Water-Supply and Irrigation Paper No. 157

DEPARTMENT OF THE INTERIOR

UNITED STATES GEOLOGICAL SURVEY

CHARLES D. WALCOTT, DlKKCTOK

UNDERGROUND WATER

IN THE

VALLEYS OF UTAH LAKE AND JORDAN RIVER, UTAH

BY

G. B. RICHARDSON

WASHINGTON

GOVERNMENT PRINTING OFFICE 

1906
CONTENTS.

Introduction..........................

Topography and drainage..............

Geology..............................

Literature........................

Descriptive geology of the highlands 

Late geologic history..............

Tertiary.....................

Quaternary....................

Climate..............................

Precipitation.. 

Temperature.. 

Wind velocity. 

Humidity.....

Evaporation-.. 

Summary.....

Hydrography......

Streams tributary to Utah Lake and Jorc an River. 

Utah Lake....................

Jordan River..................

Great Salt Lake................

Underground water..................

General conditions.............

Source....................

Distribution...............

Quality...................

Recovery.................

Suggestions.................

Occurrence....................

West of Jordan .River........

Divisions of area.......

Upland area............

Lowland area..........

East of Jordan River........

Salt Lake City.........

South of Salt Lake City. 

Utah Lake Valley...........

Lehi and vicinity.

American Fork, Pleasant Grove, and vicinity.

Provo and vicinity....... iSpringville and vicinity...

Spanish Fork, Payson, and vicinity.

Goshen Valley...........

West of Utah Lake.......

Page. 

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4 CONTENTS AND ILLUSTRATIONS.

Underground water Continued. Page.

Well data............................................................. 56

Method of measurement............................................. 56

List of typical wells................................................ 59

Index..................................................................... 77

ILLUSTRATIONS,

PLATE I. Wasatch Mountains from Liberty Park, Salt Lake City................ 5

II. Map of the valleys of Utah Lake and Jordan River, showing drainage

area..--__..._..________...___.......___.;..................... 6

III. A, Northern end of Utah Lake; B, Head-gate of Jordan and Salt Lake

City canal..................................................... 12

IV. A, Gate at head of Jordan River; B, Dead Man's Falls, Cottonwood

Canyon........................................................ 24

V. Well sections- ..................................................... 28

VI.. Sketch map showing depth to ground water in the valleys of Utah Lake

and Jordan River............................................... 30

VII. Map showing the area in which flowing wells are obtained in Jordan

River Valley................................................... 38

VIII. Map showing the area in which flowing wells are obtained in Utah Lake

Valley......................................................... 48

I.. A, Valley of Provo River below mouth of canyon; B, American Fork

at mouth of canyon.............................................. 50

FIG. 1. Diagram showing variation of annual precipitation at Salt Lake City...... 17

2. Diagram showing mean monthly precipitation at Salt Lake City............ 18

3. Diagram showing fluctuation of the surface of Utah Lake, 1889-1904...... 23

4. Diagram showing fluctuation of the surface of Great Salt Lake, 1873-1903... 26

5. Diagram illustrating flow from vertical and horizontal pipes.............. 57
U. S. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. 157 PL. I

WASATCH MOUNTAINS FROM LIBERTY PARK, SALT LAKE CITY. 

Lake in foreground is supplied by artesian wells.
UNDERGROUND WATER IN THE VALLEYS OF UTAH 

LAKE AND JORDAN RIVER, UTAH:

By G. B. RICHARDSON.

INTRODUCTION.

The valleys of Utah Lake and Jordan River are situated in north-central Utah, in the 

extreme eastern part of the Great Basin. The lofty Wasateh Range (PL I), the westernmost of the Rocky Mountain system, limits the valleys on the east, and relatively low 

basin ranges the Oquirrh, Lake, and East Tintic mountains determine them on the 

west. The valleys trend north and south, and are almost separated by the low east-west 

Traverse Range, the slopes of which constitute a dam for Utah Lake, which drains through 

Jordan River to Great Salt Lake.

The area under consideration is the most populous and flourishing part of the State, 

Salt Lake City and Provo, the first and third cities in the State, and many other thriving 

settlements are there located. At Bingham Junction and Murray a number of smelters 

treat the ores from near-by mines, but agriculture is the main industry. Water for irrigation is supplied by mountain streams, and intensive farming is successfully pursued. 

The practice of irrigation was begun by the Mormon pioneers in 1847, and has been discussed in several publications; little attention, however, has been given to the underground water resources, and, so far as the writer is aware, they have not before been 

described. The present paper outlines conditions of occurrence of the subterranean 

waters and describes their development in the valleys of Utah Lake and Jordan River.

TOPOGRAPHY AND DRAINAGE.

The drainage area of Utah Lake and Jordan River is approximately 3,300 square miles, 

of which 2,600 are tributary to Utah Lake and 700 to the Jordan north of the Traverse 

Mountains (PL II). About 2,000 square miles of the watershed are in the Wasateh 

Mountains, while the valleys themselves cover a little less than 1,000 square miles. Utah 

Lake Valley is about 38 miles long, averages 15 miles in width, and occupies about 560 

square miles, including Utah Lake. Jordan Valley is approximately 28 miles long, 15 

miles wide, and comprises 420 square miles. These valleys in late geologic time were 

occupied by Lake Bonneville, the Pleistocene predecessor of Great Salt Lake, and to 

that fact is due their characteristic topography. Almost flat unconsolidated lake sediments underlie the broad valleys, the borders of which are marked by a unique series 

of terraces that characterize the shore lines of the old lake. Descriptive details of these 

features will be given in the sections devoted to geology and to the occurrence of underground water.

The range in elevation is considerable. The present level of Great Salt Lake is approximately 4,210 feet above the sea, and that of Utah Lake is about 4,480 feet. From these 

lowest elevations the two valleys rise to their outer borders, which may conveniently be 

taken as the highest level occupied by Lake Bonneville, at approximately the 5,200-foot 

contour, above which the Wasateh Range towers up to 12,000 feet. The mountains on 

the west are narrow north-south ranges that rise abruptly from broad valleys. The

5
6 UNDERGROUND WATER IN VALLEYS OF UTAH.

Oquirrh Mountains, west of Jordan River, are 30 miles long, 5 to 10 miles wide, and their 

summits rise to elevations of about 10,000 feet. The Lake Mountains, west of Utah 

Lake, are about 15 miles long, 5 miles wide, and 3,000 feet above the lake. They are 

connected by low hills with the Oquirrh Mountains on the north and with the East Tintic 

Mountains on the south. The East Tintic Mountains border Utah Lake Valley on the 

southwest, rising 'above it about 3,000 feet. A spur from these mountains extends northeastward, constituting the southern border of Utah Lake Valley, and almost unites with 

the Wasatch Range. The steep western face of the Wasatch Mountains rises about 7,000 

feet abruptly above the broad valley and constitutes the dominant topographic feature 

of the region. To the east the range slopes away gradually in a series of broad ridges 

and narrow valleys to the mountainous plateau region. The western scarp is deeply 

dissected by canyons, through which the entire Wasatch drainage flows to Great Salt 

Lake, the chief streams being Bear, Weber, and Jordan rivers.

Utah Lake is a body of shallow water about 21 miles long and 7 miles wide (PI. Ill, A), 

covering a maximum area of 93,000 acres. Its depth over much of its extent is only 8 

.feet or less, and the maximum depth in the main body of the lake is about 13 feet. In 

its northwestern part, however, recent soundings have revealed the presence of several 

deep holes, due to springs (p. 49). The shore line of the lake is subject to considerable 

variation, owing to the changing relations of evaporation, precipitation, and inflow, and 

the margins are characteristically .swampy. Two large, shallow bays extend eastward 

and southward from the main body of the lake, one south of Prove and the other north 

of Goshen. West of the lake the Pelican Hills approach close to the shore, and the region 

is barren, but on the north, east, and south the land rises gently toward the base of the 

mountains and is dotted with flourishing settlements which are supported by irrigation.

The principal streams tributary to Utah Lake, beginning at the north and proceeding 

southward, ar&; Dry, American Fork, Battle, and Grove creeks, Provo River, Hobble 

Greek, Spanish Fork, and Peteeneet, Santaquin, and Currant creeks. Of these, Provo 

River is the largest, being approximately 70 miles long and having a drainage area of 640 

square miles. It rises in the Uinta Mountains near the sources of Weber, Bear, and 

Du Chesne rivers, flows westward and southward through Kamas and Provo valleys, and 

passes through the Wasatch Mountains in a deep canyon. On entering Utah Lake Valley 

Provo River flows almost due south for 5 miles, skirting the great Provo delta, and thence 

westward, entering Utah Lake about 3 miles west of Provo.

Spanish Fork has a watershed about equal to that of Provo River, but not so great 

a discharge. It rises near Soldier Summit, and, after receiving two main tributaries, 

North and Thistle creeks, flows in a canyon through the main ridge of the Wasatch Mountains and enters Utah Lake Valley at the head of the large embayment that extends between 

Payson and Springville.

Salt Creek rises in the southern Wasatch Mountains, on the eastern slope of Mount Nebo, 

and, after crossing the border of the plateau region, emerges into the broad valley at the 

southwestern base of the Wasatch Mountains where, in summer, it ceases to flow at the 

surface. The drainage way continues, in a narrow canyon, through Long Ridge which partially connects the East Tintic and the Wasatch mountains, and enters the southern end 

of Utah Lake in Goshen Valley, where the stream, which is fed largely by seepage, is known 

as Currant Creek.

The other tributaries of Utah Lake are relatively small. The chief ones rise in the 

Wasatch Mountains and occupy canyons in their mountain courses, where they maintain 

perennial flows. At the mouths of the canyons canals divert the water and distribute it 

over the valley, so that in the irrigation season practically all of the available supply is 

thus used and the beds of the streams in Utah Lake Vallej7 are commonly dry; but in the 

late spring and early summer, during the period of melting snow, large volumes are discharged directly into the lake.

Jordan River heads at the northern end of Utah Lake and flows northward in a meandering course of about 40 miles to Great Salt Lake. For the first 5 miles the river flows slug-
U. S. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. 167 PL. II

THE 10IXEYS OF UTAH LAKE AND

sfidjviN<> THEm ipiAiNAGE'j^i;;
TOPOGRAPHY AND DRAINAGE. 7

gishly in a broad valley, and in that distance falls only about 10 feet. In the "narrows," 

however, the river occupies a constricted channel and descends rapidly; in the first mile 

below the intake of the canals its fall amounts to about 70 feet. Below the "narrows" the 

valley spreads out and at its greatest width is about 18 miles wide. The country rises gradually toward the adjacent highlands to the base of the terraces that mark the shore lines of 

Lake Bonneville, whence the ascent is by successive steps. Between Salt Lake City and 

Great Salt Lake the topography is almost flat, and a number of small lakes of shifting outline occupy local depressions. As the shore of Great Salt Lake is approached there is a 

faint slope of the surf&ee which becomes increasingly marshy. This area west of Salt Lake 

City in general is barren and desolate and the surface in many places is white with alkali. 

On the uplands, away from the lake, alkali is scarce, but the western part of the valley, 

because of the lack of water, suffers in comparison with the cultivated eastern part, which 

is supplied by streams from the Wasatch Mountains.

North of the Traverse Mountains the principal tributaries of Jordan River are City, 

Butte, Emigration, Parleys, Mill, Big Cottonwood, Little Coltonwood, Dry Cottonwood, and 

Willow creeks, all of which issue from the Wasatch. In their mountain courses these creeks 

generally occupy narrow canyons from which they emerge on the lowlands and flow in broad 

open valleys to the Jordan. Within the mountains they are all perennial streams, but at 

the mouths of the canyons their flow is largely diverted by irrigation ditches, so that, in the 

dryest part of the year, their lower courses are generally dry. They rise in the main crest 

of the Wasatch and have small watersheds, Big Cottonwood Creek, draining about 48 square 

miles, being the largest. This stream rises at the base of Clayton Peak, is fed by a number 

of small lakes, and discharges a considerable quantity of water through a narrow canyon 

(PI. IV, B).

The vegetation is scanty. The valleys in their natural state are occupied by sagebrush, 

greasewood, and kindred desert plants, but wherever water is available, there is a marked 

contrast, and the irrigated areas of these valleys rival in productiveness any in the country. 

Sugar beets are grown in quantity; alfalfa, potatoes, corn, etc., are common crops; and on 

the bench lands a variety of fruits are successfully cultivated. The mountains on the 

western border are generally barren; sagebrush and occasional cacti are the chief growths 

on the slopes, while scrub oak and stunted spruce and pine here and there grow in^ 

patches; the summits are usually bare. The Wasatch Mountains are more favored, but 

they do not support a heavy growth of trees. At the heads of the valleys scattering 

pine, juniper, mountain mahogany, and quaking aspen locally occur, and cottonwood, birch, 

and maple are often found near the stream beds. The slopes are commonly covered with 

underbrush in varying degrees of thickness, sagebrush and scrub oak being prominent.

GEOLOGY. 

LITERATURE.

This area has been studied by prominent geologists and has inspired some classic works 

on American geology. King, Emmons, and Hague of the Fortieth Parallel Survey a interpreted the main features of the region, and Gilbert made it famous by his investigation of 

Lake Bonneville.& But although this interesting region lies contiguous to one of the main 

transcontinental routes and has been visited by many geologists, yet comparatively little 

detailed work has been done in it. Walcottc has studied the Big Cottonwood Cambrian 

section, G. O. Smith and G. W. Tower d have examined the Tintic district, J. E. Spurre has

oKing, Clarence, Systematic geology: Kept. Geol. Explor. 40th Par., vol. 1,1872; Hague, Arnold, and 

Emmons, S. F., Descriptive geology: Ibid., vol. 2, 1877.

6 Gilbert, G. K., Lake Bonneville: Mon. U. S. Geol. Survey, vol. 1, 1890.

« Walcott, C. D., Bull. U. S. Geol. Survey No. 30, 1886, p. 38.

<* Tower, G. W., and Smith, G. O., Geology and mining industry of the Tintic district, Utah: Nineteenth Ann. Rept. U. S. Geol. Survey, pt. 3, 1898, p. 601. i

«Spurr, J. E., Economic geology of the Mercur mining district, Utah. Sixteenth Ann. Rept. U. S. 

Geol. Survey, pt. 2,1895, p. 343.
8 UNDERGROUND WATER IN VALLEYS OF UTAH.

reported on the Mercur mines, and, more recently, work has been carried on in the Park 

City and Bingham mining districts by J. M. Boutwell.a The following sketch is mainly 

compiled from these reports.

DESCRIPTIVE GEOLOGY OF THE HIGHLANDS.

The Wasatch Mountains are composed of a complex mass of sedimentary, igneous, and 

metamorphic rocks that have been much folded and faulted. In age the rocks range from 

pre-Cambrian to Tertiary and constitute a thickness of about 50,000 feet. The following 

table shows in epitome the main Paleozoic divisions according to the Fortieth Parallel 

Survey:

Paleozoic section in the Wasatch Mountains.

System. Formation.

flipper Carboniferous 

< Weber quartzites wit

Big Cottonwood quar

Average 

thickness.

Feet. 

2, 500 to 3, 000 

5, 000 to 7,000 

7,000 

1,000 to 1,250 

1,000 to 1,250 

12,000

30,000

The present mountains are the eastern part of a greater mass of rocks, the Wasatch 

Range having baen raised by faulting several thousand feet higher than the western part 

of this mass, which now lies buried beneath the valley deposits. This great fault is the 

dominant structural feature of the region. The range rises abruptly 7,000 feet above the 

wide lowland at its baso, where the streams, which in their mountain courses occupy deepcut narrow gorges, flow in wide valleys. The fault cuts across the range regardless of the 

structure of the rocks, and the truncated mountain bases abut against the plain in marked 

alignment.

Beginning at the north and proceeding southward the following features may be noted: 

The spur that juts out from the Wasatch Mountains north of Salt Lake City marks the 

southern boundary of a series of pre-Cambrian rocks that constitute the crest and western 

flanks of the mountains to the northwest, almost as far as Ogden. These rocks for the 

most part consist of gneisses and mica-schists, considered to be of sedimentary origin, with 

which are associated quartzites, slates, and some igneous rocks. In general the strike is 

N. 20° W., and the prevailing dip is westerly at angles ranging from 15° to 20°. A great 

thickness of coarse Tertiary conglomerate lies high up on the northeastern flanks of the 

range, but at the southeastern end of the crystalline area Paleozoic sediments abut against 

the older series and dip southeastward.

An outlying mass of nearly horizontal coarse Tertiary conglomerate, composed chiefly of 

pebbles of limestone and quartzite, caps the spur of the mountains north of Salt Lake City 

and conceals the older sediments except along the western base of the spiir, where the 

Wasatch limestone outcrops. A small isolated body of volcanic rock outcrops in the midst 

of the Tertiary area and is bisected by City Creek. The headwaters and upper course of 

City Creek lie in Paleozoic rocks, chiefly in the Weber quartzite and Wasatch limestone, 

which dip southeastward at angles varying from 30° to 65°. Across the divide a large area 

of flat-lying Tertiary rocks cap the disturbed Paleozoic series.

o Boutwell, J. M. Progress reports Park City mining district: Bull. U. S. Geol. Survey No. 213,1903, 

pp. 31-40; No. 225, 1904, pp. 141-150; No. 260, 1905, pp. 150-153. Economic geology Bingham mining 

district: Prof. Paper U. S. Geol. Survey No. 38,1905 (with a section on areal geology by Arthur Keith 

and an introduction on general geology by S. F. Emmons).
GEOLOGY. . 9

Between City and Big Cottonwood creeks the summit and western face of the mountains 

are occupied by an immense syncline striking nearly east and west. Its western end is 

terminated by the Wasatch fault, which cuts directly across the fold and exposes the structure so that it can be plainly seen from Jordan Valley. The axis of the syncline coincides 

approximately with the course of Emigration Creek. In detail, however, the structure is 

complicated by a number of relatively minor disturbances.

East of Salt Lake City upper Carboniferous and Permian strata, consisting chiefly of limestone, outcrop between City and Red Butte creeks, and dip southward, forming the northern 

limb of the syncline. Red Butte Canyon lies in Permo-Carboniferous rocks, but near the 

mouth of the canyon "Red Beds" outcrop and continue along its southern divide. The 

"Red Beds" consist chiefly of red shales and sandstones, aggregating over 1,000 feet in 

thickness and are overlain by thin-bedded, argillaceous limestones and shales of Jurassic 

age. These rocks occupy the center of the syncline, and outcrop in the valley of Emigration 

Creek.

South of Emigration Creek the summit and western face of the Wasatch Mountains are 

occupied by the southern limb of the syncline as far as Big Cottonwood Creek, and the 

succession of rocks mentioned above is repeated in reverse order. The dips generally are 

northward, but there are minor folds and faults.

Parleys Creek rises in the Cretaceous sandstone and conglomerate that, east of the main 

Wasatch ridge, lie unconformably upon the older rocks. Aftar traversing this area it crosses 

a narrow belt of Red Beds and, for 5 miles above the mouth of its canyon, flows over calcareous and argillaceous Permo-Carboniferous rocks. Carboniferous strata occupy the divide 

between Parleys and Mill creeks, the latter of which flows for the greater part of its length 

in the Weber quartzites.

Between Mill and Big Cottonwood creeks the lower Paleozoic rocks outcrop. Big Cottonwood Creek exposes for 6 miles above the mouth of its canyon a great- thickness of Cambrian 

strata, consisting of siliceous slates and quartzites; in the upper part of its course this creek 

crosses the Weber quartzite and Wasatch limestone, and heads in the crystalline rocks of 

Clayton Peak. Little is known of the occurrenca of Silurian and D3vonian sediments in 

this area. Their presence was recorded by the early surveys, but the little detailed work 

that has been done shows that in a few localities at least these systems do not appear to be 

represented by sediments.

Little Cottonwood Creek for about 8 miles from the mouth of its canyon flows through a 

crystalline area, and heads in Paleozoic strata and igneous rocks at the foot of Clayton 

Peak. The western base of the mountains extending north and south of Little Cottonwood 

Creek is occupied by a belt of schistose rocks about 10 miles long and averaging perhaps 1 

mile in width. These rocks are of pre-Cambrian age and are over a thousand feet thick. 

They consist largely of quartzite, but includo also slates and mica-schists, having an apparent steep western dip. Up Little Cottonwood Creek, beyond the pre-Cambrian area, lies 

a large body of granitic rocks, which forms high peaks north and south of the creek, and 

through which the stream flows for the greater part of its course. The Paleozoic sediments 

arch around this granitic area, dipping away from it to the north, cast, and south, forming 

a dome the western part of which has been cut off by the Wasatch fault.

The age of the "Little Cottonwood granite" has been the subject of some discussion. It 

clearly cuts the pre-Cambrian rocks at the mouth of the canyon, but its relation to the 

Cambrian was not definitely determined by the early surveys, though the granite was 

thought to be of pre-Cambrian age. Rcc3ntly, however, it has been shown o that the 

"granite" is an intrusive mass that cuts the Cambrian quartzite, though the age of the 

intrusion is not yet known.

Partial topographic connection between the Wasatch and Oquirrh ranges is maintained 

by the Traverse Mountains near tho head of Jordan Valley, but this connection furnishes 

little information concerning the relations of the two main mountain masses, because the

"EmmoriS, S. F., Am. Jour. Scl., 4th ser., vol. 16, August, 1903, p.
10 ' TTNDEBGKOCrND WATEE IN VALLEYS OF UTAH.

Traverse Mountains are largely composed of younger lavas, which conceal the rocks upon 

which they lie.

In the " narrows " where Jordan River flows through the Traverse Mountains, practically 

horizontal Pleistocene gravels, which form the great embankment at the point of the 

mountain, are unconformably underlain near the river level by fine-textured sediments 

that dip southeastward at an angle of 40°. The lower part of these sediments consists of 

light calcareous clay and the upper part of fine sand and gravel. No fossils were found, but 

the marked unconformity and the character of the material suggest that the age of the 

lower deposits is Tertiary.

East of Utah Lake the great Wasatch fault is impressively shown by the remarkable 

alignment of the base of the mountains extending from Spanish Fork Canyon to the Traverse Mountains in an approximately straight line, and by the abrupt rise of the mountains 

above the broad valley. Second and third lines of faulting, lying parallel to the main fault 

and east of it, are suggested by the topography, which rises steplike, with two intervening 

teeads between the ascents, to the top of the main ridge, and by the unusual thickness of 

limestone exposed, which apparently requires repetition by faulting for the explanation of 

its occurrence.

In this part of the range a disturbed belt of rocks with prevailing steep westerly dips 

occurs along the western base of the mountains, beyond which the strata dip eastward at 

low angles and the summits of the main ridge are capped by limestone lying almost flat. 

The streams that cross the mountains, therefore, flow transversely to the strike of the rocks, 

in marked contrast to the creeks farther north, whose courses lie approximately parallel to 

the strike.

Excellent sections can be measured along the canyons, but very little detailed work 

has yet been done. The rocks in general are quartzite and limestone of Carboniferous age, 

but locally Cambrian sediments also occur. In Rock Creek Canyon, east of Provo, in the 

lower end of the gorge, the rocks are much disturbed and are complexly folded. Here a 

considerable thickness of white quartzite outcrops, overlain by a great mass of limestone. 

In a thin bed near the base of the limestone G. H. Girty obtained a few Cariibrian fossils, 

and about 600 feet above, in massive gray limestone, the beds being apparently conformable, 

he found Lower Carboniferous fossils.

South of Hobble Creek easterly dips prevail from the base of the mountains as far as 

Spanish Fork, beyond which the range has been very little studied. It trends southwestward and terminates at Mount Nebo, the main mass of which is composed of steeply westdipping limestone and subordinate quartzite of upper Carboniferous age. The highland 

farther south consists of a series of plateaus, which are underlain by low-lying Mesozoic and 

Tertiary rocks.

The highlands that border the valleys of Jordan River and Utah Lake on the west are^or 

the most part composed of the same rocks that occur in the Wasatch Mountains, but the 

structural relations are completely hidden by the deep filling of the intervening valleys.

The Oquirrh Range is composed mainly of Carboniferous limestones and quartzites, 

which, in the southern part of the mountains, are folded into two parallel anticlines with an 

intervening syncline. The axes of folding are obliquely transverse to the topography, the 

range extending in a north-south direction while the structural trend is northwestward. 

The structure of the northern part of the mountains is little known, but the range is probably terminated by a fault. Rocks of Cambrian age are exposed locally by a fault in the 

vicinity of Mercur, and igneous rocks, both extrusive and intrusive, also occur. The 

intrusive rocks include both acidic and basic porphyries, which are conspicuous in the 

vicinity of the mining camps of Bingham and Mercur; the extrusive rocks, largely andesitic, occur principally along the eastern base of the range and in the Traverse Mountains.

The Lake Mountains, or Pelican Hills, west of Utah Lake, are composed of Carboniferous limestones and quartzites which constitute a low synclinal fold, and are separated 

from the Traverse Mountains by a narrow strip of Pleistocene deposits. A line of hills,
GEOLOGY. 11

composed chiefly of west-dipping limestone, separate the Lake Mountains from the East 

Tintic Range the succeeding highland mass to the south. The northern end of these 

hills is capped by horizontal basalt with which light pumiceous tuff is associated.

The East Tintic Range, a complex mass of sedimentary and igneous rocks, forms the 

southwestern border of Utah Lake basin. As in Rock Canyon, the sediments consist of 

Cambrian quartzite and Carboniferous limestone in juxtaposition, indicating the absence 

of the Ordovician, Silurian, and Devonian. The main structure of the sedimentary rocks is 

synclinal,'but these constitute a relatively small part of the outcrops, igneous rocks, rhyolite, andesite, monzonite, and basalt occupying most of the region. These are of both 

extrasive and intrusive fttrigm, and are of Tertiary age. The low spur of the Tintic Mountains known as Long Ridge, which lies south of Goshen and connects with the Wasatch save 

for a narrow Pleistocene strip south of Santaquin consists of andesite in its southern part, 

while southeast-dipping Carboniferous limestones outcrop in the gorge <rf OairantOreek.

TjATE GEOLOGIC HISTORY.

The above re'sume' implies for this region a complex geologic history which need not here 

be discussed. A statement of late geologic events will, however, add to a clearer understanding of the valley deposits in which.the underground water is stored.

TERTIARY HISTORY.

After many thousands of feet of sediments had accumulated in Paleozoic and Mesozoic 

time, during which the general region was occupied by oceanic waters, profound continental 

uplift occured in early Tertiary time. Since then the ocean has not invaded the interior of 

the continent and during Tertrary time much of the Gordilleran region is believed to have 

been occupied by a number of lakes in which a considerable thickness of rocks accumulated. 

During the Eocene, according to the geologists of the Fortieth Parallel Survey, a great freshwater lake occupied the Wasatch Mountain area, and toward the close of this epoch the 

mountains were finally uplifted and the relative depression of the Great Basin originated. 

The late Tertiary witnessed the formation of several lakes whose positions were determined 

by different crustal movements, and these lakes persisted with varying relations into the 

Pleistocene epoch. The end of Tertiary time was marked by further earth movements that 

divided the Great Basin area into two main depressions, following the bases of the recently 

uplifted Wasatch Mountains and the Sierra Nevada. In Quaternary time the bordering 

mountains were occupied by glaciers, and enormous lakes accumulated in the marginal 

depressions of the Great Basin. The two largest-of these have been named after early 

explorers. Lake Lahontan covered an immense area hi western Nevada and Lake Bonneville occupied a considerable part of western Utah and extended into adjacent parts of 

Nevada and Idaho.

QUATERNARY HISTORY.

The existence of Lake Bonneville is borne witness to by a number and variety of facts, 

chief of which are the remains of shore lines and shore deposits, and the great thickness of 

sediments that accumulated in the lake" and that now constitute the valley floor. At its 

greatest extent the water of Lake Bonneville was approximately 1,000 feet above the 

present surface of Great Salt Lake. This large body of water abutted against the adjacent 

highlands and the outline of the lake was intricate. Deep bays and jutting promontories 

marked the shores, and lone mountains, partly submerged, stood out as islands.

The area considered in this report formed part of one of these bays. This 

was divided by a close stricture into an outer bay and an inner, the outer covering the valley of the 

Jordan River and the inner spreading over Cedar, Utah, and Goshen valleys and a part of Juab Valley. 

In ihe inner bay the Goshen Hills made two islands, and the Pelican Hills constituted one large 

and several small islands. Small estuaries occupied Emigration and Little Cottonwood canyons, 

connecting with the outer bay, and the inner bay sent an estuary into Provo Canyon. a,

a Gilbert, G. K., Lake Bonneville: Mon. U. S. Geol. Survey, vol. 1,1890, p. 103.
12 UNDEEGEOUND WATER IN VALLEYS OF UTAH.

During the existence of Lake Bonneville sedimentation was practically continuous in its 

lowest depression, but toward the periphery oscillations of the water level alternately covered the lakft deposits and exposed them to subaerial influences. Evidence of the earliest 

Pleistocene history of the Bonneville region is furnished by alluvial cones that extend nearly 

to the bottom of the basin. These are composed of detritus derived from the adjacent 

highlands under subaerial conditions and 'could not have been accumulated when the level 

of the lake was high. It is therefore concluded that at this early period in the history of 

the lake comparatively arid conditions prevailed, for the stage of a lake in a closed basin is 

determined by the relation of evaporation to water supply. It has also been determined 

that at this period of the history of the lake it had no outlet and that the time of duration 

of low water was relatively long.

Next succeeded a period of high water, when yellow clay, locally streaked with sand, 

was deposited in a large part of the lake. The base of the yellow clay has not been observed 

and good sections are rare, though an exposure 150 feet thick has been measured. The 

deposit locally extends to within 120 feet of the highest level attained by Lake Bonneville, 

but a study of the shore line shows that during the deposition of the yellow clay the water 

did not rise to the rim of the basin. In the lower part of the basin the yellow clay is 

unconformably overlain by a deposit of white marl, local streaks of alluvium occurring 

at the contact. The white marl is composed of a fine calcareous clay consisting of calcium 

and magnesium carbonates, microscopic siliceous organic remains, and fine clastic debris.

These facts imply (1) that after the deposition of the yellow clay the lake water subsided, (2) that the clay was eroded, and (3) that a second period of high water subsequently 

ensued when the white marl was deposited. The extent to which the waters subsided is 

undetermined, but the possibility of complete desiccation is suggested by the difference 

in character between the yellow clay and white marl. The extent of the second period of 

high water is determined by the highest shore line traceable along the adjacent mountain 

flanks. This level is approximately 1,000 feet above Great Salt Lake and is known as the 

Bonneville shore line. The lake then outflowed through Cache Valley into the Snake 

River basin.

The Bonneville shore line marks the highest stage of Lake Bonneville and the level of 

its initial outflow. Beneath this level the drainage channel was cut down by the outflow 

of the lake to a depth of approximately 375 feet. That the lake maintained its level at the 

stage of lowest outflow for a relatively long time is attested by the well-developed shore 

phenomena at the corresponding elevation. This stage determined the Provo shore line, 

so named from its great development near that' town.

The present conditions have been brought about by the recession of the lake's surface, 

due to the excess of evaporation over inflow, so that now Great Salt, Utah, and Sevier lakes 

are the sole remnants of the former great body of water. The recession has uncovered the 

great expanse of lake beds that underlie the intermontane plains and constitute the fertile 

lands at the base of the Wasatch Mountains, and has also exposed the remarkable shore 

phenomena that testify to the history of Lake Bonneville, so completely worked out by 

Gilbert.

The Bonneville basin is preeminently characterized by its many shore lines (PI. Ill, 5), 

the highest of which impinges against the mountains and the lowest of which that can be 

recognized incloses the area covered by the lake sediments. Through a vertical interval 

of 1,000 feet the story of the rise and fall of this body of water is recorded by the superposition of shore line upon lake sediment and of lake sediment upon shore line. The record 

is not in all cases perfectly legible, but the main features are unmistakable.

The work of waves is recorded by cliffs and wave-cut terraces, from which the debris 

was carried along the shore to make benches, bars, spits, and terraces. The streams loaded 

with the waste of the land areas deposited their burdens in the lake, the coarser detritus 

being laid down near shore while the finer sand and clay were carried far out before sedimentation occurred. Deltas were formed at the mouths of the larger creeks where so much 

de"bris was carried that the shore currents could not distribute it. Since the recession of
U. S. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. 157 PL. Ill

A. NORTHERN END OF UTAH LAKE. 

Oquirrh Mountains in background.

B. HEAD-GATE OF JORDAN AND SALT LAKE CITY CANAL, LOOKING SOUTH. 

Embankment at point of the mountain in background.
GEOLOGY. 13

the lake from its old shores the streams which formed the deltas have begun their destruction by cutting them in two in their progress toward the shrunken body of water.

The Bonneville is the most conspicuous of all the shore lines, not because of the relative 

duration of time during which it was formed but because being the topmost of the series, 

it emphasizes the contrast between the sharply carved subaerial erosion features of the main 

land and the broad horizontal lines due to the influence of the lake. Study of the levels 

of bars at this stage shows that the record is complex and that the water surface alternately rose and fell a few feet during the formation of the shore phenomena that mark the 

general Bonneville level.

Below the Bonneville there are a number of plainly marked shore lines which represent 

stages in the level of the lake when it was practically constant for relatively long periods. 

Of these shore lines the Provo is the most remarkable, for it records the longest occupancy 

of one approximate horizon of any of the stages of the lake. Its embankments are the 

most massive and its wave-cut terraces are the broadest, notwithstanding the fact that the 

lake at the Provo stage was considerably smaller than when the surface of the water was 

375 feet higher, its area having shrunk from 19,500 to approximately 13,000 square miles. 

The Provo shore line is characterized particularly by its deltas, which were formed at the 

mouths of all the larger streams that entered the lake.

The fall from the Bonneville to the Provo level was apparently without interruption and 

comparatively rapid. But below the Provo stage there are remnants of shore lines and 

terraces at a number of horizons that record temporary halts of greater or less extent in the 

gradual shrinkage of the lake.,,( The most conspicuous of these lower shore lines, at an 

elevation of approximately 750 feet below the Bonneville level, has been named the Stansbury shore line, from its prominent development on Stansbury Island, but the others have 

not been correlated. As many as ten distinct shore lines can be traced on the west side 

of Jordan Narrows.

In connection with the different shore lines it is of interest to note that Gilbert has found 

evidences at a few localities of oscillations of the lake level between the Provo and Bonneville horizons, which appear to record halts in the rise of the lake as it approached its 

maximum. This is unusual, for most of the observed shore phenomena were formed during 

the retreat of the lake.

Local deposits of calcareous tufa occur associated with the various shore lines, but are 

most abundant at the Provo horizon. The tufa appears to have been deposited by precipitation from the lake waters due to aeration of the waves, especially during storms, and consequent loss of carbon dioxide by which the carbonate of lime was held in solution. The 

tufa occurs as a cement to gravel and as a more concentrated deposit, from a few inches to 

a few feet in thickness, coating exposed surfaces.

Below the Provo horizon, lake beds consisting of subhorizontal or gently lakeward-sloping 

sediments are associated with shore deposits until, as the valley bottom is approached, 

shore markings become indistinct and the lake beds prevail. The deposits of yellow clay 

and white marl previously mentioned as being widely distributed in the Bonneville basin 

apparently are not typically developed in the bay of the old lake, which occupied the area 

under consideration. A number of deep wells have been sunk into the valley deposits and 

their records indicate the general composition of the sediments (PI. V). The beds are at 

least 2,000 feet thick, and consist of gravel, sand, and clay, which constitute the reservoirs 

in which ground water is stored.

CLIMATE.

Weather observations have been systematically recorded at Salt Lake City for thirtyone years, and at near-by stations, including Provo, Thistle, Heber, and Park City, for 

eight to fourteen years. The most important meteorologic data, compiled from reports of 

the United States Weather Bureau, are summarized in the following tables, which give 

details of precipitation, temperature, wind velocity, humidity, and evaporation, on which 

the supply of underground water directly depends.
14 UNDERGROUND WATER IN VALLEYS OF UTAH.

PRECIPITATION.

Monthly and annual precipitation at Salt Lake City, 1875 to 1904- 

[Inches.]

Year.

1875..............

1876..............

1877..............

1878..............

1879..............

1880..............

1881..............

1882..............

1883..............

1884..............

1885..............

1886..............

1887. .............

1888..............

1889..............

1890..............

1891..............

1892..............

1893..............

1894..............

1895. .............

1896..............

1897..............

1898..............

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

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

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

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

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

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

Mean ......

Jan.

L23

.87

1.07

1.87

.29

1.24

1.60

1.47

.71

1.48

1 91

2.36

1.52

.73

3.07

.74

1.61

.82

1.31

1.32

1.26

1.16

.58

.84

.44

.95

.80

2.11

1.45'

1.44

Feb.

0 79

1 CO

.38

3.49

.71

1.02

.42

79

9 9?

1 W

1.36

.81

2.05

.76

.68

1.64

.83

.85

.69

3.81

.38

2.98

1.30

1.77

1.17

.82

2.25

1.33

Mar.

f> fit

4 Oft

2 93

.67

,*Q

QQ

1.12

1 7^

3.69

2.60

OK

2 1ft

1.64

1.12

4.66

2.21

1.73

.81

1.99

2.20

1.71

2.93

.33

2.48

1 99

1.35

3 QQ

2.03

Apr.

i i^n

2 09

2.14

2.63

3.26

2.37

2

Q7

2 Q9

2 SO

3.47

d 4?

i 07

99

1.52

.94

1 49

1 90

2.72

1.67

.73

2.53

2.00

1.30

.81

2.91

.87

3.69

1.11

2.20

2.21

May.

2 91

A Ort

3.49

.10

1.85

2.55

.26

Oft

1 7ft

9 4Q

.06

70

34

2.97

.16

.72

1.22

2.29

3.67

.98

4 19

2.50

.44

4.27

QQ

3.55

3.08

1.62

June.

0 90

09

.80

.35

1.34

.01

.28

9 94

qq

.33

2.67

Q7

Oft

.01

.32

1.21

.04

1.38

.99

.25

.52

1.45

.96

.08

.49

.37

.74

.27

.79

July.

1.01

00

.02

.07

.20

.21

30

.10

.27

.58

T.

.08

.02

.47

T.

1.19

.82

.42

1.35

.69

.18

.42

.32

.31

.56

.14

.59

.53

Aug.

O OK

92

.28

.81

.06

.74

1.61

1.61

.62

.73

.90

.59

69

.63

.92

.79

.46

.05

.71

.87

.02

1.47

.33

1.35

1.06

.72

1.22

.15

.43

.28

.72

Sept.

1 99

.42

.90

3.15

.01

.56

.37

.13

1 91

1.29

1.88

.55

.51

.52

T.

1.19

.12

1.30

2.87

.95

.52

.48

.15

T.

1.44

.66

.05

.84

.12

.93

Oct.

1.36

Q 97

2.41

1.39

1.62

.40

2.19

2.89

2.24

.36

.59

1 98

30

80

3.85

1.44

1.26

1.58

1.02

1.01

.24

.70

1.91

1.57

2.85

1.99

.98

.52

.81

1.18

1.54

Nov.

K Of

(41

1.02

.63

.32

1.17

1.44

u

1.78

.50

3.10

.25

1.04

T.

.90

.72

l.'lS

.28

2.44

3.15

1.19

1.95

1.52

1.40

.92

1.24

2.21

.00

1.36

Dec.

2 03

1 Sift

1.11

.11

3.08

1.90

1 94

.92

2.12

.92

1.27

1 tt

4.37

.42

2.19

2.35

2.37

1.28

.89

.84

1.47

1.28

.61

.16

1.16

1.31

.51

on

1.64

Annual.

<>o f\A

91 9G

16.35

19.75

13.11

16.88

15.98

14.24

17.52

21.69

18.89

11.66

13.62

18.46

10.33

15.92

14.08

17.35

15.27

11.95

18.42

16.74

16.09

17.57

11.53

16.08

11.41

14.62

16.31

16.19

Monthly and annual precipitation at Park City, 1899 to 1904- 

[Inches.]

Year.

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

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

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

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

1903..........!...

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

Jan.

0.93

2.24

1.90

3.88

2.15

Feb.

1.87

2.35

1.18

1.34

5.00

Mar.

0.38

3.15

4.04

2.60

7.85

Apr.

3.56

1.92

1.96

95

1 £Q

May.

0.30

1.50

.67

9 SQ

2.44

June.

T

.0.20

T.

July.

0.10

.90

Aug.

0.32

1.40

1.99

Sept.

2.23

.45

.92

Oct.

0.90

.18

.30

Nov.

n on

3.50

1.40

.55

.00

Dec.

1.80

1.30

2.20

.95

Annual.

15.39

17.89
CLIMATE.

Monthly and annual precipitation at Provo, 1899 to 1904:

15

Year.

1 RQQ

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

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

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

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

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

Jan.

i id

.45

.22

.35

2.65

1.72

Feb.

2

QQ

.35

2.06

1.12

.65

2.27

Mar.

2.45

.05

1.09

1.30

1.80

3.75

Apr.

0.39

1.65

.29

2.14

.51

1.56

May.

1 37

.32

.39

.36

2.69

2.11

June.

0.18

.10

.30

.42

July.

T.

0.11

.39

.39

Aug.

0.20

.42

.45

Sept.

0.00

1.13

......

......

.72

.04

Oct.

2.79

.66

T.

.68

.55

1.56

Nov.

0.94

3.50

.85

1.55

1.14

.00

Dec.

1.05

.12

.98

1.28

.49

1.05

Annual.

.........

12.31

15.32

Monthly and annual precipitation at Heber, 1899 to 1904- 

[Inches.]

Year.

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

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

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

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

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

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

Jan.

2.95

1.06

2.20

.50

2.17

2.10

Feb.

5.85

1.50

1 03

.07

Q no

Mar.

3.00

.34

1.56

1.46

1.95

3.48

Apr.

0.89

9 <n

.31

1.88

.78

.96

May.

1.14

.16

1 79

dQ

1.42

June.

0.97

.20

08

.37

.25

.73

July.

1.61

.25

4O

.15

69

9Q

Aug.

2.10

.31

2 ftA

en

ft9

.88

Sept.

0.15

1.20

.16

.45

1.17

.16

Oct.

3 20

1.47

1.70

.45

.76

1.22

Nov.

0.85

4.42

1.40

1.77

1.90

.00

Dec.

1.55

.22

1.50

1.04

1.33

1.91

Annual.

14.26

13.66

15.29

10.09

13.32

16.74

Monthly and annual precipitation at Thistle, 1899 to 1904- 

[Inches.]

Year.

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

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

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

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

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

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

Jan.

1.60

OA

1.90

1.90

Feb.

2.40

.47

2.35

2.05

1.55

Mar.

1.30

.00

2.40

2.00

Apr.

0.05

1.77

1.15

2.23

1.75

.90

May.

0.88

.05

.85

.35

1.60

2.65

June.

T.

0.10

.05

00

.35

July.

0.10

.11

.35

.53

.32

Aug.

0.46

3.05

.20

.10

.46

Sept.

1 00

OE

DC

.66

1.90

Oct.

0.40

7E

1.15

.41

1.43

.27

Nov.

2.08

1 Sfi

.93

9 1fl

.80

.00

Dec.

O QA

2.00

1.45

1.40

1.50

Annual.

7 10

13.89

TEMPERATURE.

Mean monthly and annual temperature at Salt Lake City, 1873 to 1904-

January..................................... 27.9

February.................................... 33.0

March .......................................41.6

April.

May.. 

June.. 

July..

49.5

57.8

67.0

75.5

August...................................... 74.8

September................................... 64.3

October..................................... 52.3

November................................... 39.8

December................................... 32.7

Annual................................ 51.4

Mean monthly and annual temperature at Provo, 1890 to 1904-

January..................................... 26.6

February.................................... 29.3

March....................................... 39.3

April........................................ 49.1

May......................................... 58.0

June......................................... 64.7

July......................................... 73.2

August...................................... 70.7

September.................................. 59.8

October..................................... 48.7

November................................... 38.4

December................................... 29.2

Annual................................ 49.2
16 UNDERGROUND WATER IN VALLEYS OF UTAH. 

Monthly maximum temperature at Salt Lake City, 1899 to 1904-

Year.

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

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

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

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

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

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

Jan.

54

57

51

43

53

48

51

Feb.

51

55

55

62

42

66

55

Mar.

67

72

65

58

65

63

65

Apr.

80

78

79

78

80

78

79

May.

83

89

88

88

86

83

86

June.

96

101

90

OS

91

92

95

July.

97

99

101

Qfi

96

97

98

Aug.

91

94

95

08

08

94

95

Sept.

91

88

86

92

92

92

90

Oct.

73

76

85

81

77

83

79

Nov.

63

68

67

70

70

66

67

Dec.

59

56

vt

58

45

55

55

Monthly minimum temperature at Salt Lake City, 1899 to 1904-

Year.

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

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

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

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

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

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

Jan.

16

20

4

15

7

11

Feb.

in

10

15

19

10

Mar.

20

26

25

21

14

19

91

Apr.

30

^fi

. 32

25

30

27

May.

oc

4n

43

35

33

36

35

June.

04

47

40

42

54

44

44

July.

51

53

49

43

46

51

40

Aug.

46

52

56

52

48

46

50

Sept.

46

32

39

35

37

38

38

Oct.

30

27

36

36

32

28

32

Nov.

OQ

28

29

21

17

26

25

Dec.

g

11

15

14

7

10

WIND VELOCITY.

Average wind velocity at Salt Lake City, 1900 to 1904- 

[Miles per hour.]

Year.

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

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

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

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

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

Mean ......

Jan.

3.4

5.0

3.8

4.8

4.1

4.2

Feb.

5.2

4.0

5.5

4.5

6.3

5.1

Mar.

. 6.3

6.2

6.8

7.3

6.7

Apr.

7.3

7.8

6.7

7.3

7.2

7.2

May.

6.8

7.3

7.1

6.1

6.8

6.8

June.

6.5

6.6

6.7

6.6

6.5

7.0

July.

6.0

6.3

6.7

7.2

6.5

6.5

Aug.

6.4

5.8

6.5

6.2

5.7

6.1

Sept.

6.5

7.0

6.7

6.3

6:0

6.5

Oct.

6.5

5.0

5.7

5.3

5.4

5.6

Nov.

50

4.9

6.0

5.4

4.7

5.2

Dec.

4.5

4.8

4.7

3.7

4.9

4.5

Annual.

5.9

5.9

6.1

5.8

6.0

5.9

HUMIDITY.

Mean relative humidity at Salt Lake City, 1900 t« 1904- 

[Per cent.]

Year.

1960..............

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

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

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

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

Jan.

78

69

83

73

75

76

Feb.

65

73

74

67

Mar.

40

55

58

CO

64

54

Apr.

59

42

48

44

4fi

18

May.

41

44

43

48

49

45

June.

25

36

31

38

38

34

July.

24

26

27

30

33

28

Aug.

24

39

27

' 28

38

31

Sept.

36

30

32

38

34

34

Oct.

48

50

40

45

53

47

Nov.

62

57

56

64

45

57

Dec.

63

71

65

75

60

67

Annual.

47

49

48

51

51

49
CLIMATE. 17

EVAPORATION.

Depth of evaporation at Utah Lake a from August, 1903, to August, 1904.

[Inches.]

1903. 

August...................................... 8. 40

September................................... 6.78

October..................................... 3. 86

November................................... 2.50

December.................................... 1.50

1904. 

January..................................... 1.50

1904 Continued.

February..................................... 2.00

March...................................... 3.50

April....................................... 4. 63

May.....-.....-.-....--.--...---........... 7.72

June........................................ 8.80

July........................................ 9.41

Total................................. 60.60

SUMMARY.

The climate of the valleys of Utah Lake and Jordan River is controlled by their location 

in the central eastern part of the Great Basin, but is modified somewhat by the proximity

FIG. 1. Diagram showing variation of annual precipitation at Salt Lake City.

of Utah and Great Salt Lakes and the Wasatch Mountains. The tables show that the 

climate is characterized by low annual precipitation, moderate temperature, moderate 

wind velocity, low relative humidity, and considerable evaporation.

The mean annual precipitation at Salt Lake City is 16.19 inches, ranging between a maximum of 23.64 inches in 1875 and a minimum of 10.33 inches in 1890. Since 1900 it has 

averaged 2.2 inches below normal (fig. 1). Only about 18 per cent of the annual total

a Computed from daily measurements of a tank 3 feet in diameter. Tests were made by the engineer of Salt Lake City from 1901 to 1903, and since then they have been kept up by the Reclamation 

Service under G. L. Swendsen. See also Newell, F. H., Fourteenth Ann. Kept. U. S. Geol. Survey, 

pt. 2,1894, p. 154.

IRR 157 06 2
18 U]STDERGEOU]srD WATER IN VALLEYS OF UTAH.

occurs from June to September, and for these four months amounts to less than 3 inches. 

Between October and May the variation is not marked, but the greatest precipitation 

occurs in March and April (fig. 2). This precipitation is unUsually high for the Great 

Basin. The Wasatch Mountains serve to condense the moisture, originally derived in large 

part from the westerly winds from the Pacific Ocean, that remains in the air after crossing 

the Sierra Nevada.

Probably the precipitation is greater on the summits than at the stations where records 

have been kept, but data are not available. The melting snow of the winter's accumulation 

is the chief supply of the streams of the area under consideration.

The mean annual temperature of Salt Lake City is 51.4°. The mean monthly maximum 

ranges from 98° in July to 51° in January, while the mean monthly minimum varies between 

10° in December and February and 50° in August.

The dryness of the atmosphere is indicated by the mean relative humidity of 49 per cent, 

varying from 28 per cent in July to 76 per cent in January, and by the amount of evaporation from a free water surface, which, according to the latest measurements, is about 60

Per 

cent 

14

12 

10 

B 

6 

4 

Z 

o

Jan.

-

Feb. Mar Apr May June

*

Juty

*

Aug.

*

Sept.

'-

t

Oct.

&

«

Nov. Dec.

inches 1,44 '-3.3 2.03 221 t.62 .79 .S3 .72 .53 1.54 1.36

FIG. 2. Diagram showing mean monthly precipitation at Salt Lake City.

Mean 

Annual

1.64 16.19

inches a year. Yet the climate is not nearly as dry as in other parts of the Great Basin. 

The dryness lessens the effect of the summer's heat, so that the "sensible temperature" is 

not so great as would be Suggested by the thermometer, being modified by the cooling 

effects of evaporation.

' HYDROGRAPHY. 

STREAMS TRIBUTARY TO UTAH LAKE AND JORDAN RIVER.

Seepage from surface, streams, as shown hereafter, is the most important source of supply 

of underground water in the valleys of Utah Lake and Jordan River. A summary of 

discharge measurements therefore throws important light on the subject and, with other 

data, furnishes facts for roughly estimating the amount of water available for the annual 

replenishment of the underground reservoirs. The figures here given have been compiled 

from records of the United States Geological Survey and from data obtained through the 

courtesy of the city engineer of Salt Lake City, and are now published for the first time.

Satisfactory measurements of the flow of all the streams in the two valleys have not been 

made. However, records have been kept for a number of years of the discharge of several 

of the more important, and the combined data, with due consideration for varying conditions, may be taken as typical of the drainage of the entire watershed. The measure-
HYDROGRAPHY.

ments were made at the mouths of the canyons. Below these points, during the irrigation 

season, the water is diverted and conducted over the valley in an intricate system of 

ditches, so that the stream beds in their lower stretches are then often dry. During the 

flood season the streams discharge directly into either Utah Lake or Jordan River. Following are tables of monthly measurements for 1904, to which annual summaries for several 

years are added where figures are available:

Estimated discharge (at mouths of canyons') of streams tributary to Jordan River and Utah

Lake.

CITY CREEK. 

[Drainage area, 19 square miles.]

Date.

1904.

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

May................

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

NOT ember

Year..........

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

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

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

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

Maximum.

Sec.-feet. 

6.7

7 Q

11. a

28.8

70.1

26.5

15.3

11.4

9 3

8.7

9.2

70.1

63.1

58.2

72.0

' 31.3

121.9

Discharge

Minimum.

Sec.-feet: 

6.0

6.0

7.3

11.0

28.8

26.6

16.2

9 A

8.7

8.2

7.7

6.0

4.3

3.6

5.0

5 A

3.2

Mean.

Sec.-feet. 

6.2

6.6

8.1

22.1

55.6

39.2

19.7

13.4

10 4

Q 1

8.5

8.0

17.2

13.0

Q 8

20.0

Total.

A cre-feet. 

381

380

516

1,315

3,419

2,332

1,211

824

619

609

506

492

12,604

9,440

8,910

9,251

7,054

14,491

Per

square 

mile.

Sec.-feet. 

0.326

.347

.442

1.160

2.926

2.063

1.037

.705

.547

47Q

.447

.421

908

.685

647

.668

.517

1.053

Run-off.

Depth.

Inches. 

0.376

.374

.510

1.294

3.373

2.301

1.195

.813

.^10

.551

499

.485

12.381

9.323

8.811

9.126

7.040

14.306

Relation 

to rainfall.

Per cent. 

20.9

10.3

8.6

66.7

122.2

852.2

202.5

71.9

508.3

46.7

53.9

61.2

63.1

69.5

53.9

52.5

80.1

Rainfall.^

Inches. 

1.80

3.62

5.92

1.94

2.76

.27

.59

1.13

.12

1.18

.00

.90

20.23

14.77

12.67

16.94

13.41

17.85

EMIGRATION CREEK. 

[Drainage area, 19 square miles.]

1903.

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

Year..........

6.3

.8

11.7

12.8

19.3

18.1

4.0

1.7

1.1

2.0

3.2

.8

. 19.3

0.7

.4

3.7

5.5

4.0

.6

.6

1.1

1.0

.6

.4

1.1

.6

3.0

8.0

9.5

8.6

2.8

1.0

.8

1.2

1.3

3.2

68

33

184

476

584

512

172

61

48

74

77

43

2,332

0.058

.032

.158

.421

.500

.453

.147

.053

.042

.063

.068

037

.169

0.069

.033

.182

.470

.576

.505

.169

.061

.047

.073

.076

.043

2.304

2.3

3.1

9.2

45.6

17.9

136.5

120.7

14.2

5.3

5.5

5.9

15.6

2.95

1.0!

1.9"

i.o;

3.2:

.3'

1<

.4

.8?

.5,

1.3!

.7;

14.7'

a The record of rainfall given under City, Emigration, Parleys, and Mill creeks is the mean precipitation for Salt Lake City and Park City; that under American Fork and Proyo River is for Prove and 

Heber; that under Spanish Fork is for Provo, Thistle, and Soldiers Summit.
20 UNDERGROUND WATER IN VALLEYS OF UTAH.

Estimated discharge (at mouths of canyons') of streams tributary to Jordan River and Utah

Lake Continued.

PARLEYS CREEK. 

[Drainage area, 50 square miles.]

Date.

1904.

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

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

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

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

iQftl

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

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

]

Maximum.

Sec.-feet. 

9 2

]8. 1

QQ q

207.3

208.5

137.5

11.8

10.8

133.7

95.3

109.5

39.0

Discharge.

Minimum.

Sec.-feet. 

4.8

4.2

9 4

88.1

28.5

19.5

11.8

9 4

11.8

8.8

2

C

2.2

q n

2.9

4.0

Mean.

Sec.-feet. 

7.1

10.3

19 6

123.2

168.5

11.4

8.3

'38 9

20.5

16.7

19 y

12.6

59.8

Total.

Acre-feet. 

437

592

1,205

7,331

984

679

613

28,240

14,879

12, 116

14,490

9,0^8

Per 

square 

mile.

Sec.-feet. 

0.142

.206

quo

2.464

1 05°

.522

.d20

.228

.258

.206

.166

.777

.410

.334

.398

.251

Run-off.

Depth.

Inches. 

0.164

.222

2.749

3.886

.602

369

254

.297

.230

.191

5.581

4.544

3.431

14. 884

Relation 

to rainfall.

Per cent. 

9.0

6.1

7.6

141.8

140.8

434.8

102.0

32.7

211.7

25.2

21.2

52.3

37.8

35.9

25.6

83.4

Rainfall.

Indies. 

1.80

3.62

1.94

2.76

.27

.59

1.13

.12

1.18

.00

.90

20.23

14.77

12.67

16.94

13.41

17.85

MILL CREEK. 

[Drainage area, 21 square miles.]

1904. 

January. ...........

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

November

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

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

1899

13.0

55 9

29.7

16.8

15.9

14.0

13.0

11.3

58.2

34.4

QQ C

47.4

30.8

66.0

6.6 

3.7

11.3

25.1

29.7

13.0

13.0

1.0

2.9

1.9

1.4

1.4

9.9 

9 9

11.2

18.8

40 9

14 9

15.0

13.7

12.4

8.6

18.5

12.3

19 1

19 Q

11.5

609 

569

6S9

916

893

842

738

529

13,464

8,916

8,753

9,391

8,296

0.471 

.471

.486

895

1 971

1,948

1.224

.710

.714

.652

.590

.410

.878

.586

W5

.549

.932

0.543 

508

.560

999

2.272

.819

.797

.752

.658

.473

11.965

7.964

7.814

8.383

7.466

12. 669

30.2

9.4

51.5

82.3

239.2

72.5

664. 2

63.7

52.5

59.1

53.9

61.7

49.5

55.7

77.1

l.« 

3.65

5. &

1.94

2.7(

.2"

.5£

1.K

.12

1. If

.OC

.90

20. 2:

14.7"

12.65

16.94

13. 4]

17. 8f
HYDROGRAPHY. 21

Estimated discharge (at mouths of canyons') of streams tributary to Jordan River and Utah

Lake Continued.

BIG COTTONWOOD CREEK. 

[Drainage area, 48 square miles.]

Date.

1902.

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

December

Year..........

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

Maximum.

Sec.-feet. 

27 6

2S 4

27.7

142.9

369.7

309.5

92.3

OQ A

369.7

407.3

Discharge

Minimum.

Sec.-feet. 

13.6

17.2

27.0

108 9

91 7

28.4

21.4

13.6

11.3

Mean.

Sec.-feet. 

90 -i

24 2

24.6

70.4

210.2

62.2

27 9

62.0

68.3

Total.

Acre-feet. 

1,421

1,344

1,513

4,189

12,923

11,574

3,825

2,029

1,661

1,402

44,976

49,639

Per 

square 

mile.

Sec.-feet. 

0.481

Kf\A

.512

1.470

4.380

4.050

1.300

.688

.581

.517

.475

1.292

1.422

Run-off.

Depth.

Inches. 

0.555

.590

1.640

5.050

4.519

1.499

.793

.648

.632

.577

.548

17. 576

19.381

Relation 

to rainfall.

Per cent.

Rainfall.

Inches.

AMERICAN FORK. 

[Drainage area, 66 square miles.]

1904.

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

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

Year..........

17

16

24

109

379

310

147

64

43

41

34

28

379

15

15

' 15

23

95

131

66

35

34

28

18

15

16.1

15.4

19 1

46.9

216.0

201.0

95.3

52.8

38.1

35.9

30.0

25.3

66.0

990

886

1,174

2,791

13,280

11,960

5,860

3,247

2,267

2,207

1,785

1,556

0.244

.233

.289

.711

3.27

3.05

1.44

.800

.577

.544

.454

.383

1.00

0.281

.251

.333

.793

3.77

3.40

1.66

.922

.644

.627

.507

.442

13.62

14.7

9.5

9.2

63.0

183.0

596.0

488.0

140.0

644.0

45.1

29.8

85.0

1.91

2.64

3.62

1.26

2.06

.57

.34

.66

.10

1.39

.00

1.48

16.03
22 UNDERGKOCND WATEE IN VALLEYS OF UTAH.

Estimated discharge (at mouths of canyons') of streams tributary to Jordan River and Utah

Lake Continued.

PROVO RIVER. 

[Drainage area, 640 square miles.]

Date.

1904.

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

1898.................

1895.................

Maximum.

Sec.-feet.

9QO

861

667

680

184

146

ion

205

2,153

1,212

9 fiAH

1,760

Discharge

Minimum.

Sec.-feet. 

196

331

461

S71

134

80

79

113

113

79

146

225

Mean.

Sec.-feet.

373

388

486

1 145

14Q

386

386

a 571

423

Total.

Acre-feet. 

i ^ nnn

91 dfifl

OO OCfl

28,920

70,410

67,300

9 1 £9

6,962

6 948

8 971

9,162

97o onn

Per 

square 

mile.

Sec.-feet. 

O.oSl

fiftfi

1 79

1.77

.316

.233

.183

.177

.217

.233

.604

.60

89

.66

Run-off.

Depth.

Inches. 

0.439

g9g

699

847

2.06

1 98

364

269

.204

.204

.242

269

a20

8.19

9 07

Relation 

to rainfall.

Per cent. 

23

24

19

67

100

347

107

18

* 51

49

68

62

Rainfall.

Inches. 

1 91

2.64

3.62

1.26

2.06

.57

.34

.66

.10

00

1.48

16.03

16.71

"14.63

a Approximate.

SPANISH FORK.

[Drainage area, 670 square miles.]

1904.

May................

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

113

126

240

229

415

255

121

Q9

69

69

77

415

58

58

63

110

236

111

80

67

65

65

4Q

40

40

77.6

79 1

85.8

174.0

343.0

94.6

75.8

68.0

61.5

54.3

112.0

10,350

9,640

5,817

4,046

4,169

3,660

3,339

81,370

.118

.128

.260

.512

.242

.141

.113

.101

.101

.092

.081

.167

0.134

.127

.148

.290

.590

.270

.163

.130

.113

.116

.102

.093

2.28

8.1

7.4

4.4

28.0

25.0

41.0

39.0

19.0

13.0

11.0

8.7

15.4

1.66

1.71

3.36

1.02

2.33

.66

.42

.69

.85

1.01

.00

1.07

14.78

Comparison of the discharge of several streams shows marked differences. For instance, 

during 1901 and 1902, the only years when complete measurements of both Parleys and 

Big Cottonwood creeks are available, the discharge of Big Cottonwood (drainage area, 48 

square miles) averaged 47,308 acre-feet, while that of Parleys, with a drainage area slightly 

greater (50 square miles), averaged only 13,303 acre-feet. Again, during 1904 the discharge of City and Emigration creeks, each having drainage areas of approximately 19 

square miles, amounted, respectively, to 12,604 and 2,332 acre-feet. Provo and Spanish 

Fork rivers also afford similar results. The drainage area of Provo River (640 square miles)
HYDROGRAPHY. 23

is slightly less than that of Spanish Fork (670 square miles), yet the discharge of the 

former in 1904 was more than three times that of the latter.

It will be noticed that the flows of Spanish Fork and of Emigration Creek, streams 

which in the above comparisons figured poorly, have much in common, though their drainage areas differ greatly. The flow of the two streams, expressed in second-feet per square 

mile of their drainage areas, averaged 0.167 for Spanish Fork and 0.169 for Emigration Creek, which may be compared with an average of 0.746 for City Creek and 0.69 for 

Provo River. The amount of discharge, expressed in depth of inches, over the watershed is 

2.28 for Spanish Fork 2.30 for Emigration Creek, and 10.33 for City Creek. The run-off is 

approximately 15 per cent of the precipitation for Spanish Fork and Emigration Creek, 

and about 63 per cent for City Creek.

These and other discrepancies are due to a complex set of causes, chief of which are differences in precipitation, topography, vegetation, soils, and rocks of the several drainage areas, 

and the care that is taken to prevent fires, grazing, and destruction of timber on the watersheds. Though in general the main streams in the Wasatch Mountains have many features 

in common, the valleys of some of them are narrow and steep, while those of others are 

broader and more open. Some valleys are better adapted than others, by configuration 

and position, to collect and keep snow. Some of the streams head in lakes, while others do 

not. All are poorly clothed with trees, but some are less fortunate in this respect than others. 

The soil covering in general is thin, particularly on the steep slopes and in areas where the 

absence of much vegetation allows the products of rock disintegration to be washed into the 

valleys. But where the slopes are comparatively gentle and vegetation protects the accumulated rock debris, more of the precipitation is absorbed and (escaping flood discharge) 

seeps slowly into the valleys to maintain the perennial flow of the streams. Differences 

in the porosity of the bed rocks and in the character and quantity of debris in the stream 

beds, whereby greater or less amounts of water are absorbed, also greatly influence the

amount of run-off.

UTAH LAKE.

Utah Lake is fed from several sources, including surface streams, seepage, springs beneath 

the lake, and the precipitation that falls upon it. The measurable factors were determined

\

21

n

FIG. 3. Diagram showing fluctuations of the surface of Utah Lake, 1889-1904.
24 UNDERGROUND WATER IN VALLEYS OF UTAH.

for the period August 1903, to August, 1904, under the direction of G. L. Swendsen,« of the 

United States Reclamation Service, who found that of the total supply of 604,010 acrefeet only 471,140 were contributed by rainfall on the lake and by the measurable surface 

streams, leaving an unmeasured supply of 132,870 acre-feet. This -considerable amount 

appears to be contributed by seepage and by springs, some of which have recently been 

found in the northwestern part of the lake.

The surface of the lake is subject to considerable variation in elevation in consequence 

of the changing relations of evaporation, precipitation, inflow, and outflow. Fig. 3, prepared by the Reclamation Service, shows fluctuations of the surface from 1889 to 1904.

There is a seasonal variation of 1 to 4 feet, ranging from a minimum in the late fall to a 

maximum in late spring and early summer. The diagram also shows the variation in 

the mean level of the lake. The lowest elevation shown occurred in 1903, when the lake 

was about half a foot lower than it was in 1889. Following 1889 was a period of ten years 

of relatively high water.

JORDAN RIVER.

During the last few years anomalous conditions have existed at the outlet of Utah Lake. 

The water level of the lake has fallen so low that the normal flow has ceased, and in order to 

supply the canals in Jordan Valley it has been necessary to resort to pumping. Accordingly a pumping plant has been in operation at the head of Jordan River since August, 1902. 

(PI. IV, A.)

The following table of discharges has been prepared by Mr. J. Fewson Smith, jr., water 

commissioner:

Discharge of Jordan River and the canal systems in Jordan Narrows, and of Jordan River at 

pumping plant, April to October, 1904-

[Acre-feet.]

Month.

1904. 

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

May................

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

Total.........

North 

Jordan.

963

2,970

3,384

3,233

753

13,965

East 

Jordan.

650

3,036

5,369

5,186

5,280

27,142

City.

 

452

3,199

3,090

399

9,109

South 

Jordan.

647

5,167

6,648

5,407

5,031

5,357

2,134

30,391

Utah and 

Salt 

Lake.

720

4,150

7,878

6,719

7,110

7,992

3,367

37,936

Jordan 

River at 

weir.

75

2,911

4,225

3,894

3,668

2,767

310

17,850

Sum of preceding.

2,092

16,823

27,874

27,972

27,318

25,431

8,883

136,393

Jordan 

River at 

pumping 

plant.0

222

18,090

25,110

25,210

24,720

23,330

8,363

125,045

a Figures furnished by G. L. Swendsen.

From these figures it appears that the gain in the flow of Jordan River between the pumping plant and the intake of the canals in Jordan Narrows, a distance of about 13 miles, April 

to October, 1904, was 11,348 acre-feet. The gain is partly supplied by seepage and partly 

by the flow of wells and springs. Between Jordan Narrows and the head of North Jordan 

canal, a distance of about 9 miles, Mr. J. Fewson Smith, jr., found that the seepage into Jordan River between May and September, 1904, amounted to 13,789 acre-feet.

oThe writer acknowledges his indebtedness to Mr. Swendsen for many courtesies extended, both in 

the field and office, during the prosecution of the work.
U. S. GEOLOGICAL SURVEY WATER-SUPPLY PAPER MO. 157 PL. IV

A, GATE AT HEAD OF JORDAN RIVER.

JB DEAD MAN'S FALLS, COTTONWOOD CANYON.
HYDROGRAPHY. 25

No systematic data have been collected below the head of North Jordan canal, but in 

December, 1904, the following measurements were made by Mr. Caleb Tanner and the 

writer:

Discharge of Jordan River and tributaries between Little Cottonwood Creek and the ford, in 

sec. 4, T. 1 N., R. 1 W., December 6-7, 1904.

Second-feet. 

Jordan River above mouth of Little Cottonwood Creek ........................................ 61.38

Little Cottonwood Creek........................................................................ 8.14

Flume at Taylorville roller mill................................................................. 39.0

Big Cottonwood Creek........................................................................... 51.2

Ditch south of Mill Creek........................................................................ 2.12

Mill Creek. ................^....................................................................... 23.94

Ditch, outlet of Decker Lake.................................................................... 2.93

Parleys Creek, north and south ditches......................................................... 8.78

Eighth South street ditch....................................................................... 0.C9

Total.................:.................................................................-.. 203.58

Jordan River below North Temple Street Bridge .....................................j.. 190.22 190.22

Loss between mouth of Little Cottonwood Creek and North Temple street............... 13.36

Outlet of Hot Springs Lake.............................................................. 7.64

Sewer ditch (estimate)................................................................... 7.50

Jordan River at ford, sec. 4, T. 1 N., R. 1 W.................................................... 214.00

Total............................................................................... 205.36 205.36

Gain between North Temple Street Bridge and ford...................................... 8.64

Loss in the flow of Jordan River, instead of expected gain, is thus shown between the 

mouth of Little Cottonwood Creek and North Temple Street Bridge at the time the measurements were made, while a slight gain is shown between the bridge and the ford in sec. 4, T. 

1 N., R. 1 W. It appears that the seepage drains into the tributaries rather than directly into 

Jordan River in the area where the tributary streams are numerous and that farther north, 

where there are fewer tributaries, a small amount of seepage drains directly into the river. 

How far these figures represent conditions the year round remains to be determined.

GREAT SALT LAJtE.

Except during a lapse from 1893 to 1896, instrumental records of the surface fluctuation of Great Salt Lake have been kept since 1875, -and there is evidence less exact dating 

back to the survey of the lake by Stansbury in 1849-50. When that survey was made the 

level of the lake was extremely low, and since then it has varied considerably. In 1869 

the water surface was approximately 11 feet higher than it was in 1850; a comparatively 

low stage was reached in 1873, after which the lake rose about 4 feet to a maximum in 

1876, about equal to that attained in 1869. In 1883 the lake was about 7 feet below the 

maximum; then it rose 4 feet until 1886, since when it has gradually fallen until now it is 

at an extremely low stage, about 15 feet lower than the maxima of 1869 and 1876. Fig. 

4 illustrates the changes since 1875.

Besides the irregular fluctuations there is a regular annual variation ranging between 1 

and 2 feet, the maximum occurring in June and the minimum in the winter- This annual 

variation is due to the changing relations of precipitation, inflow, and evaporation, high 

water occurring after the spring floods, and low water during the season of feeble stream discharge and after the period of excessive evaporation. The irregular variation of the 

past can be accounted for chiefly by changes in rainfall, the earlier maxima being associated with unusually large amounts of precipitation. The gradual decrease of late years 

in the volume of the lake, after allowing for recent dry seasons, is apparently due to 

largely increased irrigation, by which the inflow of surface streams has been checked
UNDEBGBOUND WATBE IN VALLEYS OF UTAH.

through diversion into ditches. Because of the considerable evaporation and transpiration incident to such use of the water, only a small per cent of the run-off reaches the

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lake, and with the spread of irrigation it may be expected that this cause will increasingly 

tend to keep the lake level at a low stage.
SOURCES OF GBOUND WATEB. 27 

UNDERGROUND WATER.

GENERAL CONDITIONS.

SOURCE.

The underground water supply in the valleys of Utah Lake and Jordan River, as is well 

known, is maintained by the snow and rain that fall on their drainage areas. In considering the sources of the supply, the precipitation tributary to Utah Lake and Jordan River 

can conveniently be divided into that on the mountains and that on the main valley.

It has been stated that the actual precipitation in the mountains probably exceeds the 

amount shown by the recorded data. Moreover, neither the rainfall nor the snowfall is 

evenly distributed. The precipitation is greater in the northern than in the southern half 

of the area under consideration, and in contiguous localities there are differences due to 

varying topographic conditions. More precipitation is likely to occur in the vicinity of the 

higher peaks, and in the mountain recesses that are well protected from the sun large quantities of snow linger long after the general mantle has disappeared.

Of the total precipitation on the mountains, part is evaporated, part joins the run-off, and 

part becomes underground water. Evaporation occurs either directly from snow, from 

a free surface of water, and from water contained in soils and brought to the surface by 

capillary action or indirectly by transpiration through the growth of plants. Of the portion which joins the run-off part runs directly out of the mountains, part flows to small 

lakes at the head of Big Cottonwood Creek and Provo River, and part is absorbed by the 

soil and rocks over which the streams flow and joins the subterranean store. A final portion 

of the precipitation on the mountains becomes underground water directly by absorption 

by the surface on which the rainfall occurs. Part of this underground water reaches the 

surface again by capillary action in the soils and by the life activity of plants and is finally 

evaporated; another part after remaining underground a shorter or longer time reaches 

the surface again by springs and seepage, and, joining the run-off little by little, maintains the 

perennial flow of the streams; another part joins the more permanent supply of underground 

water. It is impossible, because of the complexity of the subject and the lack of data, to 

state the amount of water which annually replenishes this more permanent supply of 

underground water, but the quantity is equivalent to the precipitation minus thfe^un-off 

and the amount evaporated. From the incomplete facts at hand it appears that the riihroff, 

measured at the mouths of the canyons, although varying greatly, approximates 50 per cent 

of the precipitation, but the total evaporation is unknown. Although exact figures repreresenting the amount evaporated can not be obtained, yet experiments on evaporation from 

snow, soils, and vegetation in the mountain areas would afford valuable data.

The amount of precipitation in the valley is better known, and the figures for Salt Lake 

City and Provo are typical. Here, as in the mountains, part of the precipitation joins the 

run-off, part is evaporated, and part becomes underground water; but there are practically no measurements of these different quantities. Direct run-off of the precipitation 

on the valley is comparatively small, owing to the open nature of the country and to the 

fact that no great accumulations of snow occur, and the seepage run-off probably constitutes the main amount. Evaporation from soils and vegetation dissipates probably the 

largest part of the rain that falls on the valley, especially during the summer. The increase 

of the more permanent underground water supply due to the rainfall on the valley is consequently small. A basis for judgment is furnished by comparing the condition of the 

valley east and west of Jordan River. Precipitation is perhaps slightly less in the western 

part of the valley, but the difference is not enough to cause the marked contrast. The scarcity of ground water within easy reach of the surface in the western part of the valley, compared with the abundance easily accessible in the eastern part, implies that the rainfall on 

the valley contributes a proportionally small amount to the store of underground water. 

Existing conditions are due to the fact that on the west only a few feeble and generally 

intermittent streams are tributary to the valley, whereas on the east a number of large 

perennial streams flow from the Wasatch Mountains, supplying water that is distributed
28 UNDERGROUND WATER IN VALLEYS OF UTAH.

over the valley by canals. Seepage from these streams is the main source of underground 

supply in the valleys.

The amount of water contributed to the valleys by streams from the Wasatch Mountains 

is capable of rough numerical statement. The drainage area in these mountains tributary 

to Jordan Valley is approximately 220 square miles, and measurements of five creeks in that 

region, given in the section devoted to hydrography, show an average flow of 0.66 secondfoot per square mile of watershed. This amount is equivalent to a stream discharging 145 

second-feet, or a total amount approximating 105,000 acre-feet a year. The average of 

measurements of Provo River and Spanish Fork in Utah Lake Valley gives a flow of 0.43 

second-foot per square mile of drainage area, which, assuming the flow to be derived from 

rainfall on a watershed of about 1,670 square miles, is equivalent to a stream discharging 718 

secoryl-feet, amounting to 520,000 acre-feet a year.

Of this amount of water annually contributed by streams to the valleys of Utah Lake 

and Jordan River, part permanently runs off and is added to the supply of Great Salt Lake 

by Jordan River. This quantity has not yet been systematically measured, but it is estimated to average about 200 second-feet. The residue either evaporates, directly and indirectly, or becomes underground water. Unfortunately, no figures are available whereby 

the amount lost by evaporation can be estimated, so that the annual replenishment of the 

underground supply is unknown. Only the crude statement can now be made that, in the 

presence of influences sufficient to cause an evaporation of 60 inches a year from a free body 

of water, the amount which is not thus lost from a supply of somewhat more than 600 

second-feet joins the underground store.

Seepage measurements which have been made at different times in both valleys from 

creeks and ditches offer concrete demonstrations of the manner in which the underground 

supply is maintained. Only a few such measurements have been made in Utah Lake Valley, 

but it has been shown that in 1§ miles the Timpanogas canal lost slightly more than 25 per 

cent of the water taken in at its head.o Another set of measurements has been made on 

Provo River. The discharge a short distance above the mouth of the canyon was found to 

be 175.04 second-feet; at a station a mile west of Provo the river was dry, while the 

sum of several intermediate diversions amounted to 186.22 second-feet. The difference , 

11.18 second-feet. represents the return seepage from the vaiious canals. & In the valleys 

of creeks tributary to Jordan River more measurements have been made, of which those in 

Big Cottonwood and Mill valleys are typical. In Big Cottonwood Creek Valley Mr. E. R. 

Morgan selected for measurement two sections of the creek on which different conditions exist. 

In the upper section, immediately below the mouth of the canyon, the bed of the stream 

is composed of large loose bowlders resting on coarse gravel, and the land on either side is 

covered with comparatively scanty vegetation. In the lower section, below the head of 

Green ditch, the bed of the creek is comparatively smooth, and the land on both sides is irrigated and covered with abundant vegetation The loss in the first section, in a distance of 

2| miles, was 7.36 second-feet, a percentage of 22 6, while in the second section, also 2J 

miles long, the loss was only 0.30 second-feet, a percentage of 2.4.e In Mill Creek Valley 

Mr. Morgan also made measurements in two sections where different conditions exist. In 

one section, 2 miles long, he found a loss of 22.7 per cent; in the other, three-quarters of a 

mile long, he found a loss of 3.6 per cent.d

While seepage from the flow of the creeks and canals furnishes the chief supply of underground water to the valleys of Utah Lake and Jordan River, other sources are the underflow 

of the creeks at the mouths of the canyons, springs from bed rock, seepage at the base of 

the mountains, and the small addition, already mentioned, derived from rainfall on the valley. 

The underflow of the creeks at the mouths of the canyons is an important source, but the 

amount thus contributed is unknown. The quantity equals the remainder after subtracting the sum of run-off and evaporation from the precipitation, of which factors only the 

run-off is established, the precipitation being only approximately and the evaporation not 

at all known. The amount of the underflow can be directly determined, however, by a series

a Bull. U. S. Dept. Agric. No. 124, Office Expt. Stations, 1903, p. 123. 

6 Ibid., p. 126.

c Morgan, E. R., Irrigation in Mountain water district, Salt Lake County, Utah: Bull. U. S. Dept. 

Agric. No. 133, Office Expt. Stations, 1903, pp. 60-61. 

a Ibid., pp. 44-45.
u. s. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. 1s? PL. v

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WELL SECTIONS.

No. 1, Oregon Short Line well at Kaysville; No. 2, Southern Pacific Company's well at Strongs Point; 

Nos. 3-24, location shown on Pis VII and VIII.
SOURCE AND DISTRIBUTION. 29

of measurements which should be made in estimating the feasibility of constructing subsurface dams. The amount of water contributed to the valleys from bed-rock sources is 

also important. A remarkable series of thermal springs is associated with the great fault 

at the western base of the Waaatch Mountains. These occur at intervals along the entire 

extent of the range, and other warm springs, which may also be connected with faults, are 

located within the area under consideration. Association with faults suggests a deepseated origin, which accounts for the high temperature of the water. The last source of the 

valley water supply to be mentioned is the comparatively small amount which is derived 

by seepage from the base of the mountains from areas that are not drained by creeks.

DISTRIBUTION OF TTNDERGROTIin) WATER.

From the outline of the geology given on pages 7-13 it will be seen that the valleys of Utah 

Lake and Jordan River are occupied by a considerable but unknown thickness of gravel, 

sand, and clay derived from the disintegration of the adjacent mountains and deposited in 

the valley under alternating subaerial and lacustrine conditions. In general, the deposits 

are arranged in broad, sheet-like accumulations, the coafser-textured materials abounding 

adjacent to the highlands and the finer debris preponderating farther out. The beds lie 

practically flat in the center of the basins, but are inclined slightly away from their source, 

the attitude of deposition being practically unaltered. Conditions of deposition, however, 

were so varied that over large parts of the area considered the deposits are not widely 

uniform. For instance, while clay was being laid down in one place sand was accumulating 

in an adjacent area and at their border the two deposits were merged. Consequently the 

arrangement of the beds is broadly lenticular, as is illustrated by the well records (PI. V). 

No two records are exactly alike, and in most cases it is impossible to correlate deposits 

in the different sections. Beds of clay are most widely distributed, but the more localized, 

accumulations of sand and gravel, which are the most important reservoirs of underground 

water, are irregularly distributed.

Underground water derived from the sources stated above occupies the spaces between 

the solid particles of the clay, sand, and gravel which constitute the valley filling. In 

general, these deposits are saturated below the horizon which marks the surface of ground 

water. The position of this surface varies, depending on the supply, on the amount used 

or the intensity of evaporation, and on the character and slope of the sediments. The water 

is seldom stagnant, but tends to flow with extreme slowness from a higher to a lower level, 

the chief factors in the movement being the number and size of the interstitial spaces in 

the deposits and the pressure gradient due to gravity. The highest velocity of ground 

water ever determined is about 100 feet in twenty-four hours, but the ordinary velocity is 

much less than this, common rates in sand being between 2 and 50 feet a day.

The fluctuation of the surface of ground water is considerable. Since the chief replenishment of the supply occurs when the creeks discharge the most and when the irrigation 

canals are in full operation, ground water occurs nearer the surface in summer than in 

winter. Conditions in different areas cause a varied annual range, but 10 feet is common 

and 15 feet is not infrequent. In addition to the annual fluctuation a cumulative change 

is in progress, the ground-water surface being gradually raised in the lower parts of the 

valley in consequence of irrigation and the custom of allowing artesian wells to flow unceasingly, leading to swampy conditions in the valley bottom. Details regarding these changes 

are given on subsequent pages.

PI. VI illustrates the approximate average depths at which ground water occurs in the 

valleys of Utah Lake and Jordan River. The boundaries between the different areas 

fluctuate and can not accurately be determined. A narrow belt contiguous to the base of 

the mountains is left blank on the map because of the varying and often unknown conditions that exist there, owing to seepage and the irregular distribution of water in the 

adjacent bed rocks. In the absence of topographic maps the position of the water table 

can not be shown by contours.

Below the surface of ground water the saturated beds contain varying amounts, depending on the character of the deposits. Coarse-textured gravel and sand, having a greater 

porosity than fine-textured clay, hold and transmit relatively more water. Beds of sand 

and gravel therefore constitute the chief underground reservoirs. Typical illustrations of 

the distribution of sand and gravel are shown in PI. V. In sinking wells in this region, beds
30 UNDERGROUND WATER IN VALLEYS OF UTAH.

of sand and gravel, ranging from a few inches to a hundred feet or more and separated by 

varying thicknesses of clay, are encountered, water being commonly found in each porous 

deposit. Because of the prevailing inclination of the deposits away from the mountains, 

and of the presence of relatively impervious beds of clay above more porous sand and 

gravel, the contained water is under pressure. In the lowland areas this pressure is sufficient to cause the deep-seated water, when it is reached in a well, to rise and flow at the 

surface, and consequently artesian water is an important source of supply. Above the 

lowlands, where the surface elevation is too great for a flow to occur at the surface, the 

water rises in deep wells to a greacer or less height according to the amount of pressure.

* ttUALITY OF TJNDERGBOUKD WATER.

The accompanying analyses, gathered from a number of sources and reduced to common 

terms, illustrate the character of the water in the valleys of Utah Lake and Jordan Kiver.

Analyses of water from streams and springs in valleys of Utah Lake and Jordan Riverfl

[Parts per million.]

No.

1 

2

3

4 

5 

6

7

8 

9 

10 

11 

12

13

14

15 

16

17

18 

19

20 

21

Source and date.

CHEEKS.

City, Dec., 1882.

Red Butte,

Dec., 1882.....

Emigration, 

Dec., 1882.....

Parleys, Dec., 

1882...........

Big Cot tonwood, Oct., 1884

Little Cottonwood,Oot.,1884

Dry CottonAmerican Fork .

Santaquin......

Warm..........

EIVERS.

Spanish Fork... 

Jordan:

Utah Lake 

(outlet) ,1899.

Salt Lake City 

(near), 1899.

WARM SPRINGS.

Salt Lake City, 

Oct., 1881...

Beck's (hot) . . 

Sandy (8 mi. s.),' 

Mar. 1882.....

UTAH LAKE.

1883. ...........

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

Ca.

55.3 

88.8 

101.0 

85.1 

48.1 

17.5

17.0 

45.0 

12.0 

12.0 

47.0 

114.0

51.0 

68.0

67.6 

111.8

535.2 

694.3

141.5

55.8 

67.0

Mg.

18.9 

31.3 

31.6 

22.5 

18.9 

8.2

27.0 

24.0 

17.0 

31.0 

54.0 

48.0

29.0 

36.0

13.8 

13.7

138.4 

109.5

27.7

18.6 

86.0

Na.

2.6 

25.6 

18.1 

31.5 

Trace. 

5.9

15.0 

4.0 

22.0 

31.0 

89.0 

381.0

28.0 

46.0

233.7 

251.1

3,039.0 

3,754.9

405.0

17.7 

230.0

K.

24.3 

Trace 

9.9 

2.6 

8.6 

1.7

14.0 

10.0 

3.0 

5.0 

44.0 

92.0

22.0 

17.0

2.0

178.0 

196.9

55.0

2.0 

22.0

AljO3Fe2O3 SiO2 .

2.0

3.a

2.6 

1.8 

1.6 

1.3

0.7 

9.0......

5.1

19.9 

35.2 

24.4 

27.2 

12.6 

39.9

21.3 

31.5

50.5 

10.0

28.0

SO,.

7.3 

100.6 

126.2 

56.5 

42.1 

12.3

 3A f\

42.0 

32.0 

33.0 

115.0 

114.0

44.0

64.0 

236.7

334.5

787.5 

840.5

53.8 

130.6

378.0

HC03.

121.0

145.0 

121.0 

212.0 

181.0 

333.0

205.0

277.0

194.0

CO2.

95.1 

108.8 

102.7 

122.1 

63.6 

32.2

14.0 

14.0 

15.0 

28.0

23.7 

Trace

442.9 

204.5

272.7

60.9 

11.0

01.

19.5 

22.9 

28.6 

19.7 

7.9 

2.8

14.0 

Trace.

211.0 

703.0

28.0 

28.0

316.5 

378.9

4,968.0 

6,743.8

635.6

12.4 

337.0

Total.

244.9 

416.5 

445.1 

369.0 

203.4 

121.8

242.0 

270.0 

221.0 

338.0 

756.0 

1,813.0

397.0 

536.0

894.0 

1,090.0

10,284.0 

12,584.9

1,658.0

308.0 

1,353.0

a AUTHORITIES. Nos. 1-5,17,19, Kingsbury, J. T. Nos. 6-14, Soil survey of the Provo area, Utah: 

Bureau of Soils U. S. Dept. Agric., 1904, p. 22. Nos. 15, 20, and 21, Cameron, F. K. Water of Utah 

Lake: Jour. Am. Chem. Soc., vol. 37, No. 2, 1905. No. 16, ibid., Kept. No. 64 U. S. Dept. Agric. No. 

18, Riggs, R. B., Bull. U. S. Geol. Survey No. 42,1887, p. 148. No. 20, Clarke, F. W. No. 21, Brown, R. E.
U. S. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. 157 PL. VI

T. 2

T. I N,

T. I S

T. 2 S.

T. 3 S,

T. 5 S.

EXPLANATION

Area in which ground wafer//es 

wtfhin /O feet of the surface

T.6 S.

round wafer/ies 

between/Oand 50 feefbe/ow 

the surface

Area in which ground wafer//es 

deeper fhan $0feefbe/ow f/ie 

surface

S

Base ofmounfa/ns,approx//77a 

offheSof7nei////e shore //'ne

SCALE OF MILES 

2 O 2 -4- 6

8 S.

I ___I

T. 9 S.

R.2 W. R. I W. R.I E.

T. 10 S

R.2 E. R.3 E.

SKETCH MAP SHOWING DEPTH TO GROUND WATER IN THE VALLEYS OF UTAH LAKE AND JORDAN RIVER.
QUALITY OF UNDERGROUND WATER. 31

The average of analyses of 12 streams « coming from the Wasatch Mountains shows a 

total solid content of 319 parts per million, ranging from 122 to 536, the varying character 

of the water being due to differences in the rocks of the respective watersheds. Examination of these analyses shows that calcium is usually the most abundant base, with magnesium a poor second, while sodium and potassium generally are much less plentiful and 

vary in relative amounts. Among the acid radicals, carbonic commonly preponderates, 

being often several times more abundant than the others; sulphuric ranks next, and in a 

few streams is important, while chlorine is generally of minor occurrence. Little Cottonwood Creek ranks first, having only 121.8 parts per million of dissolved solids. It flows 

for most of its course through granitic rock and therefore contains but little calcium carbonate. The total solids in Big Cottonwood Creek water are also low and relatively little 

lime is present because a large part of the drainage is over silicious rocks. The great 

abundance of limestone on most of the watersheds accounts for the abundance of calcium 

carbonate. Red Butte, Emigration, and Parleys creeks make a relatively poor showing, 

the sulphates being especially abundant, because these streams flow over Permo-Carboniferous and Mesozoic rocks containing more or less gypsiferous matter. Provo River and 

Spanish Fork drain large areas occupied by a variety of rocks, among which limestone is 

prominent, and the analyses show rather high amounts of total solids, the carbonates 

being particularly abundant. Currant and Warm creeks are exceptional. The unusual 

amount of sodium chloride present in Currant Creek is derived from salt deposits above 

Nephi. Warm Creek rises in the springs west of Goshen, and the character of its water, 

like that of similar springs in this area, is due to unusual conditions.

The few analyses of the thermal springs in the area under consideration show the presence 

of abundant dissolved salts, of which the chlorides are the most plentiful, though considerable quantities of sulphates and carbonates are also present. Sodium is several times 

more abundant than any other base, calcium ranks second, and magnesium and potassium 

are present in small amounts. Some of the hot springs contain considerable hydrogen 

sulphide. Most, if not all, of these springs are associated with faults and have a deepseated origin, to which their temperature and composition are due. The mineral matter 

is leached from the deposits through which the waters pass, much of the salt content 

being probably derived from old lake beds.

Analyses of water from flowing wells are similar to those of surface streams. Different 

wells give different results, the quality of the water varying with the source and the nature 

of the deposits passed through underground. Analyses from the "Murray" and "Germania" wells show an unusually small content of total solids, while those from the wells 

of the Utah Sugar Company at Lehi and near Provo show amounts above the average. 

In the area contiguous to Great Salt Lake the well water contains considerable salt, but 

no analyses were obtained. In general the water from flowing wells is of admirable 

quality and often forms a marked contrast to the supply from shallow wells.

a Omitting Currant and Warm creeks, which are exceptional.
UNDERGROUND WATER IN VALLEYS OF UTAH.

Analyses of water from wells, etc., in valleys of Utah Lake and Jordan River.a

[Parts per million.]

No.

22 

23

24

25

26

27

28

29

30

31

Source and date.

Mill Pond at Lehi , July ,1895 .

Artesian well .Murray Plant, 

Am. Smelting and RefinArtesian well, Gennania 

Plant, Am. Smelting and

U. S. Mining Co. well, BingU. S. Mining Co. well, West 

Jordan, Aug., 1902. .......

Wm. Cooper's well, BingBeet-cutting station, Utah 

Sugar Co.well,near Provo, 

Jan., 1899.. ...............

Artesian well, Utah Sugar 

Co., Lehi, Jan., 1899. ......

R. G. W. Rwy. well, Springville, May, 1901.. .........

R. G.W. Rwy. well, Goshen, 

May, 1901.................

Ca.

82 

W

37

11

74

62

1 ^7

Mg.

54 

6.6

13

11

29

38

19

32

Na.

14

A12 

08. 

Fe2 

03.

16.0 

1.4

1

2.4

1.2

5

Tr.

4

,90

SiO2.

11 

14

9 7

14

13

16

58

12

18

80

SO<.

<*196 

<U4

d!2

d50

d!6

154

41

47

C03 .

6135 

42

64

56

c30

66

c!80

c91

120

127

Cl.

68

89

?1

?]

IPO

Na2 

CO3 

K2 

CO3.

124

Na2 

SO, 

K2 

SO4.

CO 

Tr.

6.8

27

44

45

116

Na 

Cl 

KC1.

152 

11

28

87

58

87

103

287

Total 

solids.

800 

10

140

29C

232

284

aw

64?

aAuTHOKiTiES. Nos. 22, 28, and 29. Dearborn laboratories. Nos. 25 and 26, Converse, W. A. No. 27, 

J. H. Parsons Chemical Co. Nos. 30 and 31, De Bernard, J. H. 

6 Prom MgCOa. 

c Prom CaCO3 and MgCO3 . 

d Prom CaSOi.

No analyses of ground water obtained from shallow wells are available, but the general 

character of such water is known. In the upland areas above the canals the water from 

shallow wells is much like that commonly obtained throughout the region in deeper ones; 

it contains a moderate amount of dissolved salts, largely calcium carbonate, and is usually 

of good quality. But in the lowlands the surface water is quite different, generally containing considerable dissolved salts, among which alkalies are abundant. Where ground 

water lies within the scope of capillary attraction from the surface, evaporation causes the 

mineral matter which is held in solution to accumulate, and in this manner the soil become? 

tainted with alkali. Consequently the water from surface wells in the lowlands is characteristically rich in dissolved salts.

Abnormal conditions prevail locally in the vicinity of the smelters in Jordan Valley 

south of Salt Lake City. Smelter smoke has lately become a nuisance to farmers by 

injuring crops and animals in the path of prevailing winds. Sulphur dioxide is the 

most abundant deleterious substance contained in the smoke, and to a minor extent locally 

finds its way into the water supply. Occasionally also ground water may become poisoned 

from accumulations of flue dust containing copper and arsenic.«

Natural gas occurs in a number of water wells in the area under consideration. Well 

drivers report the common presence of vegetable matter, chiefly fragments of wood, at 

different depths in many localities. This was entombed in the old lake deposits, and it? 

decomposition may account for the origin of the gas. Though gas occurs in numerous 

wells it has been found in quantity in only a few localities, the greatest development occuring near the shore of Great Salt Lake, about 12 miles north of Salt Lake City. & Here 

several wells were drilled averaging about 500 feet in depth; and from September, 1895,

<* Widtsoe, J. A., Relation of smelter smoke to Utah agriculture: Bull. Agricultural College of Utah 

No. 88, 1903. 

6 Richardson, G. B., Natural gas near Salt Lake City: Bull. U. S. Geol. Survey No. 260, 1905, p. 48fl.
QUALITY OF UNDERGROUND WATER. 33

to March, 1897, Salt Lake City was supplied with natural gas from this source, the total 

yield being approximately 150,000,000 cubic feet. But the supply finally became insufficient and the field was abandoned. Gas continues to be found in various parts of the valley 

and possibly other fields similar to that north of Salt Lake City may yet be found; but 

there is little reason for expecting much better results than already obtained and it is 

impossible to predict the localities where such supplies may be found.

The water of Utah Lake represents the varied sources of its supply; part is derived 

directly from surface streams, another part from seepage, still another portion from springs, 

and the whole is concentrated by evaporation. The analysis by the Bureau of Soils on 

page 30 shows the present condition of the water. Sodium predominates, magnesium and 

calcium are subordinate, and the corresponding salts are principally sulphates and chlorides. 

Comparison with an analysis of UMh Lake by F. W.Clarke twenty-one years earlier affords 

interesting data.® The total solids have increased from 308 to 1,353 parts per million, 

and the character of the water has changed from a preponderating sulphate solution to 

one containing large amounts of chlorides; the sodium has increased remarkably and 

magnesium is now in excess of calcium. These changes appear to be mainly due to man's 

occupancy of the region. The streams have been diverted for irrigation and an increasing 

supply has reached the lake as seepage after passing through the alkaline soils of the lowlands. Evaporation in the shallow lake also has tended to concentrate its waters.

The composition of the water of Great Salt Lake has been the subject of much investigation, and a list of the more important analyses is given on page 34. The lake receives 

the drainage of an enormous area, but by far the greater part of its supply is derived from 

the Wasatch Mountains, from Bear, Weber, an4 Jordan rivers. The mineral content of 

Great Salt Lake is the result of the concentration of a vast body of water during a long 

period of time, in which Lake Bonneville has given place by evaporation to the present 

lake. Great Salt Lake is shallow, and the seasonal and annual fluctuations in its level 

cause considerable differences in volume, with consequent changes in composition of the 

water. These changes are indicated by the increase of salinity from 13 per cent in 1873 

to about 24 per cent in 1892.

In August, 1892, the water of Great Salt Lake contained 238 parts per thousand of 

total solids, consisting of predominating sodium and smaller amounts of magnesium, potassium, and calcium, in the order named, the corresponding salts being chlorides and sulphates. The water of the lake is thus a concentrated brine, and in the winter months 

the point of saturation for sodium sulphate is actually reached and crystals of mirabilite b 

are deposited. The critical point for calcium carbonate is passed, so that, in spite of its 

abundance in the waters that supply the lake, none has been foimd in it. Apparently 

calcium carbonate is precipitated soon after entering the dense body of water.

aCameron, F. K., Jour. Am. Chem. Soc. -vol. 37, 1905, p. 113.

& Tannage, J. E., "Great Salt Lake, Present and Past," 1900, p. 64.

IRE 157 06 3
34 UNDERGROUND WATER IN VALLEYS OF UTAH.

Analyses of water of Great Salt Lake. « 

[Parts per thousand.]

Analyst and date.

Alien, O. D., sumBassett,H., Aug., 

1873.............

Talmage, J. E.:

Waller, E., Aug., 

1892.............

Ca.

Trace

0.2

.6

Mg.

3.8

3 0

2 9

5.1

Na.

85.3

qo n

CQ o

65.3

75. 825

K.

2.4

9.9

1 9

SO4 .

12.4

9.9

14 9H4

Cl.

124.5

84.0

90.7

B2O3 . P2 06 . Total.

222.8

149.9

134.2

167.2

195.5

&238. 12

Specific 

gravity

1.170

1.111

1.102

1.157

1.156

« Waller, E., Water of Great Salt Lake: School of Mines Quart., vol. 14, 1893, p. 59. 

t> By evaporation, duplicate test gave 237.93.

Too little care is given to the sanitary character of the waters in the valleys of Utah 

Lake and Jordan River. The mountain streams are a source of excellent purity, yet they 

are liable to contamination. General supervision of the watersheds of the creeks that supply Salt Lake City is maintained by the municipality, especially on City Creek, but elsewhere few precautions are taken to safeguard the supply. Commonly the character of 

water obtained from the deep wells is of good quality, as is also that of surface wells in 

the thinly settled uplands adjacent to the base of the mountains. But surface water generally, especially in the thickly settled lowlands, where, moreover, the mineral content is 

high, is undesirable for domestic use because of its liability to contamination.

Salt Lake and Provo are the only cities in the area that have sewer systems. The 

Provo sewer discharges through an open ditch into Utah Lake, and thereby pollutes that 

body of water. Salt Lake City's sewage is well disposed of on a "sewer farm" below 

Hot Springs Lake, and the surplus enters Jordan River near its mouth. Elsewhere no 

systematic sanitary precautions are taken, and locally conditions are bad, with consequent 

frequent typhoid fever epidemics.

It can not be too strongly impressed upon inhabitants of country districts that the welfare of the community is intimately concerned with preserving the water supply uncontaminated, and in this connection it may be of service to reproduce a section from the ninth 

annual report of the Massachusetts State board of health: «

There are a few points to be taorne in mind with reference to water supply, drainage of houses, and 

sewerage, which have been suggested by the examination of the board in this State, and may properly 

be summarized here.

1. The privy system, so common throughout the State, by which filth is stored up to pollute the air, 

soil, and water near dwellings, should in all cases be abolished.

2. Cesspools, unless extraordinary precautions be taken as to ventilation and prevention of pollution of soil and air, are little better, and should be given up for something less objectionable as soon as 

practicable.

3. Wells can not be depended on for supplies of wholesome water unless they are thoroughly guarded 

from sources of surface and subsoil pollution. Some of the foulest well water examined by the board 

has been clear, sparkling, and of not unpleasant taste.

4. Where wells have already been polluted and it is not practicable to dig new deep wells remote 

from sources of contamination or to introduce pure public water supplies, the storage of rain water, 

properly filtered, is a satisfactory method of procedure.

5. In small towns where public water supplies have not been introduced, and, indeed, wherever waterclosets are not used, some method of frequent removal and disinfection with earth or ashes should be 

adopted in place of privies, by which it should be impossible for the filth to soak into the soil or escape 

into the air. Cemented vaults are not always to be depended upon, as their walls crack from frost or 

through settling of the ground, and they thus sometimes become sources of pollution of wells, besides1 

contaminating the air. Nor is the fact of a privy being on a downward slope from the well a sufficient 

safeguard, for even then the direction of the subsoil drainage may be toward the well.

a Rafter, G. W., and Baker, M. N., Sewage Disposal in the United States,1894, p. 40.
QUALITY OF UNDERGROUND WATER. 35

6. Earth closets, with proper care, may be satisfactorily adopted, but the earth, after having been 

once used, should be placed upon the land, not stored within doors and dried to be again used, for in 

the process of drying there are emanations from it which are, perhaps, not less dangerous from the fact 

of their being imperceptible by the unaided senses or through chemical examination. With earth closets a plan similar to that in use at the Pittsfleld Hospital o may well be used for the chamber slops, 

and the kitchen waste may be utilized (with the chamber slops too, if desired) in the manner used by 

Mr. Field and Colonel Waring. * * * Less intricate methods are us.ed in scattered dwellings, but 

with the effect of having the slop water absorbed by the ground and taken up by vegetation so far 

from the house as not to involve a nuisance or danger to health.

7. Where water supplies, water-closets, etc., are introduced, sewers should follow immediately in 

most kinds of soil. Cesspools should not be used, unless with extraordinary precautions; but with a 

few hundred feet square of lawn the irrigation system by agricultural drain pipes is to be recommended, whereby the filth is at once taken up by the roots of grass. In all cases, of course, with or 

without cesspools, there should be thorough ventilation of the system of house drainage, with disconnection from the main outlet drain by means of either a ventilating pipe or rain-water spout between the 

sewer trap and the house, and whose openings at the top should be only at points remote from windows and chimney tops.

On the whole, a thoroughly satisfactory awangement of this kind, if properly looked after, is in 

many respects to be preferred to connecting with public sewers.

RECOVERY OF UNDERGROUND WATER.

A crude estimate of the amount of underground water in the valleys of Utah Lake and 

Jordan River might be made, based on an assumed thickness and porosity of the unconsolidated sediments, and the result would be many cubic miles, yet the figures would be valueless. The important fact is the amount of available water that can be recovered economically; but, unfortunately, this too, because of lack of detailed knowledge concerning the 

distribution and thickness of the bed? of sand and gravel which constitute the reservoirs, 

can not be determined. Though definite figures are not available, the general fact is well 

known that the lowlands are amply supplied with underground water within easy reach of 

the surface and that on the highlands the underground supply is relatively small.

Underground water becomes available for use both naturally and artificially. It reaches 

the surface again naturally in springs and by seepage into drainageways, and is commonly 

recovered artificially by means of wells, though occasionally tunnels and subsurface dams 

prove efficacious. Wells are the main recourse in the area under consideration, and they 

can be conveniently grouped into two classes, flowing and nonflowing.

The areas in which flowing wells are obtained in the valleys of Utah Lake and Jordan 

River are shown on Pis. VIII and IX, and the list of wells, together with the descriptions of 

the different localities, gives detailed information concerning the occurrence of artesian 

water.

The date when the first flowing well was put down has not been ascertained, but it 

appears to have been about 1878. Since then many have been sunk, and the limits of the 

areas in which flows can be obtained have been determined with fair accuracy by experiment. The map shows that flowing wells exist only in the lower portions of the valley, 

the area of flows corresponding closely with that in which ground water lies within 10 feet 

of the surface. Higher up on the benches the elevation is too great to obtain flows.

Locally, flowing wells may be obtained at a depth of less than 50 feet, but generally they 

range between 100 and 400 feet, while the few that have been sunk to 1,000 feet and more 

encountered water under pressure in the successive beds of sand and gravel. As many as 

25 distinct water horizons from which flows at the surface were obtained are reported in 

the Rudy well, sec. 6, T. 1 N., R. 1 W. The wells are usually 2 inches in diameter, though 

occasionally the shallower ones are only 1 inch, while the-deeper ones are 4 and 6 inches. 

In yield the wells vary considerably, according to location, depth, and size of pipe. The 

greatest flow measured was that in the Harry Gammon well, sec. 7, T. 6 S., R. 2 E., which 

supplies about 266 gallons a minute from a 3-inch pipe. A number of wells flow less than 

1 gallon a minute, though a common yield is between 10 and 60 gallons. The pressure is 

comparatively low, the highest measurements obtained being only 15J pounds per square

a Cottage Hospitals: Ninth Ann. Kept. Mass. State Board of Health, pp. 83-95.
36 UNDERGROUND WATER IN VALLEYS OF UTAH.

inch, and generally the greatest pressures are little more than sufficient to raise the water 

into railroad tanks.

Temperature measurements of the water from flowing wells afford some data bearing on 

the downward increment of heat in the unconsolidated valley deposits, but there are a 

number of disturbing factors. Adjacent to the mountains the waters are unusually cool; 

the presence of hot springs tends to disturb conditions, and the depths from which the waters 

flow are often not known. The common rate of downward increase in temperature appears 

to be slightly less than 1° F. in 50 feet, but the facts obtained do not warrant a closer 

statement. It may be of local interest, however, to observe that in general the temperature of the water increases with the depth of the wells at approximately that rate.

Few measurements have been made, but it is common experience that the yield of many 

flowing wells in the area under consideration has decreased. The most comprehensive 

measurements are those made of the wells owned by Salt Lake City near Liberty Park 

(p. 44). Comparing the discharge of 12 of these wells in August, 1890, with the yield of the 

same wells in September, 1902, it appears that in the interval of twelve years the flow of 

one had increased, but that those of the others had materially decreased. Such decrease, 

however, may be due largely to clogging of the pipes, for the total yield of the Liberty Park 

area has been maintained with little decrease by sinking new wells.

Decrease in yield is conspicuously apparent in Lehi a,nd Spanish Fork, where flowing 

wells formerly could be obtained much more generally than now, and is notable elsewhere 

throughout the valley, especially adjacent to the boundary of the flowing area. Decrease 

in flow of individual wells is so Tietimes due to clogging up with sand and clay, and often 

can be remedied by cleaning or by the use of casing. But the general decrease is to be 

explained chiefly by the large increase in the number of wells which draw on the general 

supply. It is also to be remembered that for the past few years the annual precipitation 

has been considerably below the mean.

The artesian wells are used for stock, irrigation, and domestic purposes. The amount 

used for stock is comparatively small, and, save for watering small gardens, artesian water 

as yet is not extensively used for irrigation, except locally. Probably over a thousand acres 

are thus irrigated in Utah Lake Valley, the principal areas being below Lehi and Payson. 

The artesian supply is much used for domestic purposes, and in general furnishes an admirable quality of water, containing much less dissolved salts and being much purer than 

shallow ground water.

An attempt was made to estimate the total number of flowing wells in the area studied, 

but the result is to be taken only as a rough approximation. There are about 5,000 flowing wells in the valleys of Utah Lake and Jordan River, and possibly somewhat more than 

half of these occur in the southern valley. Assuming an average of 15 gallons a minute, a 

total yield of about 150 second-feet is thus indicated.

Outside of the area in which flowing wells are obtained underground water is recovered 

either from shallow dug wells that tap the upper surface of underground water or from 

driven wells in which the water comes from a relatively deep horizon and is under pressure 

which causes it to rise toward the surface. To save the expense of " driving," shallow wells 

are often dug within the area in which flowing wells can be obtained. Occupying the center 

of the valley and extending approximately to the limit at which flowing wells can be 

obtained, ground water lies within 10 feet of the surface, and locally, as has been mentioned, 

swampy conditions exist. As the base of the mountains is approached the depth to ground 

water increases and is over 50 feet on much of the upland where, over large areas, the distance to water is unknown.

Water is recovered from these wells generally by buckets and hand pumps. Comparatively 

few windmills are in operation. An average wind velocity of not less than 6 miles an hour a 

is stated to be required to drive a windmill; and since the mean wind velocity at Salt Lake

a Wilson, H. M., Pumping for irrigation: Water-Sup, and Irr. Paper No. 1, U. S. Geol. Survey, 

1896, p. 27.
RECOVEBY OF UNDEBGBOpND W ATEB. 37

City from June to September, inclusive, is 6.5 miles an hour and for the entire year averages 

only 5.9 miles, the natural conditions are not very favorable for this form of power. Steam 

pumps are used only to a limited extent. The Bingham Consolidated Company has three 

3-inch wells 250 to 300 feet deep in which the water rises to within about 70 feet of the surface; 125 gallons per minute are reported to be supplied by each, the water being raised by 

compressed air. Another instance of successful pumping is at the brickyard in sec. 29, 

T. 1 S., R. 1 E., where 40 gallons a minute are reported to be obtained from a well 30 feet 

deep. Gasoline for pumping has not- been much used. Electric power can be cheaply 

developed in the canyons and affords a valuable asset. In the valleys of Utah Lake and 

Jordan River pumping on a large scale has not yet been resorted to. There is, however, a 

considerable quantity of water within easy reach of the surface which probably will not 

much longer remain unused.

Underground water is recovered in exceptional circumstances by means of subsurface 

dams, or similar contrivances, which impound the underground supply. In unconsolidated 

materials, in order that this may be successfully accomplished, certain conditions are necessary. Practically impervious bottom must exist within easy reach of the surface to pre- 

'vent excessive lowering of the ground-water level, and competent side walls, not too far 

apart, should be present to intercept lateral escape. The presence of the necessary conditions can be determined only by prospecting, and the practicability of such structures is an 

independent question, but because of the value of water in the area under consideration 

their feasibility 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 available underground water. On Emigration Creek, for 

instance, the comparatively low run-off, suggesting an unusual amount of underdrainage, 

and the quantity of water obtained from the inefficient city trench invite further testing of 

the possibilities. Below the mouths of the canyons in the several creek valleys favorable 

conditions also may be discovered by the drill to warrant the construction of infiltration 

galleries.

In the section devoted to geology it is stated that the rocks.of this region are more or less 

disturbed and broken, and an important part of the precipitation on the mountains finds its 

way into the bed rock. The water occurs in the small interstices or pores which are present 

in all rocks, in larger spaces such as fissures or solution channels, and along joints, bedding 

planes, and igneous contacts. -As would be expected, less water is found in the Oquirrh 

Mountains than in the Wasatch. Bingham is a dry camp, though more or less water is 

encountered in the workings, while the mines of Park City are wet. The Ontario tunnel, 

which drains most of the large mines of the latter district, is stated by J. M. Boutwell to discharge from Q,000 to 9,000 gallons a minute. Considerable water is being recovered by tunnels driven into bed rock along the base of the mountains. In some instances the site of 

the tunnel marks the presence of a former spring, as, for instance, Wadleys, near Pleasant 

Grove, and those in Butterfield Canyon. But in one, the Dalton and Lark tunnel, east of 

Bingham, water in quantity was not encountered until several thousand feet of rock were 

penetrated.

Another method of recovering water from bed rock is suggested by the structure of the 

mountains southeast of Salt Lake City. It will be recalled from the outline of the geology 

that a great syncline, modified by local undulations, is there developed, whose axis extends 

along the valley of Emigration Creek. The general structure is favorable for the occurrence 

of artesian water, but there are unfavorable complications. The rocks are chiefly compact 

limestones, the general disturbed and fissured conditions tend to relieve the pressure on the 

interstitial water, and the Wasatch fault has cut across the strata. Nevertheless, it is possible that locally the red sandstones contain water under pressure, but because of the limited 

intake area a large supply is not to be expected.
38 UNDERGROUND WATER IN VALLEYS OF UTAH.

SUGGESTIONS.

It is evident that in general a high degree of efficiency in the use of the water resources of 

the valleys of Utah Lake and Jordan Eiver is not maintained. Conditions can be greatly 

benefited by preventing waste whenever possible. Most prominent in this connection is the 

conservation of storm waters. Besides the construction of large impounding reservoirs 

small ones can profitably be built at many localities within the mountains. Also to a certain extent storm waters can be utilized by diverting them on the uplands and permitting 

them to spread over a larger area instead of allowing the run-off to escape rapidly in the 

natural channels. The effect would be an appreciable increase of the downstream seepage 

'and of the replenishment of the underground store. Moreover, storm discharge may be 

lessened by planting trees and by protecting the watershed from fire, lumbering, and grazing, 

thereby promoting retention of the water by absorption and the increase of seepage runoff long after the storms are over. Another important loss of water occurs because of faulty 

methods of transportation for use in irrigation. As the need of economy increases more 

efficient conduits will replace crudely constructed ditches. Water thus saved, however, 

proportionally diminishes the replenishment of the underground store. Loss also occurs by 

allowing artesian wells to flow when the water is not needed. Either the wells should be 

capped or the flow at least be partly checked when water is not used, or it should be 

collected in reservoirs.

The abundance of water in the lowlands and a dearth of it in the uplands, where the soil 

is generally fertile, free from alkali, and well adapted to the growth of fruit, suggest that a 

more efficient application of the available water supply should be practiced. Because of tho 

scarcity of the underground supply on the uplands and the possibility of distributing creek 

water there by high-level canals, and since there is not enough water in the creeks to directly 

serve both the uplands and lowlands, it would appear that steps should be taken to increase 

the upland supply from the creeks and to use wells, either flowing or pumped, in developing 

the lowlands. - The popularity of pumping plants in irrigation elsewhere, the proximity of 

underground water to the surface in the lowlands, and the availability of electric power 

that can be developed in the adjacent canyons are facts favorable to the proposed change. 

Moreover, seepage from the greater use of creek water on the uplands will increase the available underground supply in the lowlands. The upland water supply may also be increased 

by the development of. springs, by tunneling into the mountains, and possibly by the construction of subsurface dams and infiltration galleries at favorable localities.

More attention should be given to developing and preserving a pure water supply for 

domestic purposes. Surface streams should be protected from pollution, and care should be 

taken to reduce to a minimum the contamination of water in wells by using modern methods 

in the disposal of household refuse. The common location of the towns, near the base of 

the mountains, where sufficient amounts of pure water are generally available either from 

creeks or springs renders the problem of public water supply relatively simple; yet it is a 

remarkable fact that only a few towns utilize their opportunities.

OCCURRENCE OF UNDERGROUND WATER.

WEST OF JORDAN KIVER. 

DIVISIONS OF AREA.

The area west of Jordan Eiver within the region covered by this report is naturally 

divided into two parts. One is the lowland which extends from Great Salt Lake eastward 

to Jordan Eiver and thence continues in a narrow belt southward, adjacent to the river; 

the other is the upland which, from the southern and western border of the lowland, extends 

with increasing elevation to the base of the Oquirrh Mountains. . No sharp line of division 

can be drawn between these areas, for they grade into each other, yet on the whole they 

are distinct. The distribution of underground water in the two areas also is distinct, a 

convenient line of separation being that which marks the boundary between flowing and
U. S. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. 157 PL. VII

RIOAGRANDE

Area in which flowing 

wells are obtained.

Base of mountains, approximate position of the 

Bonne ville .shore line

 Wells the records 

of which are shown on 

Plate V

MAP SHOWING THE AREA IN WHICH FLOWING WELLS ARE OBTAINED IN JORDAN VALLEY.
OCCURRENCE OF UNDERGROUND WATER. 39

nonflowing wells. As shown by PI. VII, this line lies close to the Jordan in the southern 

part of its course, but across the river from Murray takes a westward turn, and, following 

the base of the upland, extends to Great Salt Lake at the northern base of the Oquirrh 

Mountains. This line also roughly marks the boundary between shallow and deep ground 

water. In the lowland area ground water is abundant and generally lies within 10 feet of 

the surface, while on the upland water is generally scarce and is found only at a depth of 

over 50 feet.

UPLAND AREA WEST OF JORDAN RIVER.

In general the upland has the aspect of a rolling plain which gradually rises to the base 

of the mountains, but in detail the plain is varied by the presence of benches and escarpments, relics of Lake Bonneville and of a few drainage ways that have incised channels 

across the plain. Locally, especially at the northern end of the Oquirrh Mountains and at 

the Narrows, where Jordan River flows through the Traverse Mountains, the shore lines 

of Lake Bonneville are unusually well marked. Different stages of the lake's history are 

recorded by a series of distinct benches, which descend one below another from the Bonneville level; at Jordan Narrows, for instance, 110 less than ten periods of pause in the lake 

level are thus recorded. Shore phenomena in general, however, are less prominently 

marked on the western margin of Jordan Valley than on the eastern, adjacent to the 

Wasatch Mountains.

Bingham Creek is the only perennially flowing stream which runs for any considerable 

extent across the plain, though Butterfield Creek flows for a short distance after it emerges 

from the mountains southwest of the town of Herriman. This area is also traversed by a 

number of arroyos which contain water only for a few days after storms and during the 

time of rapidly melting snow. The Utah and Salt Lake and the South Jordan canals, 

carrying water from the upper part of Jordan River, extend along the eastern border of 

the upland and supply irrigation water to a narrow belt. Above the upper canal the area 

is desert and practically uninhabited, except for the town of Herriman and a few scattering 

ranches which obtain local supplies of water. The Utah Lake project of the Reclamation 

Service plans to make available for irrigation a belt from 2 to 4 miles wide west of the Utah 

and Salt Lake canal, but a large part of this upland area west of Jordan River has too great 

an elevation to be cheaply irrigated from Jordan River. Some amelioration of the present 

arid conditions may be effected by constructing reservoirs at the base of the mountains, 

but the collecting area is small and no very extensive additions to the water supply are 

likely to be derived from this source. More or less dry farming is already practiced here. 

The land is fertile, is practically free from alkali, and because of its location would be very 

valuable if an adequate supply of water could be obtained. Unfortunately, so far as 

known, underground water conditions afford little prospect of a large supply from that 

source, though valuable quantities can locally be recovered.

This upland area is largely underlain by gravel and sand, and along the base of the mountains coarse gravel predominates. The material was derived from the disintegration of 

the adjacent highlands and mostly deposited offshore in the ancient lake. The constituents have been worked over and sorted during the different stages of the lake's history, 

both by wave action and by subaerial influences, so that the resulting material is heterogeneous both as to its composition and arrangement.

Drills have recorded only to a very limited extent the nature of the deposits that underlie 

the surface. Judging from the records and from conditions elsewhere, it is probable that 

bed rock lies not far from the surface contiguous to the base of the mountains, and that at 

a distance from the highland bed rock lies at a considerable, though unknown, depth. 

Nearer the mountains the unconsolidated valley filling is doubtless of coarser texture 

than farther away, and it is likely that the materials are arranged lenticularly rather than 

in continuous beds. That portion of the slight precipitation on the low, small watershed 

of the Oquirrh and Traverse mountains that is not evaporated or does not join the permanent 

run-off is absorbed by the porous deposits. Under the influence of gravity the water
40 UNDERGROUND WATER IN VALLEYS OF UTAH.

penetrates downward until a relatively impervious layer is reached, when it tends to 

spread laterally and to slowly move toward a lower level, at the same time filling, to a 

greater or less extent, the voids in the overlying material.

In the greater part of the area occupied by Lake Bonneville bed rock is so deeply covered 

by valley deposits that it is impracticable to recover the water contained in it; but along 

the border of the old lake, where the rock outcrops, water is obtained from tunnels in a 

number of places. In the development of the Bingham mines more or less water has been 

encountered, and the town is supplied from mine tunnels. Water has also been found in 

two tunnels constructed for mining purposes near the base of the mountains. The Butterfield tunnel, in Butterfield Canyon, a few miles west of Herriman, encountered considerable 

water, which has caused some litigation. After the construction of the tunnel a number 

of springs tributary to Butterfield Creek ceased to flow, and suit was brought against the 

mining company by the inhabitants of Herriman. Apparently the source of the springs 

was tapped by the tunnel, and judgment was awarded against the mining company. The 

Dalton and Lark tunnel, west of the town of Lark, struck water in the spring of 1903- 

The tunnel was driven 5,000 feet through igneous rock before the water was found. It 

occurs in quartzite that is reported to be much broken and fissured. The supply was 

estimated at first to be 2,500 gallons a minute, but in the summer of 1904 this had decreased 

to about 1,500 gallons, most of which was used for irrigation at a ranch about 2 miles east 

of the mouth of the tunnel. The quantity is reported to be greatest shortly after the 

time of melting snow, thus indicating the source. The experience of these tunnels indicates in general what may be expected by driving into the Oquirrh Range.

Springs of greater or less magnitude occur in a number of places along the base of the 

mountains. These are either supplied by seepage or by water from a deeper-seated source. 

In Rose, Butterfield, and Bingham canyons a number of springs occur, which help maintain the flow of the streams. Also at irregular intervals along the border of the upland 

there are springs which, in general, supply only a few gallons a minute. A conspicuous 

locality is in the northwestern part of T. 2 N., R. 2 W., where a local area of shallow ground 

water occurs. Along the northern base of the Oquirrh Range there is a group of large 

springs, which occur in notable alignment and apparently are associated with a fault. The 

water issues from unconsolidated de"bris and is slightly warm and brackish. The springs 

have an elevation of only a few feet above the lake, however, and are too low to be of much 

service without pumping. Analysis of one, known as the Jap Pond, shows a content of 114 

grains per gallon of dissolved salts, chiefly sodium chloride. The total discharge of 9 of 

these springs in April, 1905, amounted to 8.5 second-feet, and it is reported that the flow 

remains practically constant throughout the year.

On the upland, between the base of the mountains and the canals, the little underground 

water that is recovered is obtained from wells, but in this entire region, 'with very few 

exceptions, ground water lies over 50 feet beneath the surface. A few wells have been 

sunk on the upland away from the lines of surface drainage, and in general they have been 

failures. The most successful wells are along the courses of creeks and arroyos, and future 

search may be carried on with the best prospect by following these drainage ways where 

the water tends to accumulate.

Development in Bingham Canyon illustrates the occurrence of underground water 

beneath a surface-drainage way. More or less placer mining has been carried on in the 

creek gravels, but near the mouth of the canyon, where there is a considerable amount 

of debris, work has been seriously interrupted by the abundance of water beneath the 

bed of the creek. It is in such places, where rock walls confine a narrow channel, that 

tests might well be made with the view of constructing subsurface dams to impound the 

underflow.

Below the canals ground water lies nearer the surface, because of the lower elevation of 

the country and the increased supply derived by seepage from the canals. Ground water 

lies at a greater depth than 50 feet only in a narrow belt below the Utah and Salt Lake 

Canal, and in most of the area between the canals and the line of flowing wells ground water
OCCURRENCE OF UNDERGROUND WATER. 41

can be obtained at 10 to 50 feet from the surface. The effect of irrigation on ground 

water in this area, as elsewhere, is marked. Before irrigation was practiced the depth 

to water was considerably greater than at present; for instance, it is reported that the average level of ground water in several wells in T. 2 S., R. 1 W., now lies 30 to 65 feet nearer 

the surface than formerly. Besides this more permanent effect, the ground-water level 

fluctuates annually from 10 to 15 feet. It is also stated that the quality of ground water 

has deteriorated in recent years, containing now much more alkali than formerly. So 

marked has this change been that surface wells are but little valued, and generally water 

for domestic use is obtained from deep wells.

Inspection of the list of wells will show the typical facts of distribution and occurrence 

of underground water in this region. It will be observed that many wells are about 250 

feet deep and that the range is from less than 100 feet to 1,000 feet. No careful logs 

have been kept, but from fragmentary information it appears that there is considerable 

variation in the material encountered in drilling, implying that the sediments are irregularly sorted and that they exist in more or less lenticular arrangement. Accordingly 

there are no persistent water horizons. Water is generally found in wells wherever sand 

and gravel are encountered. In several wells a number of water beds are recorded. This 

water is always under pressure; the height to which it rises varies, according to location 

and elevation, from close to the surface down to 100 feet below it. Generally, fairly good 

water, within easy pumping distance, is obtainable in this belt of country between the canals 

and the line of flowing wells.

At the Cannon farm, in sec. 34, T. 2 S., R. 1 W., a well was sunk 1,000 feet in an attempt 

to get a flow, but although two thin water-bearing beds were found between 600 and 800 

feet, from which the water rose to within 30 feet of the surface, flowing water was not 

obtained.

LOWLAND AREA WEST OF JORDAN RIVER.

The lowland that lies topographically below the line of flowing wells west of Jordan 

River is almost a level plain which, along its margin, rises gradually toward the southwest. 

Local depressions in the plain are occupied by shallow alkaline lakes, which formerly had 

no outlet but now are drained into Jordan River. The soils oi the lowland are chiefly loam 

and sandy loam, but adjacent to the lake and in local low areas considerable clay is present.*

The nature of the underlying deposits is revealed by a number of well records, and (as 

would be expected) fine-textured materials are more abundant than nearer the mountains. 

A few deep wells have been sunk in this general region, proving the great thickness of the 

old lake deposits. The deepest is the Guffey-Galey well, drilled near the shore of the. lake, 

2 miles southwest of Farmington and about 10 miles north of Salt Lake City, in an unsuccessful search for oil.& This well was put down 2,000 feet without encountering bed rock. 

Another deep well is -that of the Rio Grande Western Railway at Salt Lake City, which 

was sunk through alternating beds of sand and clay, with very little gravel, to a depth of 

1,073 feet. This is the deepest well in the area under consideration, and its record (p. 42), 

as given by the driver, Gus Westphal, is as follows:

« A soil survey in Salt Lake Valley: Bull. U. S. Dept. of Agriculture No 64, 1900. 

& Boutwell, J. M., Oil and asphalt prospects in Salt Lake basin: Bull. U. S. Geol. Survey No. 2t>0, 

p. 471.
42 UNDERGROUND WATER IN VALLEYS OF UTAH.

Record of Bio Grande

Thickness 

in feet.

Thin strata of clay 

and sand. ....... 130

Clay and hardpan. . 

Red sand .........

Clay and hardpan . . 

Gray sand. .......

Clay and sand. ....

Sand.............

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

Sand .............

Sand.............

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

Sand .............

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

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

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

Blue sand ........

Sand and gravel . . . 

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

Gravel ...........

Gray sandy clay . . . 

Tough blue clay . . . 

Hardmn ........

. 40 

. 30

. 60

5

. 44

8

. 20

. 13

6

. 10

. 18

90

4"

. 10

19

c

. 30

. 10

1 

12 

4

. 28 

. 30 

3

Western Raili

Depth in 

feet.

1-130 

130-170 

170-200 

200-260 

260-265 

265-309 

309-317 ' 

317-337 

337-350 

350-356 

356-364 

364-374 

374-392 

392-412 

412-416 

416-426 

426-438 

438-443 

443-473 

473-483 

483-484 

484-496 

496-500 

500-528 

528-558 

558-561

vay Company's well at Salt Lake

Thickness 

in feet.

Sandy blue clay ....

Sandy gray clay ....

Clay and sand, alternating every 12 or 

18 inches. .......

Hardpan ..........

Sand and gravel .... 

Blue clay ..........

Gray clay .........

Sandy gray clay .... 

Quick sand ........

Blue clay ..........

Sandy blus clay .... 

Quicksand .........

Fine blue sand .....

Tough blue clay ....

Hard blue clay .....

40 

40 

2 

16 

18 

36 

10 

76

84 

8 

11 

16 

24 

13 

15 

21 

11 

10 

11 

3 

12 

2 

21 

4

City.

Depth in 

feet.

561-569 

569-609 

609-649 

649-651 

651-667 

667-685 

685-721 

721-731 

731-807

807-891 

891-899 

899-910 

910-926 

926-950 

950-963 

963-978 

978-999 

999-1,010 

1,010-1,020 

1,020-1,031 

1,031-1,034 

1,034-1,046 

1,046-1,048 

1,048-1,069 

1,069-1,073

Although the general composition of the old lake deposits is known, not enough information has been accumulated to enable very definite statements to be made concerning the 

detailed distribution of the sediments. "A comparison of available well records shows that 

the alternating bsds of sand, clay, and gravel, generally, can not be recognized as being 

equivalent in the several wells, and from the present evidence it appears that while there 

are great thicknesses of both sand and clay, which must have a more considerable lateral 

extent than the beds nearer the mountains, the lake deposits are lenticularly arranged. 

Sine? no correlation has been established, the structure of the lake deposits is not known. 

Apparently they are approximately horizontal, but with a slight inclination toward the 

lake from the highlands. This is indicated by the pressure obtained in artesian wells and 

is proved in a few instances by well records.

In the broad lowland west of Jordan River there is an abundance of water. Throughout 

practially all of this area ground water lies within 10 feet of the surface, and water is contained in the underlying deposits down to an unknown but considerable depth. Apparently 

flowing wells can be obtained anywhere within this area. Although the water is so generally distributed, it is profitably recovered only from the more porous, coarser textured 

deposits of sand and gravel, which constitute natural reservoirs and in which the water 

moves more readily. Accordingly, water is found at several horizons in the course of 

sinking a deep well. In the Rudy well, for instance, 1,002 feet deep, situated in sec. 5, T. 

1 N., R. 1 W., 25 water horizons from which surface flows were obtained are reported. A 

record of this well is not available, but "good strong" flows besides minor ones were 

recorded, respectively, at 400, 508, 685, 753, and 881 feet.

Though water is so abundant, this lowland region is thinly populated, the chief drawback 

to its settlement being the presence of much alkali in the soil over a considerable part of
OCCURRENCE OF UNDERGROUND WATER. 43

the area. The Bureau of Soils of the United States Department of Agriculture, in cooperation with the Utah Experiment Station, is at present engaged in a demonstration of the 

feasibility of reclaiming this land on a farm 3 miles west of Salt Lake City. But by no 

means all of the soils in this lowland area contain excessive amounts of alkali,a especially 

along Jordan River and adjacent to the border between the lowland and highland areas 

there are thriving settlements.

The map and list of wells show general conditions. The wells are grouped along the 

margins of the area, and few are located in the interior. In general they are 2 inches in 

diameter, but they vary in depth greatly. Although flows are obtained locally at only 30 

feet below the surface, commonly they are not encountered above 150 feet. Perhaps the 

average well is between 200 and 300 feet in depth. It is a striking fact that flows may be 

obtained throughout the entire area at similar, but not at regular depths, indicating only a 

slight inclination of the water-bearing horizons and their lenticular character. The flows 

are usually small, averaging perhaps under 5 gallons a minute, though there are a number 

of 15-gallon flows. The supply generally is reported rather constant, except that the 

shallower wells are subject to seasonal variation. The pressure obtained, too, generally 

is small, being only enough to cause the water to rise either barely to the surface or a few 

feet above. In general the pressure and the flow are reported to increase, with the depth 

but measurements are not available. Both the flow and the pressure are considerable 

in the deep Rudy well, sec. 5, T. 1 N., R. 1 W.

The conditions here noted apply mostly to the areas contiguous to the eastern and 

southern borders of the lowland west of Jordan River. Little information is available 

concerning the rest of this area (see list of wells pp. 59-75.) The few wells near Great Salt 

Lake were sunk to unusual depths before flowing water was obtained, this being apparently 

due to the greater development of clay in that region, though no complete logs have been kept. 

The well at the Inland Crystal Salt Company's works, in which, at a depth of 560 feet, water 

was struck which rises about 9 feet above the surface and flows about 10 gallons a minute, 

is reported 720 feet deep. Underground water in the Pleistocene deposits near the lake 

contains considerable salt.

EAST OF JORDAN RIVER.

East of Jordan River the occurrence of underground water will be described under 

the following heads: Salt Lake City, lowland area south of Salt Lake City, and upland 

area south of Salt Lake City.

SALT LAKE CITY.

Salt Lake City is built principally on the floor of the main valley, but its outskirts 

extend northward on the old delta of City Creek and eastward on the benches at the base 

of the Wasatch Mountains. Adjacent to the highlands the underlying deposits are very 

irregular in composition and distribution, consisting of'sand and gravel with intercalated 

streaks of clay. But toward the valley proper the conditions become more regular and 

the prevailing clay is interbedded with sand and gravel, though from the records obtained 

no definite sequence appears to be applicable to any considerable area.

In the lower part of the city marshy areas occur, but conditions there have been much 

improved since the early days of settlement. Formerly the lower channels of City, Red 

Butte, Emigration, and Parleys creeks were ill defined and at high-water stage the part 

of the city adjacent to Jordan River was a great slough. But by erecting embankments, 

by confining the creeks to definite channels, and by draining the western part of the city 

much of the swampy land has been reclaimed. Shallow ground water, except on the 

benches, generally lies within 10 feet of the surface.

The line separating flowing and nonflowing wells skirts the lower benches, so that in 

the larger part of the area occupied by the city artesian wells are obtained. Flows are found

"Soil survey in Salt Lake Valley: Bull. U. S. Dept. Agric. No. 64, 1900. Reclamation of Alkali 

ands: Fifth Kept. Bureau of Soils, 1903, p. 1144.
44 UNDERGROUND WATER IN VALLEYS OF UTAH.

at different horizons from about 50 feet downward, a common depth of wells being between 

100 and 300 feet. The deepest well is that of the Rio Grande Western Railway Company 

near its station, the record of which appears on page 42. This well is 4 inches in diameter 

and 1,073 feet deep. It was put down in 1895 and 15 horizons were passed through from 

which flows were obtained. At a depth of 1,048 feet the greatest flow occurred, amounting 

to 78 gallons a minute at 4 feet above the surface and to 37.5 gallons at 25 feet above. 

The most notable group of wells in this vicinity is that put down by Salt Lake City adjoining 

Liberty Park. There are 16 or more of these ranging from 2 to 9 inches in diameter and 

from 100 to 600 feet in depth. About half a dozen different water-bearing horizons, each 

furnishing a flow, are said to have been encountered in driving the wells. The greatest 

pressure reported caused the water to rise in a pipe 35 feet above the surface. Discharge 

measurements, as furnished by the city engineer, are given in the following table:

Discharge of city wells near Liberty Park, Salt Lalce City.

No. of 

well.

1....

2.... 

3.... 

4....

5.... 

6....

7.... 

8.... 

9....

Diameter.

Inches.

9 

9

8 

8 

8 

2 

2 

2 

2

Date of measurement.

Aug. 10, 

1890.

Gallons. 

201,600 

180,000 

279, 132

59, 040 

14,400 

16,000 

27,000 

54,000

July 17, 

1900.

Gallons. 

120,000 

297,000 

280,000 

215,000 

5,000 

10,000 

1,000 

500 

25,000

Sept. 29, 

1902.

Gallons. 

96,941 

60,588 

302,940 

193,882 

11,459 

5,876 

610 

206 

19, 784

No. of 

well.

10.... 

11.... 

12.... 

13.... 

14.... 

15.... 

16....

Diameter.

Inches. 

2 

2 

 2 

2 

2 

9 

2

Date of measurement.

Aug. 10, 

1890.

Gallons. 

43,200 

33,230 

36,000 

54,000

997, 602

July 17, 

1900.

Gallons. 

38,000 

19,000 

16,000 

35,000 

18,000 

98,000 

6,000

1,183,500

Sept. 29, 

1902.

Gallons. 

35,644 

15,892 

14,213 

20, 626 

13,316 

36, 172 

2,844

830,993

In the immediate vicinity of these wells there are a number of springs whose supply is 

maintained chiefly by seepage. The combined flow from these springs and wells is estimated to amount to a maximum of 2,500,000 gallons a day. In order to utilize this 

supply in the city mains a pumping plant would have to be installed, and a further disadvantage is the doubtful quality of the water. At present this source is used for street 

sprinkling and for feeding the lake in Liberty Park (PI. I).

In the northern part of Salt Lake City several thermal springs occur, the most conspicuous of which are the hot and warm springs. The hot springs issue at a temperature of 

about 130° from the Wasatch limestone at the western end of the spur of the mountains, 

with a discharge of about three-fourths second-foot,« and flow into Hot Springs Lake. 

The warm springs issue from unconsolidated deposits at the base of the spur about 2 miles 

southeast of the hot springs. The water is pumped to a slight elevation, from which it is 

piped to a sanitarium, the amount delivered being reported to average 350 gallons a minute. 

The temperature is 118° at the springs and about 100° at the sanitarium. Several other 

similar, but less important, springs occur, associated with the great Wasatch fault, along 

the base of the mountains between hot and warm springs.

The municipal water supply of Salt Lake City is derived from mountain streams and distributed through city mains. From this source there is an excellent supply of pure water 

under good pressure. The chief near-by available streams are City, Red Butte, Emigration, Parleys, Mill, Big Cot ton wood, and Little Cotton wood creeks. The discharges of 

some of these are given on pages 19-22. None of these except City Creek is entirely controlled by the city. Red Butte Creek is reserved for the army post at Fort Douglas, Emigration and Parleys creeks partly contribute to the city supply, and the others are used entirely for

a Measured by A. F. Doremus.
OCCURRENCE OF UNDERGROUND WATER. 45

irrigation and domestic purposes, under water rights owned by farmers. In order for 

Salt Lake City to utilize these streams it must buy the water rights or exchange with the 

farmers an equivalent amount of water obtained either from Utah Lake or from pumping 

plants.

The present public supply accordingly is obtained from City, Parleys, and Emigration creeks, ^he watershed of City Creek is protected from forest fires and from contamination, and floany of its springs are developed. The flow is distributed from settling tanks 

near the moirtfe of the canyon and from a reservoir on Capitol Hill having a capacity of 

approximately 1,000,000 gallons. The surplus waters of City Creek are allowed to escape 

through flood ditches. Water from Parleys Creek to the extent of 81.8 per cent of its flow 

has been obtained by Salt Lake City in exchange for an equivalent amount of water from 

Utah Lake delivered through the Jordan and Salt Lake City canal. A settling reservoir, 

holding somewhat less than 1,000,000 gallons has been constructed at the mouth of Parleys 

Canyon, whence the water is conducted through a concrete conduit to a storage reservoir 

with a capacity of about 5,000,000 gallons-situated on Thirteenth East street. An additional supply is obtained from a trench in the bed of Emigration Creek half a mile above 

the mouth of the canyon. This trench is approximately 150 feet long, 10 feet wide, and 

18 feet deep. It was dug in sand and gravel in the bed of the creek and at right angles to 

its course. A supply estimated to amount to 1,000,000 gallons a day is thus obtained, which 

is piped to the Thirteenth East street reservoir.

No direct record is kept of the amount of water used by Salt Lake City, but discharge 

measurements of the creeks at the mouths of the canyons show the amount available. 

This is insufficient during the dry months and the use of water is restricted to a per capita 

consumption of 120 gallons a day, although it is considered desirable, in this dry climate, 

where lawns and gardens have to be irrigated, to maintain a per capita supply of approximately 300 gallons a day. It is planned to obtain in the immediate future a portion of the 

flow of Big Cottonwood Creek, by exchanging therefor water from Jordan River, delivered 

through the City canal, as is being done in the case of Parleys Creek, and to make the new 

supply available by constructing a pipe line from the mouth of Big Cottonwood Canyon to 

the mouth of Parleys Canyon, a distance of about 7 miles.

SOUTH OF SALT LAKE CIT#.

Lowland area. It will be convenient to divide the area south of Salt Lake City into a 

lowland and an upland portion, taking as the dividing line that which separates flowing 

and nonflowing wells. PI. VIII shows that this line extends contiguous to, but below, 

the Jordan and Salt Lake City canal as far as Little Cottonwood Creek, after crossing 

which it turns westward to the flood plain of Jordan River. The lowland area is traversed 

by Parleys, Mill, Big Cottonwood, and Little Cottonwood creeks, which flow in open valleys, 

with broad and low intervening divides. The general aspect of the country is that of a 

slightly dissected plain that rises gently toward the upland terraces. This area is relatively 

thickly populated, and intensive farming is widely practiced.

The detailed character of the underlying lake sediments is not satisfactorily known, but 

from the well records conditions appear to be similar to those found elsewhere in the 

area under consideration. Beneath the lowlands the stratigraphy is more uniform than 

nearer the base of the mountains; fine-textured sediments are more abundant than coarse, 

and clay predominates. But a comparison of available well records fails to establish a 

correlation between the different beds of sand and gravel throughout the lowland. Well 

drivers state that all logs are different, and yet that, on the whole, general sections persist 

for certain areas in which the differences are minor. It is believed that the sediments 

slope toward Jordan River at about the same angle as does the surface. The best-defined 

sequence that has been reported occurs immediately south of Salt Lake City, where in 

general light-colored clay at the surface overlies blue clay ranging from 30 to 70 feet in 

thickness, beneath which water-bearing sands and gravels occur at a depth of about 100
46 UNDERGROUND WATER IN VALLEYS OF UTAH.

feet. At greater depths the succession appears to be more variable, but there are few 

satisfactory well records.

Ground water now lies within 10 feet of the surface over practically the entire lowland 

area, but it is reported that in the early days it did not lie so near over so large an area. 

Present conditions are largely due to irrigation. Several old residents state that below 

the level of the Jordan River canals the ground-water surface has locally risen 40 or 50 

feet since their construction. It has already been mentioned that along several of the 

drainage ways seepage water reappears at the surface and occasionally forms considerable 

streams, as at Spring Creek near its junction with Big Cottonwood Creek, where the September flow is estimated to amount to 14,000,000 gallons a day. In many places also, especially 

along the bases of benches, lines of seep springs occur that furnish considerable flows, a 

notable occurrence being those at the nursery in the southeastern part of Salt Lake City. 

But locally, as along the bluff east of Jordan River, north of the Bingham Junction 

smelters, the water appears at so low an elevation as to be of comparatively little use. 

When pumping becomes more generally practiced in the valley this ground water that lies 

so near the surface can be easily developed.

Flowing wells in this area are numerous. They are generally 2 inches in diameter and 

100 to 400 feet in depth, and they commonly yield between 20 and 50 gallons a minute, 

though there are many variations. The pressure is low, generally less than 10 pounds. 

Well drivers say that their best results are obtained in belts extending northwest and 

southeast, parallel with the creeks, and that these productive belts are separated by relatively barren ones. The water-bearing sands and gravels apparently mark the courses 

of old waterways, while finer-textured material was deposited in the intervening areas, 

These distinctions have been noticed only in the upper parts of the lowland area, and near 

the river they are said to disappear. One of the best wells is at the plant of the American 

Smelting and Refining Company at Murray. It is 4 inches in diameter, 400 feet deep, and 

is reported to flow about 400 gallons a minute under a pressure of 3 pounds per square inch. 

The record of this well is given as follows, on the authority of H. F. Yeager, well driller:

Record of American Smelting and Refining Company's well at Murray.

Thickness Depth 

in feet, in feet. 

Sand and gravel............ 5 0-5

Mud....................... 3 5-8

Sand and gravel............ 4 8-12

Blue clay.................. 6 12-18

Quicksand. _.._._........ 10 18-28

Blue clay.................. 8 28-36

Loose sand and gravel (good

pump well at 42 feet)...... 16 36-52

Jlue clay ................'.. 8 52-60

Quicksand (flow at 63 feet)... 6 60-66 

Blue clay.................. 18 66-84

Yellow clay................. 6 84-90

Loose sand and gravel (strong

flow at 95 feet)........... 15 90-105

Yellow clay................ 3 105-108

Coarse gravel and rock (strong

flow at 112 feet, and at this

point the well at office

stopped flowing).......... 8 108-116

Coarse gravel and rock...... 6 116-122

Quicksand................. 20 122-142

Clay, very hard............. 10 142-152

Quicksand................. 6 152-158

Gravel (small flow at 165 feet) 11 158-169

Thickness

in feet. 

Hard pan, very hard........^ 8

Blue clay.................. 6

Quicksand (flow at 203 feet).. 20 

Quicksand................. 16

Blue clay.................. 4

Quicksand................. 7

Blue clay.................. 8

Quicksand................. 18

Blue clay and quicksand in 

layers 2 feet thick........ 22

Quicksand................. 8

Blue clay, very hard......... 12

| River sand................. 2

i River sand................. 7

I Cemented gravel............ 12

I Yellow clay................ 7

Cemented gravel............ 17

Loose gravel............... 23

Yellow clay................ 2

Gravel..................... 7

Cemented gravel............ 12

Loose gravel............... 12

Depth 

in feet. 

169-177 

177-183 

183-203 

203-219 

219-223 

223-230 

230-238 

238-256

256-278 

278-286 

286-298 

298-300 

300-307 

307-319 

319-326 

326-343 

343-366 

366-368 

368-375 

375-387 

387-399
OCCUREENCE OF UKDEEGROUND WATEE. 47

Decrease in flow and complete failure of some wells are reported throughout this area 

and are especially apparent in the vicinity of Murray. These results are directly traceable 

to the increased number of wells that have been sunk in recent years and to the fact that 

little economy is exercised in the use of the water. Well owners should more fully realize 

that the limited water supply comes from a common source, that the wastefulness of one 

counteracts the prudence of another, and that the common interest of all demands that 

the supply be conserved.

Upland' area. The upland south of Salt Lake City includes the area lying between the 

base of the Wasatch and Traverse mountains and the area in which flowing wells can be 

obtained. This region is characterized topographically by the abundance and perfection 

of development of shore phenomena which mark different stages in the history of Lake 

Bonneville. As on the western side of the valley, the upland is in general a plain that 

rises toward the base of the mountains, but is interrupted by benches and escarpments 

and deeply cut by the creeks flowing from the Wasatch Mountains.

The Bonneville terrace extends along the mountains like a narrow shelf, its horizontal 

lines contrasting strongly with the deep, vertical furrows on the mountains. Broad deltas 

formed by the larger creeks at the Provo stage extend down to the lowlands, and successive 

escarpments mark halting places in the retreat of Lake Bonneville. The most prominent 

of all the shore phenomena in the area covered by this report is the great embankment at 

the point of the mountains east of Jordan Narrows. Here the waves, gaining energy from the 

wide expanse of the old lake, carved a great sea cliff against the mountains and distributed 

the debris to form an enormous accumulation of sand and gravel.

Prominent local features of this upland belt are the relics of glaciers adjacent to the mouth 

of Little Cottonwood Canyon and the evidences of recent faulting along the base of the 

mountains. Little Cottonwood Creek in Pleistocene time was occupied by a glacier which 

carved a broad U-shaped valley and deposited lateral and terminal moraines composed of 

a heterogeneous mass of coarse- and fine-textured debris. Along the entire front of the 

Wasatch Mountains Gilbert has found indications of recent dislocation associated with the 

great Wasatch fault. The evidence is varied, but escarpments in unconsolidated material 

breaking the even trend of alluvial slopes are conspicuous.

The underlying deposits of the upland are mostly coarse textured, being near their origin, 

and consist chiefly of sand and gravel. The creeks, where they have cut deeply, expose 

good sections, but few deep-well records were obtained.

This region in general is thinly populated, but where water is available there are settlements, 

and wherever the canals extend there are thriving farms. The contrast between the 

flourishing area which is supplied with water and the dry, barren region is striking. The 

map shows the distribution of the principal canal systems, which are supplied by the several 

creeks that flow from the Wasatch Mountains and by Jordan River. Underground water 

is used only to a limited extent. PI. VI and the list of wells illustrate conditions. Underground water is recovered chiefly in the lower (western) part of the upland, where it lies at 

depths ranging from the surface to 50 feet below. In this productive area both dug and 

driven wells are used. The driven wells are commonly 50 to 200 feet in depth, and water 

is generally found beneath a bed of cla'y in sand or gravel under sufficient pressure to cause 

it to rise within pumping distance of the surface.

In the eastern part of the upland area ground water generally lies at a greater depth than 

50 feet below the surface, and in a number of places has not been found in test wells over 

100 feet deep. In this (eastern) division of the upland, where the greater part of the valley 

deposits are coarse textured, the ground water sinks deep before a relatively impervious 

bed is encountered, and then it tends to move to the lower part of the valley. Away from 

the influence of seepage from the creeks little water is supplied to this area. Between the 

creeks the chief source of supply is seepage from the mountains. The most likely localities 

for sinking wells are along the courses of waterways, but over a large part of the upland the 

prospect is poor for obtaining underground water in quantity within easy reach of the surface. In the mouths of the canyons there is the chance of developing the underflow by
48 UNDERGROUND WATER IN VALLEYS OF UTAH.

subsurface dams or by tunnels, mentioned on page 40. Other favorable localities for prospecting are adjacent to the base of the mountains, where water may be had by developing 

springs and by tunneling into the bed rock.

Seep springs occur at several localities along the base of the mountains south of Salt Lake 

City, the most important, perhaps, being those about midway between Mill and Big Cottonwood canyons. The feeble springs there issuing from sand and gravel were formerly allowed 

to go to waste, but by developing them a flow of about 2 second-feet was obtained, and a 

considerable tract of land thus became available for agriculture. About 4 miles southwest 

of the town of Draper, in sec. 12, T. 4 S., E. 1 W., at some distance from the base of the 

mountains, there are four warm-water lakes that are fed by springs, some of which are said 

to be quite hot. The westernmost of the group is the largest and covers an area of about 5 

acres. The temperature is reported to remain at about 70° the year round.

Since underground water is so scarce beneath the upland, the most efficient manner of 

developing this area appears to be by the use, as suggested above (p. 38), of creek water in 

high-level canals to a greater extent than is now practiced.

UTAH LAKE VALLEY.

The following description of the occurrence of underground water in the valley of Utah 

Lake begins at the north and proceeds east, south, and west around the lake, the several 

towns affording subheadings for convenient reference. (PI. VIII.)

LEHI AND VICINITY.

Lehi is situated in the main valley at some distance from the distinct terraces. Dry 

Creek lies adjacent to the town, but, as its name signifies, the creek, after supplying a number of irrigation ditches, usually carries little or no water in its lower course. There is no 

public water system in the town, and the supply for domestic purposes is derived from 

numerous wells. A few shallow dug wells tap ground water at depths of 5 to 30 feet, but 

the majority are deeper and reach water under pressure. The sugar-plant mill pond is fed 

by springs and is an important local source of supply.

Lehi was one of the first towns where artesian water was found in the Bonneville area, 

flowing wells having been obtained there about 1880. Formerly a feeble first flow was 

found in gravel about 60 feet from the surface and a stronger supply at a depth of about 

160 feet, but in recent years flows, even from the second horizon, have failed during part 

of the season in consequence of the increased use of artesian wells in the area nearer the 

lake, and at times pumping has to be. resorted to. However, when water does not 

actually flow it rises in the wells to within a few feet of the surface.

The general section in the vicinity of Lehi, as reported by H. C. Comer, shows blue clay 

to a depth of 50 or 60 feet. Below this is the first water bed, consisting of about 50 feet 

of sand and gravel, separated from the second water horizon by 40 feet of light clay. This 

section does not apply in the eastern part of the town, where the log of the San Pedro Railroad well shows coarse-textured material within 100 feet of the surface. In this well the 

main supply is derived from a depth of 330 feet, the water rising to within a few feet of the 

surface. These two logs illustrate the variability of adjacent sections.

The Utah Sugar Company's plant at Lehi has several 2-inch wells, and the following flows 

in gallons per minute are reported: 80 feet, 15 gallons; 120 feet, 25 gallons; 150 feet, 20 

gallons. Logs of these wells were not kept. The Eio Grande Western Eailway well near 

the sugar factory is 3 inches in diameter and 165 feet deep. The water is reported to rise 

in a pipe to a point 30 feet above the surface and to flow about 50 gallons a minute at the 

level of the ground.

Toward Utah Lake, below Lehi, there is a considerable development of flowing wells 

from which a number of square miles are irrigated. In this district there are several 

hundred flowing wells which average about 150 feet in depth. A close relationship has 

been established between the flow of the wells in the fields below Lehi and those in town.
WATER-SUPPLY PAPER"NO. 157 PL. VIII

V/////////A

Area in which flowing 

wells are obtained

^

Base of mountains, approximate position of the 

BonneY-iUe shore liua

 Wells the recbrcLl 

of which are shown on 

Plate V

SCALE

MAP SHOWING THE AREA IN WHICH FLOWING WELLS ARE OBTAINED IN UTAH LAKE VALLEY.
OCCURRENCE OF UNDERGROUND WATER. 49

During the irrigation season, when the field wells are all flowing, those in Lehi practically 

stop, but during the winter-it is a general custom to plug the wells used for irrigation, after 

which those in town begin to flow. Measurements have not been made, but the general 

facts are well established.

Northwest of Lehi the line separating the areas of flowing and nonflowing wells continues 

to Jordan River, reaching it 3 to 4 miles north of Utah Lake. The line extends about half 

a mile west of the river and approaches close to the northv/est corner of the lake near Saratoga Springs. In the flood plain of Jordan River flows can probably be obtained continuing 

into Salt Lake Valley, but outside of the line indicated the surface elevation is too great.

The Salt Lake City authorities, about 1890, sank a number of wells in the flood plain of 

Jordan River in sec. 12, T. 5 S., R. 1 W., with the object of increasing the supply of the 

Jordan and Salt Lake Canal. These wells, about 130 in number, were mostly 2 inches in 

diameter, though a few were 6 inches, and are said to average 100 feet deep. Clay was 

encountered down to the bottom of the wells, which were in gravel. It is stated that 

water rose in pipes 30 to 40 feet above the surface, and that individual wells flowed 125 

gallons a minute. It is also stated that the combined flow amounted to 3,000,000 gallons 

a day. These wells soon interfered with neighboring ones, stopping their flow, and suit 

was brought against the city, with the result that the municipality was compelled to plug 

up its wells. After these had been plugged for some time, a number of them were temporarily opened, and in about twenty-four hours thereafter the water in one of the wells, the 

flow of which was interfered with, situated about half a mile above the city wells, had fallen 

2J feet. The city wells were then capped again and in five hours the water in the well 

referred to had regained 7 inches of its lost level.

Near the northwestern end of Utah Lake there is a group of hot springs which occur both 

on shore and in the lake. On the shore there are several springs which support the Saratoga 

resort where the water, having a temperature of 111°, issues through the lake deposits and 

is used for bathing and to a limited extent for irrigation. In the summer of 1904, during 

the survey of Utah Lake by G. L. Swendsen of the Reclamation Service, three groups of 

springs were found beneath the water of the lake. Their existence was shown by the presence of depressions occupying areas of 100 square feet to 3 acres in extent and having depths 

of 20 to 80 feet. Since the prevailing depth of the lake is much less and the bottom is composed of slimy mud, a considerable discharge is thus indicated. Hot water that flowed 

above the lake surface was obtained by sinking pipes a short distance into the bottom.

About 5 miles up Dry Creek from Lehi is the town of Alpine, located near the mouth of 

the canyon on the dissected Bonneville terrace. The settlement is supplied with water 

from irrigation ditches, and possibly not more than half a dozen wells have been sunk. 

These are 25 to 80 feet deep, and the water level is reported to vary considerably between 

winter and summer. Springs occur in Dry Creek Canyon, but they have not been developed.

AMERICAN FORK, PLEASANT GROVE, AND VICINITY.

The towns of American Fork and Pleasant Grove receive their main water supplies, 

respectively, from American Fork and from Battle and Grove creeks. These streams 

feed a number of irrigation canals, and are the chief source of underground water in this 

vicinity. (PI. IX, B.)

American Fork is built at the base of a series of terraces on both sides of American 

Fork (creek), which has cut a narrow channel through the old lake deposits. Ascending 

the valley from American Fork, five distinct terraces can be traced up to the broad Provo 

bench, between which and the Bonneville level, which forms a shelving bench against the 

mountains, traces of shore lines of pre-Bonneville age have been reported. In its lower 

course American Fork is dry throughout most of the year in consequence of the draft 

upon its waters for the canal system which supplies the uplands.

Shallow wells in American Fork are commonly less than 50 feet in depth, averaging 

possibly 25 to 30 feet, and the ground-water level is reported to vary 10 to 15 feet between 

the winter minimum and summer maximum. The water generally is found in gravel. 

IRR 157 06 4
50 UNDERGROUND WATER IN VALLEYS OF UTAH.

Deep wells have been sunk in the extreme southwestern part of the town in search of 

flowing water. The water rises in these nearly to the surface, and furnishes the main supply for domestic purposes. Well records show a variable succession of Sand and gravel, 

with comparatively little clay. The city well is typical, and probably is the deepest in 

this vicinity. It is 440 feet deep and 6 inches in diameter. Two principal water horizons are reported, at 240 and 340 feet, and the water stands in the well at a depth of 22 

feet. An electric motor pump supplies water for public purposes, but there is no waterworks system. Individual families or groups of families maintain their own wells.

The line separating the areas of flowing and nonflowing wells as mapped between Lehi 

and Pleasant Grove lies contiguous to the San Pedro Railroad, and here, as elsewhere, 

ground Water commonly lies within 10 feet of the surface. Extensive areas of marshy 

land lie contiguous to the lake shore, where conditions have grown worse since the introduction of irrigation. The flowing wells in this vicinity vary in depth, but are commonly 

about 100 feet deep. As Utah Lake is approached more nearly uniform conditions are 

revealed by the logs. Clay is commonly present at the surface and continues to a depth 

of 90 or 100 feet, below which the water-bearing gravel occurs. In the deeper wells alternating sand, clay, and gravel are reported below the first gravel, and flows are obtained 

from every coarse-textured bed. One of .the best wells in this vicinity is in sec. 23, T. 5 

S., R. 1 E. It is 147 feet deep, 2 inches in diameter, and throws a stream 3 feet 8 inches 

above the pipe, having a capacity, therefore, of about 150 gallons a minute.

A disturbed belt of rocks, dipping eastward, and locally covered by debris, lies near 

the foot of the Bonneville terrace between American Fork and Grove, creeks. Springs 

occur at about this horizon, and prospecting for water in this belt, in sec. 17, T. 5 S., R. 

2 E., has brought notable -results. William Wadley & Sons, by tunneling into bed rock, 

have developed enough water to irrigate a number of acres of fruit land, which is bringing 

in handsome returns. Several tunnels have been dug, the most important of which lies 

about 200 feet below the Bonneville level and was driven 318 feet through black shale 

into broken and cavernous gray limestone, in which the water occurs.

Pleasant Grove is located on alluvial slopes formed by Battle and Grove creeks. Its 

situation is so high that flowing wells can be obtained only in the extreme lower part of 

the town, which depends for its chief underground supply on wells from which water has 

to be pumped. Ground water can usually be. obtained at 10 to 50 feet from the surface. 

No regular sequence of deposits underlies the town, but a variable succession of clay, sand, 

and gravel is encountered in wells, the water horizon usually being underlain by clay. In 

the southeastern part of Pleasant Grove no successful wells have yet been obtained, though 

prospecting for them has extended to a depth of 100 feet: not deep enough to find an 

impervious stratum. A continuous succession of gravel beds is reported.

The high, almost flat Provo delta between Pleasant Grove and Provo is scantily provided with water. The surface is generally gravel covered, and gravel is commonly found 

in wells to depths of 30 to 60 feet, below which sand is reported. Only a small amount of 

clay appears to be present. This tract of land is well adapted for the cultivation of fruit, 

but the present supply of water is insufficient for its complete development. Water was 

first brought to the delta by canals from Provo River in 1868, and the present supply, 

whereby a maximum diversion of about 116 second-feet is obtained, was established in 1888. 

Before irrigation was practiced on the bench the depth to ground water was considerably 

greater than it is now. Old wells are over 100 feet deep, but of late years the groundwater surface has risen so that on a large part of the area water can be obtained in wells 

averaging 50 to 75 feet deep. Toward the lower margins of the bench the depths to ground 

water is less than 50 feet. Here, as elsewhere throughout this entire area, ground water 

is lowest in the winter and highest during the irrigation season. The annual variation 

on Provo bench appears to range from 5 to about 17 feet. A few examples will illustrate 

general conditions. In 1875 a dry well 100 feet deep was dug in sec. 14, T. 6 S., R. 2 E. 

In the same section, during the winter of 1878-79, N. Knight dug a well 110 feet deep which 

afforded 3 feet of water in winter and 15 to 20 feet in summer. In 1899 N. J. Knight
U. S. GEOLOGICAL SURVEY WATER-SUPPLY PAPER NO. 167 PL. IX

A. VALLEY OF PROVO RIVER BELOW MOUTH OF CANYON, LOOKING NORTH. 

Shows Provo Bench and Bonneville terrace.

B. AMERICAN FORK AT MOUTH OF CANYON.
OCCUEEENCE -OF UNDERGROUND WATER. 51

dug a third well only 60 feet deep, near the second, which afforded about 3 feet of water 

in winter and 20 in summer.«

Flowing wells can not be obtained on the bench because of its elevation, though several 

attempts have been made, without success. In 1887 and 1888 two deep wells were driven 

in the same section as those just referred to. The Colorado Fish Company put down a 

3-inch well 250 feet deep and obtained water which rose to within 80 feet of the surface. 

This was pumped for several years. In 1888 Mr. Knight drove a 2-inch well 300 feet 

deep in which water rose to within 90 feet of the surface. Both of these wells are now 

abandoned.

From Provo to Pleasant Grove along the narrow belt of lowland lying between Provo 

bench and Utah Lake there is an abundance of underground water. The line that separates flowing and nonflowing wells coincides approximately with the San Pedro Railway, 

which also marks roughly the upper limit of the area in which ground water lies within 

10 feet of the surface. Between the railroad and the base of the bench few wells have 

been driven and little is known of the conditions, but it is thought that water can be 

obtained at depths of 10 to 50 feet.

Contiguous to the railroad a number of feeble seep springs occur along the base of a 

low bluff between which and the lake the ground is almost flat. Water occurs on the 

surface in many places, rendering the land unfit for use. Before irrigation was so extensively practiced it is reported that this lowland belt was fertile farming land, but in late 

years, due to the rise of the ground-water level, the land has materially decreased in value. 

Considerable areas of available land, however, are yet to be found in this area, and flowing 

wells are used to irrigate several hundred acres. Conditions can be much improved by 

drainage. The map and list of wells show the general conditions. The deep wells in 

this belt average slightly over 100 feet and generally are 2 inches in diameter. North 

of Provo River the yield is inconsiderable, averaging, possibly, less than 15 gallons a minute 

per well; but in the vicinity of Geneva, a resort on the lake below Pleasant Grove, the 

effect of Battle Creek drainage is experienced, and some of the strongest wells of the entire 

area covered by this report occur. Harry Gammon's wells, in sec. 7, T. 6 S., R. 2 E., are 

among the best. One of these is 3 inches in diameter, 110 feet deep, and yields a flow of 

about 266 gallons a minute, the water rising in a pipe to approximately 28 feet above the 

surface. The section in this vicinity is shown on PI. V, the water occurring in gravel in 

the bottom of the well.

PEOVO AND VICINITY.

Provo derives its water supply from Provo River. A number of canals tap the river 

(as shown on the map, PL VIII), and distribute a good supply to the town; and water 

for household purposes is delivered through city mains from a direct source in the river 

near the mouth of the canyon. The quality is unsatisfactory, however, and a new system 

is being installed whereby a better supply is obtained from a number of springs that issue 

from unconsolidated debris along the base of the canyon for several miles above its mouth.

Well records show fairly uniform stratigraphic conditions about Provo. Gravel usually 

underlies the surface to a depth of from 10 to 20 feet, and is succeeded by 20 to 30 feet of 

sand, below which is a considerable thickness of clay, averaging possibly 100 feet, the 

upper 20 or 30 feet of which is yellowish and the lower part blue. Underlying the clay a 

bed of gravel occurs, which is said to be underlain by clay, though about Provo it has seldom been penetrated. With minor variations this section appears to hold good over a 

large part of the territory adjacent to the east shore of Utah Lake. Northwest from Provo 

the surface gravel disappears, but clay, light above and dark below and underlain by sand 

and gravel, is reported in the vicinity of Geneva, American Fork, and Lehi. South of 

Provo, in the vicinity of Springville, similar conditions prevail. (PI. V.)

a These facts were obtained from Mr. Caleb Tanner, to whom the writer is indebted for many 

courtesies.
52 UNDEEGEOUlSrD WATEE, IN VALLEYS OF UTAH.

The beds about Provo appear to dip toward the lake at a low angle, approximately corresponding to the slope of the surface, this being indicated by the fact that the depth at 

which the water-bearing gravel is found over large areas is approximately constant. In 

the vicinity of Provo some direct data were obtained on this point. Wells have been driver 

along Center street from Academy street in Provo westward to the shore of the lake. The 

depths at which the top of the gravel was struck in some of these wells was obtained from 

the driver, J. Westfall, and a line of levels was run along the surface by the United States 

Reclamation Service, from which it appears that the lakeward inclination of the gravel ip 

approximately 9 feet per mile, the rate decreasing as the lake is approached. Similar 

conditions probably exist throughout the area studied, the slope being greatest near the 

mountains, while beneath the broad lowlands the strata lie more nearly horizontal.

Ground water in the vicinity of Provo can generally be obtained in the upper grave1 

within 10 feet of the surface. In the vicinity of the lake the gravel disappears and clay 

generally occupies the surface. Here, as is so general throughout the entire area, swampy 

conditions prevail, owing to the lowness of the region, the recession of the lake, and the 

rise of ground water due to irrigation.

Flowing wells exist in great number in this well-populated region, and in general ar 

abundance of good water is obtained within 200 feet of the surface. The main water-bearing horizon is the bed of gravel that underlies the blue clay. Water is generally reached 

in this gravel at 150 to 200 feet from the surface, but conditions are not absolutely unifonr 

at all places, and where the prevailing section is varied by local streaks of clay, sand, and 

gravel corresponding differences exist. Feeble flows are sometimes found at 100 feet, and 

a few wells obtain water from a depth of 360 feet, but this depth is unusual in the vicinity 

of Provo. The wells about Provo are generally 2 inches in diameter, and their flow may 

possibly average 50 gallons a minute. Among the best wells in this vicinity are those at 

the stations of the San Pedro, Los Angeles and Salt Lake Railroad and the Rio Grande 

Western Railway. These are 3 inches in diameter and 190 and 176 feet deep, respectively. 

In November, 1904, the Rio Grande Western well was found to flow approximately 120 

gallons a minute at 2 feet above the surface under a pressure of 15J pounds per square inch.

SPKINGVILLE AND VICINITY.

Between Provo and Springville the lowland contiguous to Utah Lake extends to the Rio 

Grande Railroad, above which the surface rises at a steep grade to the base of the mountains. The lowland for the most part is marshy, and the line that separates flowing and 

nonflowing wells lies only a short distance east of the railroad. A low scarp, which apparently marks a Pleistocene fault, can be traced immediately west of the county road for a 

mile or more beyond the Utah County Infirmary toward Springville. Springs occur at 

the base of the scarp, and the large springs at the head of Spring Creek may be associated 

with faulting. A number of small lakes mark the presence of these springs, and Spring 

Creek, whose main supply is thus derived, flows about 1,600 second-feet.

The deepest well in this area is that of the infirmary, situated near the road about midway between Provo and Springville. The well is 3 inches in diameter and 270 feet deep, 

and water is reported to rise in a pipe to a point 3 feet above the surface, flowing about 30 

gallons a minute. In this vicinity a feeble first flow is reported at depths of 65 to 80 feet.

Springville is situated on the plain about 3 miles below the mouth of Hobble Creek Canyon, the channel of the creek passing through the town. During the irrigation seasor 

practically all of Hobble Creek water is diverted by canals that head near the base of the 

mountains.

Ground water in Springville is obtained from wells that usually range in depth from 20 

to 30 feet, the water occurring in the top gravel. The general level of ground water in the. 

town is reported not to have changed since the early days, and only an annual difference 

of a few feet is noticed between winter and summer conditions-^

o Stevenson, J. B., well driver.
OCCURRENCE OF UNDERGROUND WATER. 53

Records of wells in the vicinity of Springville show rather uniform conditions. The town 

generally is underlain by gravel 5 to 40 feet thick, below which blue clay occurs to a 

depth of about 130 feet, underlain by sand and gravel down to 180 feet; then about 50 

feet of light-colored clay is encountered, followed by sand and gravel at a depth of about 

230 feet. In the area nearer the lake the top gravel generally is wanting, but otherwise 

similar sections are reported in that locality.

Flowing wells are obtained from the two lower gravel horizons at depths of approximately 130 and 230 feet. The common occurrence of water at these two horizons implies 

unusual uniformity of underground conditions, and suggests a low lakeward dip, approximately corresponding to the surface inclination. The wells are commonly 2 inches in diameter, though a few are 3 inches, and they yield on an average possibly 20 to 50 gallons a 

minute. One of the best in Springville is a 3-inch well belonging to A. Cox. It is 230 feet 

deep, flows about 120 gallons a minute, and its water is reported to rise in a pipe to a point 

18 feet above the surface. The Rio Grande Railway Company has two wells in Springville, which are 216 and 304 feet deep. In the deeper the first flow was struck at 126 feet, 

a second at 216, a third at 260, and a fourth at 292. The shallower well is 3 inches in diameter, and is reported to flow about 200 gallons a minute at the surface, which is reduced to 

about 12 gallons a minute at the top of a tank about 30 feet above the surface.

Mapleton Bench is the local name for the Provo Delta, lying between Spanish Fork and 

Hobble Creek. The delta is here prominently developed, and constitutes valuable farming land. Flowing wells are not obtained on Mapleton Bench because of its elevation, but 

there are a number of dug wells. It is reported that in the early days the wells on the 

bench were 60 feet or more in depth, but since irrigation has been practiced the groundwater level has been considerably raised, and now the wells average possibly only 30 feet 

in depth. There is a marked difference in the depth to ground water in winter and summer, the range in some instances amounting to over 10 feet. Along the outer margin of 

the bench there is a line of springs, many of which did not exist before the ditches were 

dug. Big Hollow Creek, a stream that flows from the bench about 2 miles south of Springville, is a conspicuous example. In the early days scarcely any water is said to have 

flowed in its channel, whereas it now irrigates over 100 acres.

Considerable amounts of water are obtained by a few tunnels that have been dug along 

the eastern edge of Mapleton Bench. The entrances to the tunnels are commonly at the 

sites of springs. Some begin and end in unconsolidated materials, while others penetrate 

bed rock. The. longest noted is in sec. 24, T. 8 S., R. 3 E. Its length is 275 feet. Water 

enough to irrigate about 100 acres comes through crevices in bed rock.

SPANISH FORK, PAYSON, AND VICINITY.

The town of Spanish Fork is situated on the general lowland at the base of Mapleton 

Bench and immediately north of Spanish Fork, about 5 miles below the mouth of its 

canyon. From the few well records available it appears that sand and gravel commonly underlie the surface to a depth of about 30 feet and are succeeded by 150 feet of 

clay, below which water-bearing gravel is usually encountered at a depth of 180 feet. The 

log of the well recently completed at the San Pedro station, about a mile west of the town, 

shows a greater thickness of clay, amounting to 205 feet, beneath which sand and clay were 

found to 390 feet, where water-bearing gravel occurs.

Spanish Fork is rather poorly supplied with underground water. Dug wells commonly 

reach water at depths ranging from 10 to 25 feet, but its quality is not good. Flowing 

wells were formerly obtained, but in recent years the flows generally have ceased and pumping has to be resorted to. A city waterworks system was installed in 1904, the supply 

being derived from Evans Spring, near the mouth of Spanish Fork Canyon, about 5 miles 

above the town, and an excellent supply is now available. The line separating flowing 

and nonflowing wells now lies in the extreme northwest corner of the town. The first flow 

occurs at a depth of about 180 feet and a second flow between 350 and 400 feet. The creamery well, 2 inches in diameter and 220 feet deep, is typical. Water was struck at 180 feet
54 UNDEEGEOUND WATEE I1ST VALLEYS OF UTAH.

which in 1900 flowed 9 gallons a minute, while in 1904 it stood about 4 feet below th" 

surface with little or no variation. In 1904 the San Pedro, Los Angeles and Salt Lake 

Railroad Company put down a well 415 feet deep at its Spanish Fork station and obtained 

a flow of 36 gallons a minute through a 2-inch pipe from gravel in the bottom of the wel1 -

Between Spanish Fork and the Goshen divide there are a number of settlements tha.t 

are adjacent to the line separating flowing and nonflowing wells.

Salem is situated at the lower end of the Provo Bench, about midway between Spanish 

Fork and Payson. In the northwestern part of the town the water table lies close to the surface and throughout the greater part of the settlement water can be obtained within 10 feet cf 

the surface. There are many springs, the most important of which supply Salem Pond, which 

covers about 13 acres ,and averages possibly 12 feet in depth. The line separating flowing 

and nonflowing wells passes about midway through Salem. The flowing wells are generally feeble and the quality of the water is poor. A first flow is commonly obtained at 

about 160 feet and a second at about 250 feet.

Payson is situated on and near the delta formed by Peteneet Creek at the Provo stage 

of Lake Bonneville, part of the town being built on the delta and part on the subjacent 

plain. Flowing wells are not obtainable because of the elevation, and the underground 

water supply is furnished by dug wells. These vary considerably in depth because of the 

irregular distribution of the delta deposits. Their depth ranges from 15 to 115 feet and 

probably averages between 30 and 40 feet. As an instance of local variation it may be 

mentioned that in one well ground water is obtained at 18 feet while on the opposite side 

of the street a well was dug 90 feet without encountering water. The level of ground 

water is reported to fluctuate but little. A number of families in Payson are supplied by 

pipe lines, the water being derived from tunnels driven into the base of the bench.

The town of Spring Lake is situated near the base of the mountains. The line separating 

flowing and nonflowing wells passes along the foot of the Provo Bench and lies about hal" 

a mile west of the town. In this locality ground water is found commonly within 10 fee* 

of the surface and there are a number of shallow wells, but the chief supply comes froir 

springs. Spring Lake covers an area of about 12 acres and discharges a stream of abou4; 

2 second-feet. It is made by damming a small creek that is fed by springs. Springs occur ir 

the vicinity of the base of the mountains between Spanish Fork and Spring Lake. Most o* 

them appear to be seep springs, but some that lie near faults that adjoin the base of the 

mountains may be of deeper seated origin. Many of the springs flow 20 to 50 gallons a minute.

Santaquin is built on a delta of Santaquin Creek, near the base of the mountains, far 

above the general level at which flowing wells are obtained. The town is chiefly supplied 

with water for both household and irrigation uses by Santaquin Creek, and only a few 

wells have been dug. About a dozen wells strike water in gravel at depths of between 15 

and 25 feet on a low bench in the southeastern part of the town. Tunnels are also dug into 

this bench, from which two pipe lines supply a number of families with water. Below the 

bench in Santaquin there are very few wells; two had to be dug about 80 feet before water 

was obtained.

Below the line separating flowing and nonflowing wells between Hobble and Santaquir 

creeks the valley plain slopes gently to Utah Lake. Throughout this area ground water 

lies within 10 feet of the surface, and adjacent to the lake and in certain isolated localitier 

swampy conditions occur. This area is mostly underlain by clay, which is reported tc 

predominate in all of the wells. Little or no gravel is encountered in well driving and the. 

layers of clay alternate with layers of sand. Few satisfactory well records from thif 

region have been obtained, and no con-elation of the underground deposits has been possible. Different conditions seem to exist in neighboring wells, indicating a lenticular arrangement of the deposits.

The towns of Palmyra, Lake Shore, and Benjamin are situated below the line of flowing 

wells. Many farms are scattered over this area, but in a few localities north of Spanish 

Fork, for instance alkali is so prevalent as to discourage settlement. Much of the water 

used in irrigating this tract is derived from canals supplied by Spanish Fork, but flowing 

wells also are used to a considerable extent.
OCCURRENCE OF UNDERGROUND WATER. 55

Plowing wells have been obtained throughout this area at depths of 50 to 500 feet, as 

shown by the list. Flows are usually found in every considerable bed of sand encountered 

in drilling, and six or more water-bearing beds are sometimes struck in a 400-foot well. 

Shallow wells are not the rule in this region, for, though many are 150 to 200 feet deep, the 

majority are nearer 400 feet deep. Because of the general absence of gravel and of persistent beds of sand there are few especially good wells. The flows obtained are generally 

under 50 gallons a minute and frequently are less than 10. The pressure is low, seldom 

being sufficient to cause the water to r'se more than a few feet above the surface.

At the southern end of the lake, north of West Mountain, just above low-water level 

there is a warm spring that was estimated to flow 200 gallons a minute. Its temperature 

is 88°.

GOSHEN VALLEY.

Goshen Valley can be divided into a highland and a lowland portion, a convenient line 

of division for present purposes being that which separates areas where ground water lies 

above 10 feet from the surface, from those in which it lies below that depth. The highland lies contiguous to the mountains and merges into the lowland which adjoins the lower 

course of Currant Creek and the southern extremity of Utah Lake. The lowland is chiefly 

underlain by clay and the soils contain abundant alkali.a Throughout the entire area 

ground water lies close to the surface and marshy conditions exist, especially toward the 

lake.

The area of flowing wells in Goshen Valley embraces about 15 square miles and extends 

from Utah Lake to within about a mile of Goshen. Within it flowing wells are obtained 

at depths ranging from 50 to 400 feet. From the few available records it appears that 

varying stratigraphic conditions exist in this area, the prevailing clay being irregularly 

interbedded with sand, usually in thin streaks, with very little gravel. The flows obtained 

are small, averaging possibly about 5 gallons a minute, and the pressure is sufficient to 

cause the water to rise only a few feet above the surface.

Goshen itself is furnished with surface water from ditches supplied by Currant Creek and 

by springs located at the base of the hills about 2 miles east of the town. The underground 

supply is derived from wells that usually range from 25 to 75 feet in depth. The wells 

are put down through clay to sand in which water is found under pressure sufficient to 

cause it to rise almost to the surface, the usual depth to water being 3 to 20 feet. A 

number of unsuccessful attempts to get flowing wells have been made, the deepest being 

the railroad well put down near the station. It is 334 feet deep, and water is reported to 

have risen in it to within a few feet of the surface.

The highland area is underlain chiefly by coarse detritus derived from the adjacent 

mountains and distributed either as shore deposits in Lake Bonneville or as alluvial accumulations. This higher portion of Goshen Valley is poorly supplied with water, the chief 

sources being Kimball Creek, a small stream which seldom flows below its mountain course, 

and Currant Creek, which flows perennially and supplies the lower valley. The discharge 

of Currant Creek, however, is insufficient for the needs of the upland. A reservoir has been 

built by damming Currant Creek at the entrance to its canyon course through Long Ridge, 

and a canal constructed which skirts the upper part of Goshen Valley, but the enterprise 

has been a failure.

A few springs occur along the eastern base of the Tintic Mountains and some successful 

attempts have been made there to develop underground water by tunneling. In the upper 

valley of Kimball Creek there are a number of springs which flow about 100 gallons a minute, 

and smaller ones occur in several gulches. About 2 miles east of Goshen there is a group 

of springs at the base of Long Ridge, where water issues through debris and accumulates 

in several small ponds, the temperature of which is reported to stay at about 70° F. throughout the year. These springs constitute the source of Warm Creek, and their combined 

flow in November, 1904, was estimated at about 5 second-feet. Water has been developed

a Sanchez, A. M., Soil survey of the Provo area, Utah: Bull. Bureau of Soils, U. S. Dept. Agric., 

1904.
56 UNDERGROUND WATER IN VALLEYS OF UTAH.

by tunneling at several localities along the eastern slope of the Tintic Mountains. In the 

valley of Kimball Creek, in sec. 11, T. 11 &., R. 2 W., there is a tunnel 200 feet long in volcanic rock, which furnishes about 20 gallons a minute, and water sufficient for milling 

purposes has been developed by drifting into the alluvium and bed rock at the head of 

Homansville Canyon.a

Away from the bordering mountains in the highland portion of Goshen Valley, very 

little underground water has been obtained, and considering the slight run-off and the small 

tributary drainage area, not much can be expected. The most favorable locations for sinking wells are along the courses of drainage ways. The most successful are along the course 

of Kimball Creek, but even there water commonly is not obtained at depths less than 150 

feet. A number of dry wells havV been sunk in the upland area.

WEST OF UTAH LAKE.

The narrow strip of lowland between the western shore of Utah Lake and the Lake Mountains is very scantily provided with water. The low, narrow mountains catch relatively 

little precipitation; there are no perennial streams, and the arroyos carry water only for 

a few days during the year. From the foot of the Bonneville and Provo terraces that 

extend along the base of the mountains the surface slopes gradually lakeward and is underlain chiefly by coarse-textured deposits.

Along the shore of the lake a number of seep springs occur near water level. They are most 

abundant from Lehi southward, and there are also a few 2 or 3 miles beyond Pelican Point, 

where their presence is marked by low, marshy areas, one of which is utilized in the cultivation of a few acres of alfalfa. Near Pelican Point there is a feebly flowing well 90 feet 

deep, in which water was obtained at a depth of 60 feet; and in a near-by well a feeble flow 

is also obtained, which is said to come from a depth of 154 feet.

Few if any other attempts have been made to recover underground water in this region. 

Judging from the wells at Pelican Point one might expect to obtain similar results along 

the western shore of the lake, but if flows were obtained the water would be at so low an 

elevation as to make it of little use without pumping. Away from the shore flows can 

hardly be expected. It may be, however, that limited amounts of water can be found to 

rise in wells to within pumping distance. Prospecting for shallow wells might be attempted 

in the arroyos, but because of the limited watershed and precipitation the prospect is not 

good for obtaining enough underground water for extensive irrigation. Pumping directly 

from the lake presents attractive possibilities.

WELX, DATA.

The writer is indebted for the subjoined list of wells to Messrs. F. D. Pyle and T. F. 

McDonald. Mr. Pyle worked in Utah Lake Valley and west of Jordan River. Mr. McDonald, whose assistance was obtained through the courtesy of Mr. George W. Snow, 

engineer of Salt Lake City, collected data east of Jordan River. The yield of flowing wells 

was commonly measured by means of tables which are here inserted, together with accompanying explanation, because the method aroused popular interest and because the edition of the bulletin in which the tables were published has been exhausted.

METHOD OF MEASUREMENTS

Tables for determining the discharge of water from completely filled vertical and horizontal pipes 

were prepared a number of years ago by Prof. J. E. Todd, State"geologist of Soulh Dakota, who issued 

a private bulletin describing simple methods of determining quickly, with fair accuracy and with little 

trouble, the yield of artesian wells. In the following notes the tables and explanations relating to 

vertical and horizontal pipes are taken from this bulletin. The explanations have been appended by 

the present writer.

a Smith, G. O., and Tower, G. W., Description of the Tintie district: U. S. Geologic Atlas, special 

folio 65, U. S. Geol. Survey, 1900. 

6 S'-ichter, 0. S.: Water-Sup, and Irr. Paper No. 110, U. S. Geol. Survey, 1905, pp. 37-42.
WELL DATA MEASUREMENT. 57

In determining the flow of water discharged through a pipe of uniform diameter all that is necessary 

is a foot rule, still air, and care in taking measurements. Two methods are proposed one for pipes 

discharging vertically, which is particularly applicable before the well is permanently finished, and 

one for horizontal discharge, which is the most usual way of finishing a well.

The table [on page 68] is adapted to wells of moderate size, as well as to large wells. In case the well 

is of other diameter than given in the table its discharge can without much difficulty be obtained from 

the table by remembering that, other things being equal, the discharge varies as the square of the 

diameter of the pipe. If, fo example, the pipe is one-half inch in diameter its discharge will bo onefourth of that of a pipe 1 inch in diameter for a stream of the same height. In a similar manner the 

discharge of a pipe 8 inches in diameter can be obtained by multiplying the discharge of the 4-inch 

pipe by 4.

In the first method the inside diameter of the pipe should first be measured, then the distance from 

the end of the pipe to the highest point of the dome of the water above in a strictly vertical direction 

a to b in the diagram [fig. 5]. Find these distances in table [p. 58, A] and the corresponding figure will 

give the number of gallons discharged each minute. Wind would not interfere in this case so long as 

the measurements are taken vertically.

The method for determining the discharge of horizontal pipes requires a little more care. First measure the diameter of the pipe, as before, then the vertical distance from the center of the opening of the 

pipe, or some convenient point corresponding to it on the side of the pipe, vertically downward 0 inches, 

a to b of the diagram, then from this point strictly horizontally to the center of the stream, b to e.

IO inches 

71.7ga//oas 

per minute

FIG. 5. Diagram illustrating flow from vertical and horizontal pipes.

With these data the flow in gallons per minute can be obtained from table [p. 58, B]. It will readily be 

seen that a slight error may make much difference in the discharge. Care must be taken to measure 

horizontally and also to the center of the stream. Because of this difficulty it is desirable to check 

the first determination by a second. For this purpose columns are given in the tables for corresponding 

measurements 12 inches below the center of the pipe. Of course the discharge from the same pipe should 

be the same in the two measurements of the same stream. Wind blowing either with or against the 

water may vitiate results to an indefinite amount. Therefore measurements should be taken while 

the air is still.

Whenever fractions occur in the height or horizontal distance of the stream, the number of gallons 

can be obtained by apportioning the difference between the readings in the table for the nearest whole 

numbers, according to the size of the fraction. For example, if the distance from the top of the pipe 

to the top of the stream in the first case is 9^ inches, one-third of the difference between the reading in 

the table for 9 and 10 inches must be added to the former to give the correct result.

In case one measures the flow of a well by both methods he may think that the results should agree, 

but such is not the case. In the vertical discharge, there being less friction, the flow will be larger; so, 

also, in the second method differences will be found according to the length of the horizontal pipe used.

As pipes are occasionally at an angle, it is well to know that the second method can be applied to 

them if the first measurement is taken strictly vertically from the center of the opening and the second 

measurement from that point parallel with the axis of the pipe to the center of the stream, as before. 

The measurements can then be read from the table.
58 UNDERGROUND WATER IN VALLEYS OF UTAH.

Table for determining yield of artesian wells. 

[Gallons per minute.]

A. Flow from vertical pipes.

Height 

of jet.

Inches.

i

1

2

3

4

5

6

7

8

9

10

11

12

13

14

15

16

17

18

19

20

21

22

23

24

25

26

27

28

29

30

36 

48 

60

72

84

96

108

120

132

144

Diameter of pipe in inches.

1.

3.96

5.60

7.99

9.81

11.

6.2

8.7

12.5

15.3

U8.91 .

12.6

18.0

22.1

11.33 17.7 25.5

12.68 19.8

13.88 21.7

14.96 ' .23.6

16.00 25.1

17.01 26.6

17.93 28.1

18.80

19.65

20.46

21.22

21.95

22.67

23.37

24.06

24.72

25.37

26.02

26.66

27.28

27.90

28.49

29.05

29.59

30.08

30.55

30.94

34.1 

39.1 

43.8 

48.2

51.9

55.6

58.9

62.2

65.1

68.0

29.5

30.7

31.8

33.0

34.2

35.2

36.3

37.5

38.6

39.6

40.6

41.6

42.6

43.5

44.4

45.3

46.1

46.9

47.5

48.2

53.2 

61.0 

68.4 

75.2

81.0

86.7

92.0

S8.0

102.6

106.4

28.5

31.2

33.7

36.0

38.3

40.3

42.3

44.2

45.9

47.6

49.3

50.9

52.5

54.1

55.6

57.0

58.4

59.9

61.4

62.8

64.1

65.3

66.4

67.5

68.5

69.4

76.7 

88 0 

98.6 

108.0

116.8

125.0

132.6

139.9

146.5

153.1

2.

15.8

22.4

32.0

39.2

45.3

50.7

55.5

59.8

64.0

68.0

71.6

75.2

78.6

81.8

84.9

87.8

90.7

93.5

96.2

98.9

101.6

104.2

106.7

109.2

111.6

114.0

116.2

118.2

3.

35.6

51.4

71.9

88.3

102.0

113.8

124.9

134.9

144.1

153.1

161.3

169.3

176.9

184.1

190.9

197.5

203.9

210.3

216.5

222.5

228.5

234.3

240.0

245.6

251.1

256.4

261.4

266.1

120.3 270.4

121.9 274.1

123.4 i 277.6

136.3 

156.5 

175.2 

192.9

207.6

222.2

235.9

248.7

260.4

272.2

306.6 

352.1 

394.3 

434.0

467.0

500.0

530.8

559.5

585.9

612.5

B. Flow from horizontal pipes.

Horizontal 

leigth 

of jet.

Inches.

6

7

8

9

10

11

12

13

14

15

16

1-inch pipe.

6-inch 

level.

7.01

8.18

9.35

10.51

11.68

12.85

14.02

15.19

16.36

17.53

18.70

17 19.87

18 21.04

19 22.21

20 23.37

21 24.54

22 25.71

23 26.88

24 28.04

25 29.11

26 30.38

27 31.55

28 32.72

29 33.89

30 35.06

31 36.23

32 37.40

33 38.57

34 39.64

35 40.45

36

Contin

12-inch 

level.

4.95

5.77

6.60

7.42

8.25

9.08

9.91

10.73

11.56

12.38

13.21

14.04

14.86

15.69

16.51

17.34

18.17

18.99

19.82

20.64

21.47

22.29

23.12

2-inch pipe.

6-inch 

level.

27.71

32.33

36.94

41.56

46.18

50.80

55.42

60.03

64.65

69.27

73.89

78.51

83.12

87.74

92.36

96.98

101.60

106.21

110.83

115.45

120.07

124.69

129.30

23.95 133.92

24.77 138.54

25.59

26.42

27.25

28.08

28.64

41.60 29.46

ae by adding fo 

1.15 0.82

143.16

147.78

152.39

157.01

161.63

166.25

12-inch 

leveL

19.63

22.90

26.18

29.45

32.72

35.99

39.26

42.54

45.81

49.08

52.35

55.62

58.90

62.17

65.44

68.71

71.98

75.26

78.53

81.80

85.07

88.34

91.62

94.89

98.16

101.43

104.70

107.98

111.25

114.52

117.79

r each inch 

4.62 3.27

NOTE. To convert results into cubic feet, divide the number of gallons by 7.5, or, more accurately, 

by 7.48.

The flow hi pipes of diameters not given in the table can easily te obtained in the following manner: 

For }-mch pipe, multiply discharge of 1-inch pipe by............................................. 0.25

For f-inch pipe, multiply discharge of 1-inch pipe by............................................. .56

For IJ-inch pipe, multiply discharge of 1-inch pipe by............................................ 1.5f

For IJ-inch pipe, multiply discharge of 1-inch pipe by............................................ 2.25

For 3-inch pipe, multiply discharge of 2-inch pipe by........................................._.. 2.2f
LIST OF TYPICAL WELLS. 59

For 4-inch pipe, multiply discharge of 2-inch pipe by............................................. 4.00

For 4J-uich pipe, multiply discharge of 2-inch pipe by ........................................... 5.06

For 5-inch pipe, multiply discharge of 2-inch pipe by............................................. 6.25

For 6-inch pipe, multiply discharge of 2-inch pipe by............................................. 9.00

For 8-inch pipe, multiply discharge of 2-inch pipe by............................................. 16.00

LIST OF TYPICAL WELLS.

Weds in Jordan River and Utah Lake valleys. 

[Height of water above surface indicated by plus 4-; below surface indicated by minus .]

Name of owner.

B. Young.............

C. R. Savage.......... 

G. A. Hatch...........

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

J. C. Hansen .......... 

W. S. McDonald..... . 

Gun Club.. ............

C. A. Anderson........ 

P Olene

S. Bamberger . ........

J. Withers.............

A. J. Davis............ 

F.W. Kettle..........

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

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

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

P.Cline....... .......

J.W. Haddock.......

H. Price..............

R.Griffith............

Location.

T. 1N..R. IE., sec. 31..... ...... 

....do...........................

....do. ..........................

T. 1 N., R. 1 E., sec. 32 ........... 

T. IN., R. 1 W., sec. 1.......... 

.....do. ..........................

T. IN., R.I W., sec. 3..........

T. IN., R. 1 W., sec. 4..........

T. IN., R. 1 W., sec. 5..........

T.1N., R.I W., sec. 9... .......

.....do...........................

T. IN., R.I W., sec. 15......... 

T. IN., R. 1 W., sec. 17......... 

T.1N., R.I W-, sec. 21. ........ 

T. IN., R. 1 W., sec. 22.........

.....do...........................

T. IN., R. 1 W., sec. 23......... 

.....do...........................

T. 1 N., R. 1 W., sec. 25. ........ 

.....do...........................

.....do...........................

.....do...........................

T. IN., R. 1 W., sec. 27........ 

.....do...........................

.....do...........................

.....do...........................

.....do...........................

T 1 "NT "R 1 W QP/» ^

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

Diameter.

Inches.

2 

2 

24 

6 

2 

14 

14 

1J 

2 

2 

2

14 

2

2 

14 

14 

2

2 

2 

2 

li 

2 

2

H 

2 

2 

1J 

2

li

1J 

2 

2 

14 

14

1J 

2

2

Depth.

Feet. 

75 

61 

48 

 35 

18 

312

1,002 

497 

150 

250 

50 

479 

400 

450 

160 

330 

28 

26 

60-70 

80 

70 

400 

140 

154 

208 

408 

250 

320 

350 

140 

210 

350 

135 

130 

68 

93 

95 

123 

100 

75 

75 

75 

% 

200

Height of 

water.

Feet.

-14

+ 

+ 

+ 

+ 

+ 

+ 

+ 

-20-50 

+ 

4- 

4- 

4- 

4-

+ 

4- '

4- 

4- 

4- 

4- 

4- 

+ 

4- 

4- 

+ 

4- 

+ 1 

+ 

4- 

4- 

+ 

4- 

4- 

4- 

+

+

Yield per 

minute.

Gallons.

4

5 

14 

Many. 

6 

14 

5

40 

30 

3-7 

3

2

3 

1-2 

1

25 

.1

li

1

5 

15 

2 

3 

2 

15 

35 

30 

25 

5-20

20
60 UNDERGROUND WATER IN VALLEYS OF UTAH.

Wells in Jordan River and Utah Lake valleys Continued.

Name of owner.

S. A. Gibbs............

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

J. Walker. ............

P. J. Stone ............

S. McKay.............

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

J. E. Wesley. ..........

W. Wheeler...........

T. Golightly...........

S. K. Hansen. . ........

W. N. Sheets..........

F. Sproul..............

G. Baiber.............

City, about 16 wells . . .

E. O. Butterfield......

T. Berg................

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

W. Colton.............

J.W. Hicks......... .

T. Antisill. ............

S. M. Alley............

S. H. Calder.. .........

J. R. Miller............

J. A. Shelter...........

L. Hunt. ..............

H. E. Thorp...........

J. E. Nailor...........

(0)

M. C. Sandford........

Location.

T. IN., R. 1 W.,sec. 36..........

TIN R 2 W sec 25

.....do...........................

T. 1 S., R. 1 E., sec. 5... ........

.....do...........................

....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do................'..........

T. 1 S., R.I E., sec. 6............

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do................... .......

.....do...........................

.....do...........................

.....do...........................

T. IS., SM E., sec. 8.... .......

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

Diameter.

Inches. 

2-3

2

2

n

2

2

2-9

2

2

2

14

2

3

2

14

2

2

2

2

Depth.

Feet. 

75-80

401

465

80

16

73

45

29

40

12

75

82

387

10

100

162

100

125

170

150

100-600

178

150-200

155

160

60

165

110

50

50

26

246

390

207

41

28

42

100

130

85

51

54

56

18

32

22

20

100

200

335

15

33

Height of 

water.

Feet.

+

- 6

-12

- 6

+ .

+

+35

+

- 1

+

+

+ 12

-5-6

-65

-30-50

-46

- 4-16

- 5-14

+

- 3-11

- 3

Yield per 

minute.

Gallons. 

40

4

9

20

7

8

6-8

30

12

1

(?) 600

2-3

20-50

50

50

6

30

35

3

40

8

50

6

50

a Owner's name unknown.
LIST OF TYPICAL WELLS. 61

Wells in Jordan River and Utah Lake valleys Continued.

Name of owner.

(a)

J. J. Hurtt. ...........

W.N. Sheets. .........

M. Gray...............

E.H. Stout...........

F. Prittish............

Salt Lake Co... .......

F. Wittich............

L. A. Kelsh...........

D. Evans..............

I. Riches..............

E. S. Pierce...........

(a)

W. H. Wolstezhoh....

C. B. Stock............

H. Best...............

A. Best......... ......

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

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

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

J.Riley. ..............

G. Hall. ...............

J. O. Young...........

R. B. Young..........

M. W. Taylor.........

L. H. Kimball.........

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

W. C. Winder.........

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

A. Walker.............

(»)

T Tf Piitlor

S. Love ................

A. Hoskinson.........

Location.

T.1S.. R. 1 E.,sec. 17...........

.....do... ........................

.... .do. ..........................

.....do. ..........................

T. 1 S., R. 1 E., sec. 18...........

.....do. ..........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

T. 1 S., R. IE., sec. 19...........

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do. ..........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

Diameter.

Inches.

2

2

2

2

2

2

2

2

2

3

2

2

9

2

11

2

2

2

2

2

2

2

if

2

2

2

2

3

2

Depth.

Feet. 

33

10

14

48

325

300

100

164

160

20

72-82

500

600

636

150

40

325-3SO

501

382

17

250-300

322

560

40

298

100

50

160-170

323

296

285

437

100

94

60

176

180

90

181

84

212

75

240

150

150-160

23

26

65

40

162

156

21

Height of 

water.

Feet. 

-28

-43

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

-20

+

+

+

-14-15

Yield per 

minute.

Gallons.

4-5

30-40

30

10

18

30-40

5

12-14

(?) 150

10

18

30-40

80

(?) 100

1-13

55

20-30

10-12

5-6

8

50-60

60

25

10-£0

17-20

1

18

20-25

20-25

(?) 100

1 10

1

30

40

46

5-6

i

28

» Owner's name unknown.
62 UNDERGROUND WATER^IN VALLEYS OF UTAH.

Wells in Jordan River and Utah Lake valleys Continued.

Name of owner.

P. R. Ryon............

J. Neff.................

J. Childs....... ........

W. M. Tillman........

W. S. Timmons .......

R. Pike................

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

O. Reeee...............

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

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

L. Stutts..............

S. Hicks...............

E. E. Keithley........

H. Burnett. ...........

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

W.J. Miller. ..........

J. Tremayave .........

G. Taylor.............

G. Calder..............

(«) '

L. White..............

E.J.Williams.........

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

C. Halford............

A. M. Rymarson. ..... 

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

J.HuIse. ..............

Location.

.....do...........................

.....do.:...-.....-...........---.

.....do...........................

T. 1 S., R. 1 E., sec. 26.........

.. ...do... .................. ......

.....do...........................

T. 1 S., R. 1 E., sec. 28. ..........

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.... .do. ............... ...........

.....do...........................

.. ...do. .......... ................

.....do...........................

. ....do. ..................... .....

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

T. 1 S., R. 1 E., sec. 30.... .......

.....do...........................

.....do...........................

.....do.......--...--.--..---.--..

.....do...........................

.....do...........................

. ....do. ....................... ...

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do. ................... .......

.....do...........................

T. IS., R. 1 E., sec. 31........... 

.....do...........................

.....do...........................

.....do...........................

Diameter.

.

Inches.

..........

2

0

^

2

2

3

2

2

2

2

2

0

2

o

1|

2

2

2

2

2

li

2

2

2

Depth.

Feet. 

22

158

18

22

23

33

184

27

55

68

26

194

187

40

260

190

200

184

215

208

209

245

245

141-143

100

120

202

24

200

128

251

104

235

240

110

216

218

130

100

175

300

185-230

82-83

50

160

202

72

237

160

Height of 

water.

Feet.

__ -JO

+

- 15

- 19

- 20

-104

- 25

-37

4.

- 34

- 16

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+ 6

+

+

+

+

+

+

+

+

+

+ 

+

+

Yield per 

minute.

Gallons.

80

............

............

............

............

............

2

2

11

30

30

13

40

30

(?) 100

27

20

20

20

30

17

5

24

12

45

28

8

30

40-69

20

60

25

1

10

35 

6

20

Owner's name unknown.
LIST OF TYPICAL WELLS.

Wells in Jordan River and Utah Lake valleys Continued.

Name of owner.

J. Hulse ...............

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

C. Bell.................

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

J. Bert................

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

N. White.............

E. Huish.... ..........

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

S. W. Moyle...........

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

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

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

S. A. Cornwell.........

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

E. Bailey..............

J.W. Murphy.........

W. H. Thuers..-.. ...

P. C. Brizen. ..........

Mrs. M. Cold..........

Mrs. E. R. Wadsen....

(a)

F. J. Guth.............

Mrs. C. Bickson .......

J. Taylow.............

H. L. Eyler...........

R. Boss...............

E. B Swan............

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

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

H. J. Walk............

H. E. Evans..........

Sudbury...............

A. Bailey..............

J. Cleveland ...........

Location.

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

T.I S., R.I E., sac. 32.... .......

do

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

T. IS., R.I W., sec. 1. ..........

.....do...........................

.....do...........................

T.1S., R.I W., sec. 2. ..........

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

T. 1 S.,R.1W., sec. 3. ...........

T.I S., R 1 W., sec. 4... .........

T.I S.,R. 1 W.,sec. 5. ....... ..

.....do...........................

T.1S., R. 1 W., sec. 7...........

.....do...........................

.....do...........................

T. IS., RlW.,sec.S. ..........

T. IS., R. 1 W., sec. 9.. .........

.....do...........................

T. 1 S., R. 1 W., sec. 10 .........

T. 1 S., R.I W., sec. 11. .........

.....do...........................

.....do...........................

.....do...........................

.....do...........................

Diameter.

Inches.

2

2

2

9

2

2

2

2

3

li

li

2

2

4

2-J

9

2

li

2

li

H

3

2

2

2

2

2

Depth.

Feet. 

130

255

83

209

211

203

150

90

130

80

244

210

70

196

235

160

160

165

193

55

33

25

54 56

70-150

25

eon

350

120

1,100

114

318

ooc

95

1 072

280

I3f\f\

385

154

jnc

ooc

320

98

624 

377

130

165

456

Height of 

water.

Feet.

+

+

+

+

+

+

+

+

+

+

+

+

+

- 24

22

419

+

+

+

+

4-

+ 4i

+

+ 1

+ 1

+

+

4-

Yield per 

minute.

Gallons. 

20

30

40

20

12

(?) 110

15

J

8

28

35

6

20

1-12

1

25

1

20

o

30

11

6

91

80

16

3

7

6

10

1

30-40 

g

20-30

6-7

25

5-6

60-70

o Owner's name unknown.
64 TJNDERGEOUND WATER IN VALLEYS OF UTAH.

Wells in Jordan River and Utah Lake valleys Continued.

Name of owner.

E.Kidd.. ............. 

A. H. White...........

(a)

J.S.McCallan. ........ 

J. G. Gumman. ........ 

Schoolhouse ...........

Rockhm. ..............

G.H.Walton... ......

(a)

(a)

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

(a)

(a)

(a)

Butterworth ..........

T. West...............

N. T. West............

geles Rwy. Co. 

P. J. Reid. ............

T. Gundesser, jr .......

Location.

T. 1 S., R. 1 W., sec. 12.......... 

.....do...........................

T. 1 S.,R.1W., sec. 13.. ........

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

T. 1 S.,R. 1 W., sec. 14. ......... 

T.I S.,R. 1 W.,sec. 16.......... 

T. 1 S., R.I W., sec. 17. .........

T.I S., R.I W., sec. 21. .........

T. 1 S., R. 1 W., sec. 24..........

.....do...........................

T. 1S.,R.1 W., sec. 25. .........

.....do...........................

.....do...........................

.....do...........................

T 1 S R 1 W sec 26

T 1 Q T? 1 W aon 9S

.....do...........................

T. 1S.,R. 1W., sec. 29.. ........

.....do...........................

T.1S.,R. 1 W., sec. 31.. ........

.....do...........................

T 1 Q T? 1 W con 39

T. 1 S.,R. 1W., sec. 35. .........

.....do...........................

T. 1 S., R. 2 W., sec. 1. ..........

......do...........................

T.I S., R. 2 W., sec. 21. .........

.....do...........................

.....do...........................

.....do...........................

.....do...........................

T. 1 S. , R. 2 W., sec. 23. .........

T.I S.,R.2W., sec. 26. .........

T 1 Q R 9 AST con 97

T 1 S R 2 W sec 29

T. 1 S., R. 2 W., sec. 33. .........

T. 1 S.,R.2W., sec. 34. .........

T. 1S..R.3W., sec. 2.. .........

T.1S.,R.3 W., sec. 24. .........

.....do...........................

T.2 S.,R.1E., sec. 3. ...........

.....do...........................

.....do...........................

T. 2S., R.I E., sec. 4.... ........

Diameter.

Inches.

2

2

2

2

2

2 

2 

2

U

2

U

2

2

2

U

H

U

li

2

li

3

1J

2

1-i

li

11

li

42

4

li

4

..........

Depth.

Feet. 

475 

300

18

177

315

380

275

355 

330 

400 

412

145

385

130

120

145

350

350

182

60

345

75

140

160

260

150

30

68

150

175

40

40

90

177

27

118

84

166

720

330

134

73

540

62

65

18

Height of 

water.

Feet. 

+ 

+

+

+

+

+ 

+ 

+ 

+ 12

+

+

+ 30

+

+

-30

-51

+

+

+

+

+

+

+

+

+ .3

+ 6

+

-21

-14

-66

+ 9

+ 12

+

+

-

Yield per 

minute.

Gallons.

2f 

5-lf

6C

1C

45

io-ie

le

K 

25 

12 

25

15

5

6

1

2

5

3

10

2

15

6

12

25

5

8

20

9

3

Dry.

o Owner's name unknown.
LIST OF TYPICAL WELLS. 65

Wells in Jordan Ewer and Utah Lake valleys Continued,

Name of owner.

T. R. Brockbank ......

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

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

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

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

A. Fuller..............

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

J.Wright....... ...... 

E. Pugh. ..............

Mrs. A. D. Park.......

H. J. Bullock..........

T. Powell..............

H. Park...............

W. Hill, sr............

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

W. Hill, jr.............

J.S. Williams.........

A. E. Williams........

T. Martin.............

C. E. Warenski. .......

J. R. Miller............

W. Noble.............. 

M. M. Miller...........

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

T. H. Pierce...........

C. West...............

J. Walker.............

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

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

A. Gillard.. ........ ..

H. Brinton. ...........

J. R. Hansen ..........

L. B. Howard. ........

A. Scott...............

H.Bagley. ............

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

F. Brinton............

C. Bagley..............

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

B. Anderson ..........

Location.

T. 28., R.I E., sec. 4............

.....do...........................

.....do....................;......

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

T.2S.,R. IE., sec. 5. ........... 

.....do...........................

.....do...........................

.....do...........................

.....do...........................

T. 2 8., R. 1 E., sec. 6. ...........

.....do. ..........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

T 2 S R 1 E sec 7

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do. ..........................

T. 2 S., R. 1 E., sec. 8. ...........

.....do........................... 

.....do...........................

.....do...........................

.....do...........................

.....do............................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

T. 2 S., R. 1 E., sec. 9 ...........

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

T. 2 S., R. 1 E., sec. 10...........

Diameter.

Inches.

2

0

3

2

2

2

3

2

2

2

2

2

2

2

' 2

2

9

3

2

2

2

2

5

..........

1*

4

4

2

2

2

2

2

3

2

H

2

Depth.

Feet. 

104

102

76

78

99

232

225

70-100

65

335

122

200 

108

180

90

384

100

194

90

255

80

255

210

150

115

80

315

100

190

189

230

300

215

230 

85

82

80

172

80

80

310

120

148

96

275-250

60

100-103

92-96

100

14

Height of 

water.

Feet.

+

+

-70

+ 

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

+

Yield per 

minute.

Gallons. 

46

25

15

24

4

20-34

4

20

11

25

3-5

2

5

10

10

32

28

4

40

20

40

1

, 30

15

4

10

38

2

10

7 

(?)160

22

20

10

20

(?)130

(?)100

40

17

30

6

18

20

(?)100

43

25

20

30

-(»)

a Drv 9 months in 

IER 157 06 5
66 UNDERGROUND WATER IN VALLEYS OF UTAH.

Wells in Jordan River and Utah Lake valleys Continued.

Name of owner.

J.Spillet...............

J. Smith...............

S. F. Smith............

J. W McHenry........

J. Hobbs..............

H. V. Ballard. ........

R. M. Ballard.........

H. E. Howe...........

J. T. Erickson.........

F. C. Howe............

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

J.B.Thompson...

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

E.Taylor....... ......

E. Gillen..............

C. Turner.............

J.H. Wheeler. ........

Ward. 

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

M. Sibbs...............

N. Nelson. ............

C. Atkinson ...........

H. Wheeler............

C. B. Walder.... ......

C. J. Wright. ..........

W. Barrett............

J. E. Brown...........

H. C. L.Russell.......

J. W. Fawlke..........

A. Fawlke .............

S. Jones... ............

A. D. Brown. :........

(«)

P.M. Griffin..........

J. A. Wagstaff........

Location.

T. 2 S., R. 1 E., sec. 15. ..........

.....do...........................

T. 2 S., R. 1 E., sec. 16...'........

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

T 2 S., R. 1 E., sec. 18...........

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do............ . .. .....

.....do...........................

.....do...........................

.....do...........................

.....do...........................

T. 2 S., R. 1 E., sec. 20...

.....do............ .

.....do............. .. ....

.....do................. ........

T. 2S., R. IE., sec. 21...........

.....do...........................

.....do...........................

.....do...........................

T. 2 S., R. 1 E., sec. 26. ..........

T. 2 S., R. 1 E., sec. 27. ..........

T. 2 S., R. 1 E., sec. 28. ..........

.....do...........................

.....do...........................

Diameter.

Inches.

2

li

2

li

2

2

9

2

1-i

2

2

3

2

2

2

3

Depth.

Feet.

18

15

20

78

18-20

20

22

18

113

60

60

92

58

83

14

250

40

46

60

45

175

90

190

75

80

125

20-30

90

70-80

200

22

75-100

110

18

50

22

10

12

22

10

16

13

50

6

80

96

125

18

35

Height of 

water.

Feet.

- 16

- 10-11

- 4-17

- 40

- 8-10

- 10

- 12

- 9

+ 16

+ 8

_ g

- 12

+ - 8

-117

- 10

- 4-13

- 10

- 8

- 30

- 55

- 93

_

Yield per 

minute.

Gallons.

17

fO

50

35

20

22

60

35

35

45

60

20

40

eo

i Owner's name unknown.
LIST OF TYPICAL WELLS. 67

Wells in Jordan River and Utah Lake valleys Continued.

Name of owner.

O. G. Nelson..........

H. Larsen. ............

A. Hansen..... .. ...

E. E. Osbund.........

H. C. Monten..........

J. F. Proctor..........

H. Covert.............

Clark..................

J. M. Wood...........

E. Erickson...........

( b )

Gleason. ..............

J. Hays. ...............

J. Harper. .............

J. M. Mantell. .........

J. Mackey.. ...........

. ( 6 )

Parker .............

McAllister . .

H.McKay.............

H. Harker.............

W. H. Hague..........

P. Swendsen. .........

B. Williams...........

G. Bueger. ............

Western Pickling Co ...

S. Benson.............

D. Adamson..........

Creamery. .............

J. C. Cahoon ..........

Mrs. A. J. Plummer...

( 6)

M. Bishop.............

E. B. Tripp...........

A. S. White...........

R. P. Binghurst.......

Jones..................

Location.

T. 28., R.I E., sec. 30...........

.....do...........................

.....do...........................

T. 2 S., R. 1 Ev sec. 31. ..........

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do.............. . . . ..

T. 28., R. IE., sec. 32...........

.....do...........................

.....do.....................].....

T. 2 S., R.I E., sec. 33...........

T. 2 S., R. 1 E., sec. 34. ..........

T. 2 S., R. 1 E., sec. 35. ..........

.....do...........................

T.2S., R.I W., sec. 1. ..........

.....do...........................

.....do.................. . .....

.....do................ ..

.....do...........................

:.. ..do. ..........................

.....do...........................

T.2S., R.I W., sec.2. ..........

.....do................ . .

T. 28., R. 1 W., sec. 3...........

.....do...........................

T. 2 S., R. 1 W., sec. 6 ...........

T. 2 S., R. 1 W., sec. 8. ..........

.....do...........................

.....do........ ........

T. 2S., R. 1 W., sec. 9...........

T. 2S., R. 1 W., sec. 10..........

T. 28., R. 1 W., sec. 11..........

.....do...........................

.....do...........................

.....do...........................

T. 28., R. 1 W., sec. 12..........

.....do................ ..........

.....do...........................

.....do.................... . ....

.....do...........................

.....do...........................

T. 2 S., R. 1 W., sec. 13..........

.....do...........................

.....do...........................

.....do...........................

T. 28., R. 1 W.,sec. 14..........

.....do...........................

.....do...........................

.....do...........................

Diameter.

Inches.

2

2

2

3

0

3

3

3

2

3

2

2

2

3

3

2

01

2

Depth.

Feet. 

30

35

200

22

40-50

29-30

51

90

53

26

15

100

14

200

22

40

40

40

100

287

140

90

65

280

372

240

212

260

56

-I CA

110

141

323

DC

77

100

350

249

117

180

60

Ql

50

80

OO

175 180*

Height of 

water.

Feet. 

- 26-27

- 7-10

- 25-34

- 26

- 41

- CO

- 75

-200

- 18

25

07

60

KA

36

Q

- 30

fi 1

- 10

- 40

- 6

+

Yield per 

minute.

Gallons.

(a )

Dry.

40

2

25

8

6

35

40

15

20

20

12

o Dry in winter. 6 Owner's name unknown.
68 UNDERGROUND WATER IN VALLEYS OF UTAH.

Wells in Jordan River and Utah Lake valleys Continued.

Name of owner. Location.

School.................

M. Parker.............

(») 

C. ErickSon...........

(»)

J. B. Wright. .........

(«)

W. D. Runsal.........

Olsen. .................

R. Egbert..............

P. T. Rundquist. ......

M. Pusler. .............

T. 2 S., R. 1 W., sec. 15..........

.....do...........................

T. 2 S., R. 1 W., sec. 22. .........

.....do...........................

.....do...........................

T. 2 S., R. 1 W., sec. 23..........

T. 28., R. 1 W., sec. 24..........

T. 2 S., R. 1 W., sec. 25..........

.....do...........................

.....do...........................

T. 28., R. 1 W., sec. 26.......... 

.....do...........................

T. 28., R. 1 W., sec. 27.......... 

.....do...........................

.....do...........................

T. 28., R. 1 W., sec. 30..........

T. 2S..R. 1 W.,sec. 33.......... 

T. 28., R. 1 W.,sec. 34..........

.....do...........................

.....do...........................

T. 2S..R. 1 W., sec. 35..........

do

G. Hunt. ..............

(a )

P. J. Wolff............

H. Brown. . .

T.2S.,R. 1 W., sec. 36. .........

.....do...........................

.....do...........................

.....do...........................

.....do...........................

T. 28., R. 2 W., sec. 11..........

T. 28., R. 2 W., sec. 27. .........

T.3S..R. IE. .sec. 2. ...........

W. L. Bateman. ...... T. 3 S.. R. 1 TC.. KPC. a

C. Peterson

T. 38., R. 1 E., sec. 6. ...........

. .do. . . .

A. Yelter. ............ T. 3 S., R. 1 E., sec. 7. ...........

H. P. Hansen.........! T. 3S.,R. 1 E., sec. 8. ...........

P. Anderson. i T. 3 S.. R. 1 TC. «pn. 9

C. Williams...........

F. Olsen...............

J. P. Jenson. ..........

E. N. Fish.............

J. L. Johnson. ........

J. W. Smith...........

J. Tarry...............

A. J. Wilson...........

J. R. Alien............

J. Ennis..............

J. Boulter. ............

F. B. Ladler.

T. 3S.,R. 1 E., sec. 17...........

T. 3S.,R. 1 E., sec. 18.... .......

T. 3 S., R. 1 E., sec. 19...........

.....do...........................

T. 38., R. 1 E., sec. 22...........

T. 38., R. IE., sec. 28...........

T. 38., R. IE., sec. 29...........

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

T. 3 S., R. 1 E., sec. 33...........

.....do......... . ........

Diameter.

Inches.

3

3

3 

3

3

3 

6 

3 

3

3

3

3

4

<* Owner's name unknown. '

Depth.

Feet. 

117 

165 

345 

225 

140 

185 

30 

251 

20 

325 

230 

180 

100 

254 

137 

28 

178 

1,000 

52 

80 

217 

127 

309 

21 

225 

190 

50 

30 

174 

150 

38-40 

14-16 

40 

28 

75 

56 

125

16 

30 

40 

80 

95 

34 

65 

10 

18 

18-20 

16 

42 

70 

24 

41 

22 

66 

Dry in w

Height of 

water.

Feet. 

- 50 

- 50 

-110 

_ 40

- 90 

- 24 

 12

- 16 

- 60 

- 40 

- 20 

- 30 

+ 

- 33

- 20-30 

- 30 

- 24 

- 18

- 53 

.- 25 

- 17 

- 8 

- 75

- 17

+ 

- 6

- 25 

- 70 

- 45-52

- 28 

- 24

- 62 

- 18 

- 35 

- 17

nter.

Yield per 

minute.

Gallons.

2

Dry. 

Dry.

Dry.

( b )
LIST OF TYPICAL WELLS. 69

Wells in Jordan River and Utah Lake valleys Continued.

Name of owner.

J. Goff.................

A. J. Holt.............

B. W. Ostaorne........

W. R. Wellington.....

 R. Carlsdn............

J. O. Smith............

G. H. Donzy..........

C. H. Roberts.........

I. Langton............ 

G. Newbold...........

G. Sproul..............

H.J. Alien............

W. H. Garfleld........

W. L. Parry...........

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

D. J. Thurman........

H. T. Davis. ..........

(0)

(«)

les and Salt Lake 

R. R.

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

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

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

Location.

T.3S.,R. 1 W.,sec. 1...........

.....do...........................

.....do...........................

.....do...........................

T. 3 S., R. 1 W., sec. 3. ..........

.....do...........................

T. 3 S., R. 1 W., sec. 12....... ..

T. 3S., R. 1 W., sec. 13..........

T.3S.,R. 1 W.,sec. 15..........

.....do...........................

T. 3S., R. 1 W., sec. 23..........

.....do...........................

T. 3S..R. 1 W., sec. 24... ......

.....do...........................

....-do...........................

T. 3 S., R. 1 W., sec. 25. .........

.....do...........................

T. 3 S., R. 1 W., sec. 26... ... ..

T. 3S.,R. 1 W., sec. 27..........

T. 3 S., R. 3 W., sec. 26..........

T. 4S., R. IE., sec. 5............ 

.....do...........................

.....do..........................

T. 4 S., R. 1 E., sec. 6............

T. 4S.,R. IE., sec. 32...........

.....do...........................

T. 4 S., R. 1 E., sec. 33. ..........

.....do...........................

T. 4 S., R. 1 E .,sec. 24...........

T. 4S., R. 1 W., sec. 3...........

.....do...........................

.....do...........................

T. 5 S.,'R. 1 E., sec. 5............

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do. ...... .......|... ..........

.....do...........................

.....do..........'.................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

Diameter.

Inches. 

2

3

3

3

3

3

2

li

3

3

2

3

3

2

9

3

n

ii

ij

2

2

11

1J

2

2

U

2

2

11

3

li

Depth.

Feet. 

323

200

30

412

OQfi

250

212

137

156

255

500

50

28

30

127

28

15

133

90

225

102

400 

40

125

20

41

15

42

21

25-80

30

994

-ion

QO

15-50

1 ** A.

125

125

90-100

193

90-100

12

145

75

12

20

145

130

135

300

330

330

300

140

Height of 

water.

Feet.

+

-40

-58

43

-20

-40

-45

-85

-75

-12

_ 4

-40

+ 12

-60

+

-10

-35

- 8

-40

40

-10-40

_i_O^

8-10

22

- 8

Yield per 

minute.

Gallons. 

5

12-15

12-15

3

12

55

5

4

23

35

a Owner's name unknown.
70 UNDERGROUND WATER IN VALLEYS OF UTAH.

Wells in Jordan River and Utah Lake valleys Continued.

Name of owner.

W. Hunger. ...........

Wing..................

Barney ................

D. Wagstaff...........

American Fork, city 

well.

A. Green..............

A. K. Thornton.......

T. J. Chipman.........

A. Field...............

Mrs. K. Fox...........

(«)

D. J. Thurman. .......

Rio Grande Western 

Rwy.

G. Webb..............

W.H. Chipman.......

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

B. Willis..............

W. Howe. .............

Lott.. .................

(«)

W. Anderson. ......... 

W. D. West........... 

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

Wadley................

W.D. West...........

Location.

T. 5S., R. IE., sec. 9............ 

.....do...........................

.....do...........................

.....do...........................

.....do...........................

T. 5S., R. 1 E., sec. 10 .........

T. 5S., R. 1 E., sec. 14..........

.....do...........................

.....do...........................

T. 5S., R. 1 E., sec. 15.......... 

.....do...........................

T. 5S., R. 1 E., sec. 16..........

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

T. 5S., R. 1 E., sec. 17...........

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

T. 5 S., R. 1 E., sec. 18. ..........

.....do...........................

T. 5S., R.2 E., sec. 11...........

T. 5S., R. 2E., sec. 18...........

.....do............................

.....do...........................

.....do...........................

T. 5 S., R. 2 E., sec. 20. ..........

.....do...........................

T. 5S., R. 2E., sec. 21...........

T. 5S., R. 2E., sec. 23...........

.....do...........................

.....do...........................

.....do...........................

T. 58., R.2 E., sec. 25....... ... 

T. 58., R. 2E., sec. 29........... 

.....do........................ ..

.....do...........................

.....dc.. .........................

.....do...........................

o Owner's name unt

Diameter.

Inches.

2

li

li

2

li 

2

2

3

2

2 

3

2i 

6

2 

2 

2 

2

2 

2 

2 

2 

2 

li 

li 

' 2 

3

2 

2 

2 

2 

2 

2 

2 

2 

2 

2 

2 

2 

2 

3 

3 

3 

li 

2 

2 

2 

2 

2 

nown.

Depth.

Feet. 

145 

140 

158 

132 

130 

145 

270 

201 

460

160 

160 

140 

150 

543 

263 

33 

162 

130 

90

90 

147 

150 

350 

132 

150 

143 

140 

140 

164 

200 

165

195 

156 

147 

135 

160

290 

150 

200 

40 

100 

264

280 

280

64 

70 

74 

200 

70

Height of 

water.

Feet.

- 2 

+

+ 

- 6 

+

+ 

 25

+ 

+ 

+

_ 2

+

+ 

+

+

+

+ 

+

+

+ 3 

+ 30

+ 3 

+ 10

+ 

+ 46

+ 

+

+

+

+

+

-33

+ 18

Yield per 

minute.

Gallons.

(?)25 

9

20

20

2

40

10

5 

10 

10 

15 

20

20 

10 

20

5

50 

40

(?)200

30 

20

80 

20

60 

10

15

10 

15

35-50
LIST OF TYPICAL WELLS. 71

Wells in Jordan River and Utah Lake valleys Continued.

Name of owner.

D.M. Smith...........

(a)

(a)

L. Olsen...............

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

P. H.Aldred. .........

I. Fox.................

130 wells). 

J. M. Roberts .........

(0)

I. Cole.................

H. Gillies..............

D. A. Gillis............

J. K. Parcell..........

N. Knight.............

Colorado Fish Co......

N. J.Knight. .........

W. Knight............

J. S. Park.............

A. N. Holdaway. ...... 

M. Holdway...........

B. Larsen. ............

Wride & Alien. ........

G. A. Slumway........

J. A. Loveless. ........

A. L. Medium.

D. C. Daniels..........

H. C. Scott............ 

J. H. Clinger..........

Creamery. .............

J. W. Park........ ..

W. G. Williams.......

S. L.Aldred. ..........

W. Gammon. .........

P. H. Clufl............

T. W. Whisble........

N. Lydian. ............

S. McFee..............

A. Holliday...........

W. Cox. ...............

P. C. Bumrell......... 

Utah Sugar Co. .......

W. L. Camp...........

N. A. Nelson. .........

R. A. Hills............

Provo resort. ......... 

G. Baum. .............

W. D. Roberts........

Location.

T. 5 S., R. 2 E., sec. 29. ..........

.....do...........................

.....do...........................

.....do...........................

T. 58., R.2E., sec. 35.. .........

.....do...........................

T. 58., R. !W.,sec.l. ..........

T. 5S., R. 1 W., sec. 12..........

.....do...........................

T. 58., R. 1 W., sec. 13.......... 

.....do...........................

T. 5 S., R. 1 W., sec. 24. .........

T. 6 S., R. 2 E., sec. 5. ...........

.....do...........................

T. 6 S., R. 2 E., sec. 7... .........

.:... do.. .........................

T. 6 S., R. 2 E., sec. 8. ...........

T. 6S., R. 2E., sec. 10...........

T. 6S., R.2 E., sec. 14...........

.....do...........................

.....do...........................

.....do...........................

T. 6 S., R. 2 E., sec. 15. ..........

T. 68., R.2 E., sec. 17........... 

.....do...........................

T. 6 S., R. 2 E., sec. 18. ..........

.....do...........................

T. 6 S., R. 2"E., sec. 21...........

T. 6 S., R. 2 E., sec. 23. ..........

T. 68., R. 2E., sec. 24...........

T. 6 S., R. 2 E., sec. 26. ..........

T. 6 S., R. 2 E., sec. 28. .......... 

.....do...........................

T.6S., R. 2E., sec. 34...........

.....do...........................

.....do...........................

T. 6S., R. 2 E., sec. 35...........

.....do...........................

T. 6 S., R. 3 E., sec. 31...........

T. 7 S., R. 2 El, sec.l............ 

.....do....................... ...

T.7S., R.2E., sec. 2... .........

.....do...................... ....

.....do...........................

.....do....................... ...

T. 7S., R. 2E., sec. 3............ 

.....do...........................

.....do...........................

.....do...........................

T. 7 S., R. 2 E., sec. 4. ...........

T. 7 S., R. 2 E., sec. 9. ........... 

T. 7 S., R. 2E., sec. 10...........

T. 78., R.2 E., sec. 11...........

Diameter.

Inches. 

2

2

2

2

2

2

2-6

2

2

2

2

2

3

2

2

3

2

2-3

3

48

2

li

2

2 

2

2

2

01

2

li

2

2

Depth.

Feet. 

115

1 ^n

80

160

150

90

100

100

100

100

258 

112

210

130

110

112

110

72

110

OKfi

60

Ofifl

72

12C-140 

100

100

110

104

52

40

65

110 

98

125

110

130

210

50

217 

145

145

1 4^

1 KA

130

135 

110

TOO

oe

 50

342 

12

184

Height of 

water.

Feet. 

+20

+

+

+ 15

+

+ 30

+

+ 14

+ 11

-67

-80

-40-55

-62 .

+ 1-10

+ 12

-50

-36

-60

+

+

+

-25

-40-45

+

+

+

+ 10

+

+ 

- 4

+ !

Yield per 

minute.

Gallons. 

45

40

90

25

80

(?)2,000

32

/9\OCA

(?)100

(?) 1-200 

30

(?) 100

25

10 

10

48 

6

25

80

92

o Owner's name unknown.
72 UNDERGROUND .WATER IN VALLEYS OF UTAH.

Wells in Jordan River and Utah Lake valleys Continued.

Name ol owner.

Westron. ..............

W. B . Johnson ........

M. Christensen. . ......

B . Johnson ............

W. Carter.............

Rio Grande Western

Rwy. 

San Pedro, Los Angeles and Salt Lake 

R. R.

W. R. Pike............

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

W. J. Woodhead......

H. Manney. ..........

Hospital. .............

W. Scott..............

S; W.Sharp. ..........

Farris Bros. .........

S, Copp................

Watkins & Taylor. ....

(a)

G. T. Peay............

T. E. Thurman........

J. Anderson.. .........

H. M. Dougal.........

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

Clubhouse. ............

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

P. Boyer..............

Rio Grande Western

Rwy.

(a)

J. B. Stevenson. ...... 

D. Wheeler.............

D. Clark...............

A. Cox................

W. Findley............'

(a)

A. Oakley.............

(a)

(a.)

T . L. Mendenhall ......

S. Fuller...............

M. Dougal.............

E. P. Brinton.........

McKenzie. .........;..

Daley. ................

F. W. Phillips.........

(»)

(a)

(a)

Location.

T. 78., R. 2 E., sec. 11...........

.....do...........................

.....do...........................

.....do...........................

.....do. ..........................

T. 7 S., R. 2 E., sec. 12. ..........

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do.....'......................

.....do...........................

.....do.*..........................

.....do...........................

.....do...........................

.....do...........................

T. 7 S., R. 2 E., sec. 14...........

..... do.. .........................

T. 7 S., R. 2 E., sec. 16. ..........

T. 7 S., R. 3 E., sec. 6. ...........

..... do. ......... ..................

T. 78., R. 3E., sec. 8............

T. 7 S., R. 3 E., sec. 17..... ......

T. 78., R. 3E., sec. 29...........

T. 7 S., R. 3 E., sec. 30. .......... 

.....do...........................

.....do...........................

T. 7 S., R. 3 E., sec. 31...........

T. 78., R. 3 E., sec. 32...........

.....do...........................

T. 78., R. 3 E., sec. 33........... 

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do..................... ....

.....do...........................

.....do...........................

.....do...........................

T. 88., R. IE., sec. 11...........

.....do...........................

T.8S..R. IE., sec. 24...........

Diameter.

Inches. 

2

1J

2

2

2

3

3

H

li

2

2

2

2

li

2

2

li

2

3

2

2 

1A

2

2

3

li

li 

2

2

3

2

2

2

2

li

2

li

2

li

li

2

2

li

1J

1*

Depth.

Feet. 

180

160

168-178

150

170

175

192

248

198

168

168

180

150

197

185

175

300

145

170

137

140

333

150

270

180

220 

299

128

150

220

232

101 

131

240

230

135

115

128

105

22

120

245

25

230

130

132

145

217

138

100

Height of 

water.

Feet.

+

+

+

+

+

+ 35

+ 12

+

+

+

+

+

+

+

+

+

+ 5

+ 2

+ 20

+ 20

+

+ 10

+ 4

+

+

+

+30

+

+ 

+

+

+ 18

+

+

+

+

+

+

+

+

+

+

+

+

- 4

+

Yield per 

minute.

Gallons.

15

10

45

40

(?)120

(?)150

40

36

60

60

55

30

60

9

2

' 20

30

40

35

15

70

40

20 

5

10

18

80

15

12 

25

(?)120

25

70

30

30

20

45

10

20

10

9

65

30

10

7

a Owner's name unknown.
LIST OF TYPICAL WELLS.

Wells in Jordan River and Utah Lake valleys Continued.

Name of owner.

(a) 

(a)

J. Hall......... .......

J. E. Creer............

E. P. Thomas.........

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

San Pedro, Los Angeles and Salt Lake 

R.R......... ........

W. R. Simmons.......

(a) 

(G)

G. McClellan ..........

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

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

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

D. L. Hoff.............

C. Howe..............

(°)

(a)

(a)

(a)

F.Malley.............

G. Howe.............

(a)

Do

Location.

T. 88., R. 2 E., sec. 2............

.....do...........................

....do. ........._................

.....do...........................

.....do...........................

T S Q T? 9 TT QPf» 7

.....do...........................

.....do...........................

T. 88., R. 2 E., sec. 9............ 

.....do...........................

.....do...........................

T. 8 8., R. 2 E., sec. 12. ..........

.....do...........................

.....do...........................

T.8S.,R.2E., sec. 14.. .........

.....do...........................

T. 8S.,R. 2E., sec. 15........... 

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

.....do...........................

T. 8 S-, R. 2 E., sec. 20. ..........

.....do...........................

.....do...........................

.....do...........................

T S Q T? 9 TT Qt»r» 99

.....do.'..........................

T. 88., R. 2 E., sec. 23...........

.....do...........................

.....do...........................

T. 8S-, R. 2E., sec. 26...........

.....do...........................

.....do...'........................

.....do...........................

T. 8 8., R. 2 E., sec. 29.......... 

.....do...........................

.....do...........................

.do.

o- Owner's name uii

Diameter.

Indies.

2

U 

2 

1J 

2

2

li

o 

2 

2

li

3 

2 

2 

2

2 

2 

3 

2 

6 

2

3

li

2

2 

2 

2 

2 

li 

1J 

2 

2 

li 

2 

2 

. li 

li 

2 

2 

3 

2 

2 

2 

2 

2 

li 

2 

2 

2 

li 

li 

mown.

Depth.

Feet. 

438 

366 

380 

175 

112 

175 

225 

400 

230 

350 

400 

390 

142 

430 

280 

260 

220

405 

380 

423 

374 

380 

400 

500 

373 

160 

380 

450 

412 

387 

170 

130 

45 

475 

333 

250 

560 

400 

286

385 

360 

250 

137 

318-320 

390

425 

385 

415 

450 

175

Height of 

water.

Feet.

+ 

+ 

+ 

+ 10 

+ 

+ 

+ 

+ 12 

+ 10 

+ 

+ 

+ 10 

+ 

+ 

+ 

+

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

- 6 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+ 

+

Yield yer 

minute.

Gallons. 

25 

72 

20 

20 

10 

12

8-25 

35 

. 8

40

15 

10 

5

36 

16 

60' 

1 

60 

30 

60 

(?) 118

3

30 

15 

6 

2 

3 

10 

16 

8 

20 

10

6 

8 

35

35 

64 

14 

60 

35 

5

8 

20 

10
74 UNDERGROUND WATER IN VALLEYS OF UTAH.

Wells in Jordan River and Utah Lake valleys Continued.

Name of owner.

C. Hickman ...........

S. P. Lorensen. ........

P. J. Lundale. .........

J. J. Hansen. . .........

G. Staley..............

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

W. O. Creer...........

Creamery..............

M. C. King............

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

(a)

Sugar factory. ........

(a)

H. A. Harlan..........

J. P. Holt.............

McBeath ..............

J. Webb. ..............

. («)

(«)

(a)

(a)

(a)

(a)

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

P. Windward. .........

T TT Tioniolc

C. Long. ...............

(a)

A. Bingham ...........

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

C. Hanks..............

H. Boyle..............

J. Job.................

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

W. M. Phillippi. .......

(a)

A. Steele..............

Location.

.....do...........................

.....do...........................

T. 8S., R. 2E., sec. 32...........

T. 8S., R. 2E., sec. 33...........

.....do...........................

.....do...........................

.....do...........................

T. 88., R. 2E., sec. 35. ..........

T. 8S., R. 3E., sec. 4............

T. 8S., R. 3E.,sec. 5............

T. 88., R. 3E., sec. 7.. ..........

.....do...........................

T. 8S., R. 3E., sec. 8............ 

.....do...........................

T. 8S., R. 3E., sec. 30.. .........

.....do...........................

.....do...........................

.....do...........................

T. 9S.,R. IE., sec. 7............

T. 9 S., R. 1 E., sec. 12. ..........

T. 9S., R. IE., sec. 13... ........

T. 9 S., R. 1 E., sec. 32...........

T. 9 S., R. 2 E., sec. 1............

.....do...........................

T 9 S R 2 E sec ^

.....do...........................

T. 9S.,R. 2E., sec. 3............

.....do...........................

.....do...........................

.....do...........................

.....do...........................

T 9 S R 2 E sec 6

.....do. ..........................

T. 9S., R. 2E.,sec. 7............

T. 9 S., R. 2E., sec. 11........... 

.....do...........................

.....do. ......................... .

. ....do. ................ ..........

.....do. .................. .........

.....do...........................

T. 9S., R. 2E., sec. 30...........

T.9S., R.I W., sec. 25.. ........

T. 9S., R.I W., sec. 26..........

T. 9S. ( R. 1 W., sec. 33..........

T. 9S., R. 1 W., sec. 35..........

T. 9S., R. 1 W., sec. 36..........

T. 10 S., R. IE., sec. 6........... 

T. 10 S., R. IE., sec. 17..........

Tins ft 1 W SPP, 9.

Diameter.

Inches.

2

2

11

9

2

2

2

11

9

2

2

2

11 

2

11

11

11

2

 11

2

11

11

U

2

2

2

2

2

2

2

2

2

11

2

2

2

2

2

11

11

2

2

2

2

Depth.

Feet.

172

163

175

200

380

185

380

20

144

170

154

30 

123

22

140

30

100

360

247

180

290

155

200

200

160

375

228

50

130

300

140

116

160

217

438

196

. 275

225

175

296

279

20

90-126

50- 60

220

165

200

58

85

ion

407

Height of 

water.

Feet.

+

+

+

+

+

+

+

-15

+

+

+

+

+

+

_(_

+

+

+

+ 15

+

+ 1

+ 20

+

+ 

+

+

+

+

-16J

+

+

+

-125

+

+

-f 

- 80

- 9

Yield per 

minute.

Gallons. 

5

15

1

1

20

20

-35

10-25

30

30

12

2-3 

10

2

11

1*

27

8

30

(?) 125

30

(?) 100

55

37

3

15 

8

10

25

35

15-30

12

*

2

7-8

<* Owner's name unknown.
LIST OF TYPICAL WELLS. 75

Wetts in Jordan River and Utah Lake valleys Continued.

Name of owner.

W. M. Phillippi. .......

W. C. Albertson.......

J. Riley.. .............

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

P. Okleberry. .........

(«)

Rio Grande Western

W. Finch..............

L. E. Thomas.........

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

H. L. Cook............

Alien..................

(al

Location.

T. 10S.,R. 1 W.,sec. 4..........

T. 10 S., R. 1 W., sec. 9........'..

.....do...........................

.....do...........................

.....do...........................

T. 10S.,R. 1 W.,sec. 11.........

T. 10 S., R.I W., sec. 12.........

......do...........................

.....do...........................

T. 10 S., R. 1 W., sec. 14. ........

T. 10 S., R. 1 W., sec. 15.........

.....do...........................

.....do...........................

.....do...........................

.....do...........................

T. 10 S., R. 1 W., sec. 21.........

T. 10 S., R. 1 W., sec. 30. ........

T. 10 S., R. 1 W., sec. 33. ........

Diameter.

Inches.

2

o

2

2

2

li

2

2

2

2

2

2

Depth.

Feet. 

168

178

307

300

420

77

412

70

334

160

8

50

70

60

53

116

238

138

Height of 

water.

Feet.

-100

- 3

- 4

_ 4

- 3

- 20

- 7

- 86

-222

Yield per 

minute.

Gallons.

<* Owner's name unknown.
INDEX.

A.

Alpine, water supply of.................... 49

American Fork (town), water supply of,

source of....................... 49

wells in................................. 49-50

American Fork (stream), description of.... 6,49

discharge and run-off of, table showing. 21 

view of................................. 50

water from, analysis of................ 30

use of.............................. 49

American Smelting and Refining Company,

well of, record of............... 46

wells of, water from, analysis of........ 32

Analyses of water from various streams and

springs......................... 30,32

Artesian wells. See Wells, flowing.

B.

Battle Creek, description of................ 6

drainage of, effect of, on wells.......... 51

water of, use of......._............-.... 49

Bear River, description of................. 6

Beck's hot spring, water from, analysis of.. 30

Bed rock, water from...................... 50,53

water from, methods of obtaining...... 37,40

Benjamin, underground water conditions at. 54

Big Cottonwood Creek, description of...... 7,45

discharge and run-off of, table showing. 21,25

rocks on................................ 9

water from, analysis of................ 30

use of............................... 44,45

Big Cottonwood Creek Valley, seepage

measurements in............... 28

Big Hollow Creek, description of............ 53

Bingham, mines at, water in............... 37,40

rocks near._............................ 10

water supply of, source of.............. 40

Bingham Canyon, placer mining in......... 40

Bingham Consolidated Company, wells of.. 37

Bingham Creek, description of............. 39

Bingham Junction, smelters at............ 5

wells at, water from, analyses of....... 32

Bonneville region, Pleistocene history of... 12-13

Bonneville shore line, description of....... 12-13

Bonneville terrace, description of.......... 47

Boutwell, J. M., on discharge of Ontario

tunnel.......................... 37

on Park City and Bingham mining districts. .......................... 8

on well drilled for oil................... 41

Brown, R. E., analyses of water by......... 30

Bureau ot Soils, Department of Agriculture, 

experiments in reclaiming land

near Salt Lake City made by.... 43

Butterfleld Canyon, springs in............. 40

tunnels driven for water in............ 37

Butterfield Creek, description of........... 39

Butterfleld tunnel, water in, litigation

caused by...................... 40

C. Page.

Cambrian fossils, occurrence cf............ 10

Cambrian rocks, occurrence of........... 9,10,11

Cameron, F. K., analyses of water by....... 30

Cannon farm, well on...................... 41

Capitol Hill, reservoir on................... 45

Carboniferous rocks, occurrence and character of....................... 9,10,11

City canal, discharge of.................... 24

City Creek, description of .................. 7

discharge and run-off of, table showing. 19 

rocks on............................... 8

water from, analysis of................ 30

use of............................... 44,45

Clarke, F. W., analysis of water by......... 30,33

Climate, character of....................... 13-18

Colorado Fish Company, well of, description of.......................... 51

Comer, H. C., on general section in vicinity

of Lehi......................... 48

Converse, W. A., analyses of water by...... 32

Cooper, William, well of, water from, analysis of.......................... 32

Cottonwood Canyon, view in.............. 24

Cox, A., well of............................. 5a

Currant Creek, description of.............. &

reservoir on, failure of.................. 55

rocks on................................ 11

water from, analysis of................. 30'

use of............................... 55

D.

Dalton and Lark tunnel, description of.... 40

water in, occurrence of................. 37

Dams, subsurface, recovery of underground

water by....................... 37

De Bernard, J. H., analyses of water by.... 32

Dead Mans Falls, Cottonwood Canyon,

plate showing.................. 24

Dearborn laboratories, analyses of water by. 32 

Decker Lake, ditch at outlet of, discharge of. 25- 

Devonian rocks, occurrence of............ 8,9,11

Doremus, A. F., spring discharge measured

by.............................. 44

Drainage, character of..................... 5-7

Drainage area discussed, map showing..... 6

Draper, warm-water lakes near, description

of............................... 47

Dry Cottonwood Creek, description of..... 7

water from, analysis of................ 30

Dry Creek, description of.................. 6,48

Dry Creek Canyon, springs in.............. 49

Du Chesne River, source of................ 6

E. 

East Jordan canal, discharge of ........... 24 ~-

East Tintic Mountains, location and elevation of.......................... 6

structure of............................ 11

Eighth South street ditch, discharge of.... 25-

77
78 UTDEX.

Page.

Electric power, development of............. 37,39

Emigration Creek, description of...... ,^... 7

discharge and run-off of, table showing. 19

valley of, rocks in...................... 9

syncline developed in............... 37

water from, analysis of................. 30

use of............................... 44,45

Emmons, S. F., on descriptive geology..... 7

Evans Spring, water of, use of............. 53

Evaporation at Utah Lake................ 17

F.

Eault in Wasatch Mountains, description

of.............................. 8,9,10

Plowing wells. See Wells, flowing.

Eort Douglas, water supply of, source of. . 44

Gammon, Harry, wells of.................. 35; 51

Gas, natural, occurrence of................. 32-33

Geneva, wells at............................ 51

Geologic history, discussion of............. 11-13

Geology of the region...................... 7-13

Gilbert, G. K., on Lake Bonneville....... 7,11,13

on oscillations of lake level between

Prove and Bonneville horizons. 13 

Girty, G. H., fossils found by.............. 10

Goshen, springs near....................... 55

water supply of, source of......--..-... 55

well at, water from, analysis of........ 32

Goshen Valley, underground water conditions in...-...-.-...-...-....... 55-56

Great Salt Lake, elevation of.............. 5

fluctuations of......................... 25-26

natural gas near........................ 32

supply of, sources of.........-.----.-.. 28,33

water of, analyses of................... 33,34

Grove Creek, description of................ 6

water of, use of......................... 49

Guffey-Galey well, description of........... 41

H.

Hague, Arnold, on descriptive geology..... 7

Heber, rainfall at, table showing........... 15

Highlands, descriptive geology of.......... 8-11

Hobble Creek, description of............... 6

Homansville Canyon, water developed in... 56

Hot Springs Lake, outlet of, loss in flow at. 25

Humidity at Salt Lake City, table showing. 16

Hydrography of the area................... 18-26

I.

Igneous rocks, occurrence of........... 8,9,10,11

Inland Crystal Salt Company, well of...... 43

Irrigation by artesian wells................ 36

J.

Jap Pond, water of, character of........... 40

Jordan and Salt Lake City canal, head gate

12 

49

Page.

Jordan River, area west ofr dtvisjoBa at- . . 38-39 

discharge of ............................ 34-25

flood plain of, wells sunk in ............ 49

gate at head of, view showing . ......... 24

lowland area west of, description of. ... 41-43

sewage discharge into. ................. 34

source and course of .................... 6-7

tributaries of......................... 7,18-23

underground water east of, occurrence

of............................... 43-48

underground water west of, occurrence

of ............................... 38-43

upland area west of, description of. .... 39-41

water from, analyses of ..._.............

Jordan River Valley, area of ...............

drainage area of, map showing. ........

ground water in, depth to, map showing..............................

flowing wells in, area of, map showing.. 

location and trend of ...................

of, view of......................

wells sunk to increase supply of........

Jordan Narrows, Jordan River and canal 

systems in, discharge of........

shore lines on west side of..............

30

5

6

30 

38 

5 

in .............................. 24-25

topography and drainage of ............ 5-7

K.

Kimball Creek, springs in upper valley of . . 55 

water of, use of .................. I ...... 55

wells along ............................. 56

King, Clarence, on geology of the region. . . 7 

Kingsbury, J. T., analyses of water by. .... 30

Knight, N. J., wells of, description of ...... 50-51

L.

Lake Bonneville, description of. ............ 11-13

location of. ............................. 5

shore deposits of ....................... 39, 55

Lake Lahontan, location of ................ 11

Lake Mountains. See Pelican Hills.

Lake shore, location of ..................... 54

Lakes, warm water, occurrence of. ......... 47

Lehi, artesian wells at, irrigation from. . ... 36

flowing and nonflowing well near, line

separating ..................... 49

wells at. ................................ 48

flow of, decrease in. ................ 36

water from, analyses of ............ 32

Lehi and vicinity, underground water conditions of....................... 48-49

Liberty Park, wells at and near, flow of.... 36,44

Literature, geologic ........................ 7-8

Little Cottonwood Canyon, glaciers adjacent to, relics of ................ 47

Little Cottonwood Creek, description of. ... 7, 45

discharge of ............................ 25

rocks on ................................ 9

water from, analysis of. ................ 30

use of. .............................. 44

" Little Cottonwood granite," age of ....... 9

Long Ridge, springs at base of ....:........ 55

structure of.. .......................... 11

Lower Carboniferous fossils, occurrence of. . 10

M.

McDonald, T. F., acknowledgment to. ..... 56

Mapleton Bench, descripton of ............. 53
INDEX.

Page.

Massachusetts State Board of Health, on 

preservation of water supply 

from contamination............ 34-35

Measurement of wells, method of........... 56-59

Mercur, rocks near......................... 10

Mesozoic rocks, occurrence of............... 10

Metamorphic rocks, occurrence of.........". 8

Mill Creek, description of..:................ 7,45

discharge and run-off of, table showing 20,25 

ditch south of, discharge of............. 25

rocks on................................ 9

water of, use of......................... 44

Mill Creek Valley, seepage measurements in 28 

Morgan, E. R., seepage measurements by.. 28 

Mormon pioneers, irrigation by............ 5

Murray, smelters at........................ 5

well at, record of....................... 46

well near, decrease in................... 47

N.

Natural gas, occurrence of.................. 32-33

North Jordan canal, discharge of........... 24

Ogden quartzite, thickness of.............. 8

Oil, search for.............................. 41

Ontario tunnel, discharge of................ 37

Oquirrh Mountains, elevation and extent of. 6

springs in............................... 40

structure of............................. 10

Ordovician rocks, occurrence of............ 11

P.

Paleozoic rocks, occurrence of.............. 8,9

Paleozoic section in Wasatch Mountains,

table showing.................. 8

Palmyra, location of....................... 54

Park City, mines of, water in............... 37

rainfall at, table showing............... 14

Parleys Canyon, reservoir at............... 45

Parleys Creek, description of............... 7,45

discharge and run-off of, table showing 20,25

rocks on................................ 9

water from, analysis of................. 30

use of............................... 44,45

Parsons Chemical Company, analyses of

water by........................ 32

Payson, artesian well at, irrigation from.... 36

location of.............................. 54

water supply of, source of.............. 54

Payson Creek, water'from, analysis of..... 30

Pelican Hills, location and altitude of...... 6

- structure of............................ 10-11

Pelican Point, flowing wells near........... 56

seep springs near....................... 56

Permian rocks, occurrence and character of. 9

Peteeneet Creek, description of............. 6

Pipes, flow from vertical and horizontal,

diagram illustrating............ 57

Placer mining in Bingham Canyon......... 40

Pleasant Grove, location and underground

water conditions of ............ 50-51

water supply of, source, of.............. 49

Pleistocene fault, occurrence of............. 5?

Page. 

Pleistocene rocks, occurrence of............ 10

water in, character of.................. 43

Porous deposits, rainfall absorbed by...... 39-40

Pre-Cambrian rocks, occurrence and character of...-.----...............- 8,9

Precipitation, tables showing......... 14-15,19-22

Provo, location of.......................... 5

rainfall at, table showing.............. 15

sewage of, disposal of.................. 34

temperature at, table showing......... 15

vicinity of, underground water conditions in....................... 51-52

water supply of, source of.............. 51

wells at................................. 32,52

Provo horizon, tufa at, occurrence and

character of.................... 13

Provo River, discharge and run-off of, table

showing........................ 22

drainage area of........................ 6

source and course of.................... 6

valley of, below mouth of canyon, view

of............................... 50

water from, analysis of................ 30

Provo shore line, description of............ 12-13

Pumping plants for irrigation, favorable

conditions for.................. 39

Pyle, F. D., acknowledgment to........... 56

Quaternary history of the region .......... 11-13

R.

Rainfall, tables showing.............. 14-15,19-22

Reclamation Service, levels run by ........ 52

plans of, for Utah Lake project........ 39

" Red Beds," occurrence and character of.. 9 

Red Butte Canyon, rocks in................ 9

Red Butte Creek, description of............ 7

water from, analysis of................ 30

use of............................... 44-45

Reservoirs, profitable locations for........ 38

Richardson, G. B., on natural gas near Salt

Lake City...................... 32

Riggs,R. B., analyses of water by......... 30

Rio Grande Western Railway, wells of...... 32,

42,44,48,52 

Rock Creek Canyon, rocks in............... 10

Rose Canyon, springs in................... 40

Rudy Well, description of.............. 35,42,43

S.

Salt Creek, source and course of............ 6

Salt Lake City, authorities of, wells sunk by,

in 1890.......................... 49

humidity, mean relative, at............. 16,18

location of.............................. 5,43

lowland area south of, description of .. 45-47 

natural gas supply of, source of........ 32-33

rainfall at........................... 14,17-18

rocks in vicinity of..................... 8,9

sewage of, disposal of.................. 34

temperature at...................... 15,16,18

thermal springs at, description of...... 44

underground water conditions of....... 43-45
80 LNDEX.

Page.

Salt Lake City, upland area south of, description of..................... 47-48

water supply of, precaution to avoid

contamination of............... 34

source of........................... 44-45

wells at................................. 42, 44

flow of, decrease in................. 36

wind velocity at, table showing average. 16 

Salt Lake City Spring, water from, analysis

of............................... 30

Salem, location of.......................... 54

underground water conditions in ...... 54

San Pedro, Los Angeles and Salt Lake Railroad, wells of.-.......---. 48,52,53,54

Sandy Spring, water from, analysis of...... 30

Santaquin, location of..................... 54

water supply of, source of.............. 54

Santaquin Creek, description of............ 6

water from, analysis of................ 30

use of............................... 54

Sedimentary rocks, occurrence of......... 8,9,11

Seepage, measurements of.................. 28

Sewage, disposal of, precautions taken for. 34 

Silurian rocks, occurrence of.............. 8,9,11

Slichter, C. £., on measurement of water

flow from pipes................. 56

on method of measurement of wells.... 56-59

Smelters, smoke from, injury by........... 32

Smith, G. O., and Tower, G. W., on ground

water in Homansville Canyon.. 56 

on the Tintic district................... 7

Smith, J. F., jr., discharge data furnished

by.............................. 24

Snow, G. W., acknowledgment to.......... 56

South Jordan canal, description of ........ 39

discharge of............................ 24

Spanish Fork (town), location of........... 53

water supply of, source of.............. 53-54

wells at................................. 53-54

flow of, decrease in................. 36

Spanish Fork (stream), discharge and runoff of, table showing............ 22

drainage area of........................ 6

source and course of.................... 6

water from, analysis of................ 30

use of............................... 54

Spring Creek, flow of....................... 46,52

Spring Lake, location of................... 54

water supply of, source of.............. 54

Springs, occurrence of............. 40,44,47,50,55

water of, character of.................. 31

Springs, hot, occurrence of................. 29,49

Springville, description of.................. 53

vicinity of, underground water conditions in......................... 52-53

wells at................................. 53

water from, analysis of............ 32

Spurr, J. E., or the Mercur mines.......... 7-8

Stanbury Island, shore lines on............ 13

Streams, water of, character of............ 30,31

^Structure of the Highlands................ 8-11

Swendsen, G. L., acknowledgments to..... 24

hot springs discovered by.............. 49

T.

Tanner, Caleb, acknowledgment to........ 51

discharge measurement by............. 2-5

Taylorville roller mill, flume at, discharge

at.............................. 2.5

Temperature, tables showing.............. 15-16

Tertiary history of the region.............. 11

Tertiary rocks, occurrence of............. 8,10,11

Thistle, rainfall at, table showing.......... 15

Timpanogas canal, seepage of ............. 2f

Tintic Mountains, springs in............... 55

Todd, J. E., on measurement of water flow

from pipes...................... 56

Topography, features of................... 5-7

Tower, G. W., and Smith, G. O., on ground

water in Homansville Canyon.. 56 

on the Tintic district................... 7

Traverse Mountains, structure of......... 8-9,10

Tufa, calcareous, occurrence and character

of............................... 13

U.

Underground water. See Water, underground.

United States Mining Company, wells of,

water from, analyses of........ 32

United States Weather Bureau, meteorologic data from records of...... 13-17

Utah and Salt Lake canal, description of .. 39 

discharge of............................ 24

Utah County Infirmary, well at........... 52

Utah Experiment Station, experiments in 

reclaiming land near Salt Lake 

City made by................... 43

Utah Lake, description of.................. 6

elevation of............................ 5

evaporation at......................... 17

fluctuations of......................... 23-24

hot springs at.......................... 4f

northern end of, view of................ 12

sewage discharge into.................. 34

streams tributary to................. 6,18-23

supply of, source of.................... 23-24

underground water west of, occurrence

of............................... 56

water from, analyses of................ 3C

Utah Lake project, plans for............... 3t

Utah Lake Valley, area of................. 5

drainage area of, map showing......... f

flowing wells in, area of, map showing.. 4f 

ground water in, depth to, map showing............................. 3C

location and trend of................... 5

topography and drainage of........... 5-7"

undergrond water in, occurrence of.... 48-5f

Utah Sugar Company, wells of............. 4?

wells of, water from, analysis of....... 32

 Ute limestone, thickness of................ f

V.

Vegetation, character of.. 

Volcanic rock, outcrop of.
INDEX. 81

w.

Wadley, William1 , & Sons, water developed

by .unneling into bed rock..... 50

Walcott, C. D., oh Big Cottonwood Cambrian section................... 7

Warm Creek, source of..................... 31,55

water from, analysis of................ 30

Wasatch fault, description of............. 8,9,10

Wasatch limestone, occurrence, thickness,

and dip of...................... 8

Wasatch Mountains, elevation of.......... 5,6

geology of.............................. 8-9

Paleozoic section in.................... 8

rainfall caused by...................... 18

vegetation on.......................... 7

view of................................. 5

Water, analyses of......................... 30,32

contamination of, precaution taken to

avoid........................... 34

sanitary character of................... 34

Water, underground, depth to, map showing. ............................ 30

distribution of......................... 29-30

occurrence of........................... 38-56

quality of.............................. 30-35

recovery of............................. 35-37

source of............................... 27-28

Water resources, use of, efficiency in....... 38

Weber quartzite, occurrence, thickness, and

dipof........................... 8

Weber River, description of................ 6

IRR 157 06 6

Well sections, plate showing............... 28

Wells, data concerning..................... 56-75

method of measurement of............. 56-59

water from, analyses of..... .......... 32

Wells, flowing, area of, in Jordan _iiver Valley, map showing.............. 38

area of, in Utah Lake Valley, map

showing........................ 44

decrease in, cause of.................... 36

location and description of............. 35-36,

46,50,52,53,54-55 

recovery of water by................... 36

water of, use of...... T .................. 36

yield of, table for determining......... 58

Wells, shallow, recovery of water by....... 36

Wells, typical, list of....................... 59-75

West Jordan, well at, water from, analysis

of............................... 32

West Mountain, warm spring near........ 55.

Westfall, J., information furnished by..... 52

Westphal, Gus, well record furnished by... 42 

Widtsoe, J. A., on effects of smelter smoke. 32 

Willow Creek, description of............... 7

Wilson, H. M., on wind velocity required

for windmills................... 36

Wind velocity at Salt Lake City, table

showing average............... 16

Windmills, wind velocity required for..... 36

Y.

Yeager, H. F., well record furnished by.... 46
CLASSIFICATION OF THE PUBLICATIONS OF THE UNITED STATES GEOLOGICAL

SURVEY.

[Water-Supply Paper No. 157.]

The serial 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 the 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 may be had 

on application.

Most of the above publications may be obtained or consulted in the following 

ways:

1. A limited number are delivered to the Director of the Survey, from whom they 

may 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.

3. Other copies are deposited with the Superintendent of Documents, Washington, 

D. C., from whom they may 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 may 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; O, Underground waters; P, Hydrographic progress reports. 

This paper is the eighty-sixth in Series B, and the fifty-third in Series O, the compete 

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 Upham. 1887. 84 pp., 1 pi.

(Out of stock.) 

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 Hay. 1890. 49 pp., 2 pis. (Out

of stock.) 

B 68. The glacial boundary in western Pennsylvania, Ohio, Kentucky, Indiana, and Illinois, by G. F.

Wrijjht, with introduction by T. C. Chamberlin. 1890. 112 pp., 8 pis. (Out of stock.)
II SEEIE8 LIST.

B 67. The relations of the traps of the Newark system in the New Jersey region, by N. H. Dartor.

1890. 82pp. (Out of stock.) 

B 104. Glaciation of the Yellowstone Valley north of the Park, by W. H. Weed. 1893. 41 pp., 4 pis.

(Out of stock.) 

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.

(Out of stock.) 

B 137. The geology of the Fort Eiley Military Reservation and vicinity, Kansas, by Robert Hay.

1896. 35 pp., 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 Goshen Hole quadrangles in eastern

Wyoming and western Nebraska, by G. I. Adams. 1902. 50pp., 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 cf

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. Pattor.

1902. 167 pp., 19 pis. 

PP 10. Reconnaissance from Port Hamlin to Kotzebue Sound, Alaska, by way of Ball, Kanuti, Aller,

and Kowak rivers, by W. C. Mendenhall. 1902. 68pp., 10 pis.

PP 11. Clays of the United States east of the Mississippi River, by Heinrich Ries. 1903. 298 pp., 9 pis. 

PP 12. Geology of the Globe copper district, Arizona, by P. L. Ransbme. 1903. 168 pp., 27 pis. 

PP13. Drainage modifications in southeastern Ohio and adjacent parts of West Virginia and Kertucky, by W. G. Tight. 1903. Ill pp., 17 pis.

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.

B 209. G*eology of Ascutney Mountain, Vermont, by R. A. Daly. 1903. 122 pp., 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. 71pp., 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. Darton. 1903. 69 pp., 43 pis. 

B 217. Notes on the geology of southwestern Idaho and southeastern Oregon, by I. C. Russell. 190".

83 pp., 18 pis. (Out out stock.) 

B 219. The ore deposits of Tonopa.h, Nevada (preliminary report), by J. E. Spurr. 1903. 31 pp., 1 pK

(Out of stock.)

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. If.

Todd and C. M. Hall. 1904. 47 pp., 23 pis.

PP25. The copper deposits of the Encampment district, Wyoming, by A. C. Spencer. 1904. 107pp.,2pls. 

PP 26. Economic resources of northern Black Hills, by J. D. Irving, with chapters by S. F. Emmons

and T. A. Jaggar, jr. 1904. 222 pp., 20 pis.

PP 27. Geological reconnaissance across the Bitterroot Range and the ClearwaterMountains 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 Oklalioma, by J. A. Taff, with an appendix on reported ore deposits in the Wichiti

Mountains, by H. F. Bain. 1904. 97 pp., 8 pis. 

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. 

B 238. Economic geology of the lola quadrangle, Kansas, by G. I. Adams, Erasmus Haworth, and

W. R. Crane. 1904. 83 pp., 1 pi.
SEEIE8 LIST. Ill

PP 32. Geology and underground water resources of the central Great Plains, by N. H. Barton. 1905.

433 pp., 72 pis. 

WS 110. Contributions to hydrology of eastern United States, 1904; M. G. Fuller, geologist in charge.

1905. 211 pp., 5 pis. 

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 northwestern Illinois, by H. F. Bain. 1904. 56 pp., 5 pis. 

B 247. The Fairhaven gold placers of Seward Peninsula, Alaska, by F. H. Mofftt. 1905. 85 pp., 14 pis. 

B 249. Limestones of southwestern Pennsylvania, by F. G. Clapp. 1905. 52 pp., 7 pis. 

B 250. The petroleum fields of the Pacific coast of Alaska, with an account of the Bering River coal

deposit, by G. C. Martin. 1905. 64 pp., 7 pis. 

B 241. The gold placers of the Fortymile, Birch Creek, and Fairbanks regions, Alaska, by L. M.

Prindle. 1905. 89pp., 16 pis. 

WS 118. Geology and water resources of a portion of east central Washington, by F. C. Calkins. 1905.

96 pp., 4 pis. 

B 252. Preliminary report on the geology and water resources of central Oregon, by I. C. Russell.

1905. 138pp., 24 pis. 

PP 36. The lead, zinc, and fluorspar deposits of western Kentucky, by E. 0. 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 areal 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.,

20 pis. 

B 254. Report of progress in the geological resurvey of the Cripple Creek district, Colorado, by Waldemar Lindgren and F. L. Ransome. 1904. 36 pp.

B 255. The fluorspar deposits of southern Illinois, by H. Foster Bain. 1905. 75 pp., 6 pis. 

B 256. Mineral resources of the Elders Ridge quadrangle, Pennsylvania, by R. W. Stone. 1905.

86pp., 12 pis. 

B 257. Geology and paleontology of the Judith River beds, by T. W. Stanton and J, B. Hatcher, with

a chapter on fossil plants, by F. H. Knowlton. 1905. 174 pp., 19 pis.

PP 42. Geology of the Tonopah mining district, Nevada, by J. E. Spurr. 1905. 295 pp., 23 pis. 

WS 123. Geology and underground water conditions of the Jornada del Muerto, New Mexico, by

C. R. Keyes. 1905. 42 pp., 9 pis.

WS 136. Underground waters of Salt River Valley, Arizona, by W. T. Lee. 1905. 194 pp., 24 pis. 

PP 43. The copper deposits of the Clifton-Morenci district, Arizona, by Waldemar Lindgren. 1905.

375 pp., 25 pis.

B 265. Geology of the Boulder district, Colorado, by N. M. Fenneman. 1905. 101 pp., 5 pis. 

B 267. The copper deposits of Missouri, by H. F. Bain and E. O. Ulrich. 1905. 52 pp., 1 pi. 

PP 44. Underground water resources of Long Is]and, New York, by A. C. Veatch and others. 1905.

394pp., 34 pis.

WS 148. Geology and water resources 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. N. Dale. 1905. 52 pp., 14 pis. (Out of stock.) 

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 R. U. Goode. 1906. 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. 

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. 

B 277. Mineral resources of Keiiai Peninsula, Alaska: Gold fields of the Turnagain Arm region, by

F. H. Moffit, and the coal fields of Kachemak Bay region, by R. W. Stone. 1906. 

WS 154. The geology and water resources of the eastern portion ot the Panhandle of Texas, by C. N.

Gould. 1906. 64pp., 15 pis.

B 278, Geology and coal resources of the Cape Lisburne region, Alaska, by A. J. Collier. 

B 279, Mineral resources of the Kittanning and Rural Valley quadrangles, Pennsylvania, by Charles

Butts.
IV SEKIES LIST.

B 280. The Rampart gold placer region, Alaska, by L. M. Prindle and P. L. Hess. 

B 282. Oil fields of the Texas-Louisiana Gulf coastal plain, by N. M. Fenneman. 

WS 157. Underground water in the valleys of Utah Lake and Jordan River, Utah, by G. B. Richardson. 

1906. 81 pp., 9 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 Portier. 1897. 50 pp., 3 pis. (Out of stock.) 

WS 12. Underground waters of southeastern Nebraska, by N. H. Darton. 1898. 56 pp., 21 pis. (Out

of stock.)

WS 21. Wells of northern Indiana, by Frank Leverett. 1899. 82pp., 2 pis. (Out of stock.) 

WS 26. Wells of southern Indiana (continuation of No. 21), by Prank Leverett. 1899. 64 pp. (Out

of stock.) 

-WTS 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. 97pp., 4 pis. (Out of stock.) 

WS 34. Geology and water resources of a portion of southeastern South Dakota, by J. E. Todd. 1900.

34 pp., 19 pis. 

WS 53. Geology and water resources of Nez Perces County,.Idaho, Pt. I, by I. C. Russell. 1901. 86

pp., 10 pis. (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.) 

WS 55. Geology and water resources of a portion of Yakima County, Wash., by G. 0. Smith. 1901.

68 pp., 7 pis. (Out of stock.) 

WS 57. Preliminary list of deep borings in the United States, Pt. I, by N. H. Darton. 1902. 60 pp.

(Out of stock.) 

WS 59. Development and application of water in southern California, Pt. I, by J. B. Lippincott.

1902. 95pp., 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. 62 pp., 4 pis. 

WS 78. Preliminary report on artesian basin 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. Puller. 1904. 98 pp., 11 pis.

WS 102. Contributions to the hydrology of eastern United States, 1903, by M. L. Puller. 1904. 522 pp. 

WS 104. Underground waters of Gila Valley, Arizona, by W. T. Lee. 1904. 71 pp., 5 pis. 

WS 110. Contributions to the hydrology of eastern United States, 1904; M. L. Puller, 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; M. L. Puller, geologist in charge. 1904.

285 pp., 18 pis. 

WS 118. Geology and water resources of east-central Washington, by P. C. Calkins. 1905. 96 pp.,

4 pis. 

B 252. Preliminary report on the geology and water resources of central Oregon, by I. C. Russell.

1905. 138pp., 24 pis. 

WS 120. Bibliographic review and index of papers relating to underground waters published by the

United States Geological Survey, 1879-1904, by M. L. Puller. 1905. 128 pp. 

WS 122. Relation of the law to underground waters, by D. W. Johnson. 1905. 55 pp.
SERIES LIST. V

WS 123. Geology and underground water conditions of the Jornada del Muerto, New Mexico, by C. R. 

Keyes. 1905. 42 pp., 9 pis.

WS 136. Underground waters of 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.

PP 44. 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.

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.

WS 142. Hydrology of San Bernardino Valley, California, by W. C. Mendenhall. 1905. 124 pp., 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. Darton. 1905. 175 pp. 

PP 46. Geology and underground water resources of northern Louisiana and southern Arkansas, by

A. C. Veatch.. 1906.

WS 153. The underflow in Arkansas Valley in western Kansas, by C. S. Slichter. 19C6. 

WS 154. The geology and water resources of the uastern 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. 

WS 157. Underground water in the valleys of Utah Lake and Jordan River, Utah, by G. B. Richardson.

1906. 81 pp., 9 pis.

The following papers also relate to this subject: Underground waters of Arkansas Valley in eastern 

Colorado, by G. K. Gilbert, in Seventeenth Annual, Pt. II; Preliminary report on artesian waters of a 

portion of the Dakotas, by N. H. Darton, in Seventeenth Annual, Pt. II; Water resources of Illinois, 

by Frank Leverett, in Seventeenth Annual, Pt. II; Water resources of Indiana and Ohio, by Frank 

Leverett, in Eighteenth Annual, Pt. IV; New developments in well boring and irrigation in eastern 

South Dakota, by N. H. Darton, in Eighteenth Annual, Pt. IV; Rock waters of Ohio, by Edward 

Orton, in Nineteenth Annual, Pt. IV; Artesian well prospects in the Atlantic coastal plain region, by 

N. H. Darton, Bulletin No. 138.

Correspondence should be addressed to

THE DIRECTOR,

UNITED STATES GEOLOGICAL SURVEY, 

APRIL, 1906. WASHINGTON, D. C.

O