

Day Creek dolomite, analysis of ........... 59

occurrence and character of............ 57-59

De Barr, Edwin, work of................... 12

175
176 INDEX.

Page. 

Delhi, section near, diagram showing...... 67

Devils Canyon Mountains, view of......... 14

Dewey County, rocks and water of....... 128-129

Diacranodus ampressus(?), occurrence of .. 76 

Dielasma, occurrence of.................... 77

Diplocaxilus limbatus (?), occurrence of.... 76

magnicornis (?), occurrence of..... ... 76

salamandroides, occurrence of ......... 76

Doe Creek, section on, diagram showing... 61 

Dog Creek shales member, occurrence and

character of ........ i........... 52

Drainage, character of ..................... 18-22

Drum limestone, occurrence of ............ 29-30

E.

Eldorado, section at, diagram showing .... 71

Elevations, location and character of ...... 13-18

Embolophorusl?) sp., occurrence of........ 76

Englewood, Kans., irrigation at............ 134

Enid formation, equivalents of ............ 39

occurrence and character of ........... 39-44

Eryops megacephalus, occurrence of....... 76,77

Estheria minuta, occurrence of............. 76

Evaporation, amount of.................. 138-139

Exogyra, occurrence of..................... 78

F.

Perguson, fossils from...................... 76

section near, diagram showing......... 50,51

spar near, analysis of................... 43

Ferguson gypsum member, occurrence and

character of .................... 46-47

view of................................. 48

Ficus, occurrence of........................ 79

Fields, , work of........................ 12

Flint-Sandstone Hills region, location and

character of .................... 16,85

rocks of................................. 16

water in................................ 86

Florence flint, occurrence of............... 34

Fort Reno, well at.......................... 106

Fort Riley limestone, occurrence of........ 34

Fort Sill, works near ....................... 25-26

Fort Supply, water supply of............... 140

Fossils, occurrence of....................... 75-77

G.

Gabbro, occurrence and character of....... 25

Gaging stations, location of................ 94

Garfield County, rocks and water of ..... 119-120

Gas wells, location and character of ..... 106-107

Geology of Oklahoma ...................... 18-84

Glass Mountains, rocks of, view of ......... 44

section at, diagram showing............ 54

Gould, C. N., work of....................... 11-12

Granite, sulphur spring at, character of.... 105

Granite, occurrence of...................... 26

view of ................................. 14

Granite-porphyry, occurrence of........... 25-26

Grant County, rocks and water of........ 120-121

Granton, butte near, section of, diagram

showing........................ 56

Greaves Creek, section near, diagram showing ............................. 56

Greer County, rocks and water of........ 126-127

saltplain invocation and description of. 104

Greer formation, equivalents of............. 39

occurrence and character of............ 69-72

Gridley, B. B., work of..................... 12

Gryphaea, occurrence of.................... 78

Gypsum, amount of ........................ 74-75

bluffs of, view of ....................... 16

cave in, section of...................... 52

view of............................. 62

occurrence of.................. 11,44-52,59,61

Gypsum Hills, clay from, analyses of ...... 42-43

location aud character of ........ 17,45-46,87

springs in .............................. 98

water in ............................. 87-88,98

Gypsum members, analyses of ....... 44,47,49,63

springs from............................ 98

H.

Hackberry Creek, section at, diagram showing ............................. 69

Haystack gypsum member, occurrence and .

character of .................... 69

section of, diagram showing............ 67

Heman, Mount, selenite from, analysis of.. 44 

Henquenets Canyon, clay from, analysis of. 42

gypsum from, analysis of............... 44

High Plains, lake basins on, view of ....... 16

location and character of .............. 17,88

water in................................ 88

Hill, R. T., on red beds..................... 37

Hitchcock, section near, diagram showing. 48 

Holter, , work of ..................... 12

Hominy district, rocks of .................. 32-33

I.

Igneous rocks, occurrence of......... 15.23,25-26

Irrigation, development of............... 133-141

J. 

Jet, well at ................................. 107

Kansas, Permian and Pennsylvanian rocks

in............................... 29

Kay County, rocks and water of......... 110-111

Kenton, erosion near, view of.............. 18

section near, diagram showing......... 82

Kingfisher, well at......................... 106

Kingfisher County, rocks and water of... 118-119 

Kiowa County, rocks and water of......... 126

Kirk, C. T., work of ........................ 12

Kiser gypsum member, occurrence and

character of.................... 67-68

L.

Larkin, Pierce, work of .................... 12,30

Lava, occurrence of........................ 81

Laverne area, rocks of ..................... 73

Lawton area, rocks of ...................... 73

Lima,occurrence of................ ........ 77 -

Limestone,springs from.................... 95-97

Lincoln County, rocks and water of........ 114

Little Washita River, section on, diagram

showing........................ 65

Logan County, rocks and water of ......... 117

Long,C.A., work of........................ 12,31

Low Plains, location and character of...... 16,86

water in................................ 86-87
INDEX.

177'

M. Page.

Main Creek, section on, diagram showing.. 58 

Mangum, section at, diagram showing ..... 70

Mangum dolomite member, occurrence

and character of................ 7L

Map of Oklahoma .......................... 14

of United States, showing arid, semiarid, and humid regions ....... 14 L

Map, drainage, of Oklahoma streams....... 90

Map, geologic, of Oklahoma ................ 12

Map, rainfall, of United States.............. 142

Marion formation, occurrence and character of......................... 34

Massern ranges, location of................. 15

Medicine Bluff, reservoir site at, description

of............................... 136

Medicine Lodge gypsum member, analyses

of............................... 49-50

occurrence and character of ............ 47-51

view of................................. 48

Meekella straticostata, occurrence of....... 34

Mentor beds, occurrence of ................ 78

Mineral, fossils from........................ 79

Miocene rocks, occurrence and character

of............................... 79-81

Mortar beds, structure of, diagram showing ............................. SO

view of................................. 80

N.

Nardin, fossils from near ................... 76

Naticopsis, occurrence of................... 77

Newkirk, well at ......................... 107, ION

Noasaurus sp., occurrence of ............... 76

Noble County, rocks and water of.......... 112

North Canadian River, gaging station on .. 94 

location and character of............ 20,91-92

O.

Oil wells, location and character of ...... 106-107

Oklahoma County, rocks and water of... 116-117' 

Oklahoma Salt Company, plant of ......... 103

Optima, well at ............................ 106

Ordovician rocks, occurrence and character

of............................... 27-28

Orlando, fossils from..... .................. 76

Gsage Nation, water supply of ........... 109-110

wells in....................... 106-107,109-110

Otter Creek, gaging station on ............. 94

reservoir site on, description of ...... 136-137

Ouachita Mountains, location of........... 15

P. 

Paleontology of red beds ................... 75-77

Paleozoic rocks, erosion of.................. 15

Pariotichus ordinatus, occurrence of....... 76

sp., occurrence of....................... 76

Pawhuska limestone, occurreuce of........ 30

Pawnee County, rocks and water of...... 112-113

Payne County, rocks and water of ....... 113-114

Pennsylvanian rocks, occurrence and character of.......................... 28-34

relation of Permian rocks and ......... 28-32

Permian rocks, occurrence and character of 34-77

relation of Pennsylvanian rocks and... 28-32 

Pinna peracuta, occurrence of ............. 34

IRR 148 05 M: 12

Page.

Pisces, occurrence of ....................... 76

Pit holes, view of........................... 20

Platanus, occurrence of .. ................. 79

Pleuristion brachycoelus, occurrence of.... 76

Pleurophorus, occurrence of................ 77

subcuneatus, occurrence of............. 76

Pleurotomaria, occurrence of............... 77

Population of Oklahoma ................... 11

Populus, occurrence of............:........ 79

Pottawatoinie County, rocksand water of. 114-115

Productus semireticulatus, occurrence of .. 34

Prosser, C. S., on Kansas stratigraphy...... 34

Quanah Creek, rocks at head of............. 25

Quanah Mountain, granite on, view of..... 14

Quartermaster formation, occurrence and

character of .................... 72-73

water in ................................ 88

Quartz Mountain, reservoir site at, description of........................ 137-138

reservoir site at, view of................ 92

Quaternary deposits, occurrence and character of......................... 82-84

Quinlan, section near, diagram showing..... 60

R.

Raggedy Mountains, rocks in .............. 25

Rainfall, amount of ............... 86,138,141-142

amount of, map of United States showing ............................. 142

Rainy Mountain, Sulphur Spring at, char-

 acter of......................... 105

Reagan sandstone, occurrence and character of......................... 26-27

Red beds, age of............................ 36

classifications of........................ 37-39

distribution of.......................... 36-37

erosion of, view of...................... 42

formation of, tables of.................. 38-39

importance of .......................... 35-36

section of, diagram showing ........... 40

occurrence and character of............ 35-77

slope of, view of........................ 42

springs of............................... 97

water of ................................ 85,87

Red River, bluffs on, view of............... 16

gaging station on....................... 94

location and character of........ 21-22,93-94

Reads, C. A., work of ....................... 12

Reptilia, occurrence of..................... 76

Reservoirs, irrigation from ............... 135-139

Rocks. See Igneous rocks; Sedimentary

rocks.

Roger Mills Company, rocks and water of . 129 

salt plain of, location and description

of............................. 103-104

Roscoe, section at, diagram showing....... 53

Russell, W. J., on irrigation in Kansas... 134-135

Sagenodus sp., occurrence of............... 76

Salix, occurrence of........................ 79

Salt, manufacture of ..................... 103,104

occurrence of........................... 11
178 INDEX.

Page. 

Salt Creek, section on, diagram showing... 51

salt plain of, location and description

of............................. 102-103

shale from, analysis of ................. 42

Salt Fork of Arkansas River. See Arkansas

River, Salt Pork of. 

Salt plains, location and character of. 42,100-104

view of................................. 100

See also Big Salt Plain. 

Salt springs,location and description of. 42,100-104

view of................................. 102

Salton, section at, diagram showing ....... 68

Sand Creek, section on, diagram showing.. 60 

Sand hills, occurrence and origin of....... H2-84

Sand Hills formation, spring from ......... 98

Sandstone, springs from.................... 97

Schizodus cf. Wheeleri, occurrence of...... 76

Sedgwickia, occurrence of................. 77

Sedimentary rocks, dip of.................. 12-13

occurrence of........................... 22-23

table of................................. 23

Selenite, analyses of........................ 43-44

view of................................. 44

Shales, analyses of ......................... 42

Shawnee, well at........................... 107

Sherwin, R. 8., work of .................... 12

Shimer gypsum member, analyses of....... 52

occurrence and character of............ 51-52

South Canadian River, location and character of................... 20-21,92-93

view on ................................ 92

Spirifer cameratus, occurrence of .......... 34

Springs, classification of ................... 94

irrigation from ....................... 139-140

location and description of............ 94-105

Springs, fresh-water, location and character

of.............................. 95-100

Spring, salt. See Salt springs.

Springs, sulphur. See Sulphur springs.

Storm waters, utilization of.............. 1;8-139

Streams, erosion by, view of ............... 20

irrigation from ....................... 133-135

location and character of......... 18-22,89-94

salt in .................................. 135

Stuckg Canyon, clay from, analysis of..... 42

Sulphur springs, location and description

of............................. 104-105

T.

Taff, J. A., oil Arbuckle limestone ......... 27

on Wichita conglomerate .............. 74

Tertiary pebbles, occurrence and description of.......................... 80

view of................................. 80

Tertiary rocks, occurrence and character

of............................... 79-XL

springs from............................ 98-99

section of, diagram showing....... 99

view of-............................. 98

structure of, diagram showing......... 80

water of ................................ 85,88

Texas, Permian and Pennsylvanian rocks

in............................... 29

Topographic regions of Oklahoma, list of.. 14

Page

Topography of Oklahoma, description of... 12-22 

Trimerorhachis leptorhynchus, occurrence

of............................... 76

sp., occurrence of ...................... 76

U.

Ulrich, E. O., on Viola limestone .......... 27-28

Unconformity, occurrence of............... 77,79

view of................................. 92

V.

Van Vleet, A. H., work of................ 12

Viola limestone, occurrence ar.d character

of............................... 27-28

W. 

Washita County, rocks and water of...... 127-128

Washita River, gaging station on .....'..... 94

location and character of .............. 21,93

Water, analyses of........................ 142-154

character of ............................ 84

sources of............................... 85

Water, artesian, chances for finding...... 108-109

Water, ground, conditions of............. 107-108

Water conditions, by counties............ 109-133

Water supply of Oklahoma................ 84-133

Watonga, section near, diagram showing.. 46 

Weatherford, gypsum cave at, view of..... 62

gypsum from, analyses of .............. 63

section near, diagram showing......... 63

Wells in red beds, comparison of......... 143-145

records of ............................ 155-173

diagrams showing.................. 106

water of, analyses of.................... 143

Wells, deep, character of................... 105

irrigation from....................... 140-141

Wells, flowing, occurrence of.............. 108

Wellington shales, occurrence and character of........................... 34

West Cache Creek, rocks at head of........ 25

Whitehorse sandstone member, occurrence

and character of............... 55-57

water of...... ~........................ 88

Whitehorse Spring, fossils from ............ 77

Wichita Mountains, location and character

of ........................... 15,24,85

map of ................................. 24

rocks of ............................. 15,23,26

springs of ............................. 95,100

water of................................ 85-86

Willis, Bailey, on Oklahoma reservoirs.. 136-138 

Williston, S. W., fossil identified by........ 76,77

Windmills, use of......................... 140-141

view of................................. 88

Wingfield formation, occurrence of........ 30,34

Woods County, rocks and water of....... 121-123

salt plain in, location and description

of............................... 101

Woodward County, rocks and water of... 130-131

salt plain in, location and description

of............................. 101-102

Woodward formation, equivalents of....... 39,52

occurrence and character of........... 52-59

Wreford limestone, occurrence of....... 30,31,34

O
PUBLICATIONS OF UNITED STATES GEOLOGICAL SURVEY.

[Watei>Supply Paper No. 148.1

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ADVERTISEMENT. Ill

B 213. Cement materials and industry of the United States, by E. C. Eckel. 1905. 395 pp., 15 pis.

B 246. Zinc and lead deposits of northeastern Illinois, by H. P. Bain. 1904. 56 pp., 5 pis.

B 247. The Fairhaven gold placers of Sevvard Peninsula, Alaska, by F. H. Mofflt. 1905,. 85 pp., 14 pis.

B 249. Limestones of southwestern Pennsylvania, by F. G. Clapp. 1905. 52 pp., 7 pis.

B 250. The petroleum fields of the Pacific coast of Alaska, with an account of the Bering Elver coai

deposit, by G. C. Martin. 1905. 64 pp., 7 pis. 

B 251. The gold placers of the Fortymile, Birch Creek, and Fairbanks regions, Alaska, by L. M.

Prindle. 1905. 89 pp., 16 pis. 

WS 118. Geology and water resources of a portion of east-central Washington, by F. C. Calkins. 1905.

96 pp., 4 pis. 

B 252. Preliminary report on the geology and water resources of central Oregon, by I. C. Russell.

1905. 138 pp., 24 pis. 

PP 36. The lead, zinc, and fluorspar deposits of western Kentucky, by E. O. Ulrich and W. 8. Tangier

Smith. 1905. 218 pp., 15 pis. 

PP 38. Economic geology of the Bingham mining district of Utah, by J. M. Bontwell, with a chapter on

areal geology, by Arthur Keith, and an introduction on general geology, by S. F. Emmons.

1905. 413 pp., 49 pis. 

PP 41. The geology of the central Copper River region, Alaska, by W. C. Mendenhall. 1905. 133 pp.,

20 pis. 

B 254. Report of progress in the geological resurvey of the Cripple Creek district, Colorado, by

Waldemar Lindgren and F. L. Ransome. 1904. 36 pp.

B 255. The fluorspar deposits of southern Illinois, by H. Foster Bain. 1905. 75 pp., 6 pis. 

B 256. Mineral resources of the Elders Ridge quadrangle, Pennsylvania, by R. W. Stone. 1905.

86 pp., 12 pis. 

B 257. Geology and paleontology of the Judith River beds, by T. W. Stanton and J. B. Hatcher, with

a chapter on fossil plants, by F. H. Knowlton. 1905. 174 pp., 19 pis.

PP 42. Geology of the Tonopah mining district, Nevada, by J. E. Spurr. 1905. 295 pp., 23 pis. 

WS 123. Geology and underground water conditions of the Jornada del Muerto, New Mexico, by C. R.

Keyes. 1905. .42 pp., 9 pis.

WS 136. Underground waters of Salt River Valley, Arizona, by W. T. Lee. 1905. 196 pp., 24 pis. 

PP 43. The copper deposits of Clifton-Morenci, Arizona, by Waldemar Lindgren. 1905. 375 pp., 25 pis. 

B 265. Geology of the Boulder district, Colorado, by N. M. Fenneman. 1905. 101 pp., 5 pis. 

B 267. The copper deposits of Missouri, by H. Foster Bain and E. O. Ulrich. 1905. 52 pp., 1 pi. 

PP 44. Underground water resources of Long Island, New York, by A. C. Veatch and others. 1905. 

WS 148. Geology and water resources of Oklahoma, by C. N. Gould. 1905. 178 pp., 22 pis.

SERIES O, UNDERGROUND WATERS.

WS 4. A reconnaissance in sontheastern Washington, by I. C. Russell. 1897. 96 pp., 7 pis.

WS 6. Underground waters of southwestern Kansas, by Erasmus Haworth. 1897. 65pp., 12 pis.

WS 7. Seepage waters of northern Utah, by Sauruel Fortier. 1897. 50 pp., 3 pis.

WS 12. Underground waters of southeastern Nebraska, by N. H. Darton. 1898. 56 pp., 21 pis.

WS 21. Wells of northern Indiana, by Frank Leverett. 1899. 82 pp., 2 pis.

WS 26. Wells of southern Indiana (continuation of No. 21), by Frank Leverett. 1899. 64 pp.

WS 30. Water resources of the Lower Peninsula of Michigan, by A. C. Lane. 1899. 97pp., 7 pis.

WS 31. Lower Michigan mineral waters, by A. C. Lane. 1899. 97pp., 4 pis.

WS 34. Geology and water resources of a portion of southeastern South Dakota, by J. E. Todd. 1900.

34 pp., 19 pis. 

WS 53. Geology and water resources of Nez Perces County, Idaho, Pt. I, by I. C. Russell. 1901. 86

pp., 10 pis. 

WS 54. Geology and water resources of Nez Perces County, Idaho, Pt. II, by I. C. Russell. 1901.

87-141 pp. 

WS 55. Geology and water resources of a portion of Yakima County, Wash., by G. O. Smith. 1901.

68 pp., 7 pis.

WS 57. Preliminary list of deep borings in the United States, Pt. I, by N. H. Darton. 1902. 60 pp. 

WS 59. Development and application of water in sou them California, Pt. I, by J. B. Lippincott. 1902.

95 pp., 11 pis. 

WS 60. Development and application of water in southern California, Pt. II, by J. B. Lippincott.

1902. 96-140 pp.

WS 61. Preliminary list of deep borings in the United States, Pt. II, by N. H. Darton. 1902. 67 pp. 

WS 67. The motions of underground waters, by C. S. Slichter. 1902. 106 pp., 8 pis. 

B 199. Geology and water resources of the Snake River Plains of Idaho, by I. C. Russell. 1902. 192

pp., 25 pis.

WS 77. Water resources of Molokai, Hawaiian Islands, by W. Lindgreu. 1903. 62 pp., 4 pis. 

WS 7S. Preliminary report on artesian basins in southwestern Idaho and soiitheastern Oregon, by

I. C. Russell. 1903. 53 pp., 2 pis. 

PP 17. Preliminary report on the geology and water resources of Nebraska west of the one hundred

and third meridian, by N. H. Darton. 1903. 09 pp., 43 pis.
IV ADVERTISEMENT.

WS 90. Geology and water resources of a part of the lower James River Valley, South Dakota, by J. E.

Todd and C. M. Hall. 1904. 47 pp., 23 pis. 

WS 301. Underground waters of southern Louisiana, by G. D. Harris, with discussions of their uses

for water supplies and for rice irrigation, by M. L. Puller. 1904. 98 pp., 11 pis.

WS 102. Contributions to the hydrology of eastern United States, 1903, by M. L. Puller. 1904. 522 pp. 

WS 104. Underground waters of Gila Valley, Arizona, by W. T. Lee. 1904. 71 pp., 5 pis. 

WS 110. Contributions to the hydrology of eastern United States, 1904; M. L. Fuller, geologist in charge.

1904. 211 pp.,5 pis. 

PP 32. Geology and underground water resources of the central Great Plains, by N.H. Darton. 1904.

433pp., 72 pis. 

WS 111. Preliminary report on imderground waters of Washington, by Henry Landes. 1904. 85 pp.,

1 pi. 

WS 112. Underflow tests in the drainage basin of Los Angeles River, by Homer Hamlin. 1904. 55

pp., 7 pis. 

WS 114. Underground waters of eastern United States; M. L. Puller, geologist in charge. 1904. 285

pp., 18 pis. 

WS 118. Geology and water resources of east-central Washington, by P. C. Calkins. 1906. 96 pp.,

4 pis. 

B 252. Preliminary report on the geology and water resources of central Oregon, by 1. C. Russell.

1905. 138pp., 24 pis. 

WS 120. Bibliographic review and index of papers relating to underground waters published by the

United States Geological Survey, 1S79-1904, by M. L. Puller. 1905. 128 pp. 

WS 122. Relation of the law to underground waters, by D. W. Johnson. 1905. 55 pp. 

WS 123. Geology and underground water conditions of the Jornada del Muerto, New Mexico, by O. R.

Keyes. 1905. 42 pp., 9 pis.

WS 136. Underground waters of the Salt River Valley, by W. T. Lee. 1905. 196 pp., 24 pis. 

B 264. Record of deep-well drilling for 1904, by M. L. Puller, E. P. Lines, and A. C. Veatch. 1905.

106 pp.

PP 44. Underground water resources of Long Island, New York, by A. C. Veatch and others. 1905. 

WS 137. Development of underground waters in the eastern coastal plain region of southern California, by W. C. Mendenhall. 1905. 140 pp., 7 pis.

WS 138. Development of underground waters in the central coastal plain region of southern California, by W. C. Mendenhall. 1905. 162 pp., 5 pis.

WS 139. Development of underground waters in the western coastal plain region of southern California, by W. C. Mendenhall. 1905. 105 pp., 8 pis. 

WS 140. Field measurements of the rate of movement of underground water, by C. S. Slichter. 1905.

122pp., 15 pis. 

WS 141. Observations on the ground waters of the Rio Grande Valley, 1904, by C. S. Slichter. 1905,

83 pp., 5 pis. 

WS 142. The hydrology of San Bernardino Valley, California, by W. C. Mendenhall. 1905. 124 pp.,

12 pis. 

WS 145. Contributions to the hydrology of Eastern United States, 1905, M. L. Puller, geologist in

charge. 1905. 22 pp., 6 pis. 

WS 148. Geology and water resources of Oklahoma, by C. N. Gould. 1905. 178 pp., 22 pis.

The following papers also relate to this subject: Underground waters of Arkansas Valley in eastern 

Colorado, by G. K. Gilbert, in Seventeenth Annual, Pt. II; Preliminary report on artesian waters of a 

portion of the Dakotas, by N. H. Darton, in Seventeenth Annual, Pt. II; Water resources of Illinois, 

by Frank Leverett, in Seventeenth Annual, Pt. II; Water resources of Indiana and Ohio, by Prank 

Leverett, in Eighteenth Annual, Pt. IV; New developments in well boring and irrigation in eastern 

South Dakota, by N. H. Darton, in Eighteenth Annual, Pt. IV; Rock waters of Ohio, by Edward 

Orton, in Nineteenth Annual, Pt. IV; Artesian well prospects in the Atlantic coastal plain region, 

by N. H. Darton, Bulletin No. 138.

Correspondence should be addressed to

THE DIRECTOR,

UNITED STATES GEOLOGICAL SURVEY,

WASHINGTON, D. 0. 

DECEMBER, 1905.
LIBRAEY CATALOGUE SLIPS.

[Mount each slip upon a separate card, placing the subject at the top of the 

second slip. The name of the series should not be repeated on the series 

card, but the additional numbers should be added, as received, to the first 

entry.]

Gould, Charles Newton, 1868-

. . . Geology and water resources of Oklahoma, by 

g

| Charles Newton Gould. Washington, Gov't print, off.,

**J

1905.

178, vp. illus., XXII pi. (incl. 3 maps) diagrs. 23om (U. S. Geological survey. Water-supply and irrigation paper no.-148)

Subject series: B, Descriptive geology, 72; O, Underground waters, 47. 

1. Geology Oklahoma. 2. Water-supply Oklahoma.

Gould, Charles Newton, 1868-

| ... Geology and water resources of Oklahoma, by 

3 Charles Newton Gould. Washington, Gov't print, off,, 

1905.

178, v p. illus., XXII pi. (incl. 3 maps) diagrs. 23cm. (U. S. Geolog1 cal survey. Water-supply and irrigation paper no. 148)

Subject series: B, Descriptive geology, 72; O, Underground waters, 47. 

1. Geology Oklahoma. 2. Water-supply Oklahoma.

U. S. Geological survey.

i Water-supply and irrigation papers. 

* no. 148. Gould,. C. N. Geology and water resources 

of Oklahoma. 1905.

U. S. Dept. of the Interior.

g see also

9

| U. S. Geological survey.