Water-Supply and Irrigation Paper No. 199 Series^;

DEPARTMENT OF THE INTERIOR

UNITED STATES GEOLOGICAL SURVEY

CHARLES D. WALCOTT, DIEECTOE

UNDERGROUND WATER

IN

SANPETE AND CENTRAL SEVIER 

VALLEYS, UTAH

BY

G. B. RICHARDSON

PROPERTY QT 

;, GEOLOGICAL SURVEY

WASHINGTON 

GOVERNMENT PRINTING OFFICE

1907

CONTENTS.

Page.

Introduction_________________________________ 5

Topography __________________________________ 6

Geology ___________________ _ ____ ___ _ ___ _ __ _ 8

Bed rocks ______________________________________ 8

Jurassic system________________________________ 8

Cretaceous system__________________________ 9

Undetermined age__________________________ 10

Tertiary system.________,.__________________ 10

Igneous rocks________________________________ 12

Valley deposits ____ ___ ___________ ___ ____ ___ 12

Quaternary system_____________________________ 12

Structure _________________________________________ 13

Source of underground water______________________ 14

Precipitation _________________________________________ 15

Flow of streams_______________________________ 16

Other sources________________ __________________ 21

Distribution of underground water_______________________ 21

In bed rocks____________________________ 22

In valley deposits______________________________ 23

Recovery of underground water________ ____________________ 24

From bed rocks______________________________ 25

By springs_________________ _______________ 25

By tunnels ____________________ _____________ 26

By wells_____________________________________ 27

From valley deposits_________________________ ____ 27

By springs________________________ _ ____ 27

By tunnels __________________ _______________ 28

By nonflowing wells________________'_____________ 28

By flowing wells____________________________ 29

By subsurface dams, etc_____________________ 30

Quality of water____________________________,______ 30

Suggestions __ _ _ ______________________________ 32

Detailed descriptions________________________________ 34

Joseph and vicinity_________________ ____________ 34

Elsinore and vicinity_________ ______________ 35

Monroe and vicinity_________________________________ 36

Richfield and vicinity________________________________ 37

Salina and vicinity______________________________ 40

Gunnison and vicinity_________________________ 42

Mayfield and vicinity______________________________ 43

Manti and Ephraini______________________________ 44

Moroni and vicinity.___ ____ _____ __________________ 46

Fountain Green and Wale.__________________________ 47

Mount Pleasant and vicinity________________________ 48

Well and spring data______________________________ 51

Index ___________________ _ ______________________ 61

3
ILLUSTRATIONS.

Page. 

PLATE I. A, Sagebrush upland south of Freedom, showing alluvial fan;

B, cultivated fields south of Ephraim____________ 5

II. Reconnaissance geologic map of Sanpete and central Sevier

valleys_______________________._____ Pocket

III. Structural sections across Sanpete and central Sevier valleys_ 12

IV. A, Fault spring west of Fountain Green; B, the Wasatch

monocline and Manti Creek____________________ 14

V. Map showing approximate depth to ground water and location

of wells and springs in central Sevier Valley__________ 22

VI. Map showing approximate depth to ground water and location

of wells and springs in Sanpete Valley_____________ 24

FIG. 1. Map of Utah, showing position of Sanpete and central Sevier

valleys___________________________ 6

2. Hypothetical section across Sanpete Valley________-__ 13

3. Diagrammatic section at Richfield Spring______________ 26

4. Diagrammatic section at Morrison Tunnel Spring_________ 26

5. Section illustrating a tunnel in the valley deposits___________ 28

4
U. S. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. 199 PL. I

A. SAGEBRUSH UPLAND SOUTH OF FREEDOM, SHOWING ALLUVIAL FAN.

B. CULTIVATED FIELDS SOUTH OF EPHRAIM.

UNDERGROUND WATER IN SANPETE AND CENTRAL 

SETTER VALLEYS, UTAH.

By G. B. RICHARDSON.

INTRODUCTION.

Sanpete and central Sevier valleys are situated at the border of 

the Basin Range and Plateau provinces in south-central Utah. They 

are bounded on the east by the Wasatch and Sevier plateaus and on 

the west by the Gunnison Plateau and the Valley and Pavant ranges, 

and are drained by Sevier River, which empties into Sevier Lake in 

the Great Basin. (See fig. 1, p. 6.)

These valleys rank with the richest parts of the State. They were 

occupied a few years after the Mormon pioneers founded Salt Lake 

City, in 1847, when settlements, which soon became thriving farming communities, were established where water for irrigation was 

most available. A variety of crops, especially wheat, are successfully grown, and the valleys are popularly known as the " granary 

of Utah." Sheep raising is also an important industry, the adjacent 

highlands being used for summer pastures. The climate is arid, and 

there is a striking contrast between those areas which in their natural 

state are covered with sagebrush and grease wood and the fruitful 

cultivated tracts. (See PI. I, A and B.) Trees are normally absent 

in the valleys, but they flourish to a limited extent on the adjacent 

highlands, where there are thin growths of quaking aspen, scrub 

oak, and stunted conifers. Irrigation is necessary for the production of crops.0 Canal systems are maintained by San Pitch Creek and 

Sevier River, and the mountain streams are tapped by ditches near 

the mouths of the canyons, but this supply is insufficient and attention is being turned to the subterranean store.

This report is a preliminary statement of the general conditions 

of occurrence of underground water in Sanpete and central Sevier 

valleys. The field work was carried on in cooperation with Sanpete 

and Sevier counties through the State engineer, Mr. Caleb Tanner, 

who detailed Mr. C. S. Jarvis to collect the data embodied in the list 

of springs and wells on pages 51-60.

0 Dry farming has not yet been extensively practiced here.
UNDERGROUND WATER IN VALLEYS OF UTAH. 

TOPOGRAPHY.

Sanpete and central Sevier valleys are structural troughs filled 

with " wash" derived from the adjacent highlands. They trend 

northeast - southwest, and are occupied by relatively small streams, 

Sevier River draining the southern, and its tributary, San Pitch

FIG. 1. Map of Utah, showing position of Sanpete and central Sevier valleys.

Creek, the northern valley. Each valley is about 45 miles in length 

and averages 6 miles in width.

The main central streams have a number of tributaries, the more 

jmportant of which flow from the eastern plateaus, where the precipitation is greater than on the relatively low and narrow western 

highlands. The streams flow perennially within the mountains.
TOPOGRAPHY. 7

where they occupy steep, narrow valleys, but at the mouths of the 

canyons the discharge is largely diverted by irrigation canals, and the 

lower courses in the broad lowlands are generally dry, except during 

floods. The chief tributaries of San Pitch Creek are Cottonwood, 

Pleasant, Cedar, Oak, Canal, Ephraim, Willow, Manti, Sixmile, and 

Twelvemile creeks, all of which have small drainage areas on the 

Wasatch Plateau. Salina Creek, draining 255 square miles, is by far 

the largest tributary stream. It flows in the depression between 

the Wasatch and Sevier plateaus and joins Sevier Eiver 13 miles 

above Gunnison. The other important tributaries of the Sevier 

in its central valley are Lost and Monroe creeks, which rise in the 

Sevier Plateau.

The elevation of Sanpete and central Sevier valleys ranges from 

5,000 feet above sea level in their lower parts to about 6,000 feet at 

the upper border of the lowlands, above which the mountains rise 

from 2,000 to 5,000 feet higher.

Gunnison Plateau, bordering Sanpete Valley on the west and separating it from Juab Valley, is 35 miles long and varies from 2 to 

8 miles in width. The plateau is considerably dissected, and only 

remnants of its former surface are preserved by horizontal beds of 

limestone. At its northern end the plateau has an elevation of almost 

10,000 feet, but it slopes southward and merges into Sevier Valley at 

Gunnison. A sparse growth of vegetation is supported on the Gunnison Plateau, from which only a few feeble streams are tributary 

to Sanpete Valley.

The Wasatch Plateau borders Sanpete Valley on the east and extends as far south as the valley of Salina Creek. The crest of-the 

plateau is underlain by Cretaceous and Tertiary sediments, which, on 

the east, form a wall of erosion, beyond which the surface slopes to 

Castle Valley, a lowland underlain by shale, which separates the 

plateau from the San Eafael swell. On the west the Wasatch 

Plateau slopes toward Sanpete Valley, conforming with a great 

monoclinal flexure. The Wasatch Plateau is comparatively well 

timbered and is the source of a number of perennial streams.

Sevier Plateau forms the greater part of the eastern boundary 

of Sevier Valley, above which it rises abruptly, and extends from the 

valley of Lost Creek far to the south of the area under consideration. 

Its culminating point is Monroe Peak, whose elevation is 11,240 

feet. The plateau is underlain by a series of igneous rocks, chiefly 

Tertiary tuffs and lavas. The East Fork of Sevier River receives a 

considerable part of the drainage of Sevier Plateau, but Monroe 

Craek is the only important stream that drains directly from it into 

the area here considered.

Central Sevier Valley is bounded on the west by the Pavant and 

Valley mountains, which are the easternmost parts of the Basin
8 UNDEEGEOUND WATER IF VALLEYS OF UTAH.

Kanges in this latitude. The Pavant Mountains are about 35 miles 

long and from 4 to 12 miles wide and are much dissected, their crest 

forming a narrow ridge about 10,000 feet in elevation. The range is 

but fairly well timbered and only a few small creeks flow from it to 

the valley. The eastern slopes are underlain by east-dipping strata, 

which unconformably overlie Paleozoic limestone. The Valley 

Mountains lie between the Gunnison Plateau and the Pavant Mountains, of which they are a faulted offset. They are 25 miles long, 

average 5 miles in width, and are about 7,000 feet high. They are 

practically bare of vegetation and give rise to no important streams.

Sanpete and Sevier valleys are represented on the map of the 

Wheeler Survey ° and are described in Dutton's report on the geology 

of the High Plateaus of Utah.6 but no detailed geologic work has yet 

been done in this region. The character and structure of the rocks 

are fairly well known, however, and the following brief summary, 

together with the maps and sections (Pis. II, III, V, and VI), indicates the general geologic conditions of occurrence of underground 

water.

The rocks of these valleys can conveniently be classified as consolidated " bed rocks," which outcrop chiefly on the highlands, and 

unconsolidated deposits, which occur in the broad central valleys. 

Strata of Mesozoic and Tertiary age occupy the greater part of the 

highlands, and igneous rocks are found in their extreme southern 

portion. The valleys, on the other hand, are underlain to considerable depths by debris derived from the disintegration of the 

adjacent highlands. The underground water occurs chiefly in the 

unconsolidated deposits, but water contained in the bed' rocks is 

locally important.

BED ROCKS. 

JURASSIC SYSTEM.

So far as known, the oldest rocks of Sanpete and Sevier valleys are of Jurassic age. They consist of a considerable but undetermined thickness of fissile clay shales, generally drab in color, but 

locally red, with some intercalated layers of drab sandstone ranging 

in thickness from a few inches to a few feet. Lenses of gypsum and 

rock salt are irregularly interbedded throughout the formation. 

These rocks outcrop in a range of low hills, about 30 miles long and 

2 miles wide, that extend along the eastern margin of Sevier Valley 

from Glenwood to the vicinity of Mayfield. A less extensive outcrop

0 U. S. Geog. Surv. W. 100th Mer., Atlas.

6 Button, C. B., Geology of the High Plateaus of Utah : U. S. Geog. and Geol. Surv. 

Rocky Mt. Region, 1880.
JURASSIC AND CRETACEOUS ROCKS. 9

occurs in the center of the valley, mostly west of Sevier River, between Redmond and Gunnison. On the east a fault causes these 

Jurassic strata to abut against Tertiary beds, as mentioned later, 

but relations are generally concealed by Quaternary deposits. The 

hills are practically bare of vegetation, and the soft beds have been 

eroded into badland topography. These rocks are of no value in 

the recovery of underground water. They exert, however, an important deleterious influence upon the character of streams with which 

they come in contact because of the ready solubility of their interbedded salt and gypsum.

CRETACEOUS SYSTEM.

The Cretaceous system is represented by two divisions, the Colorado and the Laramie. A small outcrop of rocks of Colorado age 

occurs in the valley of Salina Creek just above the mouth of the 

canyon, about 3 miles from Salina. These are a thin-bedded buff 

sandstone, with subordinate drab shale carrying Inoceramus labiatus." At the western limit of their outcrop the Colorado strata stand 

almost vertical and are directly overlain by horizontal Eocene beds. 

Because of their limited exposure these rocks also are unimportant 

in the recovery of underground water.

Sandstones and shales provisionally referred to the Laramie division of the Cretaceous occupy a much greater area. The coal-bearing 

Laramie beds of Carbon County, which outcrop along the eastern 

scarp of the Wasatch Plateau, are conformably overlain by massive, 

loose-textured, buff sandstone, with subordinate interbedded buff shale. 

The thickness of these rocks has not been determined, but it amounts 

to several hundred feet.6 They locally cap the plateau and outcrop 

along its middle western flanks east of Sanpete Valley as far as 

Spring Creek, and are exposed farther south in the valleys of 

several creeks that have cut deeply into the Wasatch monocline.

The only fossils that have been found in this formation on the 

Wasatch Plateau are a few obscure fragments of leaves, but in what 

is probably the same formation, in a fault block south of Manti, in 

which the Sterling coal c occurs, a number of plant remains have been 

found. Among them F. H. Knowlton recognizes Sdbal? cf. Sabalites Gray an/us, Asimina eocenicaf Lesq., and Salix sp. ? From these 

he concludes that the formation is probably of Laramie age.

At many localities on the Wasatch Plateau these rocks are overlain, 

apparently conformably, by Eocene strata. Different sections at the 

base of the known Tertiary, however, show deposits so diverse and

0 Determined by T. W. Stanton.

"Taff, J. A., Book Cliffs coal field, Utah: Bull. U. S. Geol. Survey No. 285, p. 292. 

c Richardson, G. B., Coal in Sanpete County, Utah : Bull. U. S. Geol. Survey No. 285, 

p. 280.
10 UNDERGROUND WATER IN VALLEYS OP UTAH.

thicknesses so different that there is no conformity in the sense of a 

succession of widespread, uniform, uninterrupted deposits. In the 

vicinity of Sterling a distinct local unconformity is marked by flat 

Tertiary beds resting on highly inclined Laramie (?) sandstone.

The sandstone on the flanks of the Wasatch Plateau is a probable 

source of artesian water. (See p. 22.)

UNDETERMINED AGE.

A considerable thickness of red and buff conglomerate and sandstone, amounting to at least 2,000 feet, is exposed on the eastern 

flanks of the Pavant Mountains and Gunnison Plateau. The conglomerate is composed of rounded pebbles of quartzite and subordinate limestone of variable size, up to 1 foot in diameter, embedded 

in a sandy matrix. The main mass of conglomerate is overlain by 

fine-textured sandstone, but intercalated with the sandstone there are 

also beds of conglomerate. Drab shale of minor importance is locally 

interbedded with the sandstone. In the valley of upper Corn Creek, 

about 8 miles northwest of Elsinore, the basal conglomerate rests upon 

the eroded surface of steeply tilted Paleozoic sediments, and a similar conglomerate overlies upturned Carboniferous strata at the eastern base of Mount Nebo, about 15 miles northwest of Fountain 

Green. These conglomerates and sandstones, both on the Gunnison 

Plateau and on the Pavant Mountains, are overlain in apparent conformity by strata of Eocene age, but no fossils have been found in 

either the conglomerate or the sandstone, and the age of the rocks is 

as yet undetermined. The disconnected areas that have the same 

color on the map are grouped together only provisionally.

The conglomerate sandstone formation on the eastern flank of the 

Pavant Mountains is likely to prove a source of artesian water. 

(See p. 23.)

TERTIARY SYSTEM.

Strata of Eocene age outcrop on the summit and western flanks of 

the Wasatch Plateau, on the summit and eastern part of the Gunnison Plateau, and on the eastern slope of the valley and Pavant Mountains, and also form low ridges in Sevier and Sanpete valleys. These 

Tertiary sediments consist of at least 2,000 feet of drab, green, and 

red shales, buff and reddish sandstones, and whitish, fresh-water 

limestones. The stratigraphy is varied, and even adjacent sections 

are rarely alike. Numerous fresh-water fossils, including Sphcerium, 

Planorbis, Physa, Goniobasis, and Viuiparaf occur in these rocks, 

which are referred to the Wasatch stage of the Eocene. The following section was measured west of Wales.

a Identified by W. H. Ball.
TEBTIAKY ROCKS. 11

Generalized section of Eocene rocks on Gunnison Plateau west of Wales.

Feet. 

Fine-textured white limestone______________________________ 100+

Interval of talus___________________________________ 100

Gray limestone__________________________________^_____ 10

Brown sandstone_____________________________ 10

Interval of talus____________________________________ 150

Brown sandstone_______________________ __________ 5

Drab limestone ________________________. ______..__ 15

Brown sandstone_________________________________ 10

Drab limestone ___________________________ .__ 5

Interval of talus______________________________________ 100

White limestone ___________________________!________ 10

Drab shale _______________________________________ 50

Buff limestone__________________________________ 15

Drab shale ___________________________________ 50

Interval of talus__________________________'_________ 150

Drab limestone ________________________________________ 10

Drab shale with streaks of purple shale__________________ 150

Brown sandstone ________________________________ 20

Drab shale with few thin beds of limestone_________________ 250

Brown sandstone ____ __________________ __________ 5

Drab shale _____________ __________________ _________ 25

Brown sandstone _____________________________________ 10

Buff shale_______________________________________ 100 

Gray limestone___________________________________ 25

Black limestone______________________________ 5

Coal and bone __________ __________________ ____ 7

Black limestone-____________________________:__________ 10

Dark shale .,________________________^__________ 15

Brown sandstone _____________________ ___________ 10

Drab shale _________________________________ 10

Gray limestone.________________________________________ 5

Buff shale___________________________________1____.. 40

Sandstone _________________________________ 10

The coal noted above is locally important,'1 but is not of widespread 

occurrence.

Younger Eocene strata outcrop in low ridges in Sanpete Valley, 

extending north ward from Manti. They dip westward at low angles 

and their outcrops are surrounded by Quaternary deposits which conceal relations with the underlying rocks exposed on the flanks of the 

adjacent plateau. These younger rocks consist of light-colored sandstone, shale, and limestone, including a bed of oolitic limestone, and 

contain well-preserved specimens of fishes, turtles, etc. Cope 6 named 

them the Manti beds and regarded them as middle Eocene, corresponding to the Wind River stage. Because of insufficient knowledge concerning the base of the formation it is not differentiated here,

" Richardson, G. B., Coal in Sanpete County, Utah: Bull. TJ. S. Geol. Survey No. 

285, p. 292.

6 Cope, B. D., The Manti beds: Am. Naturalist, vol. 14, 1880, p. 303.
12 UNDERGROUND WATER IN VALLEYS OF UTAH.

but is mapped as Eocene, together with the strata referred to the 

Wasatch stage.

The varying stratigraphy of Eocene strata, the prevalence of 

shale and limestone, and the minor occurrence of more pervious 

strata render the rocks of little importance as water reservoirs. Yet 

these relatively impervious beds serve to confine water in the underlying sandstones and conglomerates, and are thus important factors 

in the occurrence of artesian water.

IGNEOUS ROCKS.

Igneous rocks are unimportant as water reservoirs in Sanpete and 

Sevier valleys, for they occupy small areas and are massive, fine 

textured, and of low porosity. Their occurrence is chiefly restricted to 

the upper part of central Sevier Valley, to the Sevier Plateau south 

and east of Richfield, and to the base of the Pavant Range, west of 

Elsinore. They constitute the northern end of a mass which is well 

developed farther south. These rocks are for the most part a complex series of lavas that were poured out upon eroded surfaces of 

the underlying strata at different intervals in Neocene time."

VALLEY DEPOSITS. 

QUATERNARY SYSTEM.

The broad central floor of Sanpete and Sevier valleys is composed 

of fine-textured soils, chiefly sand and clay loam, but toward the 

highlands the material becomes coarser and the mountains are flanked 

by alluvial fans and slopes consisting of sand and gravel, with subordinate clay, the coarser material! preponderating near the mountains. These deposits are derived from the disintegration of the 

adjacent highlands and transported to the valley by streams. In 

their mountain courses the volume and velocity of the creeks are considerable, especially during floods, and their carrying power is proportionally large, but upon entering the valley both volume and 

velocity decrease, the result being that the coarser materials carried 

by the streams are dropped near the base of the highlands while the 

finer debris is borne farther into the lowlands. Alluvial fans, consisting of heterogeneous masses of coarse sand and gravel, are thus 

formed about the mouths of the canyons (PI. I, J.), and alluvial 

slopes accumulate along the base of the mountains between the creeks, 

chiefly as the result of torrential storms.

The deposits beneath the surface of the broad valleys consist of 

gravel, sand, and clay, the thickness of ,which is considerable, but

a Dutton, C. E., Geology of the High Plateaus of Utah : U. S. Geog. and Geol. Surv. 

Rocky Mt. Region, 1880.
U. S. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. 199 PL. Ill

SECTION C-O

I

« 

6 o>

SECTION E-E

SECTION F-F

Scale ,- 

toooo zoooo 30000 feet

I. Jurassic? ^.Colorado 3. Laramie ? 4. Red and buff conglomerate and sandstone 5.Eocene 6. Quaternary 7. Igneous

STRUCTURAL SECTIONS ACROSS SANPETE AND CENTRAL SEVIER VALLEYS.

STKTJCTURE OP THE BOOKS. 13

unknown; minimum depths in the main part of the valleys are 530 

feet in Sevier and 650 feet in Sanpete Valley, as- shown by two wells,0 

in neither of which was consolidated rock found. 

Alternating beds of gravel, sand, and clay, from 

a few inches to many feet in thickness, are encountered in driving wells. Few records have 

been kept, however, and the detailed underground 

distribution of the valley deposits remains to be 

determined. In general, coarse material preponderates near the highlands and finer textured 

debris is more abundant in the lowlands, the inclination of the deposits being toward the valleys, in 

the attitude of deposition. Sections, even of neighboring wells, can rarely be correlated, which implies that the deposits, instead of having wide 

lateral distribution, as homogeneous beds, consist * 

of series of lenses, with imperfect connection, as ; 

illustrated in the section forming fig. 2. These j! 

deposits are in large part loose, porous, and satu- ^ 

rated with water, and constitute the most import- f 

ant underground reservoirs of the region. I

o

STRUCTURE. E

c

The strata that cap the highlands lie practically ? 

flat, but have been tilted and faulted along the mar- i 

gins of the lowlands, and the central valleys are I 

structural depressions. The rocks are not folded \ 

in the strict sense of the term, but incident to the \ 

uplift of the plateaus monoclinal flexures and v 

normal faults have been developed. (See PL III.)

A conspicuous structural feature of the region 

is the monocline that marks the western border 

of the Wasatch Plateau. Near the rim of the 

plateau the strata dip westward, and along the 

flanks a dip slope of large proportions is developed. (See PI. IV, B,} On this the strata that 

outcrop on the summit descend between 4,000 and 

5,000 feet in about 5 miles and pass beneath the 

valley floor. Other large monoclines appear on 

the flanks of the Pavant and Valley- ranges, where 

strata that dip eastward at a low angle descend 

toward Sevier Valley. The Jurassic shales that 

outcrop in a narrow belt between Glenwood and Mayfield constitute

0 Nos. lOla and 186, pp. 53 and 55.
14 UNDERGROUND WATER IN VALLEYS OF UTAH.

another conspicuous zone of tilted strata. Throughout their extent 

they dip eastward at an average angle of 45°.

One of the prominent faults in the area under consideration 

intersects the eastward-dipping strata of the Pavant Mountains at 

the base of the range. This fault extends along the border of the 

valley to a point about 8 miles north of Richfield, where it turns 

northwestward and causes the Eocene shales and limestones to abut 

against the underlying upthrown red conglomerates.

The abrupt rise of Sevier Plateau several thousand feet above the 

valley and the presence of springs along its base indicate a fault, and 

a number of displacements that can be traced east of the valley and 

parallel to it lie between Glenwoocl and Manti. The eastwarddipping shales there form an upthrust block bounded on the east and 

west by north-south trending faults, by which the Jurassic beds are 

brought into contact with Eocene strata. The northern end of this 

block adjoins a much-disturbed zone between Mayfield and Manti, 

wT here the area between the Gunnison and Wasatch plateaus has been 

broken by several approximately parallel faults, as shown by the 

map and sections. The southwestern flank of the Wasatch Plateau 

is traversed by a numbe* of minor parallel displacements, which fade 

away to the north and have not been traced beyond Manti Creek. 

Along the eastern base of the Gunnison Plateau a fault brings the 

red conglomerate with a high eastward dip against practically horizontal Eocene limestones and shales. The throw of some of the 

faults is considerable, but data are lacking for close measurement.

These structural features have an important bearing on the occurrence of underground water, as described on pages 25-27. A number 

of strong springs are associated with the faults, and the monoclinal 

flexures control the occurrence of water under pressure.

SOURCE OF UNDERGROUND WATER.

The underground water supply of Sanpete and Sevier valleys is 

derived from the rain and snow that fall on their drainage areas. 

Of the total precipitation, part evaporates, part flows off in streams, 

and part sinks into the ground. The relative amounts that are thus 

disposed of vary greatly under different conditions, and a complex 

series of changes ensues between precipitation and the final disappearance of the water- from the drainage basin. Evaporation occurs either 

directly from snow, from a free surface of water, and from water 

contained in soils or indirectly, by transpiration through the growth 

of plants. Of the portion of the precipitation that joins the run-off, 

part leaves the basin in surface streams and part is absorbed by the 

soils and rocks over which the streams flow. The underground supply is further augmented by direct absorption from the surface on
U. 8. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. 199 PL. IV

A. FAULT SPRING WEST OF FOUNTAIN GREEN.

B. THE WASATCH MONOCLINE AND MANTI CREEK.

SOUECE OF UNDERGROUND WATER. 15

which the rainfall occurs. Part of the subterranean waters find 

their way back to the surface in springs, another part is consumed 

by the growth of organisms and by mineralogical changes, and a 

third part joins the more permanent supply of underground water.

PRECIPITATION.

Precipitation on the highlands, especially snow, which falls early 

and lingers late, is the chief source of supply of the streams which, 

as will presently be shown, are the most important contributors to 

the store of underground water in the valleys. There are no records 

of precipitation on the highlands, but the marked difference in vegetation between the forested mountains and the naturally desert 

valleys implies a considerably greater amount on the former. In the 

valleys, on the other hand, rainfall data have been kept for a number 

of years, although this precipitation contributes relatively little to 

the supply of underground water.

The mean annual amount for the past seven years ranges from 

6.73 inches at Richfield to 11.37 at Mount Pleasant, and of this about 

40 per cent falls during January, February, and March, when the 

frozen condition of the ground is unfavorable for absorption. Besides the direct run-off, much of the precipitation in the valley joins 

the streams as seepage run-off, and, in addition to the water that is 

lost through plant growth, large amounts are evaporated from the 

ground, the supply being maintained by capillary action. A considerable part of the rainfall on the valley is therefore lost by run-off 

and evaporation. The remainder replenishes the more permanent 

supply of underground water, relatively large quantities being 

absorbed by areas that are underlain by porous sand and gravel.

The following tables of precipitation at Richfield, Manti, and 

Mount Pleasant, compiled from records of the United States Weather 

Bureau, show the amount and distribution of the valley rainfall for 

the past seven years:

Monthly and annual precipitation at Richfield from 1899 to 1905.

Year.

1899...............

IQflfi

1901...............

1902...............

 I AAQ

1904...............

1905...............

Jan.

0.30

.45

.35

.60

.55

.90

.54

Feb.

0.55

.65

.20

.65

Mar.

4.65

1.07

1.35

.67

.16

1.56

Apr.

0.70

.23

.17

.07

.29

May.

T.

.10

.32

1.03

.58

June.

0.14

T.

.07

.24

T.

.80

.31

July.

0.16

0

.14

.18

.31

.27

.21

Aug.

0.12

.07

.03

.22

.30

.37

.19

Sept.

0.07

.07

0

.64

1.00

.05

.37

Oct.

0.38

.05

.26

.83

.95

.49

Nov.

0.20

.30

1.77

0

.76

Dec.

1.05

0

.74

.47

.04

.80

.28

.56

Annual.

8.32

6.62

5.25

6.73
16 UNDERGROUND WATER IN VALLEYS OF UTAH.

Monthly and annual precipitation at Manti from 1899 to 1905.

Year.

1899..............

1900..............

1901..---.........

1902..............

1903..............

1904..............

1905..............

Mean ......

Jan.

1.90

.61

.02

.52

.73

1.10

.85

.82

Feb.

2.00

.25

2.50

.90

1.18

1.13

3.42

1.63

Mar.

0.10

1.50

1.16

1.71

1 90

1.23

Apr.

0.80

1.08

1 22

no

1.54

1.11

May.

1.00

49

2.20

2

fiQ

2.25

1.59

June.

0

0.15

.04

.28

05

.18

July.

1.02

0

.22

.26

.63

.61

.53

Aug.

1.13

T.

.11

«>7

.20

.61

Sept.

T.

0.08

.83

98

1.09

Oct.

2.38

.60

1.05

.40

94

.54

1.02

Nov.

0.31

.80

.50

1.38

.20

0

2.99

1.03

.Dec.

1.30

0

.55

. .86

40

1.50

1.10

.95

Annual.

9 10

8.26

11.20

17.93

11.35

Monthly and annual precipitation at Mount Pleasant from 1899 to 1905.

Year.

1899..............

1901.............. 1909

1904..............

1905..............

Mean..^. ..

Jan.

1.40

.36

.56

.52

1.24

1.10

80

.85

Feb.

3.60

.60

on

1.10

1.71

1.93

1.71

Mar.

«> Q7

1 t*f\

2.20

1.76

1.66

Apr.

0

^7

2

£fi

1 Q

I

ftW

1.41

1.12

1.47

1.19

May.

1.02

QO

KQ

49

1 49

2 11

1.25

1.03

June.

0 99

on

04

.59

.76

.53

July.

T.

1Q

Oft

.56

1.12

.17

.51

Aug.

1.24

.16

1 64

T.

T.

.87

Sept.

0

1.78

.16

.83

1.57

.36

.94

Oct.

1 80

.59

1 °<9

40

.58

.88

0

.93

Nov.

0.88

1.56

1.38

.20

0

1.15

.97

Dec.

2.10

T.

1.14

.86

.20

1.90

1.10

1.22

Annual.

16.65

8.03

11.21

8.26

10.34

13.70

11.37

FLOW OF STREAMS.

The streams of Sanpete and Sevier valleys are of three distinct 

types the relatively long master streams, the shorter transverse 

tributaries, and the canals. The master streams, as already stated, 

meander in a gentle grade in broad waste-filled valleys of structural 

origin. San Pitch Creek, wT hich is confined to the northern, valley, is 

fed by the direct but varying flow of its tributary streams and by 

more constant seepage. Sevier River, on the other hand, while having similar sources of supply within the portion of its valley under 

consideration, is fed chiefly from sources in the high plateaus in the 

southern part of the State.

The tributary streams are very different. In their mountain 

courses they occupy narrow, steep-graded, eroded valleys, and at the 

base of the highlands they emerge from their canyon-like courses 

and enter the broad debris-filled lowland, across which they flow at 

a lessened grade until they join the master stream. These tributary 

streams are fed almost entirely by the precipitation on their mountain watersheds through direct and seepage run-off, and as the main 

precipitation on the mountains occurs as snow, the discharge is 

heaviest in late spring and early summer. Figures are not available 

to show the run-off of the streams in the area under discussion, but 

the streams in Jordan Valley under similar conditions discharge 

during April, May, and June about 60 per cent of the annual run-off. 

Besides the annual floods, occasional violent summer storms temporarily increase the discharge of the streams. Conditions are different in each watershed, the discharge varying with the precipitation,
STREAM FLOW. 17

topography, vegetation, and soils, and with the care that is taken 

to prevent fires, excessive grazing, and the destruction of timber. 

Seepage run-off is greater in valleys of relatively low relief that are 

abundantly clothed with vegetation, for under these conditions the 

products of rock disintegration are not readily washed into the 

valleys, and debris accumulates to absorb a large quantity of the 

precipitation, which thus escapes flood discharge and seeps slowly 

into the streams, maintaining their perennial flow. Below the 

mouths of their canyons the tributary streams, in the upper parts of 

their way across the broad valley, receive no augmentation to their 

flow, but, on the contrary, lose much by evaporation and absorption, 

which will presently be referred to, while in their lower courses, 

before they enter the main streams, their flow is generally increased 

by seepage. During the irrigation season the tributaries make small 

contribution directly to the master streams, for their water at the 

mouths of the canyons is diverted by canals and distributed over the 

valley.

Irrigation canals tap both master streams and tributaries, the 

tributaries at or near the mouths of the canyons, and San Pitch Creek 

and Sevier River at intervals throughout their courses, as shown 

on the map. Water is thus distributed over the valley where normally it would not flow.

The amount of water contributed by streams to Sanpete and Sevier 

valleys has not been measured. An indication, however, of the discharge of the most important ones is afforded by the following 

measurements, made with a .current meter by C. S. Jarvis during 

the summer of 1905, but it must be borne in mind that at the time 

when most of the data were collected the streams were at a low stage.

Discharge measurements of streams in Sevier and Sanpete valleys in 1905.

 Stream, with place of measurement. « -

Do...........................................................................

Twin Creek

Date.

....do...

....do...

June 29

July 11

Aug. 3

Aug. 10

Ano- 17

Sept. 18

Sept. 19

....do...

....do...

Sept. 22

Discharge.

Sec.-fl. 

310.4

51.0

269.4

17.0

48.2

6.3

1.1

30.7

16.5

13.6

8.3

3.5

4.8

1.5

8.1

8.3

1.6

4.1

tt If locality is not stated, the stream was measured at or near the mouth of its canyon. 

6 Estimated from gage reading,

1KB 199^07 M 2
18 UNDERGROUND WATER IN VALLEYS OF UTAH.

Although the quantity of water tributary to Sanpete and Sevier 

valleys is not known, the amount that leaves them by San Pitch 

Creek and Sevier River near Gunnison has been measured for the 

last five years and is shown by the following tables, compiled from 

records of the United States Geological Survey:

Estimated discharge of San Pitch Creek near Gunnison.

Date.

1905.

April. . ..................................................

IMay

July.....................................................

Total..............................................

1904 .....................................................

1903.....................................................

1902.....................................................

1901.....................................................

Discharge in second-feet.

Maximum.

15 

24 

15 

94 

338 

304 

166 

720 

82 

46 

35 

30

338

264 

158 

155 

125

Minimum.

11 

9 

8 

13 

82 

90 

110 

64 

30 

26 

22 

20

8

6 

3

7 

9

Mean.

13.3 

14.1 

12.1 

24.2 

136.0 

179.0 

143.0 

126.0 

40.5 

32.0 

28.1 

23.9

64.3

43.7 

37.3 

27.0 

30.0

Total in 

acre-feet.

818 

783 

744 

1,440 

8,362 

10,650 

8,793 

7,747 

2,410 

1,968 

1,672 

1,470

46,860

31,920 

27,184 

19,855 

21,803

Estimated discharge of Sevier River near Gunnison.

Date.

1905.

April ....................................................

July........... .........................................

Total. .............................................

1904.....................................................

1903 .....................................................

1901a....................................................

Discharge in second-feet.

Maximum.

319 

573 

367 

92 

651 

525 

26 

69 

62 

101 

95 

116

651

355 

366 

194 

239

Minimum.

254 

254 

87 

41 

41 

17

n

24 

41 

58 

87 

93

17

10 

8 

5 

5

Mean.

303.0 

318.0 

199.0 

67.0 

222.0 

164.0 

18.4 

32.3 

46.2 

89.3 

91.4 

98.3

81.1

54.0 

56.0

Total in 

acre-feet.

8,414 

17,660 

12,240 

3,987 

13,650 

9,759 

1,131 

1,986 

 2, 749 

5,491 

5,439 

2,925

95,009

58, 490 

73,000 

38, 677 

40,481

a Five days missing in this year.

If the figures for 1905 represent normal conditions, the flood discharge of San Pitch Creek occurs in May and June, the maximum 

occurring in June, after which the flow gradually decreases to the 

period of low water in January, February, and March, the minimum 

occurring in March. By comparing the total discharge of San Pitch 

Creek for the last five years it appears that the flow is irregular, the 

Discharge in 1905 being more than double that in 1902, The flow of
STEEAM FLOW. 19

Sevier River, which drains a much larger area, is even more irregular. In 1905 the maximum occurred in February, and the discharge 

in May was large, while the minimum occurred in July and August. 

The annual discharge varies considerably and in the dry year of 1902 

was less than half that in 1905. The flow of Sevier Kiver is much 

affected by irrigation, return seepage, and absorption, as is shown by 

the fact that on June 17, 1905, the discharge of the river below Clear 

Creek, at the head of central Sevier Valley, was 429.6 second-feet, 

while 45 miles below, at Gunnison, the discharge amounted to only 51 

second-feet. Similar results were obtained on June 29.

Although figures are lacking for estimating the quantity of water 

available for replenishing the underground store from the flow of 

streams, the data given below indicate that the amount is considerable. 

Absorption from stream beds is, in fact, the chief source of underground water in Sanpete and Sevier valleys.

A few measurements to illustrate the amount of water absorbed 

from individual streams in parts of their courses were made by C. S. 

Jarvis in the summer of 1905, as follows:

Ephraim Creek on August 30, flowing 8.2 second-feet near the 

mouth of its canyon, in a course of 0.6 mile over a gravelly bed lost 

0.8 second-foot, amounting to 16 per cent a mile.

Oak Creek on September 18, flowing 4.88 second-feet at a point 3 

miles southeast of Spring City, in a course of 2.5 miles lost 0.46 

second-foot, amounting to 3.7 per cent a mile.

Twin Creek on September 19, flowing 8.1 second-feet at a point 

3.5 miles southeast of Mount Pleasant, in a course of about 2.75 miles 

lost 3.1 second-feet, amounting to 13.8 per cent a mile.

Moroni upper canal on September 12, flowing 6.38 second-feet, in 

a course of 7 miles lost 1.76 second-feet, amounting to 3.8 per cent a 

mile.

These figures clearly indicate the manner in which the underground supply is maintained by streams.

An instructive example of the role played by seepage is afforded 

by the flow of Sevier River between the mouth of Clear Creek and 

Gunnison, a distance of 45 miles. At three places between these 

points dams have been constructed across the river, and at each place 

canals divert practically all of the flow of the stream, yet below each 

dam the seepage into the river is sufficient to supply the next succeeding canals. This fact is illustrated by the following measurements made by Caleb Tanner in 1902, which show that between 

Clear Creek and Rocky Ford the flow of the river was augmented 

through seepage by 26.06 second-feet, between Rocky Ford and Redmond Ford by 18.2 second-feet, and between Redmond Ford and 

West View Bridge by 22 second-feet.
20 UNDERGROUND WATER IN VALLEYS OF UTAH.

Seepage in Sevier Valtey between Clear Creek and Gunnlsonfl

[Measurements made by Caleb Tanner, August 13-16, 1902.]

BETWEEN CLEAR CREEK AND ROCKY FOBD.

Surface water entering Sevier Valley : Sec. ft. 

Sevier River above Clear Creek_____ ___________ 47.5

Clear Creek________________________________ 7.3 

Monroe Creek_______________________________ 3. 9

Thompsons Creek_______________________________ .2

Redbutte and Cottonwood creeks_______________ .3

Water Canyon Creek______ ___________________ .3 

Spring Creek _________ __________________ 5. 3

Cove Creek_________________________________ ._. 9. 5

Cedar Ridge Creek________________________ .5

 74.8

Surface water diverted from Sevier Valley:

Clear Creek canal_________________ __________ 1.38

Joseph canal_______________________________ 3.85

Wells canal_______________________________ 2.38

Isaacsoii canal___________________________ 3. 03

Monroe canal_____________________________ 7.25

Elsinore canal _______________________________ 2. 75 

Brooklyn canal_________________________________ 5. 50

Richfield canal_____________________ _ ___ __ 17. 50

Annabelle canal _____________________________ 11.18 

Candor canal____________________________..____ .50

Vermilion canal______________________________ 9. 04

Surface water leaving valley:

Sevier River ___________ ___ .___________ 36. 5

Total diverted and remaining in stream______ _________ 100.86

Seepage __________________________ _____________ 26. 06

BETWEEN ROCKY FORD AND REDMOND FORD.

Surface water entering Sevier Valley:

Sevier RiA^er at Rocky Ford_____________________ 36. 5 

Lost Creek ________________________________ .7 

Salina Creek_______________________________ 7. 8

 45.0

Surface water diverted from Sevier Valley:

Rock Ford canal___________________________ 35.0 

Other canals________________________________ 8.5

Surface water leaving valley:

Sevier River___________________________ 19. 7

Total diverted and remaining in stream______________ 63.2

Seepage _____________________________________ 18.2

0 Water Sup. and Irr. Paper No. 85, TL S. Geol. Survey, 1903, pp. 91-94.
SOURCE OF UNDERGROUND WATER. 21

BETWEEN BEDMOND FOBD AND WEST VIEW EIDGE.

Surface water entering Sevier Valley : Sec. ft. 

Sevier River at Redmond Ford_________________ 10. 7

Willow Creek _______________________________ .5 

San Pitch Creek,___-_______________________ 15.2

 35.4

Surface water diverted from Sevier Valley:

Robbing canal ________________________ 8.14

Westview canal_____________________________ 4.20

Other canals_____________________________ 15. 70

Surface water leaving Sevier Valfey:

Sevier River__________________ ___________ 18. 7 

Dover canal______________________________ 10. 7

Total _____________________________________ ______ 57. 44

Seepage _____________ _ -.__ ___________:______ 22. 04 

OTHER SOURCES.

The undergrown water supply of Sanpete and Sevier valleys is 

augmented not only by rainfall that is directly absorbed by the surface on which it falls and by absorption from creek beds, but also 

by the flow of springs from bed rock, by the return waters of irrigation, and by the underflow from the creeks at the mouths of their 

canyons.

The occurrence of springs is described on pages 25-26, but it should 

be noted here that, in addition to many seeps, a number of springs that 

issue along fault lines convey water to the valley from a distant 

source in bed rock. The total discharge of these fault springs 

amounts to a constant flow of about 95 second-feet, and absorption 

of a part of the flow adds an appreciable amount to the underground 

waters.

In the practice of irrigation part of the water applied to the fields 

is absorbed by the soil and, percolating below the reach of roots and 

beyond the sphere of capillary action, joins the underground supply. 

The amount thus absorbed varies considerably from place to place, 

depending on the porosity of the soil and the quantity of water 

applied to the fields in excess of the need.

The underflow of the creeks at the mouths of their canyons also 

contributes an important quota to the underground supply of the 

valleys. No data are available to show this amount, but it can be 

determined by measuring the cross-section of the valley filling, its 

porosity, and the velocity of the underflow.

DISTRIBUTION OF UNDERGROUND WATER.

Underground water, derived from the sources that have been 

stated, is contained in both the unconsolidated deposits and the bed 

rocks of Sanpete and Sevier valleys. The former are the more valu-
22 UNDERGROUND WATER IN VALLEYS OF UTAH.

able reservoirs, but some of the consolidated deposits also are important. All rocks, even the most dense, are to a certain extent 

porous, and the great mass of underground water is contained in rock 

pores and interstices. Fine-textured, compact deposits are relatively 

of little importance as water carriers, the chief reservoirs being the 

loose-textured, more permeable rocks.

WATER IN BED ROCKS.

As has been indicated in the preceding description of the rocks of 

this region, the general character of several of the formations renders them of little value as underground reservoirs. The massive, 

fine-textured igneous rocks, except locally, where they are cracked, 

are practically worthless in this connection; so, too, are the Jurassic 

shales. The strata of known Eocene age, which occupy a large area, 

composed as they are of close-grained shale and limestone and thin 

lenses of sandstone, have also little value for absorbing and transmitting water. On the other hand, the sandstone of probable Laramie age that outcrops on the "VVasatch Plateau and the conglomerate 

and sandstone of undetermined age on the Pavant Mountains are 

probably important water-bearing beds, although they have not been 

developed. These porous strata are of considerable thickness and 

outcrop on large areas in the mountains where the opportunities for 

absorption are good. They are overlain by relatively impervious 

beds and dip toward the valley. The conditions for obtaining artesian water in the valleys are therefore favorable, except where 

there are disturbing factors, presently to be stated.

The geologic map and sections (Pis. II and III) show that the 

Laramie sandstone occupies many square miles on the summit and 

western flanks of the Wasatch Plateau east of Sanpete Valley, extending as far south as Salina Creek, and that toward the base of the 

plateau the sandstone is capped by shales and limestones of Eocene 

age. The dip is westward toward the valley at angles ranging 

from 5° to 20°. At the base of the highlands, however, the rocks are 

concealed by unconsolidated deposits, and little information is available concerning the position of bed rock beneath the valley filling. 

At the southern end of the Wasatch Plateau the western flank is 

broken by several north-south trending faults, which fade away 

northward, and none are known to extend beyond Manti Creek. No 

evidence of faulting at the base of the plateau has been obtained in 

the northern and central parts of Sanpete Valley, where the rocks 

that 'are exposed along the flanks of the plateau probably continue 

unbroken beneath the valley nearly to its western limit. The western dip, if continued beneath the valley at the same angle, would 

carry the water-bearing beds beyond the reach of profitable drilling,
DISTRIBUTION OF UNDERGROUND WATER. . 23

hut the rocks in the ridge between Fountain Green and Mount 

Pleasant lie almost flat, and this fact suggests that the dips flatten 

out and cause the sandstone to occur possibly within profitable reach 

of the drill. Its position, however, can be determined only by 

prospecting.

The map (PI. II) also shows that a large area on the crest and eastern flanks of the Pavant Mountains is occupied by a groat thickness 

of coarse conglomerate and sandstone, which are advantageously 

located to absorb water directly from precipitation and from the flow 

of streams. These coarse-textured rocks are overlain by relatively 

impervious strata and dip gently toward the valley. They are, 

however, cut by the fault which extends along the eastern base of the 

mountains, and which, by intersecting water-bearing beds, is an important factor in connection with the water supply, as noted on page 

14. The character and position of bed rock beneath Sevier Valley 

are unknown, and the presence of this fault makes the chance of 

obtaining artesian water from this source less favorable in Sevier 

than in Sanpete Valley.

WATER IN THE VALLEY DEPOSITS.

Water absorbed at the surface percolates downward for a greater 

or less distance through the unconsolidated valley deposits until it 

reaches the zone of saturation. The upper surface of this zone i« 

known as the water table, beneath which the deposits are saturated, 

the water pccupying the spaces between the solid particles of gravel, 

sand, and clay. In Sanpete and Sevier valleys the position of the 

water table conforms in a general way with the contour of the valley 

floor. Beneath the broad lowlands the water table slopes at a low 

angle upstream, away from the central valley axis, but near the highlands the slope of the surface of saturation is less than the inclination 

of the ground. As a result, the ground water in the lowlands lies 

close to the surface, and near the base of the mountains it lies at 

considerable depths. In the town of Mount Pleasant, for instance, 

che slope of the ground is about 170 feet to the mile, while the inclination of the water table is about 95 feet to the mile.

In the absence of adequate topographic maps on which the position of the water table could be shown by contours, the approximate 

depth to ground water is shown on Pis. V and VI by lines representing areas in which ground water lies, respectively, at depths 

between 0 and 10, 10 and 50, and over 50 feet beneath the surface. 

This information was compiled from the well data given on pages 

51-57, which, with the location of the wells shown on the map, serve 

as an index to the available knowledge. Under much of the area in 

which the depth to ground water is shown as over 50 feet water can
24 UNDERGROUND WATER IN VALLEYS OF UTAH.

not be obtained within 100 feet or more, but it is impracticable to 

indicate on the map more than is shown.

The position of the water table fluctuates measurably. It is 

highest in summer, after the period of heavy stream discharge and 

during the irrigation season, and lowest in winter, when there is 

comparatively little addition to the underground supply. A fluctuation of 20 feet has been observed in some wells, and variations between 2 and 10 feet are common between the summer maximum and 

the winter minimum. The use of ground water tends to lower the 

water table, but in the area under consideration persistent decrease 

has not yet been marked, though in places, as in the fields below 

Manti, a loss of head has followed the sinking of many shallow wells. 

Locally in the lowlands there has been a permanent rise in the level of 

ground water, due to the return waters of irrigation, whereby former 

fertile tracts have been converted into meadow and sWamp lands.

The saturated beds contain varying amounts of water, their content depending on the character, thickness, and extent of the deposits. 

Coarse-textured gravel and sand, by reason of their greater porosity, 

hold and transmit relatively more water than fine-textured clay, and 

the coarser deposits therefore constitute the chief underground reservoirs. The wells that have been sunk in this region encounter beds 

of sand and gravel that range in thickness from a few inches to 

many feet and are separated by beds of clay of varying thickness. 

Locally these water-bearing beds have considerable horizontal extent, and, although the details of their distribution are not known, 

experience in sinking wells has shown that beds of sand and gravel 

are of widespread occurrence, both horizontally and vertically.

Underground water is seldom stationary, but moves very slowly 

from a higher to a lower level. The velocity varies with the head 

and with the number and size of the interstitial spaces, for the movement is not in open channels, but through the minute pores between 

the solid particles of the deposits. The rate of movement is only 

a few feet a day. The highest velocity of ground water that has 

been recorded is about 100 feet in twenty-four hours, and generally 

it is much less, the ordinary rates in sand being between 2 and 50 feet 

a day.

RECOVERY OF UNDERGROUND WATER.

The total amount of underground water in Sanpete and Sevier 

valleys, if it could be computed, would be expressed in cubic miles, 

but, by reason either of its depth or through its inclusion in finelextured deposits, which do not readily yield their content, a large 

part of the subterranean store is not available. An estimate of the 

available amount is also impracticable because of the unknown extent
U S. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO I9S> PL. VJ

T.I3S.

o i

LEGEND

Depth to ground waters 

0 \o 10 feet.

10 to 50 feet 

60 feet and over

.Approximate upper limit of the valley deposits 

WELLS AND SPK1NGS

-Nonflowing wells 

Flowing wells

Springs

Numbers ralrr to luu of wel]« and «priilge 1

Scale 

2 3466 miles

T.I45.

T. 195.

R.I W. R.I E. .£ E.

MAP SHOWING APPROXIMATE DEPTH TO GROUND WATERS AND LOCATION OF WELLS AND SPRINGS

IN SANPETE VALLEY, UTAH
RECOVERY OF UNDERGROUND WATER. 25

of the irregular lenses of sand and gravel which constitute the important reservoirs. But, although figures can not be given, it is 

evident that a considerable supply of underground water awaits 

development in this area.

RECOVERY OF WATER FROM BED ROCKS.

Bed rocks are an important, but little developed, source of water in 

this area. A number of large springs originate in these consolidated 

deposits, and conditions for obtaining artesian wells are locally 

favorable.

RECOVERY OF WATER FROM BED ROCK BY SPRINGS.

Springs are a source of much water in Sanpete and Sevier valleys, 

88 being recorded on pages 58-60. These can be classed either as 

fault springs or seep springs, the water from the first class issuing 

along a fault plane, that from the second class seeping out, generally 

in low areas, where the surface intersects the ground-water table. 

Of the 88 that are listed 30 are fault springs, yielding an aggregate 

discharge of 95 second-feet. Fault springs have their sources in bed 

rocks and commonly are located at the base of the mountains, along 

the principal planes of dislocation, prominent groups being on the 

eastern margin of Sevier Valley and on the western margin of 

Sanpete Valley, although isolated springs occur at a number of other 

places, as shown on the map. The discharge of fault springs varies 

little, if any, throughout the year; each spring commonly yields as 

much as 1 second-foot, the mean of all being over 3, second-feet, and 

one west of Fountain Green flows 12.4 second-feet. (PI. IV, A.)

The temperatures of these springs differ greatly. That of many is 

only a few degrees above the mean annual temperature of the valleys, 

about 48°, but some are distinctly hot, Joseph Hot Springs (No. 3 in 

list on p. 58 and on PL V) ranging from 135° to 156° F. and Monroe 

Hot Springs (No. 5) ranging from 144° to 156° F. The temperature 

of some of the hot springs is probably due to the proximity of heated 

igneous rocks. That of others, as Richfield Spring (No. 71), which 

is 74° F., appears to be due to the internal heat of the earth, although 

the possible influence of igneous rocks must not be ignored. If the 

temperature of the Richfield Spring be due entirely to the normal 

heat of the earth, an index is thus afforded of the depth of the water 

before it rises. If an increment of 1° F. for each 50 feet be assumed 

without allowance for cooling, a depth of 1,300 feet is indicated.

The general occurrence of fault springs, although each one differs 

from others in details, may be illustrated by the Richfield Spring. 

(See fig. 3.) Here the porous conglomerates and sandstones that out-
26 UNDERGROUND WATER IN VALLEYS OF UTAH.

crop on the Pavant Mountains dip toward the valley and are overlain 

by the relatively impervious Wasatch bends. The mountains have 

been uplifted along the fault at their base, and the water-bearing 

beds the conglomerate and sandstone have been cut by the dis-

,-Rtchfield Spring

FIG. 3. Diagrammatic section at Richfield Spring.

placement as if by a well. In consequence the water, which is under 

pressure, rises along the fault- plane, the place of actual issue being 

determined by a series of favorable conditions by which free passage 

is maintained.

RECOVERY OF WATER FROM BED ROCK BY TUNNELS.

The practicability of tunneling into fault planes to obtain water is 

suggested by the occurrence of springs along lines of displacement, 

and a notable successful tunnel is that of the Morrison coal mine east 

of Sterling. This tunnel was begun on a dry hillside and driven 

eastward toward the fault, which has not yet been reached. Water 

was encountered which in August, 1905, was found to discharge 5.6 

second-feet. The probable conditions here are shown by fig. 4. The 

source appears to be in the westward-dipping sandstone that outcrops 

on the Wasatch Plateau. The water being under hydrostatic presFIG. 4. Diagrammatic section at Morrison Tunnel Spring.

sure, rises when it reaches the fault plane. Notwithstanding the 

success of this tunnel, similar results can not be generally predicted, 

because of the ever-present possibility of unfortunate conditions, 

such as cementation along fault planes and easier escape of the water 

in other directions. Yet tunneling into fault planes along which 

strong springs occur presents possibilities that would seem to justify 

prospecting.

Tunnels may be advantageously driven not only into fault planes, 

but possibly elsewhere, for it may be profitable to explore locally the
RECOVERY OF UNDERGROUND WATER. 27

base of the mountains where water-bearing beds dip valleyward, as 

in the Pavant Range and on the Wasatch Plateau, with the idea of 

penetrating saturated strata by tunnels instead of wells.

RECOVERY OF WATER FROM BED ROCK BY WELLS.

With the exception of well No. 237 (see list on p. 56, and map 

forming PL VI), between Mount Pleasant and Fair view, no wells, as 

far as the writer is informed, have been sunk to bed rock in Sanpete 

and Sevier valleys. Nevertheless flowing wells may possibly be 

obtained from consolidated rocks in certain areas as already suggested, the most promising sources being the eastward-dipping conglomerates and sandstones on the Pavant Mountains and the westward-dipping sandstone on the Wasatch Plateau.

Steep dips and faults are locally disturbing factors, but the conditions warrant sinking test wells.

In the center of Sevier Valley, on account of the faulting, it is possible that the water-bearing beds lie at depths too great for profitable wells, since the temperature of the Richfield Spring indicates 

a depth of 1,300 feet to the water beds at the border of the valley. 

Preliminary tests might be made west of the fault in valleys where 

streams have cut deep into the rocks.

Conditions for flowing wells are more favorable in Sanpete Valley, 

especially between Fairview and Spring City. The absence of faulting has not been proved here, but the westward-dipping rocks of the 

Wasatch Plateau may extend unbroken beneath the valley, where the 

dips probably flatten out. If these conditions actually prevail it is 

likely that profitable flowing wells can be obtained from the Laramie 

sandstone. Because of the uncertainty of the dip and the variable 

thickness and unknown erosion of the Eocene strata depths can not 

be predicted, but before a test well is abandoned it should be sunk 

until the Laramie sandstone is reached.

RECOVERY OF WATER FROM VALLEY DEPOSITS.

The source of most abundant underground water in Sanpete and 

Sevier valleys is the unconsolidated material by which they are 

underlain and from which water is recovered by springs, tunnels, 

and both flowing and nonflowing wells.

RECOVERY OF WATER FROM VALLEY DEPOSITS BY SPRINGS.

Although most of the fault springs issue through unconsolidated 

deposits, their origin is obvious and they should not be confounded 

with seep springs. As already stated, springs of the first class occur 

along faults. Those of the second are independent of structure and 

commonly occur in lowlands where the surface of the ground interPROPERTY OF 

U. S. GEOLOGICAL SURVEY
28 UNDERGROUND WATER IN VALLEYS OF UTAH.

sects the water table. The discharge of seep springs is generally 

unlike that of fault springs, since it often fluctuates with the season 

instead of flowing almost constantly. The temperature of fault 

springs is also more constant, and is commonly higher than that of 

seep springs, a fact that is especially apparent during the winter.

Seep springs are numerous in Sanpete and Sevier valleys, especially in their lower stretches, and the important part played by 

seepage in maintaining the flow of the streams has been already noted. 

Seepage is so widespread and in any one spot is usually so slight that 

over large areas it is impracticable to map places of exit of seepage 

water, but points where the flow appears in springs and is concentrated into considerable streams are shown on Pis. V and VI and 

are listed on pages 58 to 60. The flow of many seep springs can be 

increased by development, but some of them are at elevations so low 

that their waters are unavailable for use in the immediate vicinity 

except by pumping.

RECOVERY OF WATER FROM VALLEY DEPOSITS BY TUNNELS.

Tunnels driven into the unconsolidated deposits have procured 

large amounts of water. Especially favorable sites for tunnels are 

places where the low lands begin to raise at an increased angle toward 

the base of the mountains. At such places the ground water tapped

FIG. 6. Section illustrating a tunnel in the valley deposits.

will drain by gravity into tunnels, as illustrated in fig. 5. A tunnel of this class is that of Madsen and Seely, west of Mount Pleasant. 

(See p. 49.)

RECOVERY OF WATER FROM VALLEY DEPOSITS BY NONFLOWING WELL4!.

Nonflowing wells, the general features of which are indicated in 

the list, pages 51-57, are the most common means of recovering underground water in Sanpete and Sevier valleys. The maps show that 

ground water lies within 10 feet of the surface under a large part of 

the valleys, this area of course being in the lowlands, and that toward 

the highlands the depth increases. The nonflowing wells are commonly dug beneath the ground-water level to a porous bed of sand 

or gravel, from which water percolates into the opening. Most of
RECOVERY OF UNDERGROUND WATER. 29

the wells are sunk several feet below the summer stage of the water 

table in order to provide for the seasonal fluctuation. There are also 

a number of nonflowing bored wells, which have been put down with 

the hope of obtaining a flow at the surface.

Water is drawn from most of these wells by buckets or hand 

pumps. A few windmills are in operation, but the wind velocity is 

apparently not great or steady enough to give them general favor. 

There are few, if any, power pumps in the valley, which affords a 

promising field for their introduction and their use in irrigation. 

Water contained in coarse beds, which insure an abundant yield, lies 

within easy reach of the surface beneath large areas, and electric 

power can be cheaply developed from the near-by mountain streams.

RECOVERY OF WATER FROM VALLEY DEPOSITS BY FLOWING WELLS.

The irregular sheets of gravel, sand, and clay that slope valleywr ard from the base of the mountains afford conditions favorable 

for pressure in their contained water. Accordingly, where beds of 

sand and gravel that lie below a confining stratum of relatively impervious material are encountered by wells which enter the zone of 

saturation, the water tends to rise in the wells, and in the lowlands 

sufficient head is developed to cause flows at the surface. Above the 

lowlands on each side of the valley the water in deep wells rises a 

greater or less distance, the height it reaches depending upon the 

elevation of the ground.

It is estimated that there are more than 100 flowing wells in the 

twT o valleys, yielding an aggregate flow of about 5 second-feet. Most 

of the wrells are 1^ or 2 inches in diameter, but a few of the larger 

ones are 3 or 4 inches. Flows are obtained at different depths between 20 and 344 feet, under pressures at the surface varying from 

0 to 6 pounds per square inch. The average yield of the wells is 

possibly about 20 gallons a minute, but the range is wide, several 

discharging less than 1 gallon a minute. The greatest flow measured 

was 160 gallons a minute, from a 3-inch pipe. Beneath the first flow 

other flows are commonly obtained from each bed of sand and gravel 

encountered in boring the well.

The flowing wells are located in the fields below the towns, which 

generally are built at elevations so high that the water of the wells 

is little used for domestic purposes, for which, by its purity, it is 

eminently adapted. It is used to some extent for watering stock, 

but chiefly for irrigation.

The use of artesian water from the valley deposits has only begun, 

and the possibilities apparently are not realized. There is need for 

a number of test wells to exploit conditions in the lower deposits, 

and where good flows are obtained more wells of larger bore may 

profitably be sunk.
30 UNDERGROUND WATER IN VALLEYS OF UTAH.

RECOVERY OF WATER FROM VALLEY DEPOSITS BY SUBSURFACE DAMS, ETC.

Under exceptional conditions ground w^ater may be recovered 

by means of subsurface dams or similar contrivances which impound 

the underflow in unconsolidated materials. These conditions are practically impervious bottom within easy reach of the surface, to prevent excessive lowering of the ground-water level, and competent 

side walls, not too far apart, to intercept lateral escape. The 

presence of these conditions can be determined only by prospecting, 

and the economic desirability of building such structures at particular places is an independent question, but because of the high 

value of water in this area their feasibility at each possible site 

should be investigated. Possible locations of subsurface dams are 

suggested by rock walls at the mouths of the narrow canyons, where 

borings in search of suitable bottom should be made. Tests of the 

amount and porosity of the valley filling at and above the mouths 

of the canyons, together with measurements of the velocity of the 

underflow, would indicate the quantity of ground water available. 

At some places below the mouths of the canyons in the several creek 

valleys conditions favorable to the construction of infiltration galleries may also be discovered.

QUALITY OF WATER.

Few analyses have been made of the waters of Sanpete and Sevier 

valleys, although their general character is indicated by a number 

of field tests. During the summer of 1900 the Bureau of Soils 0 

examined the waters of Sevier Valley, and in the fall of 1905 the 

writer made the following field assays, using the methods suggested 

by Mr. M. O. Leighton. 6 The figures given represent only approximate composition; yet, as all the tests were made under similar conditions, they afford rough comparative data:

Field assays t>f water from Sanpete and Sev-ier valleys, Utah. 

[Parts per millon.]

Name and locality.

STEEAMS.

Upper Salina Creek, 7 miles above mouth of canyon.

0 Soil survey in Sevier Valley, Utah, Kept, fie 

of Agriculture, 1900. 

* Leighton, M. O., Field assay of water : Wat 

No. 151. 1905. 

0 Samples obtained at mouths of canyons.

Calcium

(Ca).

238 

238 

890 

550 

1,150 

261 

360 

505 

410

d operatic 

er-Sup. an

Bicarbonate radicle 

(HC03 ).

234 

204 

408 

408 

377

245

245 

ns Division

d Irr. Pap*

Sulphate 

radicle 

(S04 ).

- 35

157 

237 

492 

+626 

80 

65 

76 

113

Of Soils, 1 

ir U. S. Ge

Chlorine

(Cl).

6 

Trace. 

45 

519 

1,015 

29 

19 

19 

9

J. S. Dept. 

ol. Survey
QUALITY OF WATEE. 31

Field assays of water from Sanpete and Sevier valleys, Utah Continued.

Name and locality.

STREAMS continued.

SPRINGS.

Ninemile (No. 34)....... ..............................

Glenwood (No. 12) ....................................

Richfield (No. 16) .....................................

FLOWING WELLS.

Allied ................................................

Bolitho ...............................................

DUG WELLS.

Salina (White House) ...............................

South of Salina (Colby) ...............................

Ephraim (S. Sorensen) ...............................

Calcium

(Ca).

151 

96

248

( c ) 

410 

435

96

228

380 

274 

274 

274 

340 

595

715 

595 

320 

1, 150 

650 

274 

248

Bicarbonate radicle 

(HCOS ).

265 

102

265 

326 

367

122 

265

408 

204 

367 

286 

326 

326

367 

510 

204 

551 

367 

449 

571

Sulphate 

radicle

(S04 )

127 

- 35 

53

0 

164 

459

0 

Trace.

492 

- 35 

135 

- 35 

74 

530

35

135 

108 

+626 

300 

62 

572

Chlorine

(Cl).

119 

9 

9

19 

29 

308

24 

29

297 

258 

14 

19 

59 

498

19 

218 

109 

148 

258 

59 

636

a Samples obtained at mouths of canyons. 

h Numbers are those given on Pis. V and VI. 

0 Calcium content very large.

The general composition of the waters of the area under consideration can be inferred from the outline of the geology of the watershed, 

for the mineral content of surface and ground waters is determined 

by the chemical character of the rocks and soils with which they come 

in contact. (See pp. 8-14.) The prevalence of limestone causes an 

abundance of carbonates; the waters which come under the influence 

of the Jurassic salt and gypsum bearing rocks are rich in chlorides 

and sulphates; while streams like Monroe Creek, which traverse 

igneous rocks, carry relatively little mineral matter in solution. 

Water from wells of moderate or considerable depth is usually 

similar to that of the mountain streams in the same locality, but 

that from shallow wells in the lowlands, especially in irrigated tracts, 

contains abundant dissolved salts. This mineral content is largely 

derived from the return waters of irrigation, which leach the soils, 

for in the lowlands where ground water is within reach of capillary 

action the dissolved salts are deposited by evaporation and the soil 

is impregnated with an accumulation of " alkali." The combined 

deleterious effects of the soluble Jurassic rocks and of the alkali in 

the lowlands is shown in the table by the two tests of the water of 

Sevier River. The sample collected west of Joseph, in the upper 

part of the valley, contained only 261 parts per million of calcium, 

80 sulphates, and 29 parts of chlorines, while the sample from the
32 UNDERGROUND WATER IN VALLEYS OF UTAH.

same river west of Gunnison contained 377 parts of bicarbonates, 

1,150 parts of calcium, over 626 parts of sulphates, and 1,015 parts 

of chlorine.

The natural conditions are generally favorable for obtaining good 

water for domestic purposes, but the communities give little heed 

to the sanitary character of the water, and as a result epidemics of 

typhoid fever of greater or less violence are not uncommon. As ordinary hygienic precaution will prevent most of such epidemics the 

negligence in providing pure water supplies can not be too strongly 

condemned. Ill-kept privies and cesspools are nuisances that should 

not be tolerated in settled communities. Privies should be replaced 

by " dry-earth closets," provided with a supply of dry clay loam, 

and the fecal matter should be removed at short intervals. Where 

there are public water supplies it is desirable that sewers should also 

be installed and the sewage might, if desired, be used in irrigation 

on " sewer farms." The local custom of using old wells as cesspools 

pollutes the water of neighboring wells that are still used as sources 

of drinking water, and should be prohibited. Another prevalent 

unsanitary custom is the use, for drinking and cooking, of water 

running through the towns in open ditches, into which pollution 

is free to drain.

All the towns in the area except one or two can procure water supplies either from springs or from mountain streams, which with care 

can be protected from contamination, and outlying houses can be supplied with water from deep wells. But although pure water can 

easily be obtained, only four towns in Sanpete and Sevier valleys 

Freedom, Mount Pleasant, Manti, and Richfield have public waterworks.

STJGGESTIOlSrS.

In view of the present undeveloped state of the ground waters of 

Sanpete and Sevier valleys and the need of more water, a fewT suggestions as to a more efficient use of the available resources may be 

pertinent.

As the only source of water is the precipitation on the drainage 

area tributary to the valleys, it is clear that attention should be given 

to conserving this supply by preventing waste whenever possible. 

The chief problem is to save the storm waters, and to this end large 

storage reservoirs have been built or planned, but it does not appear 

to be generally realized that the storm run-off can be saved also by 

other means. The underground supply can be considerably augmented by distributing the flood discharge over the uplands below 

the mouths of the canyons of the creeks that emerge from the mountains. The control of floods is difficult, but by placing obstructions 

in the ordinary channels flood waters can be spread over a wide area, 

so as to increase greatly the amount of water that is absorbed in the
SUGGESTIONS. 33

porous alluvial deposits. Small reservoirs can also be constructed at 

many places within the mountain watershed, whereby the storm runoff can be checked and the seepage run-off in the dry season increased. 

The advantage of preserving timber on the mountains should also be 

clearly understood. A drainage area well covered with vegetation 

is one of the most effectual checks to storm run-off. A heavy growth 

of underbrush and trees tends to prevent storms from washing away 

the products of rock decay and to accumulate a thick cover of soil 

and humus, which absorbs large quantities of water from storms and 

from melting snow, whereas if the covering of vegetation is scant, 

storms tend to keep the mountain sides relatively bare of soil by 

washing the debris into the creeks, so that the precipitation runs off 

rapidly and comparatively little is absorbed to seep slowly into the 

creeks to maintain their summer flow. The timber should therefore 

be protected from fire and from reckless cutting, excessive grazing 

should not be permitted, and trees might be planted to advantage in 

many areas.

Not only should the supply be conserved as far as possible, but 

more efficient use of the available water should be practiced. Much 

is lost by crude methods of irrigation. More water is often applied 

to the fields than is needed, and a large part is lost by seepage from 

faultily constructed ditches. The use of pipes whenever practicable 

and the construction of less permeable canals would prevent much 

waste. Much water is also lost by allowing artesian wells to flow constantly. It should be thoroughly realized that the limited supply 

of ground water comes from a common source, that the wastefulness 

of one person counteracts the prudence of another, and that the interest of all demands that the supply be rigorously conserved. Flowing wT ells should be capped, or the flow should at least be partly 

checked when water is not used, or the water should be collected in 

reservoirs for future use. A further incentive to economy in the use 

of water is the fact that by its conservation the evil of alkali accumulation and the raising of the water table too near the surface in the 

lowlands is retarded.

The distribution of underground water suggests that the most efficient use of the total supply in the valley would be to develop the 

fertile uplands toward the base of the mountains, as far as may 

be, from high-line canals, supplied by the mountain streams; and 

to use underground water, which in general is inaccessible on the 

uplands, in developing the lowlands, where the subterranean supply 

is plentiful. Owing to the present complicated ownership of water 

rights, it may be difficult to act upon this suggestion, but there can b3 

no doubt that its adoption would materially add to the amount of 

land under cultivation. Flowing wells can be obtained in large areas

JBB 199 07 M 3
34 UNDERGROUND WATER IN VALLEYS OF UTAH.

in the lowlands, and at several localities where coarse water-bearing 

sand and gravel occur near the surface there is a possibility of establishing pumping plants, for which electric power developed from the 

adjacent mountain streams is generally available. It should be 

remembered, however, that although the underground supply is considerable, it must not be recklessly used. Observations on the fluctuation of the water table should serve as a guide to development.

Since the underground water supply in Sanpete and Sevier valleys 

is but little developed and local conditions are promising, further 

testing of the resources is very desirable. Deep wells should be 

sunk in both valleys to ascertain the conditions in the unconsolidated deposits, and to determine whether flowing wells can be obtained from bed rock. Where good supplies are found pipes of 

larger bore than those now used might well be employed. Also the 

now of some of the springs can be materially increased by development, and possibly new ones found by prospecting.

DETAILED DESCRIPTIONS.

The descriptive details that follow are supplementary to the information contained in the maps forming Pis. VI and VII and the list 

of wells and springs on pages 51-60. The descriptions begin at the 

south and proceed northward, the areas described being grouped 

about the principal towns.

JOSEPH AND VICINITY.

About 6 miles south of Joseph the Sevier River emerges from a 

canyon and flows northeastward between the lava-capped foothills 

of the Pavant Mountains and a low ridge of igneous rocks. The 

town of Joseph is situated near the base of the long alluvial slope 

west of the river. Water for irrigation is furnished by the Sevier 

Valley canal, below which most of the land is under cultivation, and 

drinking water of poor quality is obtained from shallow dug wells. 

Most of the area lying below the canal is underlain by gravel and 

by subordinate streaks of sand and clay; ground water lies within 

50 feet of the surface, and the wells are between 30 and 60 feet in 

depth. The annual fluctuation of the water surface amounts to 

about 10 feet, the water being highest in midsummer and lowest in 

late winter, when some of the wells go dry. A better supply for 

drinking purposes probably can be obtained from bored wells near 

the river, 100 feet or more in depth. These would avoid contamination and at least some seepage from the canals. There is little likelihood of profitably obtaining underground water for irrigating the 

arid slope west of Joseph, although it is possible that deep wells, 

after penetrating a considerable but unknown thickness of lava and
DETAILED DESCRIPTIONS. 35

the underlying Eocene strata, would strike artesian water in the 

underlying sandstones and conglomerates.

The Joseph Hot Springs issue from calcareous tufa, deposited by 

the springs, at the batse of the low volcanic ridge about a mile southeast of the town. The temperature of the water ranges from 135° 

to 146° F., and the yield of all is estimated to be only about 30 gallons 

a minute..

ELSINORE AND VICINITY.

Sevier Valley broadens out a few miles above Elsinore, which is 

located in the midst of a prosperous agricultural district. Contiguous to the river, particularly south of it, a number of shallow wells 

have been dug, from which an abundant supply of water in coarse 

gravel is obtained at depths ranging from 20 to 35 feet. Two wells 

have been bored in this area, one, 178 feet deep, in the SE. ^ sec. 32, 

T. 24 S., E. 3 W., the other, 171 feet deep, in the SW. 1 sec. 34, in 

the same range and township. In sinking these wells the surface 

was found to be underlain chiefly by sand and gravel to a depth of 

150 feet, where stiff yellow clay was encountered, through which the 

inadequate apparatus failed to penetrate. This immediate area is 

favorable for testing underground conditions, and it is desirable 

that a deep well be sunk here to determine the possibility of obtaining flowing wells in the valley deposits. The discharge of Monroe 

Creek, on the southeast, and the seepage from Sevier Eiver in its 

sandy course below the mouth of its canyon are sources of an underground supply which may be under pressure in possible coarse deposits beneath the clay above mentioned. If flowing wells should 

not be obtained, pumping from the shallow gravels is an attractive 

possibility.

Midway between Joseph and Elsinore, near the river, in SE. | 

sec. 6, T. 25 S., E. 3 W., there is a group of about 25 wells, in which 

the water rises within 2 or 3 feet of the surface. These are 1^ inches 

in diameter and less than 50 feet deep and the yield of all amounts 

to about 1 second-foot. Trenches have been dug, in which the flow is 

conducted to the Brooklyn canal. Clay was encountered in these 

wells down to 12 feet, below which water-bearing sand and gravel 

occur.

The town of Elsinore is built on an alluvial slope at the base of 

lava-capped foothills. Water for irrigation is obtained from several 

canals that are fed by Sevier Eiver, and these also furnish an unsatisfactory domestic supply, which is supplemented by a few poor 

wells between 60 and 115. feet in depth. The chief desideratum is a 

good supply for domestic purposes. Possible sources are a number 

of feeble seep springs in the hills a few miles to the northwest, 

springs on the east side of the valley adjacent to Thompsons Creek,
36 UNDERGROUND WATER IN VALLEYS OP UTAH.

Monroe Creek, and wells. Although capable of development, the 

yield of the springs first mentioned appears to be insufficient; on the 

other hand, surface water of good quality and abundant quantity is 

available on the eastern side of the valley, but^its use necessitates a 

pipe line extending several miles. The project of sinking wells, 

however, offers attractive possibilities. These are of two distinct 

classes, deep wells in the valley deposits and wells sunk to bed rock. 

The desirability of sinking a test well in the valley south of Elsinore 

has just been mentioned. It can hardly be expected, even if a flow 

should result, that the pressure would be sufficient to carry the water 

to Elsinore, yet it is probable that water of good quality can be thus 

obtained. Another possibility is to tap the sandstones and conglomerates that cap the Pavant Mountains and dip southeastward. 

The fault along the base of the mountains complicates the situation 

and makes it desirable that the first experimental well be drilled west 

of it. Another disturbing factor in the vicinity of Elsinore is the 

cap of hard lava. This, however, can be avoided by sinking a well 

in the valley about 2 miles north of the town. The surface strata 

will probably yield water of poor quality, but this could be cased off, 

for good water under pressure is to be expected from the underlying 

beds. The depth at which water will be found can not be predicted, 

but the beds that overlie the water-bearing strata are probably several 

hundred feet thick, and if exploration is undertaken at all preparations should be made to sink a well at least 1,000 feet deep.

MONROE AND VICINITY.

Monroe is prettily situated on an alluvial slope on the east side of 

the valley, at the base of the Sevier Plateau. Monroe Creek, the 

principal source of water supply, flows throughout its course over 

cystalline rocks, and its water therefore contains relatively'little dissolved matter. In this respect it is the purest large stream in the 

entire area here considered. A number of canals, fed from Sevier 

River and Monroe Creek, furnish water for irrigation, and these 

canals are also largely resorted to for domestic supply. In view of 

the fact that excellent water is available in Monroe Canyon, it is 

surprising that the community is willing to continue using for household purposes the present relatively unsanitary supply. The depth 

to ground water is over 50 feet, and there are but few wells in 

Monroe.

The hot springs near Monroe are a valuable asset, but as yet they 

are little used. There are several groups of springs a half mile east 

of the town along a probable fault line at the base of the mountains, 

which are composed of igneous rocks. The salts held in solution by 

the water are deposited as tufa, from which springs now issue at a 

number of places. The total yield is about 100 gallons a minute, and
DETAILED DESCRIPTIONS. 37

the temperature of the water when it reaches the surface ranges from 

144° to 156° F. The proximity of the springs to the town suggests 

the desirability of attempting to increase their flow with the idea of 

utilizing the .eat.

The following analysis of the water of Cooper Hot Springs was 

obtained from the owner:

Analysis of water from Cooper Hot Springs, east of Monroe (No. 5). 

[Analyst, P. A. Yoder.]

Ca

Mg _________________ ____ ______

Na _

K

Li

Fe, Al . _ _ _

SiO, __________

SO4

C03 - _-__-_-_____ -__-

Cl ______ ___ __ __

Parts per million.

_ i _ 267.7

35.1

591.4

37.5

.6

0.0

23.5

167.6

_ _ __ _ _ 36.0

634.6

Total solids _________________________ 1,794.0

The few wells that have been sunk in the valley southwest of Monroe show that the depth to ground water is over TO feet. The most 

practicable way, therefore, of developing the area is from high-line 

canals supplied by Sevier River and Monroe Creek.

The presence of several springs between 1 and 3 miles south of the 

mouth of Monroe Canyon, along a probable fault, suggests that 

more water may be obtained by tunneling.

RICHFIELD AND VICINITY.

The portion of Sevier Valley between Monroe and Richfield that 

lies below the canals is in large part under cultivation, but the portion above them consists of desert alluvial slopes that extend up to 

the bases of the mountains. In the highlands bowlders and coarsetextured debris abound, while the lowlands are floored with sand and 

clay loam. The map forming PL VI shows that ground water 

lies within 10 feet of the surface under a considerable part of the lowlands, and that in this vicinity there are about 100 artesian wells, 

concerning wT hich representative data are given in the list on pages 

51-57. They are shallow, ranging from 50 to 95 feet in depth, and 

yield from 3 to 142 gallons a minute under a pressure at the surface 

of slightly over 2 pounds. In drilling, clay is usually encountered 

for 40 to GO feet, below which lies said and gravel, whence the flows 

are obtained. The gravel appears to be widely distributed and constitutes a valuable reservoir. By a single well, No. 59, in list on page 

52 and map (PI. V), which is 4 inches in diameter, 62 feet deep,
38 UNDERGROUND WATER IN VALLEYS OF UTAH.

and yields 132 gallons a minute, a large tract of alkali land has been 

converted into an excellent meadow.

The deepest well in this vicinity was sunk in 1900 in NE. £ sec. 7, 

T. 24, S., R., 2 W., to a depth of 324 feet. The log of this well, as reported by the owner, is given below:

' 1,0*7 of well in sec. 7, T. 2J, 8., R. 2 W., in feet.

Clay ...................................................................................

Clay ..................................................................................

Clay ...................................................................................

Thickness.

62

88

15

135

20

24

Depth.

62

150

165

300

320

324

From the upper beds of sand arid gravel in this well water rose 

within a few inches of the surface and a flow was obtained from the 

bottom, but the pipe broke and the well was discontinued. So far as 

known, this is the deepest hole in Sevier Valley proper, and the results serve to emphasize the desirability of a deep test well. The 

probabilities are that such a well will penetrate one or more beds of 

sand and gravel, bearing water under pressure great enough to cause 

flows at the surface, even if the well should be sunk at some distance 

from the river.

Not only the valley deposits, but the bed rock is an available 

source of underground water, especially along the base of the mountains, near Eichfield. The considerable outcrop of sandstone and 

conglomerate on the crest and eastern flanks of the Pavant Range, 

as already stated (p. 23), presents a large area for the absorption of 

precipitation and run-off, and the eastward dip and cap of Eocene 

strata cause the contained water to be under pressure. Although 

deep valleys drain a large portion of the porous rocks, it is nevertheless likely that a well sunk through the capping of limestones and 

shales will strike artesian water in the underlying sandstone and 

conglomerate. The fault along the base of the mountains is a disturbing factor, yet apparently it is the cause of the spring west of 

Richfield, and thus serves to emphasize the possibility of obtaining 

water under pressure. The depth at which water may be expected 

can not be closely predicated. If a test well is attempted provision 

should be made for driving 1,000 feet or more, the depth depending 

on the location of the well; the farther away from the mountains 

it may be dug the deeper it will need to be sunk to reach the waterbearing beds. A rough approximation of the depth to the Richfield 

spring water may be afforded by its temperature, 74° F., which is 

26° above the mean annual temperature. If the temperature be due 

to the internal heat of the earth, which, it is assumed, increases about
DETAILED DESCRIPTIONS. . 39

1 degree in every 50 feet, the water is derived from a depth of about 

1,300 feet. It is possible, however, that the water owes its temperature in part to the proximity of heated igneous rocks.

Inverury and Annabelle, small towns situated on opposite sides of 

the Sevier, 4 miles south of Richfield, are supported by irrigation 

from canals fed by the river. Inverury is supplied with poor drinking water from shallow wells, although water of better quality can be 

obtained by driving deeper and casing off the upper flow. Annabelle, on the other hand, derives a good supply for domestic use from 

reservoirs in the mountains south of the town.

Richfield, the commercial center of Sevier Valley, has a population 

of about 2,000. The town is situated at the foot slope of the Pavant 

Range, and derives its water supply from the Sevier Valley and 

other canals and from the spring referred to on page 25. This 

spring, discharging 3.2 second-feet, besides furnishing water for local 

irrigation, supplies the city waterworks the best system in the 

entire area considered in this report. The spring is inclosed in a 

brick structure, whence the water is piped to .a concrete reservoir 

and distributed through an 8-inch main. Before the waterworks 

were installed the town depended largely upon wells that range in 

depth from 15 to 20 feet. Some of these are still used; others have 

been abandoned and are used as cesspools, thus introducing a source 

of contamination which should not be tolerated.

Glenwood is prettily located in a cove, at the base of Sevier Plateau, 

that is separated on the west from the main valley by a low lavacapped ridge. The town and its vicinity are supplied with water for 

irrigation and domestic use by springs. East and west of the lavacapped ridge there are springs whose discharge aggregates about 20 

vsecond-feet. Those on the west side of the ridge are reported to have 

broken out since 1880, and their flow is so copious that a considerable 

area has been converted into marsh land. The conditions here can be 

improved by drainage and by conveying the surplus water where it 

is more needed. The springs on the east side of the ridge discharge 

9 second-feet and are the source of Cove Creek. At an elevation of 

250 feet above the town Glenwood Springs issue from debris at the 

base of igneous hills and form the main local supply for all purposes, 

the discharge being 7 second-feet. Although the supply is plentiful, 

a needed improvement is the installation of a waterworks system that 

would do away with the present insanitary practice of obtaining 

domestic water directly from open ditches in the streets. The springs 

also afford an excellent source of power, which is as yet undeveloped. 

North of Glenwood, along the base of the mountains, there are other 

springs, notably Herrins Hole Springs and Black Knoll Springs, 

which yield respectively 1 and 12 second-feet. All of these springs 

probably rise along faults.
40 "UNDERGROUND WATER IN VALLEYS OF UTAH. 

SALINA AND VICINITY.

Between Richfield and Salina the character of the country changes. 

On the east of the valley the Sevier Plateau, an area of igneous rocks, 

slopes rapidly northward to the interval separating it from the Wasatch Plateau, which is underlain by sedimentary rocks. A narrow 

belt of gypsiferous drab and red shales, capped here and there with 

lava, lies between the base of the plateaus and Sevier River. On the 

west side of the valley the eastward-dipping Eocene beds of the Valley Mountains are separated by a fault from the red conglomerates 

and sandstones of the Pavant Range. The appearance of the valley 

also changes. West of the river the canals water a relatively narrow 

strip, beyond -which there is a long desert slope up to the base of the 

mountains, while on the east still less land is irrigated from small 

ditches fed by creeks.

I Here, as throughout the valley, the lowlands are superficially underlain by fine-textured soils, while the foot slopes of the mountains are 

littered with coarse debris. Ground water lies between 10 and 50 feet 

from the surface in a belt contiguous to the river, where most of the 

wells have been sunk. They are chiefly driven wells, 2 or 3 inches in 

diameter and from 100 to a little over 200 feet in depth. This depth, 

unusual in Sevier Valley, is necessitated by the strongly saline 

character of the water nearer the surface, due to the proximity of the 

salt and gypsum-bearing shales. The wells first penetrate about CO 

feet of clay, below which lie alternating layers of gravel and clay. 

Each gravel bed yields water under pressure that causes it to rise 

within a few feet of the surface. Along the entire length of Sevier 

Valley, between Venice and Gunnison, the character of the ground 

wrater is impaired by salts leached from the adjacent Jurassic beds. 

These salts, however, apparently do not permeate the valley deposits 

throughout their entire thickness, but seem to be confined largely to 

the upper layers by beds of clay, so that water of better quality is 

obtained by deep wells.

i The character and structure of the bed rocks in the highlands immediately adjacent to the valley between Richfield and Salina are not 

in general favorable for storing or yielding much water, but water 

under pressure probably can be obtained in the red sandstone and conglomerate north of Richfield (p. 10). Artesian water may probably also be obtained in the valley of Salina Creek, several miles 

above Salina, a probability which, in view of the needs of the town, 

becomes important. As has been stated in the outline of the geology 

of the region (p. 9), thick sandstones that dip westward at a low 

angle and are overlain by Eocene beds outcrop in the upper valley of 

Salina Creek. Here the opportunities for absorption are good, and 

it is likely that wells that penetrate to saturated horizons of the sand-
DETAILED DESCRIPTIONS. 41

stone will strike artesian water. If a test well be sunk it should be 

located at least 5 miles up the creek from Salina, for a fault probably 

lies between the small outcrop of Colorado age and the water-bearing 

beds.

 Salina is situated at the base of the salt and gypsum bearing shales, 

near the mouth of Salina Creek. The town obtains its supply of 

water for domestic uses from ditches fed by the creek, and from dug 

wells, but the water from both sources is of poor quality. An effort 

was made in 1905 to obtain good water by sinking a 4-inch well to 

a depth of 163 feet, where water was encountered which rose within 

42 feet of the surface. The site was not particularly good and the 

depth not great, so the test proved unsuccessful.

Log of Salina town well, in feet.

Thickness.

35

91

24

13

Depth.

35

126

150

163

A sample of water from the lower sand and gravel in this well was 

analyzed by H. Harms, of Salt Lake City, and found to contain 1,708 

parts per million of dissolved solids, 728 of which are chlorine. 

This large content of salts renders the water undesirable for drinking purposes. A number of families have their drinking water 

hauled from Colby's well (No. 85 on map), about 4 miles southwest 

of Salina, which is reported to contain only 576 parts per million of 

dissolved salts, but this practice is only a makeshift. Further tests 

should be made with deep wells in the valley, away from the immediate influence of Salina Creek, and deep enough to escape seepage of 

water containing salts derived from the adjacent hills. It is desirable also that a test be made for artesian water up the valley of Salina 

Creek. The nearest good surface water is derived from feeble streams 

in the Pavant Mountains and from Salina Creek above the belt of 

saline rocks.

The small town of Aurora, 5 miles southwest of Salina, is supplied 

mainly by canals. A few wells, over 100 feet in depth, here obtain 

a fairly good supply beneath the saline surface water. The water 

rises in these wells within 20 or 40 feet of the surface. It is desirable that a deep test well be sunk in this part of the valley to determine 

whether water of good quality can be obtained under pressure sufficient to flow at the surface. It is possible that the spring 2 miles 

west of town can be developed so as to yield enough water for domestic uses.
42 UNDERGROUND WATER IN VALLEYS OF UTAH.

Redmond is plentifully supplied with water, its chief asset being 

the springs that feed Redmond Lake. These issue from the bottom 

and edges of the lake and discharge about 13.5 second-feet. The 

temperature of one small spring of the group in August, 1905, was 

70° F., which, together with the large amount of water the springs 

yield, suggests that they occur along a fault, which, however, has 

not been traced on the surface. Ditch water is generally used for 

domestic use, and little attention is given to its sanitary character. 

By fencing the lake and piping the supply used for drinking, water 

of excellent quality can be cheaply obtained. Ground water occurs 

within 10 feet of the surface in the lower part of the town, although 

there are but few wells. One well (No. 106 on the map), about a 

mile northeast of Redmond, was sunk to a depth of 180 feet passing 

through the following material:

Log of well No. 106, in feet.

Clav................ ....................................................................

Clay.... ................................................................................

Clay....................................................................................

Thickness.

83

22

3S

Depth.

103

142

180

Water in the lower gravel rises within 3.5 feet of the surface. 

GUNNISON AND VICINITY.

A few miles north of Redmond, west of the river, there is a narrow 

belt of low hills, below which the valley broadens, reaching a width 

of 9 miles at Gunnison. The lowlands are underlain by clay, while 

the slopes on both sides of the valley are composed of coarser textured deposits that extend to the base of the mountains. Canals, 

fed either from Sevier River or San Pitch Creek, supply the lower 

part of the valley, which locally is so wet as to need drainage; but 

above the ditches desert conditions prevail.

Ground water lies within 50 feet of the surface in a considerable 

area in this part of the valley, and a number of wells have been sunk 

here. West of Gunnison, near the river, there are many flowing 

wells that average only 30 feet in depth. The water occurs in gravel 

beneath about 25 feet of clay, and the wells, which are 2 inches in 

diameter, flow about 50 gallons a minute under a pressure at the 

surface of about 1 pound.

Farther up the valley, in the vicinity of Axtel, about 1 mile east of 

the river, there is a group of dug wells that average 60 feet in depth. 

The deepest bore hole in this part of the valley is \\ inches in diameter and 200 feet deep (No. 109 on the map). In this well alkaline 

water is found in sand at a depth of 45 feet, below which between
DETAILED DESCRIPTIONS. 43

160 and 200 feet of alternating beds of sand and gravel, separated by 

clay, were encountered, which yielded a better quality of water that 

rose within 26 feet of the surface. Although the strata of the valleyrange dip toward the river, the catchment area is small, the rocks are 

chiefly fine-textured shales and limestones, and the opportunities for 

absorption and transmission are poor. On the east side of the valley 

the conditions are worse, for the little water that is contained in the 

gypsiferous shales is strongly impregnated with dissolved salts.

The town of Gunnison is situated at the southern end of the Gunnison Plateau, near the mouth of San Pitch Creek. A fair amount of 

water is furnished by canals, but there is urgent need for a supply of 

pure drinking water. There are a few shallow wells which derive 

their supply largely from the seepage of the canals. The water level 

in these wells fluctuates about 10 feet a year, being highest in the 

midst of the irrigation season. South of Gunnison a number of wells, 

less than 50 feet deep, have been sunk into the valley deposits, in 

which water is found in gravel beneath the surface cover of clay. 

The supply is derived largely from the seepage from the canals, 

and the quality of the water is only fair. No deep wells have been 

sunk in this part of the valley, and although the elevation is so high 

that flowing wells can hardly be expected, it is likely that a better 

quality can be obtained beneath the upper waters, and a test should be 

made. Probably the most satisfactory domestic supply for Gunnison 

is obtainable from springs at the base of the Wasatch Plateau north 

of Mayfield, presently to be described.

MAYFIELD AND VICINITY.

Mayfield is situated on Twelvemile Creek where it emerges from 

its canyon in the Wasatch Plateau, in a narrow lowland known as 

Arapien Valley, that trends north-south along a fault. On the west 

is a range of hills composed of eastward-dipping gypsiferous shales, 

and on the east is the dip slope of the Wasatch monocline. Mayfield 

and Arapien Valley are watered by ditches that tap Twelvemile 

Creek at the mouth of its canyon. A spring near the bed of the creek 

about 1 mile above town may be utilized as a source of domestic 

supply.

A number of wells, ranging in from 45 to 60 feet, have been 

sunk in the town, but many of them go dry, or almost dry, in the 

late winter, although during the irrigation season they contain 

between 15 and 20 feet of water. The westward-dipping sandstones 

that outcrop in the upper valley of Twelvemile Creek may contain 

water under pressure. The conditions here are complicated by minor 

step faulting along the flanks of the monocline, but it is likely that 

wells sunk near the mouth of the canyon deep enough to penetrate
44 UNDERGROUND WATER IN VALLEYS OF UTAH.

the overlying Wasatch beds will strike artesian water in the sandstone.

In the hilly faulted zone between Mayfield and Manti the main 

supply of underground water is derived from springs, including both 

fault and seep springs, 14 of which yield more than 16 second-feet. 

These comprise both seep and fault springs. The most remarkable 

spring in this area is that in the Morrison coal mine (No. 28 on map), 

east of Sterling. Before the mine was opened the hillside at the 

entrance to the mine was dry, but in driving the tunnel through the 

eastward-dipping sandstone water was encountered, the amount increasing with the length of the workings, until a stream was developed 

which in August, 1905, discharged 5.6 second-feet. It is likely that 

the water is brought up through the fault east of the mine from the 

westward-dipping sandstone that outcrops on the Wasatch Plateau. 

The water being under hydrostatic pressure, rises when it reaches the 

fault plane, as illustrated in fig. 4, p. 26. This spring suggests the 

desirability of prospecting for similar occurrences.

The small town of Sterling is watered by Sixmile Creek, which 

furnishes a good supply for irrigation, but the insanitary custom 

prevails of using for domestic purposes the ditch water that flows 

through the streets. The conditions can also be improved by developing springs or by piping from the creek above the town.

MANTI AND EPHRAIM.

( Above the narrows of San Pitch Creek the valley broadens to a

width of 5 miles at Manti and becomes 8 miles wide at Ephraim. On 

the west Gunnison Plateau, which is underlain for the most part by 

Eocene strata that dip west at a low angle, rises abruptly above the 

valley along a fault. On the east low, detached hills, composed of 

westward-dipping Manti beds, lie at the base of the Wasatch monocline. Where the creeks have cut deep, small outcrops of Laramie (?) 

sandstone are exposed below the Eocene strata, which underlie the 

surface of the greater part of the monocline in this area. Water for 

irrigation is supplied by San Pitch, Ephraim, Willow, and Manti 

creeks, which are supplemented in the lowlands to a small extent by 

flowing wells. The central part of the valley between Manti and 

Ephraim is occupied by a marsh. The conditions here, however, are 

reported to have been improved since the early days of settlement by 

the diversion of the waters of San Pitch Creek for use in irrigation, 

and considerable areas have been reclaimed.

Ground water lies within 10 feet of the surface in a large area in 

the central part of the valley, where many wells have been driven, 

but toward the mountains water lies deeper and there are only a few 

dug wells. Most of the wells in the lowlands are 1| or 2 inches in
DETAILED DESCEIPTIONS. 45

diameter and between 125 and 300 feet in depth. Judging by the 

imperfect records, there is little uniformity in the distribution of the 

deposits, which appear to be lenticular masses of gravel, sand, and 

clay. A typical section is afforded by the following log:

Log of R. TayJor iccll, in ,S'T7. i sec. 33, T. 15 £., K. 3 E. CNo. 190 on p. J<>.)

Clay........................................................... ........................

Thickness.

25

115

6

XL45

3

Depth.

25

140

146

291

294

In this well the first flow was obtained at 140 feet, and a stronger 

flow, amounting to 28 gallons a minute under a pressure of 5 pounds 

at the surface, was encountered in the lowest gravel. Most of the 

wells in this area do not go beyond the first flow, which is commonly 

reached at a depth of about 125 feet, but in some wells as many as 

six flows are encountered between 125 and 300 feet. The flow of all 

the wells in this vicinity varies more or less with the season, and the 

yield of the shallower ones particularly is greater in summer than 

in winter. It is also found that the sinking of a new well in an area 

where wells are close together frequently interferes with the flow 

of the old ones. On the eastern side of the valley, whence the main 

supply is derived, the wells are better and more gravel is reported. 

It is desirable in this region to drive a deep well to test conditions 

and to sink more wells of larger bore to the lower horizons to obtain 

increased flows. In order to ascertain conditions concerning the 

available supply for pumping, experimental wells should also be put 

dowT n outside of the area where flows are obtained. It is probable 

ulso that deep wells sunk near the base of the mountains on the east 

side of the .valley will strike water under pressure in the Laramie 

sandstone, but the absorption area here is not so large as that farther 

north.

Manti is built on the alluvial fan of Manti Creek, which is the chief 

source of water supply. The towT n is underlain by coarse gravel in 

which are few wells, the deepest having been sunk about 100 feet, and 

very little water is reported to have been found. Manti is one of the 

few towns in this area that are provided with waterworks. Seep 

springs in the mountains on the south side of the creek have been 

developed, whence the water is piped to the city, and furnish a good 

supply.

Ephraim, situated on the alluvial slope about 2 miles below the 

mouth of the canyon of Ephraim Creek, is supplied with water for 

domestic purposes by a number of wells, the depth of which increases 

with the surface elevation. The wells in the lower part of town are.
46 UNDEEGEOUND WATEE IN VALLEYS OF UTAH.

only 30 feet deep, but those farther east are 90 feet. In the upper 

outskirts there are no wells, and the people depend on the ditches for 

water. A few years ago a well 2 inches in diameter and 440 feet 

deep was sunk near the town hall in search of flowing water. At 

160 feet water was found which rose to IT feet below the surface, and 

at 340 feet water stood in the pipe 60 feet below the ground. It is 

reported that the lower 100 feet of the drilling was through bed rock. 

A considerable part of the town appears to be underlain to a depth 

of from 10 to 20 feet by clay, which overlies water-bearing sand and 

gravel. « The water is therefore protected to a certain extent from 

contamination, but a better supply is available in springs a few miles 

up Ephrarm Canyon.

MORONI AND VICINITY.

Between Ephraim and Moroni the conditions are similar to those 

farther south. A number of flowing wells have been obtained in the 

lowlands, while the uplands remain to a large extent undeveloped. 

Some of the best wells in the area under consideration are located 

here. Most of them are 2 inches in diameter and about 130 feet deep, 

and discharge from 10 to 30 gallons a minute; but a well in NW. 7 

sec. 9, T. 16 S., E. 3 E., belonging to Joseph Seely, is exceptional in 

character. This well is 4 inches in diameter and 344 feet deep and 

yields 1GO gallons a minute under a pressure of G pounds at the surface. An approximate record of this well is as follows:

Approximate record of well ATo. 205, in feet.

Clay ............................................ .....................:................

Clay ...................................................................................

Depth.

15

80

130

150

344

Thickness.

15

65

50

20

194

Several flows were obtained between 130 and 344 feet, but the best 

one occurred at the latter depth, in a bed of gravel 10 feet thick. In 

one well the drill was sunk 300 feet deeper, through clay all the way. 

These results will probably encourage the sinking of other wells in 

this vicinity. The extent of the area in which these conditions prevail can be determined only by testing, but it may be conjectured 

that they persist at least over several square miles.

The town of Moroni is situated at the southern end OT the highland between the two forks of Sanpete Valley. Canals fed by San 

Pitch Creek form its chief source of water supply, but the town is 

poorly provided with water for domestic purposes. There are a 

number of dug wells, ranging in depth from 10 to 60 feet. The qual-
DETAILED DESCRIPTIONS. 47

ity of the water, however, is impaired by seepage from the upper 

canal. Probably the springs on the west side of the valley (p. 103) 

are' the most desirable source of water for the domestic supply of 

Moroni.

FOUNTAIN GREEN AND WALES.

The broad western- fork of Sanpete Valley is bordered on the east 

by a low, barren ridge, underlain by Eocene shales and limestones 

and capped by lava flows, and is limited on the west by the high and 

narrow Gunnison Plateau. The northern end of the plateau is 

underlain by beds of sandstone and conglomerate, which lie almost 

flat or dip westward at a low angle, while farther south these beds 

are capped by shales and limestones, and along the eastern border 

steep-lying, eastward-dipping beds of sandstone and conglomerate 

mark the presence of a fault. Toward the northwest the valley 

narrows, and about 4 miles above Fountain Green terminates at 

the debris-covered divide between Sanpete and Salt Creek valleys. 

No perennial streams are fed by the run-off in this area, but a remarkable series of springs issue along the base of Gunnison Plateau.

Between Moroni and Fountain Green, ground water lies within 10 

feet of the surface in a narrow belt, above which it lies at greater, 

depths, as shown on. the map (PL VI). In this region there are a 

few flowing wells and a number of pumping ones, but the main water 

supply is derived from springs.

Within a distance of 10 miles between Wales and Fountain Green, 

associated with the fault at the base of Gunnison Plateau, there are 

seven springs, the aggregate yield of which amounts to 15.9 secondfeet. These springs have many features in common. . Their temperature is about the same, approximating the mean annual temperature of the region; the water of all contains abundant calcium 

carbonate, which is deposited as tufa; and the flow, except that of 

one spring, is reported not to vary. The discharge of these springs 

is not affected by heavy showers, and in view of the small tributary 

drainage area and the scarcity of limestone, a distant though unknown source is indicated. Possibly the water is derived from the 

westward-dipping sandstone that outcrops on the Wasatch Plateau 

and probably underlies the valley. This chance suggests the desirability of sinking a deep well in the valley in search of artesian water 

from bed rock (pp. 22-23). The dip of the sandstone may flatten out, 

for the low temperature of the springs does not imply a deep-seated 

source, but the depth to the water-bearing beds can not be predicted.

It is reported that the flow of one of these springs (No. TO on map) 

was increased fivefold by driving a tunnel through debris to bed rock. 

This, together with the general facts of occurrence, suggest that 

prospecting might profitably be undertaken along the fault line with
48 UNDERGROUND WATER IN VALLEYS OP UTAH.

the idea of increasing present supplies and of developing new 

ones.

Another point should be mentioned. The springs are separated 

from the settlements by a mile or more of sand and gravel, in which 

loss occurs by absorption, although aeration of the water causes the 

precipitation of calcium carbonate, which tends to seal the channels, 

especially in their upper part. Much of this loss could be prevented 

by using pipes instead of ditches. . ;

Wales is situated on the alluvial slope near the base of the plateau 

and is supplied with water principally from Wales Creek and from 

springs northwest of the town. There are a few wells in Wales, 

ranging from 30 to 90 feet in depth, and the fields below the town 

are irrigated from a reservoir below Moroni. The quality of the 

domestic supply can be much improved by using pipes instead of 

open ditches to convey water from the springs.

The small town of Freedom is noteworthy as being one of the few 

settlements in the area under consideration that have public water 

systems. The flow of Current Spring, amounting to about 1 secondfoot, is distributed through pipes and furnishes a very satisfactory 

supply.

Fountain Green is suppled almost entirely by the large spring at 

the base of the plateau about a mile and a half west of the town. (PI. 

IV, A.) The yield of this spring, as measured by C. S. Jarvis in 

September, 1905, amounted to 12.4 second-feet. It is reported that 

the winter discharge falls off perceptibly, but figures to verify this 

report are not available. The domestic supply would be bettered in 

quality if the water were distributed in pipes instead of open ditches.

There are a number of dug wells in and about Fountain Green, 

ranging from 10 to 50 feet in depth; and about 1896 the town sank a 

2-inch well to a depth of 285 feet, the log of which is given below:

Log of well at Fountain Green, No. 218.

Clay ...................................................................................

Clay ...................................................................................

Thickness.

15

98

87

60

25

Depth.

15

113

200

260

285

MOUNT PLEASANT AND VICINITY.

The eastern fork of Sanpete Valley is occupied by the headwaters 

of San Pitch Creek. On the west the low hills that separate the two 

forks are underlain by Eocene shales and limestones that dip westward at a low angle and are locally capped by lava, and on the east 

the Wasatch Plateau towers above the valley. In this part of the
DETAILED DESCRIPTIONS. 49

plateau the summits and most of the western flank are formed of 

Laramie (?) sandstone, and Eocene strata outcrop on the lower 

slopes. Here, as farther south, the monocline is well developed, and 

the rocks that cap the plateau dip beneath the valley filling. Spring 

City, Mount Pleasant, Fairview, and Milburn are situated on the 

east side of the valley, and their water supply is derived from the 

main creek and its branches, supplemented by a number of wells and 

springs.

The central part of the valley is occupied by a narrow belt in 

which ground water lies within 10 feet of the surface. Above the 

lowlands the surface rises to the base of the mountains at a rate of 

slightly over 100 feet a mile. The upper portion of this slope, above 

the canals, is a sagebrush-covered desert, beneath which ground 

water lies at a considerable but unknown depth.

The wells in the lowland are chiefly shallow dug ones, possessing 

no unusual features, and the main supply of underground water is 

derived from springs. These are situated in low meadows adjacent 

to creeks and are all seep springs, of which there are several groups 

in this portion of the valley. An important group includes those 

belonging to the sugar company, located about 3 miles east of Moroni, 

adjacent to Cedar Creek, which in all discharge 3.8 second-feet. Another group, about 2 miles northeast of these, flows 2| second-feet. 

Above Mount Pleasant, adjacent to San Pitch Creek, there are numerous seeps, and in the vicinity of Fairview the total discharge of 

springs, determined by gaging the creek above and below the town 

in September, 1905, amounted to 12 second-feet.

The Madsen and Seely tunnel, about half a mile west of the railroad station at Mount Pleasant, affords an instructive example of 

the successful development of a spring. There the flow of a small 

seep has been increased several fold by tunneling, and the experiment 

might be repeated elesewhere to advantage. (See p. 28.)

The extensive outcrop of sandstone on the crest and flanks of the 

Wasatch Plateau east of upper Sanpete Valley affords an excellent 

opportunity for absorption, and the westward dip and. capping of 

Wasatch beds at the base of the plateau are favorable for obtaining 

water under pressure in wells sunk into the sandstone. . These conditions are well developed between. Spring City and Milburn. If 

results- are favorable, it is likely that flows can be obtained well up 

on the barren slopes toward the base of the mountains.

Spring City is situated near the base of a long alluvial slope in an

embayment that is partly separated from the main valley by a low

ridge of westward-dipping Manti beds. The main water supply is

obtained from ditches fed by Canal and Oak creeks, supplemented

IBS 199 07 M 4
50 UNDERGROUND WATER IN VALLEYS OF UTAH.

by springs and wells. Ground water lies within 10 feet of the surface in a narrow stip adjoining the lower part of the town, but in 

the upper part the depth to water increases to 50 feet or more. 

There are a few flowing wells in the valley deposits southwest of 

Spring City. Wells Nos. 194 and 195 are 2 inches in diameter, 200 

feet deep, and yield an average flow of 20 gallons a minute under 

a pressure of 3^ pounds at the surface. A feeble first flow was obtained at 150 feet and the main flow at 200 feet. Similar results can 

doubtless be obtained in other wells. There are a number of seep 

springs in and near the town, the discharge of which ranges between 

4 and 44 gallons a minute. It is likely that the yield can be increased 

and other springs developed by tunneling.

Mount Pleasant, located on the alluvial slope about midway between San Pitch and the base of the mountains, has lately installed public waterworks. Water is diverted from Pleasant Creek 

near the mouth of its canyon and flumed to a reservoir, whence it is 

distributed throughout the town. The success of this project shows 

what can be accomplished at small cost by most of the settlements 

in Sanpete and Sevier valleys. The depth to ground water ranges 

from 10 feet in the lower part to more than 100 feet in the upper 

part of the town. Approximate measurements show that the slope of 

the ground-water surface is less than that of the ground, the figures 

being respectively 95 and 1TO feet in a mile. The annual fluctuation 

of the ground-water surface between summer maximum and winter 

minimum is reported to average about 10 feet.

Fairview and Milburn are situated near San Pitch Creek, at the 

base of the alluvial slope. In the lower part of the towns ground 

water lies near the surface, and swampy places exist, while on the 

upper slopes depth to water is considerably over 50 feet. Springs 

can be developed in this vicinity, and it is desirable that a deep test 

well should be sunk in the lower part of the valley.
WELL AXD SPRING DATA.

Data concerning wells in Sanpete and Seiier Galleys

No.

1

9.

4

5

6

7

§

10

11

19,

13

14

15

16

17

1S

1Q

20

21

22

<?Q

94

or;

9,fi

97

28

29

3A

31

QO

.00

QA

85

'

Name.

J. H. Levi ..............................................

W. F. Bridges ..........................................

G. W.~R088.. ...........................................

H. Tuft. .................................................

C. Winget. ............................................

.....do.................................................

J.Willes......... ......................................

P P Washbum

O. P. Lee ..............................................

sunk.

1905

1890

1 QO9

1900

1897

1 QAA

1890

1892

1899

1881

1895

1900

1898

TQAO

1905

loop;

1901

1895

1900

1889

1885

1893

1887

1896

Township.

25 S...

25 S...

OK O

OR Q

25 S...

258...

25S...

25S...

25 S...

OK Q

25 S...

25 S

OK C

25 S...

25 S...

25 S...

26 S...

OK Q

25 S...

25 S...

25 S...

26 S...

24 S...

24 S...

248...

24S...

24 S...

24S...

Loca.,

Range.

4 W...

4 W...

4 W...

4 W...

4 W...

4 W...

3 W...

O M T

3W...

4W...

4 W...

4 W...

q \v

3 W...

^ w

q w

3 W...

3 W...

q w

3 W...

4W...

4W...

4W...

q MU

3 W...

3 W...

Q W

3W...

3 W...

ion.

Section.

NE. i,32 ....

SW. i,28 ....

NW.i,21....

NE. i, 22 ....

NW.i,15....

SE.i,15.....

SW.i,14....

NE.i,14....

NE. i, 15 ....

NW.i,14....

NW.i,14....

SW.A,10....

SW.i.lO...-

SE. i, 8 ......

SW.i,ll----

SW. i, 11 ....

NW.i, 11...

NW. I, 3....

SE. i, 5.....

SE. i, 5.....

SW. J, 6.....

SW. i, 6.....

SW. A, 6.....

NW. I, 6....

SW. J, 1.....

SE. |,2.....

SW.i.2.....

>JW l qfS

NW. i, 35...

SW. ^ 34....

NW. J, 34...

NK. i, 33....

NW. i, 33...

ter.a

Inches.

1*

1*

U

Dep

Fe

1

a If bored. Wells whose diameter is not given or queried (t) are dug. 

& Height of water below surface indicated by minus mark ( ); height to which water rises above surface 

"D.=Domestic; S.=Stock; I.^Irrigation.
Data concerning wells in Sanpete and fievier valleys, Uta

No.

37 

38 

39 

40 

41 

42

44 

45 

46 

47 

48 

49 

50 

51 

52 

53 

54 

55 

56 

57 

58 

59 

60 

61 

62 

63 

64 

65 

66 

67 

68 

69 

70 

71

72

73

74

75

Name.

J. F. Shaw ..............................................

C O Keeler

J. W. Nunley ...........................................

G. W. Williams .........................................

W. F. Wright ...........................................

.....do..................................................

.....do........................... ......................

G Petersen *

.....do..................................................

J. M. Bolitho ..........................................

.....do..................................................

.....do..................................................

H Neilsen

P Jen

J. M. Kirkman .........................................

Year 

sunk.

1897

1887 

1892 

1898 

1904 

1892 

1902 

1890 

1903 

1903 

1903 

1898 

1896 

1903 

1897 

1899 

1902 

1900 

1895 

1900 

1900 

1900

1901 

1890 

1901 

1901 

1901 

1890

1901 

1901 

1901

1887 

1898

1903

1905 

1902

1900

Location.

Township.

248...

248... 

248...

448... 

248... 

248...

248...

24 S... 

248... 

248...

24 S... 

248... 

24 S... 

24 S ... 

248...

248... 

248...

24 S... 

24 S...

248... 

24 S... 

248...

23 S'.'.'.

238... 

238...

23 S... 

238... 

238... 

238...

OQ C!

23 S... 

238... 

23 S...

00 0

23 S... 

23 S...

238...

Range.

3 W...

3 W... 

3W...

3 W... 

3 W... 

3 W...

3W... 

3 W... 

3 W... 

3 W...

3 W... 

3 W... 

3 W... 

3W... 

2 W...

2 W... 

2 W...

3W...

2 W...

2W... 

2 W... 

2W... 

3W... 

2 W...

2 W... 

2W...

2W... 

2 W... 

2 W. .. 

2 W...

2W... 

2 W... 

2 W...

3 W

3 W...

3 W...

3 W... 

2W...

2 W...

Section.

NW. i, 33...

NE - 3^ E. i*BZ ".'.'."

NE. i, 32.... 

SW. i, 32.... 

NE. i, 32....

SE. i,29 .... 

SE. i, 29 .... 

SE. i, 29 .... 

NE. i,29....

NE. i,29.... 

NE. i, 29.... 

SE. i,23 .... 

NW. J, 23... 

SW. i, 18....

SE. i,18 .... 

SW. i, 18....

NE. i, 12.... 

NE. i, 7.....

NW. i, 6.... 

NW. i, 6.... 

NW. i 6.... 

NW. A, 36... 

NE. 1,31....

NE.i.Sl ....

NE.i,31 .... 

NE. i,32 .... 

NE. i,32 ....

SE.},26.....

SW * 29

NW 1 29

SE i*25

NE.1,26 ....

NE. 1,26....

SE.1,23.....

SF ' 15 4>

Diameter.

Inches.

 - 

-^i

2

3 

6 

..... 

4

4 

3 

3

2 

3 

4

4 

.........

2

De

Fe

3

5

4

4

4

3

5

5

6

6

11

9

4

2

6

6

3

4

6

6

5

6

1

6

7

7

7

7

6

1

2

8

9

8

1

8

20

5

7

8
76

77

78

79

80

81 

82 

83

84

85

86 

87 

88 

89 

90 

91 

92 

93 

94

95

96 

97 

98 

99 

100 

101 

lOla 

102 

103 

104 

105 

106 

107 

108 

109 

110 

111 

112 

113 

114 

115 

116 

117 

118 

119

E. Wall........... ......................................

F. Glenhill .............................................

J.Colby ................................................

G. S. Williams ..........................................

J. Anderson ............................................ 

H. C. Neilson ..........................................

A. J. Scott .............................................

L. M. Breinholt. .......................................

S. Whiting .............................................

C. C. Larsen. ...........................................

1901 

1898

1896

1899 

1901

1902

1898 

1903

1905

1901

1898 

1902 

1900 

1905 

1905 

1898 

1900 

1893 

1888

1905

1889 

1899 

1889 

1901 

1892 

1888 

1905 

1890 

1901 

1890 

1902 

1903 

1898 

1894 

1889 

1880 

1898 

1895

1895 

1884 

1885 

1891 

1900 

1899

23S...

23 S...

23 S...

22 S...

22 S...

22 S...

22 S...

22 S...

22 S...

22 S...

22 S...

228...

22 S...

228...

21 S...

21 S...

21 S... 

21 S...

21 S... 

21 S...

91 Q

21 S... 

218... 

21 S... 

21 S... 

21 S...

21S... 

21 S...

21 S... 

208...

208...

20 S... 

20 S...

20S... 

20 S... 

20S...

20 S...

19 S...

19 S...

19S...

10 Q

198...

2 W...I SE.A. 15.....

2 W...

2 W... 

2 W...

2 W...

2 W...

2 W...

1 W...

1 W...

1 W...

1 W...

1 W...

1 W...

1 W...

1 W...

1 W...

1 W...

1 W...

1 W... 

1 W...

1 W... 

1 W...

1 W...

1 W... 

1W... 

1 W... 

1W... 

1 W...

1 W... 

1 W...

1 W...

1 W... 

IE ...

IE ...

IE ... 

IE ...

IE ... 

IE ... 

1 W...

IE ... 

IE ...

IE ...

2E ...

2E ...

NB. 1,1 .....

NE.1,1 .....

SE.A.36.....

SE.A, 36.....

NE.A, 25....

NE.-1.25....

NW.A, 19 ...

NE.A, 19....

SE.1,4......

SW.1,4.....

NE.A, 4.....

NW.A, 4.....

SE.1,5......

SW.A, 5.....

SE. 1,34.....

NE. 1,26....

NE.A, 26....

NW.1,25. ..

NW. 1,25....

NW.A, 25.... 

NE.A, 25....

NE, in 25 ....

NE. A, 25 .... 

NE. A, 24 .... 

NW. A, 22... 

NE.A, 19.... 

SB. 1 , 13....

SW.A., 15.... 

NE.A, 11....

SW.A.,1.....

NE.A. I.....

NW. A, 29...

SW.A, 20....

SE.A, 19 .... 

SE.A, 19 ....

SW.A, 16.... 

NW.^9....

SE A, 5 ..... 

NE. * 32....

NW.A, 33...

SE. 1,32....

NE * 39

NW.A, 32...

2 

2

H 

2 

14

2

2 

2 

2

9

2

4

2

2

9

1*

::"f:

a Gallons per day. 
Data concerning u-etts in Sanpete and Sevier valleys, U

No.

120 

121 

122 

123 

124 

125 

126 

127 

128 

129

130

131 

132 

133 

134 

135 

136 

137 

138 

139 

140 

141 

142 

143 

144 

145 

146

147

148

149 

150 

151 

152 

153 

154 

155 

156 

157 

158

Name.

J Olsen

.....do..................................................

.....do..................................................

.....do..................................................

.....do..................................................

.....do..................................................

.....do..................................................

C W Perkins

F. Swalberg ............................................

H. A. Larsen .............. ............................

.....do..................................................

F Tuttle '

W. Tuttle ..............................................

.....do..................................................

.....do..................................................

T. S. Luiid. .............................................

Year 

sunk.

1897 

1901 

1884 

1890 

1890 

1890 

1904 

1897

1895 

f 1902 

J. 1903 

I 1904 

1904 

1904 

1904 

1904

1883 

1890

1890 

1880 

1885 

1889 

1890 

1899 

1889 

1889 

1883

1904

1890 

1890 

1894 

1894 

1892 

1892 

1897 

1898 

1900 

1888

Locatic n.

TS" Range19 8

19 S..

1 Q <J

19 S.. 

198..

198.. 

198.. 

19 S-.

19 S

19 S.. 

 198..

198.. 

198.. 

198.. 

19 S.. 

19 S..

19 S..

19 S

198..

198..

19 S

19 S.. 

198..

188.. 

188.. 

188..

188.. 

178..

17 S..

178..

178.. 

178..

178.. 

178.. 

178.. 

178.. 

178..

17 S..

2 E

IE....

IE....

IE.... 

IE....

IE.... 

IE.... 

1W...

1 W...

1 W... 

1W...

1 W... 

1 W... 

1 W . . . 

1 W... 

IE....

IE....

IE....

IE....

IE....

IE....

IE.... 

2E

2E.... 

2E....

2E.... 

2E....

2E....

2E

2E.... 

2E.... 

2E.... 

2E.... 

2E.... 

2E... 

2E....

3E... 

3E....

Section.

NE. 1, 28....

SW. i,28....

SE. 1,29..... 

NW. 1,29...

NW. 1, 30...

NW * 30

NE. i*'22....

NW. J, 23...

SW. 1,24....

SW. i, 24.... 

SW. 1,24....

SW. 1,24....

SW. i, 24.... 

NE. i, 20....

NE. 1,20....

SW.i,17....

SE. i, 17.....

SW. 1,16....

NW. 1,13... 

NE.i,4.....

NW. 1, 14 ...

SE. 1, 3.....

SE.J, 3.....

SE. 1, 34 ....

NE. 1, 34 ...

C. i, 35 .....

NE. 1,35 ...

NE. 1, 35 ...

NW. i, 25... 

SE. i, 22.... 

NE. 1,22....

SE. i, 15.... 

SE. 1, 15....

NE. 1, 18 ...

SE. f, 17....

Diameter.

Inches.

2 

3

2

2

o 

2 

2 

2

H

(?) 

2

2

11 

2 

1*

1* 

11 

li

11 

l*

I*

11 

11

D

 

I 

t 
WELL DATA. 55

T-H rH IN t~ 1C IM

! I'O I!!!! I !'.! '.!;!!!!!! 1 !!!!' !"C ''O !!!'. I !

O> O> O

> > t>

Cv C3

oo '"aSoooooooooooooo "3 o o 173 I

:o .0020000

.o S £ 413 S

iC^OOOO .OOiCOOiCCOiO -W i I C iM C^-CO COiOOS^-M! I -t-» Tf -^ <M OQ O TH -- 

XlC^iOr

41 41

CO i-HC^i

,0.^0,^ ' 'f ^coo-1.

co 

co

-CO COM iMfM 01 C^

COCO CO COCOCOCOCOCOCOCOCOMCOCOCOC^CJC-ICOCOCOCOCO^WMCOCOCO^COMCOCO^

CBCC OQ xcccoc/JcoMcococoaQcocoxa3xcocococococo

!>t>- 1^* I^I^I^l^-l^l^l^t^t^l^l^l^r^l^I^l^^O^OOOcDOO^OOiO^iCiC'iO^^^^'^

S o o

MT3 -O

o
Data concerning wells in Sanpete and Serier valleys, Uta

j

No.

209 

210 

211 

212 

213 

214 

215 

216 

217 

218 

219 

220 

221 

222 

223 

224 

225 

226 

227 

228 

229 

230 

231 

232 

233 

234 

235 

236 

237 

238 

239 

240 

241 

242 

243 

244 

245 

246 

247 

248 

249 

250

Name.

8. R.Neilson ...........................................

.....do.................................................

C. F. Peel. ..............................................

A jVlirlev

.....do ................................................

A . Frandsen ..................................... ......

Year

sunk.

1894 

1890 

1879 

1901 

1895 

1890 

1890 

1880 

1885

1895

1895

1899 

1891 

1889 

1885 

1896 

1899 

1875 

1903 

1895

1900 

1899 1904' 

1895

1900 

1875 

1904 

1894 

1896 

1903 

1894 

1904 

1895 

1895 

1893 

1905 

1896 

1885 

1903

1890 

1905

Location.

Township.

158... 

158...

158...

158...

15 S. . . 

15 S...

15 S

Range.

3E.... 

3E....

3E....

3E....

3E....

3E....

3E....

SE....

3K_...

158... '3E....

158... 4E....

158 4K..__

158...

15 S...

15 S...

158...

158...

158...

158...

148... 

148...

148...

148...

14 S... 

148... 

14 S... 

14 S... 

14S...

148...

148... 

14S...

148...

148...

i A a

148...

148...

US...

4E....

4E....

4 E ...

4E ...

4E ...

3E ...

3E ...

3E ... 

4E ...

4 E . . .

4E ... 

4E ... 

3E ... 

3E ... 

2E ...

<> jf

2E ...

4E ...

3E ...

2E...

2 E . . .

3 E ...

Section.

SW. i, 8..... 

SW * 9

SE. i, 9 .....

SE. i, 9 .....

SW i 10

Diameter.

Inches.

NW. ' 10 ...

NE. ^ 9.....

SE. i, 9 .....

OP I O

NE. i, 10....

SE. i, 10 ....

SW. i, 7.....

SW. i, 7.....

SW. J, 8.....

SW. i, 2.....

NW. J, 2 ....

NW L 4

NW i*6

SE 1+ 5

gW *i 4

SW. 1,6.....

SW.f,33. ... 

SW. 1,34....

NE. i,29....

NE. i 27....

NE.'i, "21 ..'.'.

SW.'i,'l9 ....

NE.i.ll....

NE. i,7 .....

SW. 1,6.....

SW. i, 0.....

SE. i, 1 .....

........

H

14

2

ji

H

H

(?)"

(' )

Dep

' Fe

11

1

1

1

2

3

6

5

3

2

1

10

1

5

1

5

8

3

2

13

1

5

8

4

5

4

1

1

13

20

3

5

1

7

1

2

4

5

1

1

2
OPLO

353

254

OKK

Of^fi

257

258

OKQ

W1

264

1896

1 Qfil

1900

1875

1897

1903

1889

1903

1898

14 S...

14 S...

14 S...

138...

14S...

14 S...

13 S...

138...

138...

1 Q Q

13S...

1 Q Q

3E...

3E ...

4E...

4E...

4E...

5E...

4E...

4E...

4E...

4E...

NW. i,6....

NW. i.e....

SW. i,31 ...

SE. A, 2.....

SW A,2.....

SE. i, 35 ....

SE. i,31....

SE. i, 24....

SW. i,24....

SE. A, 11 ....

NE. A, 12....

2

« Gallons per day. b Gallons per m
Data concerning springs in Sanpete and Sevier vall

No.

1 

2 

2a 

3 

4 

5 

5a 

6 

7 

8 

9 

10 

lOa

11

lla

12 

13 

14 

15 

16 

17 

18 

19 

20 

21 

22 

22a 

23

24

25 

26 

27 

28 

29 

30 

31 

32 

33

Name.

T T TnV»o

Red Butte ..................

Rock .......................

Richfield. .................

Wall........................

Black Knoll ................

Mud........................

0 Q 14.

Carlsons ....................

Gunnison ..................

Location.

T.

25 S...

25 S...

25 S...

25 S...

25 S...

25 S...

25 S...

25 S...

24 S...

24 S...

24 S...

248...

21S...

23 S...

248...

23S...

23 S...

238...

238...

238...

238...

23 S...

'22 S... 

228...

228...

218...

21 8...

21 S. . .

208... 

198...

198... 

19 S...

198...

198...

19 S...

198...

19 8...

R.

4 W...

3 W...

3 W...

4 W...

% w

3 W...

3 W...

3 W. ..

3 W...

2 W...

3 W...

4W...

4W...

2 W...

2W...

2 W...

2 W...

2 W...

2W...

3 W...

2W...

2W...

2 W . . .

2 W . . . 

2W...

2 W...

1 W . . .

IE ...

1 W...

2E ... 

2E ...

2E ... 

2E ...

1 E ...

2 E . . .

2 E ..

2E ...

IE ...

Sec.

NE.A, 32....

NE. i, 27 ....

SW.A, 23....

NE.A, 23....

SB.*, 10.....

NW.A.ll....

SW. i, 6.....

NW. i, 25...

SW. A, 29....

SW. A, 24....

11...........

JNE. A, and 

\ SB. A. 33. 

INW. i, and 

\ SW. A, 4. 

SW. A, 36....

SW. A, 25....

NW. A, 25...

NE.A, 26....

NW. A, 23 ...

NW.i,12....

SB. A, 36..... 

SW. },!.....

NE.A,!.....

NW. A, 20....

fNE. A & 8E. 

1 t, 11.

INW. A &

[ SW. A, 12. 

SE.A.32..... 

SB. A, 33 .....

SW. A, 20....

SB. A, 20.....

NW. A, 23 ...

SW. A, 18....

SW. A,18....

SW. A, 18....

SB. 1. 18.....

Temperature.

59 

80 

50 

135 to 146

144 to 1«6

154 

65 

58.5 

49 

56

I 52 to 61

57 

60 

60 

60 

74 

63 

52

55

""""59"' 

61

53 

72 

60

70

58 

50 

52 

51.5 

57 

54 

49 to 50 

53 to 58 

61

Use.a

D.S.......

R.I. .......

D.I.......

I..........

D S I

D.I.......

I..........

D.S.I..... 

D.S.I..... 

D.S.I..... 

S .........

S .........

S.I........

D.S.I..... 

D.S.I..... 

D.S.I.....

Q T

D.S.I..... 

S. I.......

D.S.I.....

D.S.I..... 

I.......... 

S .........

s

S .........

ID. s.i.....

8. I .......

I..........

S.I.......

D. S. I.... 

I....... 1...

I..........

I..........

D. S.I.... 

S .........

Yield.

&100 + 

6180 

622 and 11 

630+

617 

660+

6670 

625+ 

618+ 

635+ 

66+

64,600+

63,285 

660+ 

675 + 

"9 

61,440 

6450+

MOrh

cl2.5 

<-35 

615+ 

^3 +

612

b 1| +

cl3. 5 

615+

690+ 

d. 75

c5 

6180 + 

68±

In grave

In igneo

Near cre

In calca

!>4, 5, and 

Marsh n

Igneous 

In bed o

Igneous 

Several 

On lava 

Group o

In debri

In igneo

Do. 

Group o

Joints in 

In igneo

In clay i

In debri

Seep spr

Debris o

Do.

In debri

Group o

Debris n

In clay 

In mead

Along fa

In mead

Near cre

Do. 

Do. 

Do.
34 

35 

36 

37 

38 

39 

40 

41 

42 

43 

44 

45 

46 

47 

48 

49 

50 

51 

52 

53 

54 

55 

56 

57 

58 

59 

60 

61 

62 

63 

64 

65 

66 

67 

68 

69 

70 

71 

72 

73 

73a 

74 

75 

76 

77 

78 

79 

80

Nine Mile Cold............. 

Nine Mile Warm ........... 

Pettyville ..................

Morrison Tunnel ........... 

Barithwaite ................ 

Funk's .....................

Do......................

Lowry ......................

Livingston Warm ..........

City ........................ 

Manti ......................

Manti Silver.... ............ 

Temple.....................

Beck ....................... 

Larsen ......................

Ellis.. ......................

Harris ......................

Ford........................ 

Separator ................... 

Freeman ................... 

Jensen ......................

A. Zabriskie ................ 

Sugar Factory .............. 

Silver Creek............ ....

Freedom ...................

Christian ................... 

McArthur .................. 

Zabriskie South ............

Jensen ......................

19 S... 

19 S... 

19 S... 

19 S...

18 S... 

188... 

188... 

18S...

188... 

18S...

188... 

18 S... 

18 S...

18 S... 

188... 

18 S... 

188... 

178...

168...

158... 

15S... 

158...

15 S...

15 S... 

15 S... 

158... 

15 S... 

158...

158...

15 S...

15 S

158... 

15 S... 

158...

15 S... 

14 S...

15 S...

]5S...

15 S...

158... 

14 S... 

148... 

148...

14 S...

148...

2E.... 

2E.... 

2E....

2E.... 

2E.... 

2E.... 

2E....

2E.... 

2E....

2E.... 

2E.... 

2E....

3E.... 

3E.... 

3E.... 

3E.... 

3E....

2E....

4E.... 

4E.... 

4E ...

4E ... 

4E ...

4E ... 

4E ... 

4E ... 

5E ...

O TT

2E ...

2 E ...

4E ...

4E ... 

4E ... 

3E ... 

3E ...

2E ... 

2E ...

4E ...

4E ...

4E ...

4E....

5E.... 

4E.... 

4E.... 

4E....

4E....

4E....

NW. i,9..... 

SE. i, 4.....

SE. i,5.....

NW J- 5

SE. i, 35.... 

SE. i, 34 .... 

SW. i, 33.... 

NE. i, 26....

SE. ^, 23.... 

SW. i,22....

NE. i,23.... 

SW. i,13.... 

SW. i, 13....

NW. i, 17... 

NW. i,17...

NW. i, 17... 

NE. 1,7..... 

NE. J, 18....

NE. A, 12....

SE. 1,31.... 

SW. i, 32....

SW. },29.... 

,q\y i 09

SW.i,29.... 

SE. i, 30. .... 

NW. 1,36.... 

SE.i, 30..... 

N.i, 24......

SW.i-,13...-

NW.1,13....

SE.i,12.....

NW.i,ll.--- 

SW.i,7 .....

NE.},2 ..... 

SE.i,26.....

SE.1,5......

SE.i,5......

NE.i,8 .....

NW.i,3..-..

SW.i,6 ..... 

SW - 28

NW.4|,27".!!!

NW. 1,27....

NW. i,27....

SE.i, 22.....

53.5

72 

57 

56 

61 

55,56 

50 to 53 

53 

56, 59. 5 

54 

62 

73 

57 to 62 

57 

59 

65 

57

54 

51. 5 

51,53 

57 

50 

50 

52 

52 

4S. 5 

43 

57 to 60 

58 

62 

51 

51 

50 to 52 

51

51.5 

51.5 

48.5 

56 

49 to 55

51 

45.5 

54 

51 

55 

49 

48.5

S.I.......

D.S.I.....

I..........

I..........

I..........

I.......... 

I..........

D.S.I.....

D... ......

D. ........

D.........

D.I.......

S.I.......

D.S.I..... 

D.-S.I..... 

S.I....... 

D. S.I .... 

D. S. I.... 

D. S. I.... 

D.S.I.... 

D. ........ 

S.I....... 

D.S.......

D. S. I.... 

D. S.I.... 

D. S.I.... 

D. 8 ......

D. S. I.... 

D.S.I.... 

S.I.......

S.I.......

D. S. I .... 

D. S. I....

8. I .......

S.I.......

S. I.......

D.S.I..... 

D.S.I..... 

S.I .......

D.S.I.....

I..........

D.S.I..... 

S.I .......

c'2.2 

el 

cO. 25+ 

<-0.2 + 

c5. 64 

el. 2 

el + 

67 

620 

olii 

620 

<?0.61 

610 +

^8 

620 + 

612 

&60+ 

665+ 

66 

644 

&20+ 

630 

697

64± 

616 

64± 

620 

6i 

cO.35 

c 0. 08 

cO, 45 

2.3 

20± 

c3. 8 

cO.6 

c2.4 

cO. 97 

c 0. 15 

620± 

6270 

cO.9

cO.21 

640 

eO.61 

c-0.27 

61,5

C0.2

oO.lS-H

Along f

Along f

In mead

Near riv

In coal 

Along f

Near cr

In sand

Do. 

In debr

Do.

Do.

Do. 

In debri

Do.

Do.

In debr

In mead

In debri

In mead

Do.

Near cr

In soil i

In stree

In soil i

In mead

In footh

In debr

In debr

In debr

In debr

In debr

In sand 

In mead

Along c

Group o

In debr

Do. 

In mead

Do.

Do.

Small s

In debr

Seep ne

In mea

Do.

Do.

Do.

aD.=Domestic; S.=Stock; I.=Irrigation. 6 Gallons per minu
Data concerning springs in Sanpete and Serier valleys, Ut

No.

81 

82 

83 

84 

85 

86 

87 

88

Name.

Alfred...... ................

Spring Branch .............

Location.

T.

US...

US...

14 S...

13S...

13 S...

148...

1 o q

138...

R.

3E....

2E...

4E....

4B..,..

4E-...

2E-...

4p:....

4E....

Sec.

NE.},23....

NE. i,23 ....

SW.i.ll....

NE. J,!!....

NW. i,12....

NW.i,2.....

SE.i,ll.....

SE.i,2......

Temperature.

op 

55.5 

51 

48 

50 

46 

53 

53 

47.5

Use."

D.I.......

D.S.I..... 

S.I .......

S.I .......

S.I .......

D.S.I..... 

D.I.......

D.S.I.....

Yield.

612 

fl.53

cO. 25 +

} «"

c 12. 37 

?'20± 

c-0.6

In debris 

In meado

Do.

In dtSbris 

Near cre

Do.

l> Gallons per minute
INDEX.

A. Page.

Alluvial fan, view of........................ 5

Annabelle, water supplies at................ 39

Asimina eocenica Lesq., occurrence of...... 9

Aurora, water supplies at.................. 41

Axtel, wells near........................... 42-43

B.

Bed rocks, occurrence and character of..... 8-12

water in................................ 22-23

recovery of......................... 25-27

Black Knoll Springs, character of.......... 39

C.

Canal Creek, flow of........................ 17

Canals, flow of.............................. 20-21

supply of............................... 17

,Cedar Creek, flow of........................ 17

Cedar Ridge Creek, flow of................. 20

Clear Creek, flow of......................... 17,20

Climate, character of....................... 5

Colorado rocks, occurrence and character of. 9 

Cope, E. D., on the Manti beds............. 11

Corn Creek, rocks on....................... 10

Cottonwood Creek, flow of................. 17,20

Cove Creek, flow of......................... 20

Cretaceous rocks, occurrence and character

of............................... 9-10

Crops, character of......................... 5

Current Spring, flow of..................... 48

D.

Dams, subsurface, recovery of water by.... 30 

Dry Creek, water of, analysis of............ 31

E.

Elsinore, water supplies near............... 35-36

Eocene rocks, occurrence and character of. 9,10-12 

Ephraim, water supplies at................ 45-46

Ephraim Creek, flow of..................... 17,19

seepage from........................... 19

F.

Fairview, water supplies near.............. 49,50

Fault springs, flow of...................... 25

occurrence of........................... 35-50

structure at, section showing........... 26

view of................................. 14

Faults, occurrence and character of........ 13-14

Fountain Green, springs near, description

of............................... 47-48

springs near, temperature of........... 25

view of............................. 14

water of, analysis of................ 31

Fountain Green, water supplies near....... 47-48

well at, record of....................... 48

Freedom, alluvial fan near, view of......... 5

water supply of......................... 48

G. 

Geology, account of........................ 8-14

map showing........................ Pocket.

Glenwood, description of................... 39

Glenwood Springs, description of.......... 39

water of, analysis of.................... 31

Goniobasis, occurrence of................... 10

Gunnison, flow near........................ 18

water supplies near..................... 42-43

.Gunnison Plateau, description of........... 7

rocks of................................. 10

section on.............................. 11

Herrins Hole Springs, character of. 

I.

Igneous rocks, occurrence and character of. 12

Inoceramus labiatus, occurrence of......... 9

Inverury, water resources of............... 39

Irrigation, methods of, crudeness of....... 33

J. 

Jarvis, C. S., work of..................... 5,17,19

Joseph, water supplies near................ 34-35

Joseph Hot Springs, description of......... 35

temperature of......................... 25,35

J urassic rocks, occurrence and character of. 8-9

Knowlton, F. H., fossils determined by.... 9 

L.

Laramie formation, occurrence of........ 9-10,22

water in................................ 22

Lost Creek, flow of......................... 17,20

M.

Madsen and Seely tunnel, spring in........ 49

Manti, precipitation at..................... 16

water supplies at....................... 44-45

well near, record of..................... 45

Manti beds, occurrence of.................. 11-12

Manti Creek, flow of........................ 17

water of, analysis of.................... 30

view of................................. 14

Map of Utah, showing location of valleys... 6 

Map, geologic, of Sanpete and central Sevier

valleys........................ Pocket.

61
62 INDEX.

Page.

Map, underground water, in Sanpete Valley. 24

in central Sevier Valley................. 22

Mayfleld, water resources near............. 43-44

Milburn, water supplies near............... 49,60

Monroe, water supplies near............... 36-37

Monroe Creek, flow of...................... 17,20

water of, analysis of.................... 31

Monroe Hot Springs, description of........ 36-37

temperature of......................... 25,37

water of, analysis of.................... 37

Monroe Peak, elevation of.................. 7

Moroni, water supplies near................ 46-47

well near, record of..................... 46

Moroni canal, flow of....................... 19

seepage from........................... 19

Morrison Tunnel Spring, structure at, section showing................... 26, 44

water of, analysis of................... 31

Mormons, settlement by................... 5

Mount Pleasant, precipitation at........... 16

water supplies near..................... 4S-50

N.

Nebo, Mount, rocks on...................

Ninemile Spring, water of, analysis of....

North Creek, flow of......................

O.

Pavant Mountains, description of..........

rocks of.............................. 10,

Physa, occurrence of.......................

Pianorbis, occurrence of....................'

Pleasant Creek, flow of.....................

water of, analysis of....................

Precipitation, amount of...................

disposal of..............................

R.

22,23 

10 

10 

17 

30

15-10 

14-15

Rainfall. See Precipitation.

Redbutte Creek, flow of.................... 20

Redmond, water supplies of................ 42

well near, record of..................... 42

Reservoirs, recommendation for........... 32-33

Richfield, precipitation at.................. 15

water supplies near..................... 37-39

well near, water of, analysis of......... 38

Richfield Spring, description of............. 38-39

structure at, section showing........... 26

temperature of......................... 25

water of, analysis of.................... 31

S. 

Sabal, occurrence of........................ 9

Sabalites grayanus, occurrence of.......... 9

Salina, description of....................... 41

water supplies near..................... 40-42

well at, record of....................... 41

Salina Creek, artesian wells on............. 40

flow of.................................. 17,20

water of, analyses of.................... 30-31

Salix sp., occurrence of..................... 9

San Pitch Creek, character of.............. 16

flow of.................................. 18,21

irrigation from......................... 5

tributaries of........................... 7

water of, analyses of.................... 30

See also Sanpete Valley. 

Sanpete Valley, geology of................. 8-14

geology of, map showing............ Pocket.

location of.............................. 5

sections across, figures showing........ 12,13

springs in, data on............... 42-50,58-60

topography of.......................... 6-8

underground water in.................. 14-34

depth to, map showing............. 24

water resources in...................... 14-34

wells in, data on................. 42-50,53-57

Seep springs, occurrence of................. 27-28

Seepage, gain and loss by.................. 19-21

Sevier Plateau, description of.............. 7

Sevier River, canals from................... 5

character of............................ 16

flow of............................... 17,18-21

seepage on.............................. 19-21

tributaries of........................... 6-7

water of, analysis of.................... 30

Sevier Valley, geology of................... 8-14

geology of, map showing............ Pocket.

location of.............................. 5,7-8

sections across, plate showing.......... 12

springs in, data on .................. 35-44,58

topography of.......................... 6-8

underground water in.................. 14-34

depth to, map showing............. 22

water resources in...................... 34-44

wells in, data on.................. 34-44, 51-54

Sixmile Creek, flow of...................... 17

water of, analysis of ................... 30

SphtErium, occurrence of................... 10

Spring City, water supplies near........... 49-50

Spring Creek, flow of....................... 20

Springs, flow of.................... 21,25-26,27-28

list of................................... 58-60

location of, maps showing.............. 22,24

occurrence of........................... 35-50

structure at, figure showing............ 26

Sterling, rocks near......................... 9,10

water supplies of....................... 44

Streams, character of........................16-17

flow of.................................. 16-21

water of, analyses of................... 30-32

Structure, character of..................... 13-14

section showing........................ 13

T.

Tanner, Caleb, cooperation of.............. 5

flow measurements by.................. 19

Tertiary rocks, occurrence and character of. 10-12 

Thompsons Creek, flow of-................. 20

Topography, description of................ 6-8

Tunnels, recovery of water by..... 26-27,28,44,49

recovery of water by, figures showing.. 26,28 

Twelvemile Creek, flow of.................. 17

water of, analysis of.................... 30

Twin Creek, flow of......................... 17,19

seepage from........................... 19
INDEX. 63

u.

Underground water. See Water, underground. 

Utah, map of, showing location of valleys.. 6

V.

Valley deposits, occurrence and character of 12-13 

water in................................ 23-24

recovery of......................... 27-30

Valley Mountains, description of........... 8

Vivipara, occurrence of..................... 10

W.

Wales, section near......................... 11

water supplies near..................... 48

Wasatch Plateau, description of........... 7

rocks of................................. 10,22

view of................................. 14

Water, conservation of..................... 32-34

Water, quality of........................... 30-32

Water, underground, depth to, maps showing.............................. 22,24

distribution of.......................... 21-24

pollution of............................. 32

quality of............................... 31-32

recovery of............................. 24-30

source of................................ 14-21

Water Canyon Creek, flow of............... 20

Wells, list of................................ 51-57

location of, maps showing............. 22,24

use of............................. 28-29,34-50

water of, analyses of................... 31

Wells, flowing, list of....................... 52-56

occurrence of.................. 27,29,37-38,40

prospects for........................... 27,40

use of................................... 34

water of, analyses of................... 31

Willow Creek,.flow of....................... 17,21

CLASSIFICATION OF THE PUBLICATIONS OF .THE UNITED STATES GEOLOGICAL

SURVEY.

[Water-Supply Paper No. 199.]

The publications of the United States Geological Survey consist of (1) Annual 

Reports, (2) Monographs, (3) Professional Papers, (4) Bulletins, (5) Mineral 

Resources, (6) Water-Supply and Irrigation Papers, (7) Topographic Atlas of United 

States folios and separate sheets thereof, (8) Geologic Atlas of United States folios 

thereof. The classes numbered 2, 7, and 8 are sold at cost of publication; the others 

are distributed free. A circular giving complete lists can be had on application.

Most of the above publications can be obtained or consulted in the following ways:

1. A limited number are delivered to the Director of the Survey, from whom they 

can be obtained, free of charge (except classes 2, 7, and 8), on application.

2. A certain number are delivered to Senators and Representatives in Congress for 

distribution. i

3. Other copies are deposited with the Superintendent of Documents, Washington, 

D. C., from whom they can be had at prices slightly above cost.

4. Copies of all Government publications are furnished to the principal public 

libraries in the large cities throughout the United States, where they can be consulted 

by those interested.

The Professional Papers, Bulletins, and Water-Supply Papers treat of a variety of 

subjects, and the total number issued is large. They have therefore been classified 

into the following series: A, Economic geology; B, Descriptive geology; C, Systematic geology and paleontology; D, Petrography and mineralogy; E, Chemistry and 

physics; F, Geography; G, Miscellaneous; H, Forestry; I, Irrigation; J, Water storage; K, Pumping water; L, Quality of water; M, General hydrographic investigations; N, Water power; 0, Underground waters; P, Hydrographic progress reports. 

This paper is the one hundred and seventeenth in Series B and the seventieth in 

Series 0, the complete lists of which follow (PP=Professional Paper; B=Bulletin; 

WS=Water-Supply Paper):

SERIES B, DESCRIPTIVE GEOLOGY.

B 23. Observations on the junction between the Eastern sandstone and the Keweenaw series on

Keweenaw Point, Lake Superior, by R. D. Irving and T. C. Chamberlin. 1885. 124 pp., 17

pis. (Out of stock.)

B 33. Notes on geology of northern California, by J. S. Diller. 1886. 23pp. (Out of stock.) 

B 39. The upper beaches and deltas of Glacial Lake Agassiz, by Warren Uphain. 1887. 84 pp., 1 pi.

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B 40. Changes in river courses in Washington Territory due to glaciation, by Bailey Willis. 1887.

10 pp., 4 pis. (Out of stock.) 

B 45. The present condition of knowledge of the geology of Texas, by R. T. Hill. 1887. 94 pp. (Out

of stock.)

B 53. The geology of Nantucket, by N. S. Shaler. 1889. 55 pp., 10 pis. (Out of stock.) 

B 57. A geological reconnaissance in southwestern Kansas, by Robert Hav. 1890. 49 pp., 2 pis. 

B 58. The glacial boundary in western Pennsylvania, Ohio, Kentucky, Indiana, and Illinois, by G. F.

Wright, with introduction by T. 0. Chamberlin. 1890. 112 pp., 8 pis. (Out of stock.) 

B 67. The relations of the traps of the Newark system in the New Jersey region, by N. H. Darton.

1890. 82 pp. (Out of stock.) 

B104. Glaciation of the Yellowstohe Valley north of the Park, by W. H. Weed. 1893. 41 pp., 4 pis.

IRB 199 07 5 I
II SERIES LIST.

B 108. A geological reconnaissance in central Washington, by I. C. Russell. 1893. 108 pp., 12 pis.

(Out of stock.)

B 119. A geological reconnaissance in northwest Wyoming, by G. H. Eldridge. 1894. 72 pp., 4 pis. 

B 137. The geology of the Fort Riley Military Reservation and vicinity, Kansas, by Robert Hay. 1896.

35pp., 8 pis. 

B 144. The moraines of the Missouri Coteau and their attendant deposits, by J. E. Todd. 1896. 71

pp., 21 pis. 

B 158. The moraines of southeastern South Dakota and their attendant deposits, by J. E. Todd. 1899.

171 pp., 27 pis. 

B 159. The geology of eastern Berkshire County, Massachusetts, by B. K. Emerson. 1899. 139 pp.,

9 pis. 

B 165. Contributions to the geology of Maine, by H. S. Williams and H. E. Gregory. 1900 212 pp.,

14 pis. 

WS 70. Geology and water resources of the Patrick and tioshen Hole quadrangles in eastern Wyoming

and western Nebraska, by G. I. Adams. 1902. 50 pp., 11 pis. 

B 199. Geology and water resources of the Snake River Plains of Idaho, by I. C. Russell. 1902. 192

pp., 25 pis. 

PP 1. Preliminary report on the Ketchikan mining district. Alaska, with an introductory sketch of

the geology of southeastern Alaska, by A. H. Brooks. 1902. 120 pp., 2 pis. 

PP 2. Reconnaissance of the northwestern portion of Seward Peninsula, Alaska, by A. J. Collier.

1902. 70 pp., 11 pis. 

PP 3. Geology and petrography of Crater Lake National Park, by J. S. Diller and H. B. Patton. 1902.

167pp., 19 pis. 

PP 10. Reconnaissance from Fort Hamlin to Kotzebue Sound, Alaska, byway of Ball, Kanuti, Alien,

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PP 11. Clays of the United States east of the Mississippi River, by Heinrich Ries. 1903. 298 pp., 9 pis.

(Out of stock.)

PP 12. Geology of the Globe copper district, Arizona, by F. L. Ransome. 1903. 168 pp., 27 pis. 

PP 13. Drainage modifications in southeastern Ohio and adjacent parts of West Virginia and Kentucky, by W. G. Tight. 1903. Ill pp., 17 pis. (Out of stock.)

B 208. Descriptive geology of Nevada south of the fortieth parallel and adjacent portions of California, by J. E. Spurr. 1903. 229 pp., 8 pis. (Out of stock.)

B 209. Geology of Ascutney Mountain, Vermont, by R. A. Daly. 1903. 122 pp.3 7 pis. 

WS 78. Preliminary report on artesian basins in southwestern Idaho and southeastern Oregon, by

I. C. Russell. 1903. 51 pp., 2 pis. 

PP 15. Mineral resources of the Mount Wrangell district, Alaska, by W. C. Mendenhall and F. C.

Schrader. 1903. 71 pp. 10 pis. 

PP 17. Preliminary report on the geology and water resources of Nebraska west of the one hundred

and third meridian, by N. H. Barton. 1903. 69 pp., 43 pis. 

B 217. Notes on the geology of southwestern Idaho and southeastern Oregon, by I. C. Russell. 1903.

83 pp., 18 pis.

B 219. The ore deposits of Tonopah, Nevada (preliminary report), by J. E. Spurr. 1903. 31 pp., 1 pi. 

PP 20. A reconnaissance in northern Alaska in 1901, by F. C. Schrader. 1904. 139 pp., 16 pis. 

PP 21. The geology and ore deposits of the Bisbee quadrangle, Arizona, by F. L. Ransome. 1904.

168pp., 29 pis. 

WS 90. Geology and water resources of part of the lower' James River Valley, South Dakota, by J. E.

Todd and C. M. Hall. 1904. 47 pp., 23 pis. 

PP 25. The copper deposits of the Encampment district, Wyoming, by A. C. Spencer. 1904. 107 pp.,

2 pis. (Out of stock.) 

PP 26. Economic resources of the northern Black Hills, by J. D. Irving, with contributions by S. F.

Emmons and T. A. Jaggar, jr. 1904. 222 pp., 20 pis.

PP 27. A geological reconnaissance across the Bitterroot Range and Clearwater Mountains in Montana and Idaho, by Waldemar Lindgren. 1904. 122 pp., 15 pis.

PP 31. Preliminary report on the geology of the Arbuckle and Wichita mountains in Indian Territory and Oklahoma, by J. A. Taff, with an appendix on reported ore deposits in the Wichita

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B 235. A geological reconnaissance across the Cascade Range near the forty-ninth parallel, by G. O.

Smith and F. C. Calkins. 1904. 103 pp., 4 pis.

B 236. The Porcupine placer district, Alaska, by C. W. Wright. 1904. 35 pp., 10 pis. 

B 237. Igneous rocks of the Highwood Mountains, Montana, by L. V. Pirsson. 1904. 208 pp., 7 pis. 

B238. Economic geology of the lola quadrangle, Kansas, by G. I. Adams, Erasmus Haworth, and

W. R. Crane. 1904. 83 pp., 1 pi. 

PP 32. Geology and underground water resources of the central Great Plains, by N. H. Darton. 1905.

433 pp., 72 pis. 

WS 110. Contributions to hydrology of eastern United States, 1904; M. L. Fuller, geologist in charge.

1905. 211pp., 5 pis.
SERIES LIST. Ill

B 242. Geology of the Hudson Valley between the Hoosic and the Kinderhook, by T. Nelson Dale.

1904. 63 pp., 3 pis. 

PP 34. The Delavan lobe of the Lake Michigan glacier of the Wisconsin stage of glaciation and

associated phenomena, by W. C. Alden. 1904. 106 pp., 15 pis. 

PP 35. Geology of the Perry Basin in southeastern Maine, by G. O. Smith and David White. 1905.

107 pp., 6 pis.

B 243. 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. F. Bain. 1904. 56 pp., 5 pis. 

B 247. The Fairhaven gold placers of Seward Peninsula, Alaska, by F. H. Moffit. 1905. 85 pp., 14 pl8. 

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 River coal

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B 251. The gold placers of the Fortymile, Birch Creek, and Fairbanks regions, Alaska, by L. M.

Prindle. 1905. 16 pp., 16 pis. 

WS 118. Geology and water resources of a portion of east-central Washington, by F. C. Calkins. 1905.

96pp., 4 pis. 

B 252. Preliminary report on the geology and water resources of central Oregon, by I. C. Russell.

1905. 138pp., 24 pis. 

PP 36. The lead, zinc, and fluorspar deposits of western Kentucky, by E. O. Ulrich and W. S. Tangier

Smith. 1905. 218 pp., 15 pis. 

PP 38. Economic geology of the Bingham mining district of Utah, by J. M. Boutwell, with a chapter

on area! geology, by Arthur Keith, and an introduction on general geology, by S. F. Emmons.

1905. 413pp., 49 pis. 

PP 41. The geology of the central Copper River region, Alaska, by W. C. Mendenhall. 1905. 133 pp.,

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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. (Out of

stock.) 

B 256. Mineral resources of the Elders Ridge quadrangle, Pennsylvania, by R. W. Stone. 1905.

85 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 the fossil plants, by F. H. Knowlton. 1905. 174 pp., 19 pis. 

PP 42. Geology of tlie Tonopah mining district, Nevada, by J. E. Spurr. 1905. 295 pp., 24 pis. 

WS 123. Geology and underground water conditions of the Jornada del Muerto, New Mexico, by

C. R. Keyes. 1905. 42 pp., 9 pis. (Out of stock.)

WS 136. Underground waters of Salt River Valley, Arizona, by W. T. Lee. 1905. 194 pp., 24 pis. 

PP 43. The copper deposits of Clifton-Morenci, Arizona, by Waldemar Lindgren. 1905. 375 pp., 25pis. 

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. F. 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.

394pp., 34 pis.

WS 148. Geology and water resourc s of Oklahoma, by C. N. Gould. 1905. 178 pp., 22 pis. 

B 270. The configuration of the rock floor of Greater New York, by W. H. Hobbs. 1905. 96 pp., 5 pis. 

B 272. Taconic physiography, by T. M. Dale. 1905. 52 pp., 14 pis. 

PP 45. The geography and geology of Alaska, a summary of existing knowledge, by A. H. Brooks,

with a section on climate, by Cleveland Abbe, jr., and a topographic map and description

thereof, by E.M. Goode. 1905. 327 pp., 34 pis. 

B 273. The drumlins of southeastern Wisconsin (preliminary paper), by W.C. Alden. 1905. 46 pp.,

9 pis. 

PP 46. Geology and underground, water resources of northern Louisiana and southern Arkansas, by

A. C. Veatch. 1906. 422 pp., 51 pis. 

PP 49. Geology and mineral resources of part of the Cumberland Gap coal field, Kentucky, by G. H.

Ashley and L. C. Glenn, in cooperation with the State Geological Department of Kentucky,

C. J. Norwood, curator. 1906. 239 pp., 40 pis.

PP 50. The Montana lobe of the Keewatin ice sheet, by F. H. H. Calhoun. 1906. 62 pp., 7 pis. 

B 277. Mineral resources of Kenai Peninsula, Alaska: Gold fields of the Turnagaiii Arm region, by

F. H. Moffit; and the coal fields of the Kachemak Bay region, by R. W. Stone. 1906. 80pp.,

18 pis. (Out of stock.) 

WS 154. The geology and water resources of the eastern portion of the Panhandle of Texas, by C. N.

Gould. 1906. 64 pp., 15 pis. 

B 278. Geology and coal resources of the Cape Lisburne region, Alaska, by A. J. Collier. 1906. 54

pp.,9pls. (Out of stock.) 

B279. Mineral resources of the K ttanning and Rural Valley quadrangles, Pennsylvania, by Charles

ButK 1906. 198pp., 11 pis. 

B 280. The Rampart gold placer region, Alaska, by L. M. Prindle and F. L. Hess. 1906. 54 pp., 7 pis.

(Out of stock.)
IV SERIES LIST.

B 282. Oil fields of the Texas-Louisiana Gulf Coastal Plain, by N. M. Fenneman. 1906. 146 pp., 11 pis. 

WS 157. Underground water in the valleys of Utah Lake and Jordan River, Utah, by G. B. Richardson.

1906. 81 pp., 9 pis.

PP 51.' Geology of the Bighorn Mountains, by N. H. Darton. 1906. 129 pp., 47 pis. 

WS 158. Preliminary report on the geology and underground waters of the Roswell artesian area,

New Mexico, by C. A. Fisher. 1906. 29 pp., 9 pis. 

PP 52. Geology and underground waters of the Arkansas Valley in eastern Colorado, by N. H. Darton.

1906. 90 pp., 28 pis. 

WS 159. Summary of underground-water resources of Mississippi, by A. F. Crider and L. C. Johnson.

1906. 86 pp., 6 pis. 

PP53. Geology and water resources of the Bighorn basin, Wyoming, by Cassius A. Fisher. 1906.

72pp., 16 pis.

B 283. Geology and mineral resources of Mississippi, by A. F. Crider. 1906. 99 pp., 4 pis. 

B 286. Economic geology of the Beaver quadrangle, Pennsylvania (southern Beaver and northwestern Allegheny counties), by L. H. Woolsey. 1906. 132 pp., 8 pis. 

B 287. The Juneau gold belt, Alaska, by A. C. Spencer, and a reconnaissance of Admiralty Island,

Alaska, by C. W. Wright. 1906. 161 pp., 37 pis. 

PP 54. The geology and gold deposits of the Cripple Creek district, Colorado, by W. Lindgren and

F. L. Ransome. 1906. 516 pp., 29 pis.

PP 55. Ore deposits of the Silver Peak quadrangle, Nevada, by J. E. Spurr. 1906. 174 pp., 24 pis. 

B 289. A reconnaissance of the Matanuska coal field, Alaska, in 1905, by G. C. Martin. 1906. 36 pp.,

5 pis. 

WS 164. Underground waters of Tennessee and Kentucky west of Tennessee River and of an adjacent

area in Illinois, by L. C. Glenn. 1906. 173 pp., 7 pis. 

B 293. A reconnaissance of some gold and tin deposits of the southern Appalachians, by L. C. Groton,

with notes on the Dahlonega mines, by "W. Lindgren. 1906. 134 pp.,9 pis.

B 294. Zinc and lead deposits of the upper Mississippi Valley, by H. Foster Bain. 1906. 155pp., 16 pis. 

B 295. The Yukon-Tanana region, Alaska, description of Circle quadrangle, by L. M. Prindle. 1906.

27pp., Ipl7 

B 296. Economic geology of the Independence quadrangle, Kansas, by Frank C. Schrader and

Erasmus Ha worth. 1906. 74 pp., 6 pis. 

WS 181. Geology and water resources of Owens Valley, California, by Willis T. Lee. 1906. 28 pp.,

6 pis.

B 297. The Yampa coal field, Routt County, Colo., by N. M. Fenneman, Hoyt S. Gale, and M. R. Campbell. 1906. 96 pp., 9 pis. 

B 300. Economic geology of the Amity quadrangle in eastern Washington County, Pa., by F. G.

Clapp. 1906. 145 pp., 8 pis. 

B 303. Preliminary account of Goldfield, Bullfrog, and other mining districts in southern Nevada, by

F. L. Ransome;. with notes on Manhattan district, by G. H. Garrey and W. H. Emmons,

1907. 98 pp., 5 pis.

B 304. Oil and gas fields of Greene County, Pa., by R. W. Stone and F. G. Clapp. 1907. 110 pp., 3 pis. 

WS 188. Water resources of the Rio Grande Valley in New Mexico and their development, by W. T.

Lee. 1906. 59pp., 10 pis. 

B 306. Rate of recession of Niagara Falls, accompanied by a report on the survey of the crest, by

W. Carvel Hall. 1906. 31 pp., 11 pis. 

PP 56. Geography and Geology of a portion of southwestern Wyoming, with special reference to coal

and oil, by A. C. Veatch. 1907. pp., 26 pis. . 

B 308. A geologic reconnaissance in southwestern Nevada and eastern California, by 8. H. Ball. 1907.

218pp., 3 pis. 

B 309. The Santa Clara Valley, Puente Hills, and Los Angeles oil districts, southern California, by

G. H. Eldridge and Ralph Arnold. 1907. 266 pp., 41 pis. 

PP 57. Geology of the Marysville mining district, Montana, a study of igneous intrusion and contact

metamorphism, by Joseph Barrell. 3907. 178 pp., 16 pis. 

WS. 191. The geology and water resources of the western portion of the Panhandle of Texas, by C. N.

Gould. 1907. 70pp., 7 pis. 

B 311. The green schists and associated granites and porphyries of Rhode Island, by B. K. Emerson

and J. H. Perry. 1907. 74 pp., 2 pis. 

WS 195. Underground waters of Missouri, their geology and utlization, by Edward Shepherd. 1907.

224pp., 6 pis. 

WS 199. Underground water in Sanpete and central Sevier valleys, Utah, by G. B. Richardson. 1907.

63 pp., 6 pis.

SERIES O, UNDERGROUND WATERS.

WS 4. A reconnaissance in southeastern Washington, by I. C. Russell. 1897. 96 pp., 7 pis. (Out of

stock.) 

WS 6. Underground waters of southwestern Kansas, by Erasmus Haworth. 1897. 65 pp., 12 pis.

(Out of stock.) 

WS 7. Seepage waters of northern Utah, by Samuel Fortier. 1897. 50pp., 3 pis. (Out of stock.)
SERIES LIST. V

WS 12. Underground waters of southeastern Nebraska, by N. H. Barton. 1898. 56 pp., 21 pis. (Out

of stock.)

WS 21. Wells of northern Indiana, by Frank Leverett. 1899. 82 pp., 2 pis. (Out of stock.) 

WS 26. Wells of southern Indiana (continuation of No. 21), by Frank Leverett. 1899. 64pp. (Out

of stock.) 

WS 30. Water resources of the lower peninsula of Michigan, by A. C. Lane. 1899. 97 pp., 7 pis. (Out

of stock.)

WS 31. Lower Michigan mineral waters, by A. C. Lane. 1899. 97 pp., 4 pis. (Out of stock.) 

WS 34. Geology and water resources of a portion of southeastern South Dakota, by J. E. Todd. 1900.

34pp., 19 pis. 

WS 53. Geology and water resources of Nez Perces County, Idaho, Pt. I, by I. C. Russell. 1901.

86 pp., 10 pis. (Out of stock.) 

WS 54. Geology and water resources of Nez Perces County, Idaho, Pt. II, by I. C. Russell. 1901.

87-141 pp. (Out of stock.) 

WS55. Geology and water resources of a portion of Yakima County, Wash., by G. O. Smith. 1901.

68 pp., 7 pis. (Out of stock.) 

WS57. Preliminary list of deep borings in the United States, Pt. I, by N. H. Barton. 1902. 60pp.

(Out of stock.) 

WS 59. Development and application of water in southern California, Pt. I, by J. B. Lippincott. 1902

95 pp., 11 pis. (Out of stock.) 

WS 60. Development and application of water in southern California, Pt. II, by J. B. Lippincott. 1902.

96-140 pp. (Out of stock.) / 

WS 61. Preliminary list of deep borings in the United States, Pt. II, by N. H. Darton. 1902. 67 pp.

(Out of stock.)

WS 67. The motions of underground waters, by C. S. Slichter. 1902. 106 pp., 8 pis. (Out of stock.) 

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 Waldemar Lindgren. 1903. 62pp., 4 pis. 

WS 78. Preliminary report on artesian basins in southwestern Idaho and southeastern 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. 69 pp., 43 pis. 

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 101. Underground waters of southern Louisiana, by G. D. Harris, with discussions of their uses

for water supplies and for rice irrigation, by M. L. Fuller. 1904. 98 pp., 11 pis.

WS 102. Contributions to the hydrology of eastern United States, 1903, by M. L. Fuller. 1904. 522 pp. 

WS 104. Underground waters of Gila Valley, Arizona, by W. T. Lee. 1904. 71 pp., 5 pis. 

WS 106. Water resources of the Philadelphia district, by Florence Bascom. 1904. 75 pp., 4 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.

433 pp., 72 pis. (Out of stock.) 

WS 111. Preliminary report on underground waters of Washington, by Henry Landes. 1904. 85 pp.,

Ipl. 

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, by M. L. Fuller, geologist in charge. 1904.

285pp., 18 pis. 

WS 118. Geology and water resources of east-central Washington, by F. C. Calkins. 1905. 96 pp.,

4 pis. 

B252. Preliminary report on the geology and water resources of central Oregon, by 1. C. Russell.

1905. 138 pp., 24 pis. 

WS 120. Bibliographic review and index of papers relating to underground waters, published by the

United States Geological Survey, 1879-1904, by M. L. Fuller. 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 C. R.

Keyes. 1905. 42pp., 9 pis. (Out of stock.)

WS 136. Underground waters of the Salt River Valley, by W. T. Lee. 1905. 194 pp., 24 pis. 

B 264. Record of deep-well drilling for 1904, by M. L. Fuller, E. F. Lines, and A. C. Veatch. 1905.

106 pp. 

PP44. Underground water resources of Long Island, New York, by A. C. Veatch and others. 1905.

394 pp., 34 pis.

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.
VI SEKIES LIST.

WS 139. Development of underground waters in the western coastal plain region of southern California, by W. C. Mendenhall. 1905. 105 pp., 7 pis.

WS 140. Field measurements of the rate of movement of underground waters, by C. S. Slichter. 1905. 

122pp., 15 pis.

WS 141. Observations on the ground waters of Rio Grande Valley, by C. S. Slichter. 1905. 83 pp., 

5 pis.

WS142. Hydrology of San Bernardino Valley, California, by W. C. Mendenhall. 1905. 124pp., 13 pis.

WS 145. Contributions to the hydrology of eastern United States; M. L. Fuller, geologist in charge.

1905. 220 pp., 6 pis. '

WS 148. Geology and water resources of Oklahoma, by C. N. Gould. 1905. 178 pp., 22 pis. 

WS 149. Preliminary list of deep borings in the United States, second edition, with additions, by

N. H. Barton. 1905. 175 pp. 

PP 46. Geology and underground water resources of northern Louisiana and southern Arkansas, by

A. C. Veatch. 1906. 422 pp., 51 pis. 

WS 153. The underflow in Arkansas Valley in western Kansas, by C. S. Slichter. 1906. 90 pp., 3 pis.

(Out of stock.) 

WS 154. The geology and water resources of the eastern portion of the Panhandle of Texas, by C. N.

Gould. 1906. 64 pp., 15 pis. 

WS 155. Fluctuations of the water level in wells, with special reference to Long Island, New York, by

A. C. Veatch. 1906. 83pp., 9 pis. 

WS 157. Underground water in the valleys of Utah Lake and Jordan River, Utah, by G. B. Richardson.

1906. 81 pp., 9 pis. 

WS 158. Preliminary report on the geology and underground waters of the Roswell artesian area,

New Mexico, by Q. A, Fisher. 1906. 29 pp., 9 pis. 

PP 52. Geology and underground waters of the Arkansas Valley in eastern Colorado, by N. H. Barton.

1906. 90 pp., 28 pis. 

WS 159. Summary of underground-water resources of Mississippi, by A. F. Crider and L. C. Johnson.

1906. 86 pp., 6 pis. 

PP 53. Geology and water resources of the Bighorn basin, Wyoming, by C. A. Fisher. 1906. 72 pp.,

16 pis.

WS 160. Underground-water papers, 1906, by M. L. Fuller. 1906. 104 pp., 1 pi. (Out of stock.) 

WS 163. Bibliographic review and index of underground-water literature published in the United

States in 1905, by M. L. Fuller, F. G. Clapp, and B. L. Johnson. 1906. 130 pp.

WS 164. Underground waters of Tennessee and Kentucky west of Tennessee River and of an adjacent area in Illinois, by L. C. Glenn. 1906. 173 pp., 7 pis. 

WS 181. Geology and water resources of Owens Valley, California, by W. T. Lee. 1906. 28 pp., 6 pis.

(Out of stock.)

WS 182. Flowing wells and municipal water supplies in the southern portion of the Southern Peninsula of Michigan, by Frank Leverett and others. 1906. 292 pp., 5 pis. 

WS 183. Flowing wells and municipal water supplies in the middle and northern portions of the

Southern Peninsula of Michigan, by Frank Leverett and others. 1906. 393 pp., 5 pis. 

B 298. Record of deep-well drilling for 1905, by M. L. Fuller and Samuel Sanford. 1906. 299 pp. 

WS 184. The underflow of the South Platte Valley, by C. S. Slichter and H. C. Wolff. 1906. 42 pp. 

WS 188. Water resonrces of the Rio Grande'Valley in New Mexico and their development, by W. T.

Lee. 1906. 59 pp., 10 pis.

WS 190. Underground waters of Coastal Plain of Texas, by T. U. Taylor. 1907. 73 pp., 3 pis. 

WS 191. Geology and water resources of the western portion of the Panhandle of Texas, by C. N.

Gouid. 1907. 70 pp., 7 pis. 

WS 195. Underground waters of Missouri; their geology and utilization, by Edward Shepard.

1907. 224 pp., 6 pis. 

WS 199. Underground water in Sanpete and central Sevier valleys, Utah, by G. B. Richardson. 1907^

63pp., 6 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 Bakotas, by N. H. Barton, in Seventeenth Annual, Pt. II; Water resources of 

Illinois, by Frank Leverett, in Seventeenth Annual, Pt. II; Water resources of Indiana and Ohio, 

by Frank Leverett, in Eighteenth Annual, Pt. IV; New developments in well boring and irrigation 

in eastern South Dakota, by N. H. Barton, 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. Barton, Bulletin No. 138.

Correspondence should be addressed to

THE DIRECTOR,

UNITED STATES GEOLOGICAL SURVEY,

WASHINGTON, D. C. 

JULY, 1907.

o