geology and occurrence of ground water in the townsend ... · geology and occurrence of ground...

Geology and Occurrence of Ground Water in the Townsend Valley Montana

GEOLOGICAL SURVEY WATER-SUPPLY PAPER 1360-C

Geology and Occurrence of Ground Water in the Townsend Valley MontanaBy H. W. LORENZ and R. G. McMURTREYWith a section on

CHEMICAL QUALITY OF THE GROUND WATER By H. A. SWENSON

CONTRIBUTIONS TO HYDROLOGY OF THE UNITED STATES

GEOLOGICAL SURVEY WATER-SUPPLY PAPER 1360-C

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1956'*

UNITED STATES DEPARTMENT OF THE INTERIOR

Fred A. Seaton, Secretary

GEOLOGICAL SURVEY

Thomas B. Nolan, Director

For sale by the Superintendent of Documents, U. S. Government Printing Office ^ Washington 25, D. C.

CONTENTS

PageAbstract.................................................................................................................................... 171Intioductioa.............................................................................................................................. 172

Location and extent of area................................................................................................ 172Purpose and scope of investigatioa.................................................................................. 173Previous investigations....................................................................................................... 174Acknowledgments.................................................................................................................. 174History of the area................................................................................................................ 175Well-numbering system......................................................................................................... 175

Geography................................................................................................................................... 175Climate................................................................................................................................... 175Drainage................................................................................................................................. 180Irrigation................................................................................................................................. 181Agriculture and vegetatioa.................................................................................................. 183Mining...................................................................................................................................... 183Transportatioa....................................................................................................................... 184

Geomorphology........................................................................................................................... 185Geology....................................................................................................................................... 188

Stratigraphy............................................................................................................................ 192Precambrian rocks........................................................................................................... 192Cambrian rocks.................................................................................................................. 193Devonian rocks.................................................................................................................. 195Mississippi an rocks.......................................................................................................... 195Pennsylvanian and Permian rocks.................................................................................. 195Jurassic rocks.................................................................................................................... 196Cretaceous rocks................................................................................................................ 196Tertiary-deposits............................................................................................................... l%Quaternary deposits.......................................................................................................... 198

Igneous rocks......................................................................................................................... 199Sills..................................................................................................................................... 200Dikes and stocks............................................................................................................... 200

Structure.................................................................................................................................. 201Folds................................................................................................................................... 201Faults.................................................................................................................................. 203Earthquakes........................................................................................................................ 204

Summary of geologic history.... .......................................................................................... 205Ground water.............................................................................................................................. 208

Recharge................................................................................................................................. 208Changes in storage................................................................................................................ 209Movement................................................................................................................................ 211Effects of earthquakes.......................................................................................................... 213Waterlogging........................................................................................................................... 213Discharge................................................................................................................................ 215

Evapotranspiratioa........................................................................................................... 215Seepage into streams........................................................................................................ 215Springs................................................................................................................................ 215Wells.................................................................................................................................... 218

Use.......................................................................................................................................... 219Chemical quality of the water, by H. A. Swenson................................................................ 222

Ground-water supplies.......................................................................................................... 225Pre-Tertiary rocks............................................................................................................. 225Tertiary deposits............................................................................................................... 225Alluvium.............................................................................................................................. 228Undifferentiated deposits................................................................................................. 229

Surface-water supplies.......................................................................................................... 229

III

IV CONTENTS

PageChemical quality of the water, by H. A. Swenson Continued

Suitability for use................................................................................................................. 229Irrigatioa........................................................................................................................... 230Domestic............................................................................................................................ 230

Summary and conclusions........................................................................................................ 230Literature cited........................................................................................................................ 232Index.......................................................................................................................................... 289

ILLUSTRATIONS

Page Plate 19. Geologic map of the Townsend Valley, Montana.................................... In pocket

20. Map of the Townsend Valley showing the location of wells, land under irrigation, land proposed for irrigation, waterlogged areas, and contour of ground-water surface...................................................... In pocket

Figure 29. Map showing areas in which ground-water studies have been madeunder the program for development of the Missouri River basin................. 172

30. Sketch showing well-numbering system.............................................................. 17731. Precipitation records at Canyon Ferry, 1899-1949.......................................... 17832. Precipitation records at Helena, 1884-1949..................................................... 17933. Panoramic view of the Townsend Valley........................................................... 18634. View north from the southeast corner of sec. 4., T. 5 N., R. 1 E.................. 19335. Faults in Tertiary lake beds as seen across Sixmile Creek from the

southeast corner of sec. 12, T. 5 N., R. 2 E................................................ 20436. Hydrographs showing fluctuations of the water level in observation wells.. 21037. Profiles showing relation of the ground-water surface to the land surface... 21238. Diagrammatic log of well A6-2-2db..................................................................... 22139. Cumulative amounts, in percent, of minerals in spring water from pre-

Tertiary rocks, 1921-22 and 1949.................................................................. 22640. Analyses of ground water in Tertiary deposits and alluvium.......................... 227

TABLES

Page Table 1. Irrigation canals, water rights, number of users, and irrigated acreage

in the Townsend Valley.................................................................................... 1822. Sedimentary rocks of the Townsend Valley and their water-bearing

properties........................................................................................................... 1893. Chemical analyses of water................................................................................. 2234. Measurements of the water level in observation wells.................................... 2345. Record of wells and springs................................................................................ 268

CONTRIBUTIONS TO THE HYDROLOGY OF THE UNITED STATES

GEOLOGY AND OCCURRENCE OF GROUND WATER IN THE TOWNSEND VALLEY, MONTANA

By H. W. Lorenz and R. G. McMurtrey

ABSTRACT

The Townsend Valley in west-central Montana is a 600 square-mile intermontane basin bordered by the Big Belt Mountains on the east and by the Elkhorn Mountains on the west. It extends from approximately T. 4 N., to T. 11 N., inclusive. Rocks ranging in age from Precambrian to Cretaceous crop out in the mountainous areas that surround the valley, and rocks of Tertiary (Oligocene and Miocene) age crop out on the higher valley slopes and underlie the alluvial deposits in the valley bottom. The area is drained by the Mis souri River, which enters the Townsend Valley through a gorge at the southern end of the valley and leaves through another gorge at the northern end.

The climate of the valley is semi arid; the average annual precipitation is 12.35 inches. Farming is the principal occupation. About one-third of the cultivated land is irrigated by water diverted from the Missouri River and perennial mountain streams, and the remaining cultivated land is farmed by dryland methods. Wheat, oats, barley, sugar beets, and pota toes! are the principal crops.

Mining, which was once the chief industry of the area, is now (1951) sporadic and on a small scale. Gold, silver, and lead are the chief metals mined. Small amounts of coal, marble, quartzite, and iron ore have been mined during the past 10 years.

A large reservoir of ground water underlies the valley. On the valley floor shallow well s yield an abundant supply of water for domestic and stock use, but on the higher slopes wells must be drilled to a depth of 200 to 300 feet to obtain an adequate supply.

Water is confined under artesian pressure in Tertiary beds that underlie the southern end of the valley and the area along the west flank of the Dry Creek anticline east of Townsend.

The denser pre-Tertiary formations contain water in fissures and small openings and springs are numerous where these rocks crop out. Big and Plunket (Mockel) Springs, which yield about 57 and 8.7 cfs, respectively, are the largest.

The principal sources of recharge to ground water in the younger, unconsolidated de posits are streams, irrigation canals and laterals, and irrigation floodwater. About 8,500 acres of the land is waterlogged because the transmissibility of the underlying water bearing materials is low or because the configuration of the bedrock is such that the movement of ground water is restricted. Of this total, 1,500 acres will be inundated by water impounded by the Canyon Ferry dam. Drainage of the remaining waterlogged land would greatly increase the agricultural potential of the valley.

Irrigation utilizing ground-water resources is in a pioneering stage in the Townsend Valley. In the summer of 1950 the first well for irrigation supply was drilled 3% miles southeast of Townsend and when tested, using air compressors, produced about 240 gpm.

171

172 CONTRIBUTIONS TO HYDROLOGY

Water from ground and surface sources in the Townsend Valley generally is hard bat only moderately mineralized and is suitable for most domestic and irrigation uses. The range in dissolved solids and hardness of 38 samples of ground water was 134 to 976 ppm and 84 to 602 ppm, respectively. Samples collected in 1921-22 and again in 1949 from springs in this region show about the same chemical character. The effects of waterlog ging on the quality of the ground water cannot at present be determined, but evidence in dicates that the mineral content of the ground water has not yet changed Materially.

INTRODUCTION

LOCATION AND EXTENT OF AREA

The Townsend Valley trends slightly northwest across the central part of Broadwater County and the southeastern part of Lewis and Clark County, in west-central Montana. (See fig. 29.) The val ley is bordered by the Big Belt Mountains on the east and by the Elkhorn Range on the west. The area studied extends from about T. 4 N. , to T. 11 N., inclusive. Townsend, the county seat of Broadwater County, is in the central part of the valley and is 35 miles southeast of Helena, the capital of Montana.

The part of the valley underlain by Tertiary and younger sedi ments has a maximum width of 15 miles and a length of about 45 miles. The Missouri River flows northward, entering the valley .near. Toston and leaving it at Canyon Ferry. Near its southern

EXPLANATION

Area described in this report

Areas described in other reports

Figure 29. Map showing areas in which ground-water studies have been made under the program for development of the Missouri River basin.

INTRODUCTION 173

end the valley broadens into a low, gently sloping plain which is crossed by Crow Creek. This plain, approximately 10 miles wide from east to west and 15 miles long, will be referred to as the Crow Creek area in this report.

PURPOSE AND SCOPE OF INVESTIGATION

The purpose of the study was to collect and evaluate data per taining to the general ground-water conditions of the Townsend Valley. The bottom lands of the valley are irrigated at the pres ent time (1951), and the higher parts have been proposed for ir rigation under the program of the United States Department of the Interior for development of the Missouri River basin. Fieldwork was done by the senior author between June and October 1949 and by both authors during the 1950 field season. However, periodic measurement of the water level in selected observation wells was continued by the junior author until February 1954.

Construction of the new Canyon Ferry dam across the Missouri River at the north end of the Townsend Valley was begun by the United States Bureau of Reclamation on July 22, 1949. When the water behind the completed dam reaches its maximum height (3, 800 feet above sea level), the reservoir will contain 2 million acre-feet of water and will inundate 35, 200 acres of land (see pi. 19). About 30, 000 acres within the boundary of the proposed res ervoir is farmland of which 10,000 acres is under irrigation and the remainder either dry-farmed or used for grazing.

According to plans made by the Bureau of Reclamation, about 5, 000 additional acres in the Crow Creek area southwest of Tos- tori is to be irrigated by pumping water from the Missouri River at a point about 2 miles below Lombard. Thus, the area proposed for irrigation will replace about half the 10,000 acres of irrigated farmland that will be inundated by backwater from the Canyon Ferry dam. Ground-water conditions in the area proposed for ir rigation will be changed materially as a result of the irrigation.

The geology of the area was mapped by the senior author on aerial photographs and transferred later to a base map by use of a sketchmaster. The study of ground-water conditions included an inventory of wells used for domestic purposes, watering of stock, and irrigation. Measurements of the water level in obser vation wells were made periodically; hydrographs showing the water-level fluctuation in a few typical wells and a water-table contour map were prepared. The altitude of the measuring point of the wells was determined instrumentally.


The field investigation was under the general direction of A. N. Sayre, chief of the Ground Water Branch of the United States Geo logical Survey, and G. H. Taylor, regional engineer in charge of ground-water investigations in the Missouri River basin, and un der the direct supervision of F. A. Swenson, district geologist in charge of ground-water investigations in Montana and northern Wyoming. The quality-of-water study was under the general di rection of S. K. Love, chief of the Quality of Water Branch, and P. C. Benedict, regional engineer in charge of quality-of-water investigations in the Missouri River basin.

PREVIOUS INVESTIGATIONS

The first study of the geology and the ground-water resources of the Townsend Valley was made by Par dee (1925). No further geologic work of note was done in the Townsend Valley until 1946, when the geology and mineral resources of the Canyon Ferry quadrangle, including about 300 square miles in the northern part of the valley, were mapped by the U. S. Geological Survey. In 1949 Edward T. Ruppel, 1 of the Geological Survey, mapped the geology of the Limestone Hills southwest of Townsend. Reports based on these studies, and other reports describing the geology and the mineral resources of the region, were drawn on freely in the preparation of this report and are listed at the end of the report.

ACKNOWLEDGMENTS

The writers appreciate the assistance they received from many persons during the course of the field study and in the preparation and review of this report. Both the late A. H. Tuttle, recently retired district engineer, Surface Water Branch, and his succes sor, Frank Stermitz, gave much valuable help. M. R. Klepper of the Mineral Deposits Branch spent several days in the field with the senior author, and F. C. Koopman of the Ground Water Branch aided in the construction of observation wells. Leroy Kay of the Carnegie Museum, Pittsburgh, Pa., gave much assistance in the study of Tertiary deposits. F. V. Munro and others of the U. S. Bureau of Reclamation furnished ground-water data and maps of the proposed Crow Creek irrigation unit. Clayton Ogle, work unit conservationist of the Soil Conservation Service, made available some ground-water, soil, crop> and irrigation data from Broad- water County. Many farmers furnished information about their wells and gave permission for the periodic measurement of the water level in their wells.

IRuppel, £. T., 1950, Geology of the Limestone Hills, Broadwater County, Mont., Master's diesis, Univ. Wyoming, Laramie; aZso U. S. Geol* Survey open-file rept.

INTRODUCTION 175

HISTORY OF THE AREA

Members of the Lewis and Clark Expedition were the first white men to see the Townsend Valley and to record their passage through the area. On July 21, 1805, Lewis recorded in his journal (Thwaites, 1904):

***the country was rough mountainous and much as that of yesterday until towards evening when the river entered a beautiful and extensive plain country 10 or 12 miles wide which extends upwards further than the eye could reach. This valley is bounded by two nearly parallel ranges of high mountains which have their summits partially covered with snow***.

Four days were required for the expedition to travel up the val ley from Canyon Ferry to the deep gorge where the river enters the valley near Toston. During their travel, they noted that many mountain streams joined the river and that a large number of springs fed these streams; they made specific reference to two that are now known as Big Spring and Plunket Spring.

After the departure of the Lewis and Clark Expedition, nothing of recorded historic importance occurred in the Townsend Valley for nearly 60 years. During the winter of 1864 65, gold was dis covered by some Confederate soldiers of Price's army who had fled up the Missouri River in 1861. Some of the gravel in Confed erate Gulch was reported to have the highest gold content ever found in Montana; a small amount of it yielded $1, 000 worth of gold to the pan. Word of the fabulous richness of the gravel in Confederate Gulch spread rapidly; hundreds of miners hurried into the area, and their settlement in the gulch became known as Diamond City, the mining capital of western Montana. Prosperity lasted for only a decade and the once thriving mining center grad ually became a ghost town.

In 1866 both lode and placer gold were found near Radersburg, which was then a small station on the overland route from Helena to Bozeman. For a short while, Radersburg was| the county seat of Jefferson County and, during the prosperous mining days be fore the turn of the century, it was a thriving community. When lode mining was no longer successful in the vicinity, the town dwindled to a small trading post.

After the discovery of gold at Diamond City and the opening of the lode mines at Radersburg, the demand for food and farm pro duce greatly increased. A large grist mill, powered by water, was built and operated at Bedford during the 1870's. The remains of the mill, one of the oldest in the State, can be seen near U. S. Highway ION, 3 miles northwest of Townsend.


Hassel, at one time called St. Louis, was situated along the banks of Indian Creek, 6 miles west of Townsend, and was the center of a gold- and silver-producing area for many years. At one time, one of the largest and most elaborate ore concentrators in Montana was located near Hassel on the Diamond Hill property. Large-scale mining ceased about 1900; eventually the town was abandoned and the last of its dwellings removed.

After mining became less profitable, many miners turned to farming, which later became the principal means of livelihood in this area. Townsend, founded in 1883, became the trading post. In 1897 it became the county seat of Broadwater County and soon grew to be the largest town in the valley.

WELL-NUMBERING SYSTEM

Wells described in this report are numbered according to their location within the U. S. Bureau of Land Management's system of land subdivision (fig. 30). The first letter of a well number indi cates the quadrant of the meridian and baseline system in which the well is located. The quadrants are identified by capital let ters, beginning with A in the northeast quadrant and proceeding counterclockwise. All of the wells described in this report are in the northeast (A) or northwest (B) quadrants of the principal me ridian (Montana) and baseline system. The township in which a well is located is indicated by the first numeral of the well num ber, the range by the second numeral, and the section by the third. The two lowercase letters following the section number indicate the location of the well within the quarter section and the quarter-quarter section, respectively. The letters are assigned in a counterclockwise order, beginning with a in the northeast quarter or quarter-quarter section. Serial numbers are appended to the last lowercase letter if two or more wells are located with in the same quarter-quarter section.

GEOGRAPHY

CLIMATE

The climate of the Townsend Valley is characterized by low rainfall and humidity, great temperature extremes, and an abun dance of sunshine. Midsummer days are warm and occasionally hot, but, because the humidity is usually low, they are tolerable and pleasant. The extreme cold of winter also is tempered by the dry atmosphere. Often, cold spells are terminated by warm winds, or chinooks.

GEOGRAPHY 177

R.2W. I 234567 R.8E.

\ABASELINE

7. 10 N.

9

8

7

6

5

4

3

2

.WELL B9-|-22cd

R.2E.

e;

7

IB

19

30

31

5

8

17

20

29

32

4*~

9

16

21

28

33

-~--~ 3

10

15

22

27

34

2

II

14

23

26

35

1

12

13

24

25

36

WELL A6-2-40C

Section 4

4. 4 -I

a | b

d 1 c

Figure 30. Sketch showing well-numbering system.


In the summer, light thunderstorms occur frequently in the val ley. Usually the storms move from west to east and are of short duration and of local extent. Generally much more moisture falls on the mountains than in the valley. The strong winds and hail that often accompany the rainstorms sometimes damage the farm crops. Precipitation on the valley floor is not sufficient for most crops.

The annual rainfall recorded by the United States Weather Bu reau station at Canyon Ferry for aperiod of 51 years (1899 1949) averaged 11.35 inches. (See fig. 31.) An average of 37 percent of the annual precipitation falls during May and June; an average of 20 percent falls during June, the wettest month. Only 3 per cent falls during February, the driest month. During the 51-year period, the annual precipitation has ranged from a minimum of 6.01 inches in 1919 to a maximum of 17.43 inches in 1947.

A longer record of precipitation has been made by the Weather Bureau station at Helena, which is approximately 15 miles west of Canyon Ferry. There, the average annual precipitation for a 66-year period (1884-1949) was 12.56 inches. (See fig. 32.) About 33 percent of the annual precipitation falls during May and June; an average of 18 percent falls during June, the wettest month. Only 5 percent falls during February, the driest month.

CUMULATIVE DEPARTURE FROM AVERAGE PRECIPITATION

10Average 11.35

ANNUAL PRECIPITATION

Total of the maximum shown, 33.4 in.

Total of the overage shown, 1135 in.

Totol of the minimum shown, 0.66 in.

From records of the U. S. Weather Bureau

Figure 31. Precipitation records at Canyon Ferry, 1899-1949.

GEOGRAPHY 179

30

CUMULATIVE DEPARTURE FROM AVERAGE PRECIPITATION

ANNUAL PRECIPITATION

EXPLANATION

Total of the maximum shown, 41.68 in.

Total of the average shown, 12.56 in.

Total of the minimum shown, 0.82 in.

From record* of the U.S. Weother Bureau

Figure 32. Precipitation records at Helena, 1884-1949.


The graph (fig. 31) showing the cumulative departures from average precipitation at Canyon Ferry indicates that the periods 1899 1917 and 1937 50 were characterized by above-average pre cipitation and the intervening period, 1918 36, by below-average precipitation. Somewhat in contrast, precipitation records for Helena indicate that the period 1890 1927 was characterized by above-average precipitation and the period from 1928 47 by below- average precipitation.

The mountains and canyons surrounding the valley influence the movement of air masses across the valley floor; consequently, some parts of the valley have a longer frost-free growing season and also receive less damage from hail than do other parts. In the southern part of the valley, the average frost-free period is reported by Gieseker (1944, p. 13) to extend from late May to early September; in the northern part, however, it extends from early May to late September. The mean annual temperature at Canyon Ferry is 43.7° F. The lowest recorded midwinter temper ature is -41° F and the highest recorded midsummer temperature is 104° F. January is the coldest month and has a mean tempera ture of 19. 9°F; July is the warmest month and has a mean tem perature of 68. 6° F.

The mean annual temperature recorded at Helena is 43. 8° F. The lowest recorded midwinter temperature was -42° F on Janu ary 31, 1893, and the highest recorded midsummer temperature was 103°F on August 21, 1940. January is the coldest month and has anaverage temperature of 20.5°F; July is the warmest month with an average temperature of 67. 8°F.

DRAINAGE

The Missouri River and its tributaries drain all the area cov ered by this investigation. The river enters the Townsend Valley through a double-horseshoe gorge southeast of Toston and leaves the valley through a gorge at Canyon Ferry. A concrete dam, now (1951) under construction at Canyon Ferry, will regulate the flow of the Missouri River where it leaves the Townaend Valley. The_altitude of the river near Toston is 3,900 feet and downstream at Canyon Ferry its altitude is 3,660 feet; the gradient of the riv er is a little more than 5 feet to the mile. The mean annual flow of the river at Toston for the periods 1910 16 and 1941 45 ranged from 5,060 to 6,990 cfs and the average flow was about 5,800 cfs. The maximum discharge of 29,800 cfs was measured June 1, 1913; the minimum discharge (regulated by power and storage dams upstream) of 562 cfs was measured on April 30, 1941. The minimum daily discharge (estimated) of 1, 100 cfs occurred on

GEOGRAPHY 181

February 10, 1914 (Pardee, 1925, p. 9). Since 1940 the Broad- water Canal, which has a capacity of 350 cfs, has diverted water for irrigation from the river 3 miles above the gaging station at Toston.

Eleven perennial streams enter the Missouri River in the Town- send Valley. Deep Creek is the largest of the streams that issue from the Big Belt Mountains to the east of the valley. Crow Creek and Beaver Creek are the largest perennial streams that head in the Elkhorn Mountains west of the valley.

Two random measurements of the flow of Deep Creek, made about 10 miles east of its confluence with the Missouri River, are as follows: October 30, 1910, 17.4 cfs, and May 12,1911, 45 cfs (U. S. Geol. Survey, 1911, p. 48, 49). The flow of Crow Creek, about 5 miles northwest of Radersburg, was measured during the period 1919 22; the maximum discharge was 817 cfs, the mini mum discharge was 2. 5 cfs, and the average discharge was 60.0 cfs (Colby and Oltman, 1938, p. 39). Deep Creek and Crow Creek contribute about half the total volume of water that is discharged by the perennial streams entering the Missouri River in the Town- send Valley. After they leave the mountains, all the perennial streams lose a large volume of water by seepage into the under lying sand and gravel. During the spring and summer months, much of the water in these main streams is diverted for irriga tion; consequently, only a small fraction of the water in the upper stretches of the streams reaches the Missouri during that part of the year. However, many intermittent tributaries issue from the terraces and benchlands that border the river.

IRRIGATION

Irrigation in the Townsend Valley began during the early devel opment of the area. The first water right for Crow Creek was recorded in 1865, for Deep Creek in 1866, and for Greyson Creek in 1867. By constructing small dams in the streams, the stock men diverted the perennial flow and floodwaters onto meadowlands for the production of wild hay.

Since 1900 irrigation developments have been on a much larger scale. The irrigation systems are mostly privately owned, al though a few companies or associations have been organized for the development and improvement of these and new systems. In 1901 the Montana Ditch Co. was organized to irrigate the lowlands northeast of Townsend. A number of smaller systems, which de pended chiefly upon floodwater, also were developed. In 1939 the State Water Conservation Commission completed a diversion dam


south of Toston in the double-horse shoe canyon of the Missouri River. (See fig. 33.) Water is diverted into a large canal that parallels the river downstream for about a mile and then branches into two smaller canals of unequal capacity. The larger of these canals crosses the Missouri River through a steel flume and fur nishes irrigation water to about 15, 000 acres of low-terrace land and benchland north of Toston. The smaller canal continues west erly along the south side of the river and irrigates about 3, 000 acres in the lower part of the Crow Creek area. Water was first diverted into these canals in the spring of 1940. Water from Big Spring is diverted into another irrigation canal that supplies lands north and west of Toston.

About 35,500 acres is assessed as irrigated land in Broadwater County. The following table summarizes the water allotment for each canal, the number of users, and the number of acres irri gated by each major canal or irrigation project in the Townsend Valley. In addition to the land indicated in table 1, a considerable

Table 1. Irrigation canals, waiter rights, number of users, and irrigated acreage in.Townsend Valley

[From records of U. S. Soil Conservation Service office for Broadwater County, Townsend, Mont.]

Name of canal

Missouri River Water Users Association (Broad-

Irish Ditch...................................................Big Spring Ditch...........................................

Water right (Cubic feet per

second)

1400110

50507010.6

Number of

users

2097

1212

Acres irrigated

18, 0002,200

8001,2001.200

640

JCanal capacity 350 cfs.

acreage is privately irrigated. The type of agriculture on the larger irrigation projects in the valley has been gradually chang ing from stock raising and hay production to more diversified farm practices; increasingly larger acreages of small grains, sugar beets, peas, and potatoes are being planted. Uncontrolled flooding is practiced on many of the irrigated farms and, in places, this has resulted in the waterlogging of much land. A sprinkler-type irrigation system was introduced in the valley during the 1949 season and was viewed with much local interest. Several of these sprinkler-type systems were installed during the 1950 irrigation season, and this new and currently popular method may become increasingly important in future irrigation practices in the valley.

GEOGRAPHY 183

AGRICULTURE AND VEGETATION

After the decline of mining activity, agriculture became the principal means of livelihood in the Townsend Valley. About one- third of the cultivated land in the valley is irrigated, and the re maining two-thirds is farmed by dryland methods. Wheat, oats, barley, and rye are the important small grain crops that are raised on irrigated land. Sugar beets and potatoes, which are grown on a commercial scale', have been introduced in irrigated areas in recent years. The sugar beets are processed at Mis- soula, and the potatoes are shipped to eastern markets. Spring and winter wheat are the main crops raised on nonirrigated lands. In 1940, 43 percent of the total harvested acreage (dryland and ir rigated land) was in small grains. Small acreages of alfalfa, clover, and timothy are raised for forage. The remaining land within the valley, including that too rough for cultivation and the swampy waterlogged bottom land, is utilized chiefly for grazing. Large numbers of sheep and cattle are raised in this area each year.

Native plants growing in the uncultivated areas include western wheat, grama, needle-and-thread grass, nigger wool, and sage brush. Groves of cottonwood, dense thickets of willow, wild rose, alder, and other phreatophytes grow along the poorly drained flood plains of the Missouri River. Saltgrass, salt bush, grease- wood, and buffalo bush are confined largely to the saline bottom lands, especially in the Crow Creek area. The high mountains are covered by fair stands of Douglas fir and lodgepole pine.

MINING

During its early development, the Townsend Valley was prin cipally a mining region, but now the more highly mineralized areas are mined only sporadically. One of the outstanding dis coveries of gold in Montana was made at Confederate Gulch in 1864. Estimates of the total value of placer gold that has been produced from this area are from $10 million to $30 million (Pardee and Schrader, 1933, p. 172). Although most of the gold was mined by 1870, small-scale placer mining with new and im proved equipment still continues. The Radersburg district, which is known principally for its rich lode gold mines, also contains placer deposits along the streams that drain the area. By 1929 production from this district totaled about $6,130,000 (Pardee and Schrader, 1933, p. 304); however, there is only sporadic small-scale lode mining at the present time. Since 1870 the Park, or Hassel,district, which is on the east side of the Elkhorn Moun tains west of Townsend, has continued to produce moderate

394090 O - 56 - 2


amounts of gold, lead, and some silver from lode and placer de posits. Some of the precious metals are recovered by a small stamp mill, which is situated on Indian Creek near the central part of the district. The Iron Mask mine produces lead ore, which is shipped to East Helena to be smelted. The mine was operated for a short time in 1949 but was closed when lead prices declined. Placer mining, however, has continued along Indian Creek to the present time. Accurate reports on the total production are not available, but it is estimated to be not less than $1 million for the period 1870-1928 (Pardee and Schrader, 1933, p. 309). Mr. O. A. Ellis, who has recently reworked the placer gravel along Indian Creek, estimates that the total value of gold produced since 1928 is about $500,000.

Since 1928 marble from the Meagher limestone, quartzite from the Flathead quartzite, and iron ore have been mined in small quantities from the Limestone Hills between Townsend and Rad- ersburg. The dark mottled marble from the Meagher limestone is mined and processed by the Vermont Marble Co. and is sold primarily as a decorative building stone. The quartzite and iron ore are used in the manufacture of cement at Trident, Mont.

The small amount of coal mined from the Tertiary beds near Toston is used locally.

TRANSPORTATION

The main line of the Northern Pacific Railway traverses the Townsend Valley; it parallels the Missouri River as far north as Townsend and continues northwestward to Helena through the gap between the Elkhorn Mountains and the Spokane Hills. The main line of the Chicago, Milwaukee, St. Paul, & Pacific Railroad crosses the southeast corner of the area; it crosses the Missouri River at Lombard and continues southward to Three Forks. These transcontinental railways provide freight transportation to eastern and western markets.

U. S. Highway ION crosses the area; it parallels the Northern Pacific Railway between Helena and Toston, crosses the Missou ri River at Toston, and thence continues southwestward to Three Forks. State Highway 6 crosses the area between Townsend and White Sulphur Springs, 40 miles to the northeast in Meagher County. Both highways are hard surfaced and facilitate the trans portation of large amounts of perishable food from the valley to surrounding markets. Dirt and gravel farm-to-market roads traverse the rural areas.

CONTRIBUTIONS TO HYDROLOGY 185

GEOMORPHOLOGY

The Townsend Valley is in the north-central part of the North ern Rocky Mountains physiographic province (Fenneman, 1931, p. 223). It is one of the largest intermontane basins in the region. The southern part of the valley trends slightly northeast and the northern part of the valley trends northwest; consequently, the main axis of the valley is a moderate curve that is concave to the west.

The Big Belt Mountains, one of the front ranges of the Rocky Mountains, border the valley on the east and trend in a northwest erly direction. This prominent range rises from 3, 000 to 4, 000 feet above the valley floor and two of its summits, Mt. Baldy and Mt. Edith, northeast of Townsend, are 9,600 feet above sea level..

A low, broad ridge projects west from the Big Belt Mountains, between Sixmile and Sixteenmile Creeks, and continues south and west, forming the southeast margin of the Crow Creek area. Where the Missouri River enters the Townsend Valley, it has cut a deep double-horseshoe gorge through this ridge. (See fig. 33.) The ridge flattens to a low, broad rim as it curves to the south end of the Elkhorn Range, which borders the valley on the south west. This range has approximately the same altitude as the Big Belt Mountains but the steep ridges form a more rugged divide.. Elkhorn and Crow Peaks, west of Townsend, are summits of this range and are a little more than 9, 000 feet above sea level. A low, wide gap separates the north end of the Elkhorn Range from the Spokane Hills, which rise about 1,000 feet above the river and border the valley on the northwest. The Spokane Hills are sepa rated from the Big Belt Mountains by a deep gorge through which the Missouri River leaves the Townsend Valley. It is in this gorge that the Canyon Ferry dam is being built (1951).

The most striking topographic features within the valley are the gently sloping plains that extend from the mountain fronts toward the Missouri River. These slopes, which are modified by over lying alluvial fans and are dissected by youthful streams, repre sent ancient erosional surfaces cut on rocks of Tertiary age.

A lowland ranging in width from 1 to 6 miles borders the Mis souri River, Crow Creek, and Warm Spring Creek. The low plain along Warm Spring Creek slopes northeastward at the rate of 4 feet to the mile and that along Crow Creek slopes eastward at the rate of 8 feet to the mile. Between Toston and Canyon Ferry, the Missouri River is bordered by bottom land that slopes northward at an average rate of 6 feet to the mile. The bottom land is main ly on the east side of the Missouri River and is widest about 5


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GEOMORPHOLOGY 187

miles north of Townsend. The smooth surface of these low plains is interrupted only by the incised stream beds of the smaller trib utaries and, in the Crow Creek area, by a small knoll of Pre- cambrian shale. Nearly one-third of the area of the Townsend Valley consists of lowland bordering the stream.

Areas of flat to nearly flat land that are separated from the valley bottom and from one another by steep to moderate slopes were referred to by Pardee (1925) as benches. The highest of these surfaces was designated bench 1, the intermediate was des ignated bench 2, and the lowest was designated bench 3.

Remnants of bench 3, which are 100 feet to 1 mile wide, border the east side of the valley bottom between Toston and Townsend. This bench, carved largely on Tertiary deposits, slopes westward at a rate of about 80 feet to the mile. In places it is separated from the bottom land by a much steeper slope that is 15 to 60 feet high but in other places the surface of the bench grades almost imperceptibly into the valley bottom. Varying thicknesses of unconsolidated alluvial materials mantle the Tertiary deposits.

The next higher erosional surface, bench 2, is an area of near ly 52 square miles along the east side of the Missouri River be tween Canyon Ferry and Gurnett Creek. This surface, which has its upper margin near the base of the Big Belt Mountains at an al titude of nearly 4, 300 feet, slopes southwestward at a rate of about 100 feet to the mile and ends with a sharp break, or escarp ment, at an altitude of about 3, 800 feet, or nearly 100 feet above the bottom land. The surface is widest between Avalanche and White Creeks where it is about 5 miles wide; north of Gurnett Creek it extends westward from the base of the mountains for a distance of 2 miles.

Remnants of the highest and oldest erosional surface border the Big Belt Mountains between Gurnett and Fivemile Creeks. Bench 3 is best preserved in the area between Deep and Greyson Creeks. From an altitude of 4, 700 feet, it slopes westward for nearly 4 miles at a rate of about 100 feet to the mile and it is 150 to 300 feet above the bottom land of Deep and Greyson Creek val leys. Both north and south of this area, bench 3 has a steeper gradient and does not extend as far from the mountains. Broad smooth surfaces slope toward the Missouri River between Town- send and Winston and also border Warm Spring Creek in the Crow Creek area. These probably represent different erosional levels but grade into each other without a break in slope.


GEOLOGY

A thick sequence of sedimentary rocks is exposed in the Town- send Valley. (See table 2.) In general, the rocks older than Ter tiary have been strongly deformed by mountain-building proc esses, whereas those of Tertiary and Quaternary age are warped only slightly or are flat lying. Rocks of igneous origin, which have intruded the sedimentary rocks in many places in the valley, also are exposed.

Tab

le 2

. Se

dim

enta

ry r

ocks

of

the

Tow

nsen

d V

alle

y an

d th

eir

wat

er-b

eari

ng p

rope

rtie

s

Sys

tem

Qua

tern

ary

Ter

tiar

y

Cre

tace

ous

Jura

ssic

Per

mia

n

Pen

nsyl

vani

an

Pen

nsyl

vani

an

and

Mis

siss

ip-

pian

Mis

siss

ippi

an

Ser

ies

Rec

ent

and

Ple

isto

cene

Mio

cene

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goce

ne

Upp

er a

nd

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er

Low

er

Upp

er

Mid

dle

Low

er

For

mat

ion

All

uviu

m

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tena

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dran

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mes

tone

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lim

esto

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(fee

t)

4,0

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1530

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145

1325

1260

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105

1595

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and

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STRATIGRAPHY

PRECAMBRIAN ROCKS

The oldest rocks exposed in the area described by this report belong to the Belt series of Precambrian age. Only 5 of the 8 Precambrian formations recognized by Walcott (1899) in this general region are present in this area. The oldest formation is the Newland limestone. It is best exposed in the mountains north of Confederate Gulch and consists mainly of finely crystalline, dark-bluish-gray, thin-bedded dolomitic limestone. The beds ap pear buff on weathered surfaces and show slaty cleavage in many places. The upper part of the formation includes argillaceous limestone and shale beds. Although the base is not exposed, the formation is estimated to be about 2,000 feet thick (Mertie, Fischer, and Hobbs, 1951, p. 18).

The Greyson shale, which overlies the Newland limestone, is well exposed along Deep Creek Canyon. It consists of dark-gray siliceous and arenaceous shale in its upper part, bluish-gray fis sile shale in the middle part, and dark co'arse arenaceous and siliceous shale and thick interbedded quartzite in the lower part. In the type section between Deep Creek and Greyson Creek, the thickness of the formation is 3, 000 feet.

The Spokane shale, which overlies the Greyson shale, was named by Walcott because of its occurrence in the Spokane Hills. The formation is well exposed along the east and west flanks of the folded rocks southwest of Townsend. It is chiefly a massive to thin-bedded deep-red siliceous shale, but it contains some siltstone in its lower part. Much of the Spokane shale is mottled by spots and bands of green shale, particularly in the transitional zone between it and the overlying formation. East of the Spokane Hills, in the canyon of White Creek, the formation is nearly 1,500 feet thick (Pardee, 1925, p. 13).

The Empire shale overlies the Spokane shale and is a meta morphosed siliceous greenish-gray shale or argillite containing some thin beds of quartzite and gray limestone in its upper part. This formation crops out mainly in the northern part of the area. At Canyon Ferry the Empire shale is the bedrock on which the new dam is being built, and the construction has exposed fresh sections of the formation on both sides of the canyon. Outcrops along the west side of the low ridge south of Toston are less con spicuous; the beds here are not typical because they have been thrust over younger rocks and intruded by granitic and basaltic dikes and sills. The formation is estimated to be about 1,000 feet thick in this area.

GEOLOGY 193

The Helena limestone, the youngest Precambrian formation exposed in this area, is best exposed north and east of. Canyon Ferry. It is predominantly an impure thinly bedded bluish-gray dolomitic limestone containing a few beds and partings of shale; on weathering it is buff. It is about 500 feet thick at Hellgate Gulch and possibly a little thicker in the vicinity of White Gulch; but owing to an erosional unconformity, this formation thins to a featheredge in the valley of Magpie Creek (Mertie, Fischer, and Hobbs, 1951, p. 20).

CAMBRIAN ROCKS

Rocks of Cambrian age are well exposed in the Limestone Hills, which is a prominent ridge of steeply dipping beds southwest of Townsend. (See fig. 34.) Six well-defined Cambrian formations, all conformable to one another, have been recognized. Their combined thickness is about 1, 700 feet.

Figure 34. View looking north from the southeast corner of sec. 4, T. 5 N., R. IE.. showing exposure of Cambrian, Devonian, and Mississippian formations in the south end of the Lime stone Hills, 8 miles southwest of Townsend. The beds dip steeply to the west except in a few places where they are slightly overturned and dip to the east.

The Flathead quartzite of middle Cambrian age unconformably overlies the Spokane shale in the Limestone Hills and also the Empire shale and the Helena limestone at different places in the northern part of the area. It is a vitreous fine- to medium- grained grayish-pink to pink well-bedded to massive quartzite. In most places a thin bed of conglomerate is present near the base of the formation. The formation is about 100 feet thick in the Limestone Hills.


The Flathead quartzite is overlain by the Wolseyshale, which is a soft dark-gray to greenish micaceous and calcareous shale with interbedded limonitic sandstone layers. In places the Wolsey shale contains small limestone concretions at the base and thin beds of calcareous shale in the upper part. It is 390 feet thick in the Limestone Hills.

Overlying the Wolsey shale is the Meagher limestone. It is a thin-bedded dark-gray limestone that is conspicuously mottled and banded. An examination by Ruppel* of the samples collected by him in the Limestone Hills showed that the mottling is due to dolomitic limestone. In the Limestone Hills, the formation has been metamorphosed to a finely crystalline marble. Remains of trilo- bites are locally abundant in the shale partings in the lower part of the formation. The Meagher limestone is 510 feet thick in the Limestone Hills.

The Park shale, which overlies the Meagher limestone, is a thin-bedded olive-gray shale containing a few lenticular beds of fine-grained sandstone. It weathers readily and usually forms a covered slope between the Meagher limestone and the overlying Pilgrim limestone. The Park shale is 205 feet thick in the Lime stone Hills.

The lower unit of Pilgrim limestone is massive dark-gray limestone that is mottled on weathered surfaces; the middle unit is thin-bedded gray limestone having crinkly ribbons of yellowish dolomite between the bedding planes; and the upper unit is light- gray, massive, very resistant dolomitic limestone. The Pilgrim limestone is 420 feet thick in the Limestone Hills, where it forms a prominent ridge. (See fig. 34.)

The Dry Creek shale, which is the youngest Cambrian forma tion of this area, overlies the Pilgrim limestone. The lower part of the formation consists mainly of brownish-yellow and pink sandy shale and siltstone. The upper part is light-gray limestone that is mottled and interbedded with thin shale partings. It is 110 feet thick in the Limestone Hills. In most places the Dry Creek shale is poorly exposed; a low saddle marks its position between the Pilgrim limestone and the overlying Jefferson limestone. The Dry Creek shale and the Pilgrim limestone were mapped as an undifferentiated unit. (See pi. 19.)

2See footnote on p. 174.

GEOLOGY 195

DEVONIAN ROCKS

The Jefferson limestone, which is 400 to 600 feet thick and which is of Late Devonian age, lies disconformably upon the Dry Creek shale of Late Cambrian age. It is a fetid, dark-gray or brown dolomitic limestone containing zones of breccia. Although it is bedded where fresh, it appears to be a massive rock having a sugary texture where it is weathered.

The Three Forks shale, which is about 300 feet thick and which also is of Late Devonian age, overlies the Jefferson limestone. The lower part contains beds of reddish and brownish-yellow cal careous shale and grayish-brown limestone. The middle part consists of fossiliferous, argillaceous, and calcareous shale that is green, olive-gray, and black; locally it contains a conspicuous, highly fossiliferous limestone bed. The upper part consists chief ly of laminated yellow sandstone and siltstone.

MISSiSSlPPIAN ROCKS

In this area the Lodgepole and the Mission Canyon limestones comprise the Madison group of early Mississippian age. The Lodgepole limestone consists of gray thin-bedded fossiliferous limestone. It is 595 feet thick where measured in the Limestone Hills and conformably overlies the Three Forks shale. The upper beds are more massive in the zone of transition between the Lodgepole and the overlying Mission Canyon limestone. The Mis sion Canyon limestone, which is about 1, 600 feet thick, is an im pure massive white to light-gray limestone that is not as fossil iferous as the Lodgepole limestone.

PENNSYLVANIAN AND PERMIAN ROCKS

Overlying the Mission Canyon limestone is the Amsden forma tion, which is of late Mississippian and early Pennsylvanian age and which is 260 feet thick. The lower part of this formation is characterized by beds of reddish shale and siltstone, and the up per part of the formation consists of beds of yellowish, red, and grayish-brown dolomitic limestone and interbedded shale. The Quadrant formation, also of early Pennsylvanian age, and the Phosphoria formation of Permian age were mapped as a single unit. (See pi. 19.) The Quadrant formation is predominantly a light-colored quartzitic sandstone that is interbedded with lime stone and dolomite. The overlying Phosphoria formation consists of chert and quartzite and is in part phosphatic.


JURASSIC ROCKS

Mesozoic rocks are poorly exposed in this region. They con sist mainly of variegated sandstone, calcareous shale, siltstone, and several conspicuous gastropod-bearing limestone beds. The formations are less resistant to weathering than those of Paleo zoic and Precambrian age and, consequently, they form the foot hills of the mountainous areas where the high ridges have been carved from the older formations.

Rocks of Triassic age are not present in this region; conse quently, rocks of Jurassic age rest unconformably upon the Pale ozoic formations. A reddish-brown fossiliferous marine sand stone having thin beds of limestone is believed to be the Sawtooth formation of the Ellis group; it unconformably overlies the Phos- phoria formation. These marine beds are overlain by a buff to reddish nonmarine shale and lenticular sandstone, which probably belong to the Morrison formation. The Jurassic formations, which have an average thickness of about 550 feet, are well exposed along the low ridge east of Toston and poorly exposed along the west side of the Limestone Hills.

CRETACEOUS ROCKS

The Kootenai formation of Early Cretaceous age overlies the Morrison(?) formation. It consists of dark-colored sandstone, red and green shale, and a bed of gastropod-bearing limestone near the4 top. It is about 500 feet thick and is well exposed in the hills east of Toston. The Colorado shale of Early and Late Cre taceous age overlies the Kootenai formation. It is the youngest formation of Mesozoic age present in the area and is composed chiefly of dark-colored shale and some sandstone and quartzitic sandstone beds. An undetermined thickness of these rocks is poorly exposed along the flanks of the Elkhorn Mountains west of Townsend.

TERTIARY DEPOSITS

Tertiary deposits of Oligocene and Miocene age (commonly re ferred to as "lakebeds") underlie a large part of the Townsend Valley. They unconformably overlie the eroded surfaces of the folded and faulted older rocks and apparently underlie most of the younger sediments of the valley. The older Oligocene deposits consist mainly of light-colored fine-textured sediments and small amounts of interbedded sand and gravel. Much of the finer grained material is volcanic ash. Thin beds of coal are present in the

GEOLOGY 197

area northeast of Toston. Locally there is an occasional stratum of diatomaceous earth. The younger Oligocene beds consist of coarser textured elastics that probably were deposited as alluvial fans or outwash from the surrounding mountains. They, too, con tain large amounts of tuffaceous material.

Mertie, Fischer, and Hobbs (1951, p. 30) subdivided the rocks of Oligocene age in the Canyon Ferry quadrangle into four units, which they described as follows:

***Unit 1, of the Oligocene sequence, consisting of conglomerate, interbedded with red shale and some bentonitic beds, lies along the east side of the Spokane Hills. Unit 2, composed of volcanic conglomerate, tuffs, and other beds, extends eastward to the flats of the Missouri River. The principal deposits of bentonite occur at the base of this unit. Unit 3, composed mainly of reworked tuffaceous .material without bentonite, extends from the Missouri River eastward, and occupies most of the foreland southwest of the Big Belt Mountains. Unit 4, consisting mainly of conglomerate with a calcareous matrix, lies still farther east, extending to the hard rock of the Big Belt Mountains. No unconformities or disconformities are known to separate units Ito 3. On the contrary, all evidence indi cates that these three units grade imperceptibly into one another; and the only basis for their separate delineation is the observable differences in their lithology. Unit 4, how ever, may lie unconformably on unit 3 ***.

The only Oligocene formations identified so far in the valley are the Chadron and Brule formations in an anticline extending from Sixmile Creek to north of Deep Creek (Leroy Kay, personal communication).

The first reported collection of vertebrate fossils from the Oligocene deposits in the Townsend Valley was made by Douglass (1902, p. 238-79, pi. 9). It included eight species from the "Toston beds, " which are several miles northeast of Toston. In recent years Leroy Kay (personal communication) and others have collected a much larger number of species from these beds and also from the well-exposed Oligocene beds that border the east flanks of the Spokane Hills. The first fossil insects of Oligocene age were recently found in the bluffs that face the Missouri River north of Beaver Creek.

Miocene deposits in this area are poorly exposed and are diffi cult to recognize; however, fossil remains of Miocene age have been found in several exposures in bluffs that border the east bank of the Missouri River between Confederate Gulch and Can yon Ferry. Douglass (1902) reported fossil horse remains from the bluffs north of Confederate Gulch and from exposed deposits in the Deep Creek valley. Kay and others collected Miocene fos sils from the bluffs along the Missouri River, southeast of the old Canyon Ferry dam. The Miocene deposits in these localities consist of light- to buff-colored sandy clay and sand and gravel beds that, in places, are overlain by conglomerate. In many


places a 2- to 4-foot thickness of tuffaceous sand cemented with calcium carbonate is present near the base of the conglomerate that forms the upper unit of the deposit. The correlation of beds exposed in different parts of the valley is impossible because the lithologic character of the deposits changes considerably in a short distance; fossil remains are about the only means of dating the deposits.

The total thickness of Tertiary rocks in the Townsend Valley is estimated to be between 4,000 and 6,000 feet. A complete section of the deposits cannot be measured because the few exposures are incomplete. Tertiary beds dipping 10° to 15° to the northeast are exposed along the north side of the Deep Creek valley for a distance of about 5^ miles (from near the center of sec. 30, T. 7 N., R. 3E., to the east side of sec. 25, T. 7 N., R. 3E.). K the beds have not been duplicated by unsuspected faulting or fold ing, a total thickness of 5,000 to 6,000 feet of Tertiary sediments is exposed. Pardee (1925, p. 27) states that the total minimum thickness of the Oligocene beds that are exposed in the southeast ern part of Townsend Valley is 800 feet and that the thickness of a section of Oligocene rocks that is exposed along Beaver Creek in the southeastern part of T. 9 N., R. IE., is 2, 800 feet. Mertie, Fischer, and Hobbs (1951, p. 29) recognized between 6,000 and 10, 000 feet of Tertiary beds in the north part of the valley.

An oil test well was drilled in the SW$ sec. 36, T. 7 N., R. 2 E., between 1925 and 1930, and penetrated about 700 feet of unconsolidated Recent and Tertiary sediments before bedrock was reached. According to Edward Jacobson of Townsend, Mont., the hole was drilled to a depth of 1, 310 feet, and no oil was found. Another test well for oil in sec. 7, T. 8 N., R. 1 E.,reportedly penetrated Tertiary sediments to a depth of 1, 780 feet.

The Tertiary sediments of the Townsend Valley are shown as a single unit on plate 19.

QUATERNARY DEPOSITS

A small terminal moraine of a valley glacier lies at the foot of Mount Baldy in sec. 13, T. 8 N., R. 3E.,and is about three- fourths of a mile long and half a mile wide. Its uneven surface is about 50 feet above the high erosional plain near the base of the mountain. Materials composing this semicircular ridge are typ ical glacial deposits and consist of unsorted debris containing faceted granite and quartzite cobbles.

GEOLOGY 199

Much of the Townsend Valley is mantled by a layer of alluvium that is of Pleistocene to Recent age. The alluvium consists of large cobbles, gravel, sand, silt, and clay and was deposited by streams as alluvial fans, as bottom-land deposits, and as a thin mantle over the benchland (the latter is often referred to as "bench gravel"). These alluvial deposits, which were deposited on the folded and eroded surface of Tertiary and older rocks, are usually thicker and coarser textured near the mountain and are thinner and finer textured toward the valley. Along Crow Creek the alluvium consists chiefly of large andesite cobbles, coarse gravel, and sand; along Warm Spring Creek it consists largely of fine-textured sediments; and along the Missouri River consists of sand and gravel and interbedded layers of clay. The maximum thickness of the Quaternary sediments is estimated to be not more than 60 feet.

IGNEOUS ROCKS

Igneous rocks intruded into the sedimentary deposits in the Townsend Valley occur as dikes, stocks, sills, and small plugs. The intrusive rocks were divided and mapped as five principal types, which are (1) granitic rocks (including chiefly monzonite, quartz monzonite, granodiorite, aplite, and latite), (2) monzonitic lamprophyres, (3) andesite and andesite porphyry and breccia, (4) diabase, and (5) diorite and gabbro. Extrusive igneous rock basaltic lava also is present in the Townsend Valley. Analyses of rock types have been reported by Haynes (1916); Mertie, Fischer, and Hobbs (1951); Pardee and Schrader (1933); Ruppel"; and Stone (1911).

The largest areas underlain by rocks of igneous origin include the north end of the Elkhorn Mountains between Winston and Townsend, the east slopes of the Elkhorn Mountains west of Rad- ersburg, and Lone Mountain, a prominent butte 5 miles south of Radersburg. Rocks of the andesite type are most abundant in these areas; they include many varieties and are of both intrusive and extrusive origin. According to Pardee and Schrader (1933, p. 306), gold and small amounts of silver are present in the an desite of post-Cretaceous age at Radersburg. Lead, gold, and silver are included in the andesite in the Winston area. Dikes and sills of andesite, diorite, gabbro, and diabase occur throughout the west slopes of the Big Belt Mountains and intrude all the for mations of the Belt series except the Empire shale and the Helena limestone (Mertie, Fischer, and Hobbs, 1951, p. 48). Granitic and andesitic intrusive bodies occur in the Spokane Hills.

See footnote on p. 174.

394090 O - 56 - 3


SILLS

Igneous rock occurs as sills in the sedimentary rocks of the Limestone Hills in many places. A dark-brown diabase sill, which is nearly 200 feet thick, intrudes the Spokane shale about 3, 000 feet below the contact of the Flathead quartzite and the Spokane shale. The intrusion extends 8 miles along the strike of the west limb of the anticline. Its location is marked by a deep topographic saddle between two parallel ridges. Along the zone of contact, the reddish Spokane shale was metamorphosed to a dark greenish- gray hornfels, which is more resistant to weathering than the dia base or the surrounding unmetamorphosed shale.

A granodiorite sill, which is nearly 3, 000 feet thick, occurs in the central section of the Limestone Hills. The granitic mass in trudes the Three Forks shale and, in most places, is in contact with the Jefferson and Lodgepole limestone. According to Ruppel*, the sill is a hornblende granodiorite, which is composed of ande- sine, hornblende, quartz, orthoclase, and a minor amount of epi- dote and magnetite. To the west, smaller sills in the Kootenai formation are composed of about the same minerals, but some of the minerals are more characteristic of dioritic rocks. Sills in the Colorado shale, both north and south of Indian Creek, are andesite and andesite porphyry. Many small sills occur in the Spo kane Hills. Most of these are dark-colored medium-grained monzonitic lamprophyres and are closely related to quartz monzonite.

DIKES AND STOCKS

In the double-horseshoe bend, which is 2 miles west of Lom bard, the Missouri River has cut a steep-walled gorge into an in trusive mass of granite. (See fig. 33.) The granite is light gray, of medium-fine texture, and somewhat porphyritic. In places the rock is almost entirely without quartz and grades into a syenite. A similar fine-grained granitic rock projects as a small butte above the benchland east of Warm Spring Creek. An irregular dikelike intrusion of diabase,which is 100 to 500 feet wide and which apparently follows the plane of the thrust fault that cuts across the double-horse shoe bend of the Missouri River is ex posed about 1 mile west of Lombard. The intrusion has meta morphosed the adjoining country rock, particularly the Kootenai formation on the east side of the thrust fault. Where fresh, the diabase is dark greenish gray; where exposed, it is rusty brown and generally deeply weathered. Haynes (1916, p. 290) believed

*See footnote on p. 174.

GEOLOGY 201

,that the age of the intruded body could not be closely determined, but that it clearly was later than the overthrust and, therefore, of 'Tertiary age. Northeast of Toston, at the mouth of Sixmile Creek, 'is a small plug of dark-colored diabase. It resembles the dikelike intrusion west of Lombard and probably is of similar origin.

The Canyon Ferry stock covers an area half a mile to 1 mile wide and nearly 4 miles long. The intrusion, which is situated along the east edge of the Spokane Hills, trends southeastward from the New Canyon Ferry dam site. At its north end the stock is primarily a coarse-grained medium-gray biotite-rich granite; farther south it grades into quartz monzonite. Building stone for the old Canyon Ferry dam and power plant was obtained from the stock. Small dikes of aplite and large intrusive bodies of lamprophyres are associated with the principal intrusion. All these in trusions are of Tertiary age (Mertie, Fischer, and Hobbs, 1951, P. 47).

Another large granite stock, referred to as the Gurnett stock, borders the east side of the valley between Duck and Ray Creeks. It is a light-gray fine-grained granite rich in plagioclase feld spar. The granitic mass intrudes shale of the Belt series and is of pre-Oligocene age; weathered pieces of the rock occur in the upper Oligocene beds. Mineralization, resulting chiefly in small concentrations of gold associated with iron sulfides, has taken place along the granite and shale contact at the north end of the stock.

STRUCTURE

The Townsend Valley is a broad structural trough, which was formed by downwarping and faulting. The upland surrounding the valley consists of closely folded strata cut by many faults.

FOLDS

Throughout this area the sedimentary rocks of Cretaceous age or older have been intricately folded; by comparison, the beds of Tertiary age have been only slightly deformed.

The most prominent fold within the area is an asymmetrical anticline between Townsend and the lower course of Crow Creek. The axis of the fold trends nearly due north. Truncation of the fold by erosion has exposed Precambrian beds. A complete se quence of Paleozoic and Mesozoic rocks (the "Limestone Hills section") is well exposed on the steeply dipping west limb of the


anticline. Beds younger than the Spokane shale of Precambrian age have been eroded from the east limb of the structure. In the southwest corner of the Limestone Hills, Pennsylvanian and Per mian formations have been tightly folded into a small anticline and syncline, both of which pitch to the south.

A syncline of folded Cambrian, Devonian, and Mississippian rocks borders the east rim of the valley between Deep Creek and Sixmile Creek. It pitches southward from sec. 34, T. 7 N., R. 3 E.,to sec. 22, T. 6 N., R. 2 E., where it curves to the south east. The north end of the syncline is nearly symmetrical; to ward the south, however, the east limb of the syncline is over turned. Between Greyson and Dry Creeks the syncline is faulted, Precambrian shale having been thrust over Cambrian rocks.

South of Lombard, rocks of Cambrian to Cretaceous age are folded into a north-trending tightly folded syncline. The west limb of the fold is overturned and where the plane of the Lombard overthrust crosses this limb, shale of Precambrian age overlies beds ranging in age from Cambrian to Mississippian. Cambrian and Devonian formations are not exposed on the east limb of the fold, which is truncated and covered by younger sediments. Only the north end of this structure is in the area described by this report.

Along the east flank of the Spokane Hills, Devonian and Missis sippian formations are folded into a small syncline. The axis of this structure, which trends northwest, is about 1 mile west of Lake Sewell.

A fold in the Tertiary rocks, which is referred to as the Dry Creek anticline, can be traced northwestward from Sixmile Creek fora distance of nearly 11 miles. North of Deep Creek the struc ture is barely discernible. The fold is nearly symmetrical and, in general, the beds dip 5° to 20° to the east and west. According to a personal communication from Leroy Kay, light-colored clay beds of the Oligocene series (Chadron and Brule formations) crop out along the eroded axis. Sand, gravel, and conglomerate of Miocene age are exposed along the flanks of the anticline.

Between the Spokane Hills and the Big Belt Mountains, beds of Tertiary age have been folded into a broad syncline. The best ex posures are on the west flank of the fold, where the dip of the beds ranges from 5° to 30° to the east. Within a mile or two of the mountain front (formed by Paleozoic rocks) the dip of the beds gradually decreases and, near the foot of the mountains, along Cave and Magpie Creeks, it reverses and is about 20° toward the west.

GEOLOGY 203

FAULTS

The Lombard overthrust is one of the most important structural features of this area. It extends for about 14 miles from sec. 18, T. 5 N., R. 3 E., southward to the hills north of Three Forks (15 miles south of Lombard). The fault plane is well exposed in the horseshoe canyon of the Missouri River west of Lombard, where it dips about 40° to the west. Here strata of the Belt series (Pre- cambrian) have been thrust over strata of Cretaceous age. Haynes (1916, p. 271, 273) described this fault as follows:

The maximum displacement on the fault plane near Lombard cannot be very closely esti mated, but it is approximately two miles, and the strata which are stratigraphically about 6,800 feet apart are here in contact

The age of the fault, according to Haynes, is very late Cretaceous or early Tertiary.

In the Limestone Hills are many northwest-trending normal faults. Although the horizontal displacement along most of these faults is small, the displacement along two of the faults is more than 1,000 feet. The maximum stratigraphic displacement of the northernmost normal fault is about 1,400 feet where the Flathead quartzite of Middle Cambrian age is in contact with the Pilgrim limestone of Late Cambrian age. The fault trends approximately N. 45° W. The other large normal fault, known as the Indian Creek fault, trends approximately N. 50° W. For a short distance Indian Creek lies on the west extension of this fault. In sec. 16, T. 6 N., R. IE., the east extension of the fault splits into smaller normal faults. Two minor strike faults occur in the south part of the Limestone Hills. One cuts strata of Cambrian and Devonian age and the other cuts the Mission Canyon, Amsden, Quadrant, and Phosphoria formations, which are of Mississippian to Per mian age.

Northwest-trending normal faults, which are similar to those of the Limestone Hills, cut across strata of the Spokane Hills, but the stratigraphic displacement along these faults is not as great as that along those in the Limestone Hills.

Numerous small normal faults, only a few of which are shown on plate 19, have displaced Tertiary deposits throughout the val ley. In sec. 12, T. 5N., R. 2 E., a well-exposed section of light- colored Oligocene clay beds, overlain by reddish siltstone and gravel, has been cut and displaced by four distinct normal step faults. (See fig. 35.) These faults strike approximately N. 20° to 30° W., dip 20° to 40° to the southwest, and are within a distance of less than 2,000 feet. The normal faulting has lowered the small


. After J. T. Pardee, 1925BM, Belt Mountains; B, conspicuous bench or erosional plain developed on

Tertiary deposits; MV, Missouri River valley bottom; p b, pre-Cambrian shale and intrusive' diabase

Figure 35. Faults in Tertiary lakebeds as seen across Sixmile Creek from the southeastcoroef of sec. 12, T. 5 N.. R. 2 E. BM, Belt Mountains; B, prominent bench or erosional plain developed on Tertiary deposits;. MV, Missouri River valley bottom; pCb, Precambrian shale and intrusive diabase.

fault blocks toward the valley and has exaggerated the apparent thickness of the Tertiary beds. Similar faulting probably has oc curred in other parts of the valley where, however, the faults are poorly exposed and the repetition of Tertiary stratigraphic units cannot be recognized.

EARTHQUAKES

Earthquakes are not uncommon in the Townsend Valley; the area was severely shaken in 1925 and 1935. Pardee (1926, p. 7 23) believed the epicenter of the 1925 earthquake to have been a short distance southeast of Lombard where crustal movement ap parently took place along a deep-seated north-trending fault along

GEOIOGY 205

the west flank of the Big Belt Mountains. The intensities of the shock (Rossi-Farrel scale) in the Townsend Valley were as fol lows: Lombard 9+, Toston 9, Townsend 8+, Radersburg 8+, and Canyon Ferry 7+. Schoolhouses near the epicenter of the earth quake, including one at Radersburg, were damaged considerably. At most places within a radius of 75 miles of the epicenter, the damage from the shock consisted mostly of breaks in chimneys, plaster, and plate glass windows. Rock masses were shaken down from the steep slopes and cliffs within a radius of 12 or 15 miles of the epicenter. The railroad tracks near Lombard were broken. The ground cracked over a large area. One of the cracks was at Canyon Ferry, a distance of about 40 miles from the epicenter. Apparently the cracks were due to shaking and were not due to slippage along the line of a deep-seated fault. A week later, a chimney that was cracked by the earthquake caused a fire which destroyed most of the buildings on the main street of Toston. Six- mile Creek, the source of the town's water supply, is reported to have become dry as a result of the earthquake and no water for fighting the fire was available.

The Townsend Valley was also severely shaken by the 1935 earthquake, whose epicenter was near Helena, about 35 miles northwest of Townsend. The intensity rating of this earthquake near its epicenter was 9; hence, this earthquake was slightly less intense than the one of 1925. In the Townsend Valley the damage from the earthquake consisted mainly of broken chimneys, plas ter, and plate glass windows; however, at Helena, four persons lost their lives, and property damage totaled millions of dollars.

SUMMARY OF THE GEOLOGIC HISTORY

In late Precambrian time the Townsend Valley was in a basin of subsidence in which was deposited a thick series of sediments, named the Belt series by Walcott. The absence of characteristic Cambrian fauna and the length of the erosional period following deposition of the sediments were considered by Walcott to be suf ficient evidence for placing the entire Belt series in the Pre cambrian (Barrell, 1907, p. 23). These sedimentary rocks, which are about 8, 000 feet thick in the Townsend Valley, comprise two limestone formations and three shale formations containing a few thin beds of sandstone.

After their deposition these sediments were slightly folded and warped. Erosion then reduced the surface to a peneplain before the sea again advanced over the area in Middle Cambrian time. The basal sediments of Cambrian age overlie the Precambrian formations with no discernible angular discordance, but the mag-


nitude of the unconformity is evident inasmuch as the basal sed iments rest on several different formations of the Belt series.

The Cambrian sequence of Flathead quartzite, Wolsey shale, and Meagher limestone indicates that a transgressive sea inun dated this area after the Belt series was partly removed by ero sion. During later Cambrian time, the sea fluctuated and Park shale, Pilgrim limestone, and Dry Creek shale were deposited successively.

As no rocks of Ordovician or Silurian age are present in this region, this part of Montana is believed to have been a land mass that was slightly above sea level and that was subjected to very little erosion during these periods. Late in Devonian time the area was again inundated by the sea and the Jefferson limestone was deposited unconformably upon the eroded surface of the Dry Creek shale. Fine elastics, known as the Three Forks shale, were deposited over the limestone, probably during a slight re cession of the sea during late Devonian time.

The entire region apparently remained under stable marine conditions during Mississippian time when great thicknesses of limestone of the Madison group were deposited. In late Missis sippian or early Pennsylvanian time, the sea began to recede, and fine elastics of the Amsden formation were deposited. Sandstone and some limestone of the Quadrant formation were deposited in the Pennsylvanian sea. The Phosphoria formation appears to have been deposited upon the Quadrant formation without a break in sedimentation; this suggests that there was no withdrawal of the sea between Pennsylvanian and Permian times.

At the end of Permian time, the sea withdrew and left an emerged land mass that remained comparatively high during Tri- assic and part of Jurassic time. During Late Jurassic time the land surface again was submerged, sandstone and some thin limestone beds of the Sawtooth formation were deposited, and then the land surface reemerged and remained above sea level during the deposition of the nonmarine sediments of the Morrison formation. Deposition of nonmarine sediments of the Kootenai formation continued during Early Cretaceous time. After the deposition of the Kootenai formation, submergence of the land occurred for the last time and silt of the Colorado shale was de posited in the shallow sea that covered the area.

All the formations deposited from Precambrian to Early Cre taceous time appear to be conformable or nearly so. Evidently no large-scale folding or warping of the earth's crust took place in this region until after Early Cretaceous and before Oligocene

GEOLOGY 207

time the Oligocene beds rest with angular discordance on the steeply folded older rocks. The folding probably took place dur ing the Laramide revolution. Igneous intrusions are believed to be related to this period of movement, although some intrusions also occurred in early Tertiary time.

The structural deformation of the older rocks resulted in the formation of the Townsend Valley and the bordering mountains. The period of deformation was followed by a period of erosion that extended to Oligocene time. During this period the principal drainage courses were deepened and the surrounding mountain ranges were dissected; remnants of this mature topography are now evident among the mountain heights. The continental divide at this time is suggested by Atwood (1916, p. 697 740) to have been about 150 miles east of its present position that is, along the crest line of the Big Belt Mountains, the Bridger Range, and the Gallatin Mountains. If these mountains formed the divide, the drainage of this area was in a southwesterly direction and was part of the ancestral Snake River system.

In Eocene or early Oligocene time the drainage systems in southwest Montana were closed either by renewal of crustal movement or, perhaps, by the great outpouring of lava in the Snake River region. The closed troughs became sites of aggrada tion in which were deposited the "lakebeds" or "Bozeman beds, " which were so named by Peale (1896). In the Townsend Valley most of the lower beds consist of volcanic ash and other fine- textured sediments, which appear to have been laid down in shal low lakes or swamps. The coarser materials from the surround ing mountains were apparently deposited as broad alluvial fans. The large amount of tuff in these clastic beds indicates that vol canic activity occurred in this region during Oligocene time. Patches of these sediments occur on the high mountain slopes; hence, the troughs probably were filled to a much higher level during Tertiary time than at the present. A renewal of mountain growth, which probably came near the close of the Miocene epoch, warped the Tertiary sediments within the valley and elevated the Tertiary sediments that overlay the growing mountainous area.

Degradation followed the uplift and, during Pliocene and Pleis tocene time, streams developed drainageways across and within the major troughs; and beds of the troughs were lowered and erosional plains were left above them. These now remain as dis sected benchlands. The streams flowing over younger deposits were superposed across bedrock divides, which separated the neighboring structural basins. At these places the streams carved deep, narrow channels, such as the rocky gorges above Toston and at Canyon Ferry. Atwood (1916, p. 714) believed that the


Missouri River had worked its way westward at the beginning of this erosional period and, through piracy, captured this region of closed drainage. When the drainage of southwest Montana was opened to the northeast, the continental divide gradually shifted westward to its present position.

Degradation of the Tertiary sediments and older rocks in the Townsend Valley has continued to the present time. Glaciation apparently occurred late in the Pleistocene epoch. A small mo raine lies at the foot of Mt. Baldy on the west side of the Belt Mountains, and fresh moraines and recently cleaned out cirques are present on the east slopes of this summit. Similar cirques are present on the slopes of the summits of the Elkhorn Range.

GROUND WATER

A large reservoir of ground water underlies the Townsend Val ley. Part of the ground water in the Quaternary and Tertiary de posits is under water-table conditions and part is confined under artesian pressure. Most of the water in the pre-Tertiary forma tions is contained in fissures or solution channels.

RECHARGE

The pre-Tertiary aquifers that crop out in the higher mountain ous area surrounding the Townsend Valley receive nearly all their recharge from rainfall and snowmelt. The chief sources of ground-water recharge in the valley are the perennial mountain streams, irrigation canals and laterals, and seepage from irri gation water, In parts of the valley the Tertiary deposits evident ly are recharged by the upward migration of ground water from the underlying older rocks. Most of the precipitation that falls in the Townsend Valley penetrates to only a shallow depth and is lost later by transpiration and evaporation. Precipitation directly re charges the ground-water reservoir only in the lower parts of the valley where the water table is near the surface.

Many of the streams that head in the mountains lose a large part of their water to their underlying gravel before they reach the Missouri River. During the spring and summer, water from these tributary streams is diverted for the irrigation of the benchland that borders the bottom land. Influent seepage from the irri gation distribution system recharges the ground-water reservoir beneath these higher lands.

i GROUND WATER 209

In the Crow Creek area the source of much ground-water re charge is Crow Creek and its tributary, Warm Spring Creek. During the summer months the entire flow from .these perennial streams is diverted for irrigation. The water is carried to the farms in the lower parts of the valley by canals that traverse the coarse gravels of the benchland. A large part of the water is lost from the canals by seepage and much of the water that is spread on the fields for irrigation also is added to the ground-water reservoir.

Water diverted from the Missouri River and Big Spring is dis tributed to the farmland in the valley bottom between Toston and Canton by a series of five principal irrigation canals. As the wa ter level in many of the observation wells in this part of the valley is highest late in the irrigation season, when little precipitation falls and when streams have a minimum flow, the ground water obviously is recharged largely by irrigation water.

CHANGES IN STORAGE

The stage of the water table is a general indication of the quan tity of water in the ground-water reservoir; therefore, water- level fluctuations indicate changes in ground-water storage. In general, the fluctuations are an indication of the net recharge to or discharge from the ground-water reservoir. Monthly meas urements of the water level in about 150 wells throughout the val ley were made as part of this investigation. (See table 4.)

The greatest observed fluctuation of the water level occurred in wells along the upper course of Crow Creek; a difference of 20 feet between the high and low water-level readings was recorded in well A5-l-4cc. (See fig. 36.) This well penetrates the upper part of the alluvial fan of Crow Creek and the water level in the well depends to some extent upon the stream level. The rise of the water level in the early winter is caused by ice jams in the creek which cause backwater and flooding.

The water level in wells in the finer textured deposits of the bottom land shows the least fluctuation; the water level in several wells fluctuates less than a foot a year.

The hydrographs of most wells (fig. 36) indicate a decline of the water level during the winter months. In general, the water level in wells in the Crow Creek area (A5-l-4cc, A5-l-10cb, and A5- 2-20bcl) is highest during the spring when the flow of the streams, which are the principal source of recharge, is greatest. Else where, however, as in the valley bottom between Toston and

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GROUND WATER 211

Townsend and in the valley bottom north of Townsend, the winter decline ends in the spring when irrigation is begun. After a short period, which is dependent on the permeability of the soil in the area and on the amount of water applied, the recharge from irri gation is sufficient to overbalance the natural discharge from the reservoir and the water table begins to rise. (See hydrographs for wells A6-2-16aa, A7-2-4bal, and A7-2-10bb.)

MOVEMENT

The rate of movement of ground water is dependent on the per meability of the aquifer and the hydraulic gradient of the water table or piezometric (artesian-pressure) surface. The permea bility of an aquifer or water-bearing material is its capacity to transmit water through its interstices.

Contour maps, which show the configuration of the upper sur face of the zone of saturation or of the piezometric surface, in dicate that the ground-water gradient in some parts of the valley differs considerably from that in other parts of the valley. The ground-water gradient is steepest in the Crow Creek area and in the vicinity of the mountain front near Duck Creek, where the land slope is fairly steep, and the gradient is least along the fair ly flat flood plain of the Missouri River. (See pi. 20 and fig. 37.)

Ground water moves from a position of high altitude to a posi tion of low altitude in the direction of the steepest gradient. In the Townsend Valley the ground water moves from the bordering mountains toward the Missouri River in a direction that is almost parallel to the tributary streams and, therefore is nearly at right angles to the river. As the water nears the river, it veers in a downstream direction. Deep Creek contributes a considerable amount of water to the ground-water reservoir; in the alluvial fan of the creek the ground water moves northwestward toward Townsend. A large marsh has developed south of Townsend as the result of the recharge from this creek.

The slope of the ground-water surface in the Crow Creek area is 30 to 50 feet per mile. In the area between Toston and Town- send the slope is about 20 feet per mile, but it decreases to 10 feet per mile in the vicinity of Townsend. The ground-water gra dient near the mountain front between Duck Creek and Confederate Gulch is about 70 feet to the mile. Ground-water contour maps could not be prepared for either the area north of Confederate Gulch or the area west of the Missouri River north of Crow Creek because of the small number of wells. However, the ground water in those areas is believed to move more or less directly from the mountain front to the Missouri River.

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re 3

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GROUND WATER 213

EFFECTS OF EARTHQUAKES

The severe earthquake in 1925 is reported to have caused some springs within a 50-mile radius of the epicenter to increase in flow and others to decrease. Springs that fed Sixmile Creek, which was the source of the Toston municipal water supply, near ly discontinued flowing after the severe tremors, and consequent ly, inhabitants of the town resorted to dug or drilled wells for their water supply. Big Spring is reported to have been muddy for 2 days after the earthquake. The flow of Plunket Spring is said to have increased but, as the flow in 1950 was slightly less than that in 1921, the increase apparently was temporary.

South of Lombard several cracks appeared in the bottom land along the Missouri River, and water and sand spouted up for sev eral hours after the earthquake. Similar sand spouts were re ported near Townsend. A few wells are reported to have gone dry and others to have become muddy. The earthquake in 1935, which had its epicenter near Helena and which caused property damage in the Townsend Valley, caused no apparent change in ground- water conditions in the Townsend Valley.

WATERLOGGING

About 8, 500 acres in the Townsend Valley are waterlogged. More than half of this land is unproductive at the present time and the productivity of the remainder has decreased greatly. The ex tent of the waterlogged land was mapped from field observations and by inspection of aerial photographs. (See pi. 20.)

About 1, 500 acres of the waterlogged land is west of Canton; most of this land is suitable only for grazing, but small plots are used for wild hay. This land will be covered by backwater from the Canyon Ferry dam.

Between Townsend and the lower course of Deep Creek an area of about 2, 000 acres is waterlogged. Twenty-five years ago this land reportedly was productive, but now only small tracts can be farmed, and the remaining marsh land is barely suitable for graz ing. In 1921 the water level in well A7-2-33cd was 12 feet below the land surface (Pardee, 1925, p. 51), and in August 1949 the water level in the same well was only 0.50 foot below the surface. The maximum yearly fluctuation of the water level in several wells nearby ranges from 0. 50 to 1.5 feet. During recent years land upslope from the waterlogged area has been irrigated and influent seepage from the irrigation canals and laterals and from irriga tion water applied to the fields has recharged the ground-water


reservoir. The alluvial fan, through which the ground water is moving, is not sufficiently permeable and does not have sufficient gradient to transmit the extra recharge; consequently, some of the ground water is discharged at the surface in the form of springs and effluent seeps. Apparently the nearness to the sur face of relatively impermeable bedrock affects the movement of the ground water in this part of the area. Precambrian shale is exposed for a distance of nearly 1,000 feet along the north bank of the Montana irrigation canal about half a mile east of Townsend and it underlies the gravel-covered benchland. An exposure of similar bedrock along the west bank of the Missouri River west of Townsend suggests that the alluvium in the vicinity of Townsend is thinner there than in other parts of the valley. (No known wells have been drilled into the alluvial fill in or near Townsend.) A drainage study of the waterlogged land east of Townsend was made by the U. S. Soil Conservation Service (Long and James, 1948), and plans for drainage ditches are now being made (1951).

Most of the remaining 5,000 acres of waterlogged land is in the Crow Creek area. Ground water is discharged by many springs and effluent seeps along the lower Crow Creek valley. The land is poorly drained, supports a heavy growth of phreatophytes, and is suitable only for grazing. The sediments beneath the valley land adjoining the lower course of Warm Spring Creek are fine textured and support a capillary fringe which, in many places, extends to the land surface. Clay and silt deposits ranging in thickness from 1 to 45 feet were penetrated when observation wells were jetted in this part of the valley. Wells (A4-2-5bb; A5-l-36cc, -36dc; A5-2-27bbl, -27bb2, -27bb3; A5-2-29cc, -29dd; A5-2- 31cc2, -31da; and A5-2-32cd) ranging in depth from 5 to 28 feet were jetted into light-gray and bluish-gray clay without encoun tering gravel beds. The remaining jetted wells were terminated in gravel beds of an undetermined thickness. Well A5-2-33ac, the deepest jetted hole, reached a water-bearing layer of gravel after penetrating 45 feet of light-colored clay and silt.

A small waterlogged area in the NWi sec. 27, T. 5 N. , R. 2 E., is of particular interest because it indicates the effect of the irrigation of benchland on the ground-water conditions of the ad joining lowland. The ground-water surface in the valley bottom is 4 to 6 feet below land surface in the winter season. In the spring as soon as water is in the Broadwater irrigation canal, the ground- water surface begins to rise and a small marshy area forms be low the break in slope between the benchland and the valley bot tom. Influent seepage from the irrigation canal appears to be the chief source of recharge to the ground-water reservoir; and, be cause the valley sediments are relatively impermeable, the added recharge is forced to the surface instead of percolating laterally through the alluvium.

GROUND WATER 215

DISCHARGE

The ground water in the Townsend Valley is discharged by wells and springs, by evaporation and transpiration, and by seepage in to the Missouri River and tributary streams.

About 330 wells are in use in the Townsend Valley. (See pi. 20 and table 4.) Because most of these wells supply water only for domestic and stock needs, the discharge by wells is only a small part of the total ground-water discharge. The pumpage from all wells in the Townsend Valley probably does not exceed 200 acre- feet per year.

Some of the water that is discharged from the ground-water reservoir by springs is returned to the ground-water reservoir in the lower parts of the valley. Other springs, however, issue from the alluvium close to the Missouri River and discharge wa ter directly into the river.

EVAPOTRANSPI RATION

The amount of ground water lost by evapotranspiration varies with the season. The rate of loss is highest during the growing season when the temperature is high and is lowest in the winter when relatively little plant growth takes place. In many places in the Townsend Valley the capillary fringe above the water table is close to the land surface. It is from these areas that large amounts of water are discharged from the ground-water reservoir during the growing season.

SEEPAGE INTO STREAMS

It is believed that more water is discharged from the under ground reservoir into the effluent streams than by any other means. The Missouri River is effluent in its entire course through the Townsend Valley and is the principal drain for discharge of the ground water. Crow Creek, its tributaries, and Beaver Creek are effluent in their lower reaches, and all discharge ground wa ter from the area.

SPRINGS

Big Spring (A4-3-5cc), which is on the east bank of the Missou ri River 4 miles south of Toston, is the largest of the springs that issue from the older rocks in and around the valley. The water

394090 O - 56 - 4


issues from a talus-covered slope that overlies the basal red shale of the Amsden formation. Because some faulting is evident in this vicinity, the water is thought to follow a fault zone that connects with a cavernous reservoir in a limestone of the Madison group. One and one-half miles south of the spring the Missouri River, joined by Sixteenmile Creek at Lombard, flows across the upper dip slope of this limestone at an altitude '30 feet higher than the spring. As several large caverns are exposed in the Madison near Lombard, Pardee (1925, p. 47) stated:

These relations suggest that most of the water discharged by this spring may come through underground channels that tap the river or Sixteenmile Creek in the neighborhood of Lombard.

However, as the temperature of the water that issues from Big Spring is relatively high (59° F) and as it remains constant through out the year, the distance to the source of recharge for the spring is thought to be greater than was suggested by Pardee; possibly it is much farther east along the course of Sixteenmile Creek. The flow of the spring is almost constant throughout the year and var ies little from year to year. The flow in May 1922 was measured as 64.4cfs (Pardee, 1925, p. 46), and the flow on May 5, 1951, was 56. 7 cfs. The temperature of the water in July 1921, Sep tember 1949, and June 1950 was 59°F. During the spring and summer months most of the flow is diverted by a small concrete dam into a canal and is used to irrigate land north and west of Toston. A small amount spills into the river.

Plunket Spring (A4-l-27ab), which is known also as Mockel Spring, is near the head of Warm Spring Creek in the south- central part of the Crow Creek area. The water gushes from sev eral openings in a small outcrop of the thin-bedded Lodgepole limestone, which is the older formation of the Madison group. The flow from this spring, which is reported to remain constant throughout the year, was 8.7 cfs in August 1949; this is 1 cfs less than that reported for May 1922 (Pardee, 1925, p. 47). The tem perature of the water was 62°F both in July 1921 and in Septem ber 1949; this moderately warm temperature indicates relatively deep circulation. The water from the spring collects in a shallow pond, which is impounded by a small dam constructed to divert the flow for irrigation of the land along Warm Spring Creek.

The largest of the springs issuing from Tertiary beds is Bed ford Spring (A7-l-23ba), 3 miles northwest of Townsend. The water issues over a small area and has an aggregate flow of about 3. 0 cfs. In September 1949 the temperature of the water was 74° F; this indicates that the water probably rises from the bed rock that underlies the Tertiary deposits. The water percolates

GROUND WATER 217

to the surface through small openings in the younger coarse- textured deposits. The flow is reported to remain constant through out the year, and the water is used for irrigation and domestic supplies. It is said that the water was used in the 1870's to power a grist mill about a mile north of the spring.

A smaller spring, known as Kimpton Spring (A5-l-22ca), bub bles through a small pool on the flood plain of Crow Creek, 3 miles southeast of Radersburg. Its flow in September 1949 was estimated to be less than 100 gpm. The temperature of the water was 64° F. The water is believed to rise from deep within the Tertiary beds and probably reaches the surface through small fis sures or cracks in the overlying sediments.

Other small springa issue at many places in the lowland near the confluence of Crow and Warm Spring Creeks. They form swampy patches that are the principal sources of several smaller tributaries to Crow Creek.

A short distance east of U. S. Highway ION and 7 to 9 miles northwest of Townsend, springs cause several small swampy areas on the gently sloping benchland. Antelope Springs (A8-1- 21ba, -21bd, and -28ad) issue from the sand and gravel overlying the Tertiary sediments. Some of the water collects in a small concrete reservoir and supplies stock water for the Cook ranch. No wells or bedrock exposures in this area indicate the ground- water conditions, but the northwest-trending line of small springs indicates that ground water moving from the base of the mountains toward the river is forced to the surface by warped or faulted im permeable beds.

A short distance north and west of Canton in sees. 19, 20, 29, 30, and 31, T. 8 N., R. 2 E., effluent seepage has caused most of the land adjoining the Missouri River to become swampy. Small springs issue from the alluvium and form a small creek.

Many small springs also issue from the gentle valley slopes east of Canton. The south end of the spring zone is in the central part of sec. 11, T. 7 N., R. 2 E., and the zone extends north ward about 3 miles to sec. 26, T. 8 N., R. 2 E. The aggregate flow from springs in this zone is estimated to be 5 cfs. Part of the water is used for domestic and stock supplies and, in the sum mer, a small amount is used for irrigation. The temperature1 of two small springs nearly three-fourths of a mile apart on the Harold Marks ranch (sec. 2, T. 8 N., R. 2 E.) was 52°F on June 21, 1950. Although the temperature does not indicate a deep source, other ground-water conditions indicate that the water is suing in these springs is probably reaching the land surface along


a fault plane that connects confined aquifers in the underlying Ter tiary beds with the surface. Only a short distance west of this area, the water level in wells A7-2-3da and A7-2-10aa is report ed to be 60 to 70 feet below the land surface.

WELLS

The pre-Tertiary rocks that surround the Townsend Valley are strongly folded or faulted. The few ranchers who live in areas of pre-Tertiary rocks obtain water either from springs or from shallow wells that have been drilled or dug into the alluvium in the valleys of the perennial streams. No wells are known to tap the pre-Tertiary formations. The water level in the mines that penetrate the igneous rocks west of Radersburg is reported to range from 200 to 250 feet below the surface.

Well A4-2-8bb2 was drilled in Tertiary rocks to a depth of 71 feet in the lower reaches of the benchland that adjoins Warm Spring Creek valley. The water level in this well is about 32 feet below the surface, and the well furnishes an adequate water supply (8 gpm) for stock use and garden irrigation. Another well, A4-2- lObb, on the higher part of the benchland, was bottomed in sand and gravel at a depth of 200 feet. The water level in this well is about 171 feet below the surface, and the yield of 10 gpm is ade quate for a large herd of range cattle.

Wells drilled in Tertiary rocks on the higher benchland between Deep and Sixmile Creeks reach water at depths of 150 to 200 feet and yield an adequate supply (8 to 10 gpm) for domestic and stock use.

In the lower part of the Townsend Valley many of the wells drilled into the coarse permeable gravel of Pleistocene and Re cent age yield at least 8 to 10 gpm. In the vicinity of Townsend, wells driven 20 to 30 feet into the coarse-textured alluvial fan of Deep Creek yield an adequate supply of water for domestic and stock needs. Dug and drilled wells between Deep Creek and Tos- ton penetrate water-bearing layers of sand and gravel at depths of 20 to 60 feet; these wells yield an adequate water supply for do mestic and stock use. Dug and drilled wells in the Crow Creek valley obtain an ample supply of water from coarse-textured gravel and cobble deposits.

Several wells drilled on the lowland adjoining Warm Spring Creek were reported to penetrate a considerable thickness of "quicksand" overlying an indurated clay bed, which is locally called hardpan. The hardened clay layer is probably of early

GROUND WATER 219

Oligocene age and is underlain by sand and gravel, which yield an adequate water supply for domestic and stock use. Apparently, as a result of differential subsidence, the Tertiary beds in the Crow Creek area form a shallow basin; and, in general, the beds dip toward the center of the area. Precipitation and seepage from ir rigation canals and streams enter the permeable beds where they are exposed on the higher valley slopes. The water then moves down the dip of the permeable beds and becomes confined below the less permeable beds. Wells drilled in the central part of the area penetrated a small reservoir of confined water. In well A5- 2-31bd, reported to be 75 feet deep, the water is under sufficient artesian pressure to flow at the surface. Several wells nearby also tap confined water, but the artesian pressure is not sufficient to cause the water to flow at the surface.

The only other artesian wells in the area are three wells east of Townsend; they appear to have penetrated aquifers on the west limb of the Deep Creek anticline. Well A6-2-2ca was drilled to a depth of 78 feet and the water level rose to within 4 feet of the land surface when the aquifer was penetrated. Well A6-2-2db, which was drilled to a depth of 164 feet to obtain a water supply for irrigation, penetrated four artesian aquifers, and the water in the well rose to a level about 5 feet below the land surface. Well A7-2-22bb penetrated an artesian aquifer at a depth of 156 feet, and the water level rose to within 30 feet of the land surface.

USE

In the Townsend Valley, ground water is used mainly for do mestic and stock supplies. A few wells supply water for irriga tion of garden plots and one well was recently drilled for an irri gation supply.

The older wells in the valley were dug by hand, but the newer wells are either drilled or driven. The dug wells are 3 to 5 feet in diameter, the drilled wells 4 to 6 inches, and most of the driven wells are U inches. As most of the wells extend only a few feet below the water table, they are limited to a small drawdown and, consequently, to a small yield. The yield, however, is sufficient for all domestic and stock needs.

The first well drilled to obtain a water supply for irrigation was constructed in 1950 on the property of Edward Heuer (A6-2- 2db) about 3| miles southeast of Townsend. The well is 164 feet deep and 12 inches in diameter and yields water from sand and gravel of both Quaternary and Tertiary age. The casing is close ly perforated opposite the water-bearing strata, but elsewhere is


sparsely perforated. Upon completion the well was bailed at ap proximately 60 gpm, and the water level was drawn down 35 feet. The yield of the well was increased by development, and the well is expected to yield about 350 gpm with a drawdown of 60 feet. The driller's log of the well is given below and also is shown dia- grammaticallyin figure 38. Much local interest was shown in this irrigation well and, if it proves successful, other such wells prob ably will be drilled.

Driller's log of irrigation well A6-2-2db

Topsoil, sandy clay.......................................................

Soft clay.. ............................................................ .......

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

Thickness (feet)

644

1028121610

72838

1412

13754

Depth (feet)

6101424526480909799

107110118132144145148155160164

Townsend, which has a population of 1,300, obtains its munici pal water supply from Deep Creek. In 1946 the old infiltration galleries (Pardee, 1925, p. 51 52) were abandoned, and a new collecting system was installed. Water is now diverted from Deep Creek into open sumps or settling basins. From the sumps, the water is transported 2| miles through a 10-inch pipe to two open concrete reservoirs, which have a combined capacity of 360, 000 gallons. The reservoirs are at an elevation about 220 feet above the town, and the water is delivered under the pressure of gravity through several miles of wood stave pipe mains. The daily water consumption in 1950 was estimated to be 300,000 to 400,000 gallons.

Since 1925, when the earthquake changed the flow of Sixmile Creek, the town of Toston has not had a municipal water supply. The residents obtain water from shallow wells.

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CHEMICAL QUALITY OF THE WATER

In the autumn of 1949 and 1950, samples were collected for chemical analysis from 47 water supplies in the Townsend Valley; the location of the sampling points is shown in plate 20. These samples represented supplies from the following ground and sur face sources:

Source SamplesSprings in pre-Tertiary rocks..................................................................... 2Springs in Tertiary deposits....................................................................... 4Wells in Tertiary deposits......................................................................... 16Wells in Quaternary alluvium.................................................................... 13Wells in undifferentiated deposits............................................................... 3Missouri River........................................................................................ 1Minor streams........................................................................................ 8

Total................................................................................................ 47

The analytical results are reported in table 3. The chemical character of ground water at a given locality usually remains fairly uniform in relation to time. An exception to this general statement is the change in the quality of the shallow ground water in irrigated tracts during the irrigation season. The chemical character of the surface supplies, which varies much more than that of the ground water, depends on conditions of flow; the higher concentrations of dissolved solids usually occur at times of low discharge. The analyses of ground-water samples in table 3 prob ably represent general range in composition of the ground water in the valley. The chemical examination of samples from the Mis souri River and minor streams indicates the character of the wa ter only at the time the samples were collected.

Information relating to the chemical quality of water in the Townsend Valley is useful in the evaluation of present supplies, the development of supplies for future needs, and the evaluation of changes that may occur as the result of irrigation or other ac tivities of man.

Tab

le 3

. C

hem

ical

an

alys

es o

f w

ater

in T

own

sen

d V

alle

y, M

ont.

[Ana

lyse

s in

par

ts p

er m

illi

on e

xcep

t as

ind

icat

ed]

Sou

rce

Pre

-Ter

tiar

y r

ocks

A

4-l

-27ab

(P

lunk

et S

prin

g)...

..

Ter

tiar

y de

posi

ts

A4-2

- 8bb2..

....

....

....

....

....

...

-lO

bb

....

....

..................

A5-l

-22ca

(K

impt

on S

prin

g)...

-35ca............

....

....

....

..A

5-2

-28

cd

....

....

....

....

....

....

..

-31bd..........................

A6-2

- 2ca..........................

-27

cc..

....

....

....

....

....

....

A7-l

-23ba

(Bed

ford

Spr

ing)

....

A7-2

- 2b

b (S

pri

ng).

..............

-22bb..........................

A8-1

- 6cbl7

........

....

....

....

...

- 6

cc2

....

....

................

-28a

d (A

ntel

ope

Spr

ing)

.. A

8-2

- 8ca..........................

-lla

b..........................

-14

bb

....

....

..................

A9

-2-

6d

d..

....

....

....

....

....

....

-33

cd

....

....

....

....

....

....

..A

10

-l-2

8ad

.«..

....

... ..

..

§ Date

of

collect!

9-30

^19

9-3

0-4

9

9-3

0-4

99-3

0-4

99-

30-4

910

- 3-

4910

- 3-

49

9-30

^19

9-

1-50

10-

3-49

10-

3-49

9-

1-50

9-

3-50

9-

1-50

9-

1-50

9-

1-50

9

- 3-

50

9-

1-50

9-

1-50

9-

3-50

9-

3-50

9-

3-50

Depth

of

well (fee

t)

71.0

200.

1

78.7

62.3

75.0

78 35.1

156.

550 80

""85

*9*

142

107

400 60

.510

0+

O~

55-

ri

u a P4

C/J

18 23 23 38 20 24 25 31 15 36 21 21 9.9

18 22 21

10 14 12 15 25 15

"aT b 0.03 .0

2

.86

.05 n/i

.77

.64

.02

.10

.22

.03

.10

5.2 .08

.36

.09

1.8 .1

0.1

3.2

410

.36

Calcium

(Ca) 44 44 70 40 9,4

50 109, 86 79

,76 59

,90 46 49

,46 44

63 59

,91 54 42 10

7

Magnesium

(Mg

21 18 31 21 5.7

19 47 23 26 17 19 31 20 14 9.5

9.5

39 20 30 37 47 .61

"tt s, 1 C/J

23 13 22 24 6.0

41 68 55 15 16 13 23 12 22 20 21 17 8.8

84 10 66 79

Potassium

(K)

3.2

6.4

5.6

13 4.8

6.4

10 11 2.6

8.0

3.2

8.4

4.5

3.1

1.4

1.8

9.3

4.6

76

3.4

5.6

3.7

o" Bicarbonate

(HC 188

199,

9,16

160

104

9,3f

i31

6

128

311

302

150

310

195

167

139

145

9,69

104.

278

167

420

287

0*

!£> <u 4-» i c« 81 59

,

131 85 14 71 298

292 48 39 103

114 48 58 70 46 Qfi 61 9,

4111

6 8R 308

Chloride

(Cl)

10 7.0

31 16 4.0

10 40 29 4.5

12 7.0

12 15 6.0

4.5

16

13 2.5

35 31 4.5

34

Fluoride

(F)

0,6 .2 6 .6 .0 .0 6 6 .1 .0 .3 3 .1 .3 .1 .1

.4 .9, .1 .4 T.9, .5

Nitrate

(NO^) 1.

6 .8 6.2

8.4 .4

20 4.4

8.2

1.2

4.6 .7 6.9 .5 3.6

2.6

2.0

16 1.3

6.7

7.5

2.4

86

Boron

(B)

0.14 .1

4

.20

.16

.10

.10

.20

.16

.12

.14

.10

.13

.02

.08

.09

.08

.04

.05

.14

.17

.28

Dissolved

solids

306

9,66

449,

39,0

134

366

748

620

340

358

306

476

9,58

9,79

,9,

5624

2 40

4

9,60

674

398

500

906!

Har

d as

Cs

"rt S H 197

184

309,

187 84 9,

0344

8

309

9,85

9,60

9,08

350

199

163

154

149

319

9,19

,34

99,

859,

9951

7

ness

iC

O,

Noncarbonate

43 9.7

19,5 56 0 9

189

9,04 30 19

,85 96 39 9,

640 30

98 53 19,1

148 0

282

Percent

sodium 9,0

13 13 9,0 13 30 9,4

9,7 10 11 19,

19,

11 9,9,

9,9,

23

10 8 34 7 39,

27

tance )

Specific

conduc (m

icromhos

493

419

676

492

201

533

1,02

0

868

566

571

451

723

437

399

379

376

648

421

982

591

770

1.24

0

£ 75

74

7.1

7.4

7(1

76

7.5

7,1

7 6

7.2

7,4

7.9

7.4

7.1

7.6

7.9

7.7

7,5

8,0

7.5

8.0

7.9

Tab

le 3

. C

hem

ical

ana

lyse

s of

wat

er in

Tow

nsen

d V

alle

y, M

ont.

Con

tin

ued

Sou

rce

All

uviu

m

A4

-1-

2ca3

....

....

....

....

....

....

A5-l

-23cc2........................

A5-2

- 4

db

....

....

....

....

.«..

....

.-l

Oad

....

....

....

....

....

....

..-2

1ad

....

....

....

....

....

..

.

-23ca4........................

A6-2

- 9

dd

l...

....

....

....

....

....

.A

7-2

-15

CC

....

....

....

....

....

....

..-2

9ca

2... ..

..

....

...

-31db..

....

...^

,........M

....

-33cdl.

.«....^..«.«

.......

A8

-2-2

9d

c2

,...

«^..

....

«.^

...

-32db2........................

Und

iffe

rent

iate

d A

7-2

- 2b

d . ..

........

-lO

bb

...........

....,-

....

Sur

face

wat

er

Mis

sour

i R

iver

nea

r T

oat

on.....

Con

fede

rate

Gu

lch

....

....

....

....

Date

of

collection

9-3

0-4

9

9-3

0-4

9

10-

3-49

10

- 3^

19

10

- 3-

49

10-

3-49

1

0-

3-49

10

- 3-

49

10-

3-49

&

- 3-

50

10-

3-49

1

0-

1-50

9-

1-50

9-

1-50

9

- 1-

50

9-

1-50

9-30

-49

9-30

-49

9-

3-50

9-

30-4

9 9

- 1-

50

9-

1-50

9-

1-50

9

- 3-

50

9-

1-50

Depth

of

well (fee

t)

28.5

42

,2

25.2

61

.2

16.2

28.4

36

.9

115,

0 38

.0

20 20.0

30

18 117 62

.5

39

....

....

.

.........

J

2. ri

O r4

(/}

50

22

37

30

43 23

22

22

25

25 16

26

29 19

13

14 22

20

25

20

17 15

15

12

16

<u fc. .02

.07

.97

.04

.09

.02

.03

1.5 .1

3 .1

0

.42

.14

.11

.16

.42

.14

.02

.04

.02

.02

.02

.01

.02

.02

.02

Calcium

(Ca)

102 40

62

172

103 61

47

106 67

64 63

75

83 70

84

60 42

21

68

53

48 41

37

57

13

Magnesium (Mg)

17 6.2

.24 42

37 17

16

45

25

21 21

23

23 26

42

21 14 3.9

13

19

16 10

12

26 .9

I =§ t/i 44 8.7

54

46

61 27

32

14

35

21 8.2

32

54 14

34

16 24 2.2 8

12

5 5 5 16 5

g 0,

11 4.0

11

5.6

11 5.6

4,8

7.2

9.6

5.0

4.8

5.8

6.3

5.2

6.8

5.1

4.8

3.2

3 6.

4 .3 .8

.8 .3

Bicarbonate

(HCOj)

462

158

308

270

362

228

244

146

324

271

212

331

297

295

320

193

192 74

272

234

188

162

151

199 43

1 <u s 3 CA

46

17

90

130

204 68

50

15

4 66

55 52

50

70 55

128 70 46

12

13

50

34 19

27

110 10

Chloride

(Cl)

3.0

4.4

16

51

37 17

11

136 14

6.0

16

13

49 8.0

37

26 13 3.0

3.0

6.0

4.5

1.5

1.0

3.0

1.0

£ <u o | tb

"*T

1.0 .8

""Jo" .2

.2 .2

.5

1.

2 .4

.2

.3 1.0

....

...

.0

.4 .2

.2

.8

.2

Nitrate (NO,)

18 .2

4.

2 36

4 4.4

5.6

2.4

14 .4

1»

5

2.0

6.0

35 6.3

7.5

3.3 .6

.0

.3

.1 .7 1.3

1.2 .6

.3

Boron

(B)

.20

.10

.30

.40

.10

.14

.10

.20

.10

.15

.22

.17

.05

.14

.07

.20

.06

.07

.10

.03

.08

.05

.13

.01

Dissolved solids

518

180

448

976

712

358

306

702

406

346

290

395

506

362

535

334

276

102

276

296

234

186

192

344 74

Har

dnes

s as

CaC

Oj

1

H 325

126

253

602

409

222

184

450

270

244

236

280

302

282

382

234

163 69

223

211

186

144

142

249 36

(U

4-1 ri

§ e ri z. 0 0 0 38

1 11

2 35 0 33

0' 4 22 62 9 58 40

120 76 6 8 0 19

32 11

18

86

1

Percent

sodium 22

13

31

14

24 20

27 6 21

15 7 19

27 10

16

13 24 6 8 11 6 8 8 12

24

Specific

conductance (microm

hos)

789

293

708

1,34

0 98

8

540

509

979

651

524

465

631

791

575

825

522

426

155

432

455

362

297

298

521 94

;* 7.3

7.5

7.4

7.3

7.3

7.2

7.4

7.2

7.2

7.8

7.4

7.5

7.5

7.6

7.8

7.5

7.6

7.2

8.2

7.8

8.1

8.0

7.9

8.2

7,3

CHEMICAL QUALITY OS THE WATER

GROUND-WATER SUPPLIES

225

<PRE-TERTIARY ROCKS

Big Spring, south of Toston, and Plunket (Mockel) Spring, near the head of Warm Spring Creek, issue from pre-Tertiary rocks. The water from both springs is hard and is similar in character to water known to have been in contact with limestone or dolo mite. From a comparison of present analyses with earlier anal yses reported by Pardee (1925, p. 57) it is concluded that the properties of the spring water have undergone little change in a period of about 30 years. The results of these analyses are shown below:

Analyses of spring water

[Parts per million]

Constituent

Silica (SiCfe)......................................

Sulfate(SO4).....................................Chloride (Cl).....................................Nitrate (NOj).....................................

Big Spring

1922

20 46 17 17

183

57 8.0

.49 185 259

1949

23 44 18 19

192

52 7.0

.8 184 266

Plunket (Mockel) Spring

1921

22 70 34 32

332

92 11

314 408

1949

18 44 21 26

188

81 10

1.6 197 306

Although the chemical properties of the two samples of water from Plunket Spring differed somewhat, the difference was one of concentration rather than composition. The cumulative amounts, in percent, of the mineral solids for the two periods was in good agreement, as seen in figure 39.

TERTIARY DEPOSITS

Hard water of moderate mineral content is typical of supplies from Tertiary deposits in Townsend Valley. For 20'samples the average hardness and mineral content were 264 and 414 ppm, re spectively. Water issuing from Kimpton Spring, 3 miles south east of Radersburg, was the softest (84 ppm) of samples in this group.

The sample of water from Bedford Spring, 3 miles northwest of Townsend, was similar in chemical character to spring water

10

0

90

80

70

60

§5

0

CC

LxJ

Q^

40

30

20

10 0 Si(

BIG

S

PR

ING

I

//

Sr

// Ye tr

\r

if If

1 il 1 1

1 1 or

52

»9

1/

''

^^

:»=

Dis

solv

ed

solid

s, in

pa

rts

per

mill

ion

25

9

266

D2

Co

IMg

Na+

K

C0

3 S

04

Cl

NC

MIN

ER

AL

CO

NS

TIT

UE

NT

Fig

ure

39

. C

um

ula

tive

am

ou

nts

, in

perc

ent,

of

mil

IOO 90

80

70

60

h-

Z

UJ

0

50

or UJ a.

40

30

20

JO

0

PL

UN

K E

T

/

,&

*

SP

RIN

G

I

y ^ '

Ye ir\

-

19

1

j

f ar 21

49

r 7 // i Dis

solv

ed

solid

s, i

n pa

rts

per

mill

ion

408

30

6

to

to CT>

Si0

2 C

oM

g N

atK

C

03

S0

4 M

INE

RA

L C

ON

ST

ITU

EN

TCl

N03

CHEMICAL QUALITY OF THE WATER 227

A Ch -2_ ad Sodjum + potassium

42.2 20.0 It 61.2ALLUVIUM

Figure 40. Analyses of ground water in Tertiary deposits and alluvium, Townsend Valley.

0«pth - 200.1 100+ (f««t) TERTIARY DEPOSITS


from the pre-Tertiary rocks. The analysis also shows about the same concentration and chemical composition as reported for a sample collected in 1921 (Pardee, 1925, p. 57). These analyses of the water from this spring are shown below:

Analyses of water from Bedford SpringIf arts per million j

Silica (SiOz).... .....................................................

Bicarbonate (HCOz).... ............................................

Sulfate (SO4)........................................................Chloride (Cl)........................................................Nitrate (NO;).......................................................,

1921.......................... 16.......................... 60.......................... 19.......................... 18........................... 151

.......................... 127

........................... 8.0

.......................... 228 ........................... 336

1949215219ID

150

1037.0

.7 208 306

The dissolved solids and hardness of shallow ground water are generally greater in the irrigated areas of the Townsend Valley than in the nonirrigated areas. For example, the sample from well A5-2-28cd, drilled 62. 3 feet deep, contained 748 ppm of dis solved solids and had a hardness of 448 ppm. This greater min eralization is probably the result of the mixing of the ground wa ter with recharge water that has reached the Tertiary sand and gravel as subsurface drainage from irrigated farmland.

Bar diagrams showing analyses of ground water from Tertiary deposits are shown in figure 40.

ALLUVIUM

Ground water from the alluvium is very similar in chemical properties to supplies from Tertiary deposits. For 13 samples from wells in alluvial deposits, the average dissolved-solids con tent and hardness were 473 and 300 ppm, respectively. Most of the wells from which water samples were collected are shallow wells drilled or dug in areas under irrigation. Because the allu vium is recharged largely by downward-percolating irrigation wa ter, the mineral content of the ground water in the alluvium is determined in part by the chemical character of the irrigation water.

The sample of water from well A7-2-33cdl, in the waterlogged area southeast of Townsend, contained 290 ppm of dissolved sol ids. An earlier sample of water from this well, which was col lected in 1921 (Pardee, 1925, p. 57) when the water level in the well was 12 feet below the surface, contained 306 ppm of dissolved

CHEMICAL QUAIITY OF THE WATER 229

solids. Although the total mineral content of the water has re mained about the same, the composition of the dissolved solids has changed as follows:

Analyses of water in well A7-2-33cdl

[Parts per million] 1921 1949Silica (SiOz)................................................................................... 14 16Calcium (Ca)................................................................................. 48 60Magnesium (Mg)............................................................................. 22 21Sodium and potassium (Na + K).......................................................... 21 13Bicarbonate (HCOj).......................................................................... 188 212

SulfatefSO^.................................................................................. 87 52Chloride (Cl).................................................................................. 8.0 16Nitfate^NOj).................................................................................. .5 2.0Hardness (as CaCOj)......................................................................... 210 236Dissolved solids............................................................................... 306 290

Analyses, in equivalents per million, of water samples from the alluvium are shown in figure 40.

UNDIFFERENTIATED DEPOSITS

Samples were collected from three wells that produce water from aquifers that could not be identified. As these samples were similar in chemical character to water from Tertiary and alluvial deposits, it is thought that the source of the water was one or the other of these deposits, or both.

SURFACE-WATER SUPPLIES

Analyses of water samples from the Missouri River and eight minor streams (table 3) show that the surface water in the valley generally is less mineralized and is also softer than the ground water, although some exceptions occur. As previously noted, analyses of stream samples show the chemical character of the surface supply at the time of sampling only. The results cannot be interpreted as necessarily representing the quality of the wa ter at all stages of flow.

SUITABILITY FOR USE

In the Townsend Valley springs and surface sources furnish water for irrigation, whereas water from wells is used largely for domestic purposes. In the following discussion, supplies from both ground and surface sources are considered in regard to their suitability for use.


IRRIGATION

Ground- and surface-water supplies sampled in 1949 and 1950 are suitable for use as irrigation water in accordance with per missible limits proposed by Wilcox (1948, p. 25-28) for electrical conductivity, percent sodium, and boron, Ratings of water from different sources are tabulated below:

Suitability of water tor irrigation

Source

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

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

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

Number of samples

21

1458521117

Rating

21232323212

Grade

Good.Excellent.

Good.

Good.Excellent.Good.

DOMESTIC

Except for hardness, the water for which analyses are reported in table 3 is generally satisfactory for domestic use, although iron is present in objectionable amounts in some ground-water supplies. Well A5-2-10ad, pumping water from alluvium, should not be used as a source of drinking water because of the high con centration (364 ppm) of nitrate in the water. Surface contamina tion is probably reaching this water, for the well is dug near a large stock-feeding corral.

SUMMARY AND CONCLUSIONS

Ground water in quantities large enough to supply domestic and stock needs can be obtained from wells drilled into the alluvial deposits of the valley bottom, or into the Tertiary deposits that flank the valley bottom for much of its length in the Townsend Valley. In parts of the valley, wells drilled into the alluvial de posits could probably obtain several hundred gallons of water per minute. Where conditions are favorable, limited supplies can be obtained from wells drilled into the limestone and sandstone for mations of Paleozoic age. Springs issuing from pre-Tertiary sedimentary rocks supply domestic and stock water to ranchers who live in the higher parts of the valley and are the principal source of water that maintains the flow of perennial streams.

SUMMARY AND CONCLUSIONS 231

Ground water is under artesian pressure in the Tertiary depos.- its in the Crow Creek area and along the west flank of the Dry Creek anticline east of Townsend. In the Crow Creek area water supplies that are only large enough for domestic and stock needs are produced from the confined reservoir. Well A5-2-31bd is a flowing well. East of Townsend the artesian aquifers are capable of greater yields; the yield of well A6-2-2db is used for irriga tion, and additional wells in this area probably could produce large enough water supplies for the same purpose.

The principal sources of ground-water recharge in the valley are the streams that flow across the area, the irrigation canals and laterals, and seepage from irrigated fields. In the lower parts of the valley where the water table is near the surface, a small amount of precipitation also reaches the ground-water reservoir. Influent seepage from streams and precipitation are the sources of recharge to the reservoirs in the older rocks of the mountain ous area.

In general, the ground water in the Crow Creek area moves northeast toward the Missouri River, and the hydraulic gradient is 30 to 40 feet to the mile. In the valley bottom north of Toston, the water table slopes to the west at an average rate of 20 feet to the mile, and the movement of the ground water nearly parallels the perennial streams.

Waterlogging in the Townsend Valley is primarily the result of geologic conditions that control ground-water movement and of recharge from irrigation water. The high water table in parts of the valley makes the land suitable only for the growth of wild hay and for grazing.

The application of additional irrigation water to the benchland flanking Warm Spring Creek will increase the extent of waterlog ging in the bottom land unless provision is made for more ade quate drainage. In this part of the valley the Tertiary sand and gravel deposits, which are mantled by permeable windblown soil, are underlain by beds of hardened clay, locally referred to as "hardpan. " If water is applied to these lands, a gradual rise in the water table will take place. This rise will result in the in creased flow of existing springs in the lower part of the valley, and new springs will appear along the slope from the benchland to the valley bottom. In this area the valley bottom is underlain by relatively impermeable fine-textured clay. The capillary fringe above the water table will rise to the surface in much of the bottom land, saline soil will develop, and the land will eventually become unproductive. Waterlogging will become more extensive if irri gation water is applied to the benchland that lies at a higher

394090 O - 56 - 5


elevation than the present irrigated land unless provision is made for more adequate drainage. This condition will exist not only in the Crow Creek area but also in other parts of the valley where additional irrigation is planned.

Backwater from the Canyon Ferry dam will raise the water table under the land adjoining the reservoir. To keep most of the farmland around the reservoir in production, adequate drainage facilities must be provided.

Water supplies in the Townsend Valley generally are hard but moderately mineralized. The quality of water from springs was about the same in 1949 as in 1921 or 1922. Ground water is used almost exclusively for domestic purposes or for watering of stock and, except for hardness, is generally satisfactory. Iron is pres ent in objectionable amounts in some supplies. The effects of wa terlogging on the quality of the water cannot be defined at the present time; a water sample from a shallow well in an area that is now waterlogged was only slightly different in quality from a sample from the same well before the area became waterlogged. Water both from ground and surface sources is satisfactory for irrigation on the basis of ratings that have been proposed by Wilcox.

LITERATURE CITED

Atwood, W. W., 1916, The physiographic conditions at Butte, Mont, and Bingham Canyon, Utah, when the copper ores in these districts were enriched: Econ. Geology, v. 11, no. 8, p. 697-740.

Barrell, Joseph, 1907, Geology of the Marysville mining district, Montana: U. S. Geol. Survey Prof. Paper 57, 178 p.

Colby, B. R., and Oilman, R. E., 1938, Gaging-station records in the Missouri River basin: U. S. Geol. Survey Water-Supply Paper 1077.

Douglass, Earl, 1902, Fossil mammalia of the White River beds of Montana: Am. Philos. Soc. Trans., new sen, v. 20, p. 237-279.

Fenneman, N. M., 1931, Physiography of western United States: New York, McGraw-Hill Book Co., Inc.

Gieseker, L. F., 1944, Soils of Broadwater County: Montana State Coll. Agr. Expt. Sta. Bull. 421, 58 p.

Haynes, W. P., 1916, The Lombard overthrust and related geological features: Jour. Geol ogy, v. 24, p. 269-290.

Knopf, Adolph, 1913, Ore deposits of the Helena mining region, Montana: U. S. Geol. Sur vey Bull. 527, 143 p.

Long, W. F., and James, J. S., 1948, Survey report on Townsend drainage area: U. S. Dept. Agriculture Soil Conserv. Service Survey rept., 18 p.

Lyden, C. J., 1938, Gold placers of Montana: Montana Bur. Mines and Geology Mem. 26, p. 14-21.

Meinzer, 0. E., 1949, Hydrology: New York, Dover Publications, Inc., p. 452-453.Mertie, J. B., Fischer, R. P., and Hobbs, S. W., 1951, Geology of the Canyon Ferry quad

rangle, Montana: U. S. Geol. Survey Bull. 972, 96 p.Pardee, J. T., 1925, Geology and ground-water resources of Townsend Valley, Montana:

U. S. Geol. Survey Water-Supply Paper 539, 61 p. 1926, The Montana earthquake of June 27, 1925: U. S. Geol. Survey Prof.

Paper 147, p. 7-23.Pardee, J. T., and Schrader, F. C., 1933, Metalliferous deposits of the greater Helena

mining region, Montana: U. S. Geol. Survey Bull. 842, 318 p.

LITERATURE CITED 233

Peale, A. C., 1893, The Paleozoic section in the vicinity of Three Forks, Mont.: U. S. Geol. Survey Bull. 110, 56 p.

1896, Description of the Three Forks quadrangle, Montana: U. S. Geol. Sur vey Geol. Atlas, folio 24, 7 p.

Scott, H. W., 1936, The Montana earthquakes of 1935: Montana Bur. Mines and Geology Mem. 16, 47 p.

Stone, R. W., 1911, Geologic relation of ore deposits in the Elkhom Mountains, Montana: U. S. Geol. Survey Bull. 470-B, p. 75-98.

Thwaites, R. G., 1904, Original journals of the Lewis and Dark expedition, 1804-1806, v. 2: New York, Dodd, Mead, and Co.

United States Geol. Survey, 1911, Surface-water supply of the United States, pt. 6: U. S. Geol. Survey Water-Supply Paper 306.

Walcott, C. D., 1899, Pre-Cambrian fossiliferous formations: Geol. Soc. America Bull., v. 10, p. 199-244.

Weed, W. H., 1901, Geology and ore deposits of the Elkhora mining district, Jefferson County, Mont., with an appendix on the microscopic petrography of the district, by Joseph Barrell: U. S. Geol. Survey 22d ann. tept., p. 399-549.

Wilcox, L. V., 1948, The quality of water for irrigation use: U. S. Dept. Agriculture Tech. Bull. 962, 40 p.

Wilmarth, M. G., 1938, Lexicon of geologic names of the United States: U. S. Geol. Sur vey Bull. 896, 23% p.

Measurement of water level in observation wells


Table 4. Measurements of the wafer /eve/ in observation wells

[In feet below land-surface datum]

Date Water level Date Water

level Date Water level

A4-l-lba

June 29, 1949July 26Aug. 26Sept. 27

1.552.172.551.28

Oct. 21, 1949Dec. 7Mar. 7, 1950Apr. 5

0.96.87.80.85

May 10, 1950June 6July 10Aug. 7

0.751.31.21.42

A4-l-2ab

May 2. 1949June 24July 28Aug. 25Sept. 27Oct. 20

7.584.516.657.988.298.19

Dec. 6, 1949Jan. 10, 1950Feb. 7Mar. 7Apr. 5May 9

8.088.078.488.488.298.14

June 6, 1950July 10Aug. 7Sept. 11Oct. 9Nov. 15

1.815.566.657.777.807.50

A4-l-2bdl

June 30, 1949July 28Aug. 25Sept. 27Oct. 20Dec. 6

4.156.828.258.528.408.36

Jan. 10, 1950Feb. 7Mar. 7Apr. 5May 9June 6

8.398.728.768.729.256.97

July 10, 1950Aug. 7Sept. 11Oct. 9Nov. 15Dec. 13

5.967.087.917.988.538.50

A4-l-2ca3

May 2, 1949June 24July 29Aug. 25Sept. 27Oct. 20Dec. 6Jan. 10, 1950Feb. 7Mar. 7Apr. 5May 9June 6July 10Aug. 7Sept. 11Oct. 9

21.8018.5018.0119.1019.9220.4021.0621.3422.82

124.6023.9622.0420.7717.5818.2319.4119.80

Nov. 15, 1950Dec. 13Jan. 10, 1951Feb. 14Mar. 16Apr. 13May 11June 16July 18Aug. 15Sept. 19Oct. 8Nov. 19Dec. 17Jan. 16, 1952Feb. 14Mar. 17

20.3520.7321.0321.6421.5421.1321.7718.9218.6219.3320.3920.0820.5820.7521.2021.6421.54

Apr. 21, 1952May 20June 16July 14Aug. 13Sept. 18Oct. 21Nov. 21Dec. 19Jan. 22, 1953Feb. 19Mar. 19Apr. 20May 18June 18July 16

21.5220.2217.4417.1718.4419.5820.1720.4320.5620.7220.9021.0221.2121.4916.4216.31

A4-l-2cbl


8.109.71

10.8511.4511.6011.85


12.0012.3012.3912.3712.3610.74

July 10, 1950Aug. 7Sept. 11Oct. 9Nov. 15

8.539.49

10.7711.0711.35

^Pumping.

TABLE 4 237

Table 4; Measurements of the water level in observation wells Continued


levelDate Water

level

A4-l-10cb

May 2, 1949June 24July 29Aug. 25Sept. 27Oct. 20Dec. 6Jan. 10, 1950Feb. 7Mar. 7Apr. 5May 9June 6July 10Aug. 7Sept. 11

95.8095.5394.7894.6294.4594.5594.7094.6594.9295.0894.9695.1395.0395.6693.8993.50

Oct. 9, 1950Nov. 15Dec. 13Jan. 10. 1951Feb. 14Mar. 16Apr. 13May 11June 16July 18Aug. 15Sept. 19Oct. 8Nov. 19Dec. 17Feb. 14, 1952

93.5293.7994.1493.8194.0594.0193.9193.8794.2894.2694.0693.6993.8993.7293.8293.98

Mar. 17, 1952Apr. 21June 16July 14Aug. 13Sept. 18Oct. 21Nov. 21Dec. 19Jan. 22, 1953Feb. 19Mar. 19Apr. 20May 18June 18July 16

93.8993.9594.0094.3693.2893.0393.6692.9092.7792;8493.2292.8393.1293.2893.4293.14

A4-l-llab

May 2, 1949 June 24

16.50 9.50

July 27, 1949 Aug. 25

14.15 13.57

Sept. 27, 1949 14.51

A4-l-12bd

May 2, 1949June 24July 29Aug. 25Sept. 27Oct. 20

6.976.128.308.947.557.92


7.307.026.756.776.707.25


7.088.118.538.128.098.27

A4-l-13cc

Oct. 5, 1949 \ 35.00 7, 1949 37.01

A4-l-14cc


53.8053.7053.5553.0052.3352.61


51.8148.9450.2850.7552.0752.64

July 10. 1950Aug. 7Sept. 11Oct. 9Nov. 15

52.6953.4152.1451.7352.03

A4-2-5bb

Nov. 15, 1950Dec. 13Jan. 10, 1951Feb. 14Mar. 16Apr. 13May 11June 16July 18Aug. 15Sept. 19

4.764.574.464.554.392.642.033.744.885.365.20

Oct. 8, 1951Nov. 19Dec. 17Jan. 16, 1952Feb. 14Mar. 17Apr. 21May 21June 16July 14Aug. 13

4.994.644.584.754.414.252.542.233.874.464.86

Sept. 18, 1952Oct. 21Nov. 21Dec. 19Jan. 22, 1953Feb. 19Mar. 19Apr. 20May 18June 18July 16

5.365.114.484.544.244.113.713.693.743.854.86


Table 4. Measurements of the water level in observation wells Continued

Date Water level

Date Water level

Date Water level

A4-2-5bc

Aug. 29, 1949Sept. 29Oct. 21Dec. 7Jan. 10. 1950Feb. 7Mar. 7Apr. 5May 9June 6July 10Aug. 7Sept. 11Oct. 9Nov. 15Dec. 13

8.207.737.547.437.427.347.326.095.947.127.547.527.917.567.577.52

Jan. 10, 1951Feb. 14Mar. 16Apr. 13May 11June 16July 18Aug. 15Sept. 19Oct. 8Nov. 19Dec. 17Jan. 16, 1952Feb. 14Mar. 17Apr. 21

7.407.487.446.334.997.337.998.157.917.578.098.058.097.907.905.93

May 21, 1952June 16July 14Aug. 13Sept. 18Oct. 21Nov. 21Dec. 19Jan. 22, 1953Feb. 19Mar. 19Apr. 20May 18June 18July 16

5.507.967.088.498.488.207.687.807.707.687.527.367.687.878.41

A4-2-5bd

July 29, 1949Aug. 25Sept. 27Oct. 21Dec. 6Jan. 10, 1950

7.247.797.417.126.806.84

Feb. 7, 1950Mar. 7Apr. 5May 9June 6

6.906.485.895.386.16


7.017.447.477.276.78

A4-2-5cc

July 29, 1949Aug. 25Sept. 29Oct. 20Dec. 7Jan. 10, 1950Feb. 7Mar. 7Apr. 5May 9June 6July 10Aug. 7Sept. 11Oct. 9Nov. 15

22.5022.6022.7622.8522.9822.8022.8422.8822.8622.8322.7922.8022.7922.8222.9222.96

Dec. 13, 1950Jan. 10, 1951Feb. 14Mar. 16Apr. 13May 11June 16July 18Aug. 15Sept. 19Oct. 8Nov. 19Dec. 17Jan. 16, 1952Feb. 14Mar. 17

22.9722.9322.9222.9422.9122.6822.6722.6922.7822.8122.9122.9422.9222.9122.8622.95


22.7622.7322.5722.7622.8322.5322.6522.7422.7722.7522.8022.7222.7922.6522.6022.57

A4-2-6aa

Aug. 29, 1949Sept. 27Oct. 21Dec. 7Jan. 10, 1950

6.026.386.205.835.69


5.655.474.402.253.93

July 10, 1950Aug. 7Sept. 11Oct. 9

5.074.776.156.01

A4-2-6cc

Nov. 15, 1950Jan. 10, 1951Feb. 14Mar. 16Apr. 13May 11June 16July 18Aug. 15Sept. 19Oct. 8

5.063.934.023.812.743.194.585.516.016.335.18

Nov. 19, 1951Dec. 17Jan. 16, 1952Feb. 14Apr. 21May 21June 16July 14Aug. 13Sept. 18

4.764.314.362.702.242.024.284.485.405.10

Oct. 21, 1952Nov. 21Dec. 19Jan. 22, 1953Feb. 19Mar. 19Apr. 20May 18June 18July 16

4.904.193.863.373.543.413.543.964.195.37

TABLE 4 239

Table 4.-* 4feasuremenfs of the water level in observation wells Continued



A4-2-6cd

June 29, 1949July 29Aug. 25Sept. 27Oct. 20Dec. 7Jan. 10, 1950Feb. 7Mar. 7Apr. 5May 9June 6

7.157.407.577.207.006.947.006.946.766.586.598.13

July 10, 1950Aug. 7Sept. 11Oct. 9Nov. 15Dec. 13Jan. 10, 1951Feb. 14Mar. 16Apr. 13May 11

7.247.227.176.976.856.826.786.887.696.666.83

June 16, 1951July 18Aug. 15Sept. 19Oct. 8Nov. 19Dec. 17Feb. 14, 1952Mar. 17Apr. 21May 21

6.867.427.487.527.486.996.967.016.826.396.28

A4-2-8bb


32.5032.5232.5632.6632.6832.77

Dec. 7, 1949Jan. 10, 1950Feb. 7Mar. 7Apr. 5

32.8832.8532.8532.8533.76

May 9, 1950June 6July 10Aug. 7Sept. 11

33.7233.8333.7133.7533.77

A5-l-4cc

July 7, 1949Aug. 9

25Sept. 27Oct. 20Dec. 6Jan. 10, 1950Feb. 7Mar. 7Apr. 5May 9June 5July 10

11.2014.9519.4022.7823.8525.1022.2221.7014.7316.9019.975.197.74

Aug. 7, 1950Sept. 8Oct. 9Nov. 15Dec. 13Jan. 10, 1951Feb. 14Mar. 16Apr. 13May 11June 16July 18Aug. 15

10.2619.2422.5119.6517.5318.5319.5420.7112.9511.415.869.33

14.85

Sept. 19, 1951Oct. 8Nov. 19Dec. 17Jan. 16, 1952Feb. 14Mar. 17Apr. 21May 20June 16July 14Aug. 13Sept. 18

18.1216.1716.9018.4618.4514.6615.0616.006.407.708.43

13.4920.14

A5-l-8cd2


11.6013.9213.8614.5915.3116.3717.1717.5217.5315.9313.2410.9112.7713.1713.6614.87

Dec. 13, 1950Jan. 10, 1951Feb. 14Mar. 16Apr. 13May 11June 16July 18Aug. 15Sept. 19Oct. 8Nov. 19Dec. 17Feb. 14, 1952Mar. 17Apr. 21

15.5116.2317.5217.1317.4615.7112.5412.8413.8411.7113.8214.2115.9216.4118.1918.47


16.6914.9613.7014.2015.0816.0517.2417.1718.5318.6119.0818.8317.2115.0512.42





A5-l-10cb

July 6, 1949Aug. 9

25Sept. 27Oct. 20Dec. 6Jan. 10, 1950Feb. 7Mar. 7Apr. 5May 9June 5July 10Aug. 7Sept. 8

11.9115.8016.6017.2617.6018.3720.1019.6520.1820.6421.0420.6016.4916.2617.13

Oct. 9, 1950Nov. 15Dec. 13Jan. 10, 1951Feb. 14Mar. 16Apr. 13May 11June 16July 18Aug. 15Sept. 19Oct. 8Nov. 19Dec. 17

17.6818.2718.7319.1919.7920.3820.6619.8911.7913.8416.1017.1017.4217.8618.00

Jan. 16, 1952Feb. 14Apr. 21May 20June 16July 14Aug. 13Sept. 18Oct. 21Nov. 21Dec. 19Jan. 22, 1953Feb. 19Mar. 19Apr. 20

18.2719.1417.895.837.19

13.4515.2017.0317.6117.9018.5018.9819.2119.8219.90

A5-l-llcd

July 7, 1949Aug. 9

25Sept. 27Oct. 20Dec. 6

5.856.106.176.286.306.80


6.576.726.85

18.60iS.SS6.34


3.455.956.226.358.72

A5-l-22bb

July 6, 1949Aug. 9


4.758.139.94

12.9215.0018.95

Jan. 10, 1950Feb. 7Mar. 7Apr. 5June 5

21.8323.8225.2526.2016.26


9.367.71

10.4411.9814.48

A5-l-23bd


2.372.002.251.921.751.582.273.804.905.005.406.646.575.836.215.895.02

Nov. 15, 1950Dec. 13Jan. 10. 1951Feb. 14Mar. 16Apr. 13May 11June 16July 18Aug. 15Sept. 19Oct. 8Nov. 19Dec. 17Jan. 16, 1952Feb. 14Mar. 17

4.454.314.835.555.936.595.135.425.535.214.103.643.073.293.804.235.00


4.643.323.943.342.762.081.811.822.593.824.825.665.778.042.524.91

1Pumping.

TABLE 4 241


Date Water level Date

Water level Date

Water level

A5-l-23ccl

June 29, 1949July 28Aug. 25Sept. 27Oct. 20Dec. 6Jan. 10, 1950Feb. 7Mar. 7Apr. 5May 9June 6July 10Aug. 7Sept. 11Oct. 9Nov. 15

2.953.834.636.586.197.409.15

10.4211.3011.6813.029.093.895.677.257.147.58


7.828.78

10.4610.5711.237.674.114.426.147.327.107.018.169.419.83

11.51


10.064.501.501.844.955.815.908.598.73

10.0010.5910.8610.9612.522.522.97

A5-l-24db


1.482.232.872.702.462.05


2.663.132.562.132.753.45


3.051.253.903.733.49

A5-l-26ac2

June 29, 1949July 25Aug. 25Sept. 27Oct. 20

3.454.124.304.264.14


4.585.125.525.755.70


5.895.113.754.11

A5-l-26cd


8.515.066.897.567.757.708.038.508.848.898.989.058.266.485.767.477.64

Nov. 15, 1950Dec. 13Jan. 10, 1951Feb. 14Mar. 16Apr. 13May 11June 16July 18Aug. 15Sept. 19Oct. 8Nov. 20Dec. 17Jan. 16, 1952Feb. 14Mar. 17

7.838.048.268.648.918.868.755.395.587.047.489.007.537.888.368.508.78


8.617.645.533.246.477.267.347.577.718.278.538.608.529.105.324.79

A5-l-34aa


13.3015.7716.5116.6617.2417.72


18.1318.4718.6218.9817,44


14.4513.7115.7216.2816.81


Table 4. Measurements of the water level in observation wells -Continued


level Date 1 Water | level

A5-l-35ca

May 2, 1949 June 24

8.40 6.35

July 28, 1949 Aug. 25

6.78 8.02

Oct. 6, 1949 17.04

A5-l-35cd

June 30, 1949July 28Aug. 25Sept. 27Oct. 20Dec. 6Jan. 10, 1950Feb. 7Mar. 7Apr. 5May 9June 6July 10Aug. 7Oct. 9Nov. 15

4.495.937.457.347.026.706.967.426.926.606.477.074.926.246.586.41


6.356.507.017.016.126.061.895.617.206.886.646.195.946.946.746.56


5.786.024.874.205.487.016.716.136.406.006.165.996.136.775.315.91

A5-l-36ad

Aug. 29, 1949 Sept. 27 Oct. 21

4.38 4.12 3.92

Dec. 7, 1949 June 6, 1950

3.183.76

July 10, 1950 Aug. 7

3.94 4.06

A5-l-36cc


0.42.31.31.35.30.37.11

1.192.362.651.17

Oct. 8, 1951Nov. 19Dec. 17Jan. 16, 1952Feb. 14Mar. 17Apr. 21June 16July 14Aug. 13Sept. 18

0.45.49.45.45.45.20.57

1.562.122.561.97


0.99.49.55.55.55.31.56.76

1.482.80

A5-l-36dc


3.983.423.573.673.631.942.133.135.306.075.36


4.893.983.834.043.472.731.983.654.414.725.60


5.014.234.292.822.782.462.832.913.345.32

TABLE 4 243




A5-l-36dd

Aug. 29, 1949Sept. 27Oct. 21Dec. 7Mar. 7, 1950Apr. 5May 9June 6July 10Aug. 7Sept. 11Oct. 9

2.481.861.40.66.40.15

+.02.08

1.151.96.66.62

Nov. 15, 1950Dec. 13Apr. 13, 1951May 11June 16July 18Aug. 15Sept. 19Oct. 8Nov. 19Apr. 21, 1952June 16

0.53.34.46.31.49.80

1.31.97

1.28.98.51.40

July 14, 1952Aug. 13Sept. 18Oct. 21Nov. 21Dec. 19Jan. 22, 1953Mar. 19Apr. 20May 18June 18July 16

0.51.83

1.111.16.98

1.10.60.37.33.30.26.57

A5-2-8bd


15.0814.5015.3915.2615.2715.64


15.8316.0015.8415.9214.3614.91


15.5815.1615.7915.8715.34

A5-2-8cc

June 27, 1949July 29Aug. 25Sept. 27Oct. 20Dec. 6Jan. 10, 1950Feb. 7Mar. 7Apr. 5May 9June 5

16.4116.0516.9417.2117.3417.7417.9818.2018.3218.2816.8617.03


16.8516.7516.8217.6717.9918.1818.4718.5618.9818.7019.01

June 16, 1951July 18Aug. 15Sept. 19Oct. 8Nov. 19Dec. 19Jan. 16, 1952Feb. 14Mar. 17Apr. 21

16.4016.9216.5117.1517.6117.9318.3218.3918.4318.3617.91

A5-2-10ad

July 7, 1949July 29Aug. 26Sept. 29Oct. 24Dec. 7Jan. 11, 1950Feb. 8Mar. 8Apr. 6May 10June 6July 11Aug. 8Sept. 12Oct. 10Nov. 15

40.9239.6240.1040.7341.6643.5244.0943.3643.8244.6745.1144.0041.5640.4440.3241.0542.48


43.2244.0944.7945.2445.0345.2543.0241.2439.6340.7641.5942.9743.8244.2344.4843.92


46.3243.7941.6541.1940.2540.7141.6242.3642.8143.8944.5545.0745.2145.6343.0741.04


Table 4, < Measurements of the water level in observation wells Continued


levelDate Water

level

A5-2-14dd

Apr. 30, 1949June 24July 25Aug. 1

26Sept. 29Oct. 24Dec. 7Jan. 11, 1950Feb. 8Mar. 8Apr. 6May 10June 6July 11Aug. 8Sept. 12

68.4064.8463.0062.9062.7363.5564.6966.3767.4267.7568.2768.8068.8867.5365.1063.3663.35

Oct. 10, 1950Nov. 15Dec. 13Jan. 10, 1951Feb. 14Mar. 16Apr. 13May 11June 15July 18Aug. 15Sept. 19Oct. 8Nov. 19Dec. 17Feb. 14, 1952Mar. 17

64.2466.1766.5167.5168.4469.0369.2369.0766.9163.8861.9262.8764.4166.0967.0567.4169.08


69.1867.8465.4665.2062.4062.2362.8165.6666.4267.4267.8968.7368.9170.1467.8864.48

A5-2-15dal

July 7, 1949Aug. 9


10.4310.5710.8611.1611.5712.70


11.8313.2813.9814.2913.37


10.3310.3910.9111.3812.22

A5-2-16db


6.958.409.658.71

Oct. 20, 1949Dec. 6Jan. 10, 1950

9.149.629.48

Feb. 7, 1950Mar. 7Apr. 5

6.358.659.67

A5-2-19adl


3.873.965.285.785.865.50


4.775.385.785.334-.744.82


4.804.664.985.705.635.36

A5-2-20bcl

June 27, 1949July 28Aug. 25Sept. 27Oct. 20Dec. 6Jan. 10, 1950Feb. 7Mar. 7Apr. 5May 9June 5July 10Aug. 7Sept. 8Oct. 9

4.365.165.535.525.224.735.215.544.734.754.604.924.734.935.435.23

Nov. 15, 1950Dec. 13Jan. 10, 1951Feb. 14Mar. 16Apr. 13May 11June 16July 18Aug. 15Sept. 19Oct. 8Nov. 19Dec. 17Mar. 17, 1952Apr. 21

5.045.095.125.275.134.704.614.294.835.305.265.124.945.145.204.25


3.744.564.795.085.355.054.744.984.815.024.835.015.163.454.78

TABLE 4 245


Date Water II level || Date Water II

level || Date Water level

A5-2-20dbl

May 2, 1949June 24July 28Aug. 25Sept. 27Oct. 20Dec. 6Jan. 10, 1950Feb. 7Mar. 7Apr. 5May 9June 5July 10Aug. 7Sept. 8

3.773.844.444.554.584.424.404.364.734.504.003.874.164.074.174.46

Oct. 9, 1950Nov. 15Dec. 13Jan. 10, 1951Feb. 14Mar. 16Apr. 13May 11June 16July 18Aug. 15Sept. 19Oct. 8Nov. 19Dec. 17Mar. 17, 1952

4.254.324.314.334.574.423.753.693.444.124.094.053.994.244.354.40

Apr. 21. 1952May 20June 16July 14Aug. 13Sept. 18Oct. 21Nov. 21Dec. 19Jan. 22, 1953Feb. 19Mar. 19Apr. 20May 19June 18July 16

3.623.073.974.044.124.303.924.124.444.054.113.783.814.264.023.96

A5-2-21ad

May 2, 1949 June 24

13.04 8.00

July 27, 1949 Aug. 25

8.05 10.29

Sept. 27, 1949 Oct. 20

10.16 11.77

A5-2-21bc


4.203.111.903.523.203.86


4.454.774.904.734.63


3.883.751.382.633.68

A5-2-21bd


7.047.137.447.898.077.276.734.794.683.875.90


6.446.937.187.587.667.946.936.124.604.944.79


6.306.647.087.177.547.707.817.935.205.145.87

A5-2-22ad

May 2, 1949 June 24

20.63 17.60

July 28, 1949 Aug. 25

19.20 20.47

Sept. 27, 1949 Oct. 20

19.10 19.70

A5-2-23ca3

June 30, 1949 July 25 Aug. 1 Sept. 29 Oct. 24 Dec. 7

17.30 17.10 17.00 18.15 18.93 20.14

Jan. 11, 1950 Feb. 8 Mar. 8 Apr. 6 May 10 June 6

21.23 21.50 21.84 20.51 20.16 17.67

July 11, 1950 Aug. 8 Sept. 12 Oct. 10 Nov. 15 Dec. 13

16.05 15.33 15.90 16.94 18.06 18.71


Table 4. Measurements of the water level in observation wells- Continued



A5-2-23ca3 Continued

Jan. 10, 1951Feb. 14Mar. 16Apr. 13May 11June 15July 18Aug. 15Sept. 19Oct. 8Nov. 19

19.5920.4220.9420.0319.4617.0215.6314.6616.5617.1818.35

Dec. 17, 1951Jan. 16, 1952Feb. 14Mar. 17Apr. 21May 20June 16July 14Aug. 13Sept. 18

19.2420.1220.6821.0220.2117.5215.5415.8013.3215.96


17.1118.0418.8419.3920.0720.5220.9618.7816.3015.70

A5-2-23ca6


16.6617.1217.8017.9218.2218.73


19.4319.2219.5719.6519.7218.01


16.0116.4817.8917.7717.80

A5-2-23dcl

July 1, 1949Aug. 1Sept. 29Oct. 24Jan. 11, 1950

30.6530.2532.2427.7534.85


35.3735.6335.8934.6832.13


33.3031.4331.2632.2233.34

A5-2-26ac

July 1, 1949 Aug. 25

17.20 18.16

Sept. 29, 1949 Oct. 24

18.76 19.24

Dec. 7, 1949 19.77

A5-2-26ca3


8.759.00

10.0510.6211.1412.41


13.0413.0012.7512.808.80


7.518.819.42

10.0110.84

A5-2-27bb2


1.542.363.153.954.452.413.231.59+.18.23

+.18

Oct. 8, 1951Nov. 19Dec. 17Feb. 14, 1952Mar. 17Apr. 21June 16July 14Aug. 13Sept. 18

0.311.672.523.804.433.831.12.11

+.74+.06


0.691.412.102.783.373.623.711.861.201.04

TABLE 4 247




A5-2-27bb4


4.615.185.766.647.025.035.944.683.633.412.34

Oct. 8, 1951Nov. 19Dec. 17Feb. 14, 1952Mar. 19Apr. 21June 16July 14Aug. 13Sept. 18

3.124.435.186.276.585.853.983.131.332.87


3.564.364.975.455.886.166.374.794.113.31

A5-2-27bc

Aug. 29, 1949 Sept. 29

0.40 .65

Oct. 21, 1949 1.25 Dec. 7, 1949 2.55

A5-2-29bc


7.638.609.009.158.908.58


8.478.588.658.308.27


8.306.728.537.868.81

A5-2-29cc

May 3, 1949 June 24 July 29

6.57 6.30 7.40

Aug. 25, 1949 Sept. 29 Oct. 21

6.96 6.94 6.85

Dec. 7, 1949 Jan. 10, 1950 Feb. 7

6.76 6.91 7.12

A5-2-29cc2


3.873.893.864.204.093.072.362.731.832.932.29


3.603.653.874.414.283.912.382.27.53

3.643.83


2.854.264.284.374.133.863.763.73.80.01

3.25

A5-2-29dd


6.586.867.107.697.926.616.591.154.434.505.69


5.846.446.837.407.747.906.653.793.674.055.32


6.066.216.642.442.373.463.616.694.133.32

394090 O - 56 - 6


Table 4.-* Measurements of the wafer level in observation wells Continued



A5-2-31cd


6.106.727.006.605,265.49


5.624.631.781.634.09


5.365.895.766.176.53

A5-2-31da

Nov. 15, 1950Dec. 13Jan, 10, 1951Feb. 14Mar. 16Apr. 13May 11June 16July 18Aug. 15Sept. 19

3.363,343.133.403,321.87.93

2.574.104.294.61


4.163.543.353.623.392.82.98.89

2.703.553.93


4.864.964.084.213.373.122.702.652.512.514.29

A5-2-32aa

Aug. 29, 1949Sept. 29Oct. 21Dec. 7

6,656.436.487.15

Jan. 10, 1950Feb. 8Mar. 7Apr. 5

DryDryDryDry


5.783.744.724.99

A5-2-32ab

Aug. 29. 1949} 3.86 I) Sept. 29. 1949 I 3.40

A5-2-32cd

Nov. 15, 1950Dec. 13Jan. 10, 1951Feb. 14Mar. 16Apr. 13May 11June 16July 18Sept. 19Oct. 8

4.323.883.714.103.811.921.963.254.564.954.60

Nov, 19, 1951Dec. 17Jan. 16, 1952Feb. 14Mar. 17Apr. 21June 16July 14Aug. 13Sept, 18

3.873.814.463.673.442.023.464.114.515.38


5.044.684.303.793.322.742.953.003.044.86

A5-2-32dc

Aug. 29, 1949Sept. 29Oct. 21Dec. 7

5.705.385.134.72

Jan. 10, 1950Feb. 8Mar. 7Apr. 5

4.935.264.383.05


2.153.404.314.99

A5-2-32ddl


10.5810.8412.1512.5212.3212.29

Dec. 7. 1949Jan. 10, 1950Feb. 8Mar. 7Apr. 5

12.1412.4012.9212.2011.62


11.0411.601J..9611.3411.74

TABLE 4 249


Date Water II level || Date Water


A5-2-32dd2

Nov. 15, 1950Dec. 13Jan. 10, 1951Feb. 14Mar. 16Apr. 13May 11June 16July 18Sept. 19Oct. 8

2.362.812.943.323.311.812.062.392.993.012.89

Nov. 19, 1951Dec. 17Jan. 16, 1952Feb. 14Mar. 17Apr. 21June 16July 14Aug. 13Sept. 18

2.642.823.372.972.971.732.372.613.033.29


3.123.023.022.802.582.212.452.522.223-.04

A5-2-33bbl

July 11, 194929

Aug. 25Sept. 29Oct. 21Dec. 7Jan. 10, 1950Feb. 8Mar. 7Apr. 5May 10June 6July 11Aug. 7Sept. 12Oct. 9

14.3214.6914.8913.7615.0615.2415.9717.2617.4217.3214.0914.8214.1013.2113.5813.73

Nov. 15, 1950Dec. 13Jan. 10, 1951Feb. 14Mar. 16Apr. 13May 11June 16July 18Aug. 15Sept. 19Oct. 8Nov. 19Dec. 17Feb. 14, 1952Mar. 17

15.3115.8216.0716.7117.0315.5316.0112.6812.7812.0413.1114.5515.4415.7916.5716.97

Apr. 21, 1952June 16July 14Aug. 13Sept. 18Oct. 21Nov. 21Dec. 19Jan. 22, 1953Feb. 19Mar. 19Apr. 20May 18June 18July 16

16.0715.8915.4113.6611.5414.1614.6815.4215.8916.0816.2816.3317.2415.4313.38

A5-2-33cb

June 16, 1951July 18Aug. 15Sept. 19Oct. 8Nov. 19Dec. 17Jan. 16, 1952

7.329.61

10.2111.0711.6912.4612.4113.51

Feb. 15, 1952Apr. 21June 16July 14Aug. 13Sept. 18Oct. 21Nov. 21

13.7912.5410.549.718.629.60

11.7512.20

Dec. 19, 1952Jan. 22, 1953Feb. 19Mar. 19Apr. 20May 18June 18July 16

12.7212.9113.0013.1013.2111.2010.197.81

A6-2-4ac

Aug. 8, 1949Sept. 29Oct. 25Dec. 12Jan. 11, 1950Feb. 11Mar. 8Apr. 6May 17

0.90.67.98

1.311.531.801.621.32Dry

July 11, 1950Aug. 8Sept. 12Oct. 10Nov. 16Dec. 11Jan. 8, 1951Feb. 12Mar. 14

1.10.87.66.80.72

1.03.99.99

1.42

Apr. 11, 1951May 9June 16July 18Aug. 15Sept. 19Oct. 8Nov. 20Dec. 17

0.26.29.78.53.62

+.301.05DryDry

A6-2-4cdl

Aug. 9, 1949Sept. 29Oct. 25Dec, 12Jan. 11, 1950Feb. 11

1.844.935.386.346.556.71

Mar. 8, 1950Apr. 6May 17June 9July 11Aug. 8

6.676.606.523.712.183.67

Sept. 12, 1950Oct. 10Nov. 16Dec. 11Jan. 8, 1951Feb. 12

3.794.444.565.345.695.87





A6-2-4cdl Continued

Mar. 14, 1951Apr. 11May 9June 16July 18Aug. 15Sept. 19Oct. 8Nov. 20Dec. 17Jan. 16, 1952

5.736.095.323.672.433.915.376.207.267.637.42

Feb. 14, 1952Apr. 21May 20June 16July 14Aug. 14Sept. 18Oct. 22Nov. 21Dec. 17

7.618.247.427.535.074.995.306.106.806.91

Jan. 23, 1953Feb. 19Mar. 19Apr. 21May 18July 6Aug. 7Sept. 9Oct. 8Nov. 10

7.627.728.268.287.495.66.15.45.26.2

A6-2-4db

Aug. 9, 1949Sept. 29Oct. 25Dec. 12Jan. 11, 1950Feb. 11Mar. 8Apr. 6May 17June 9July 11Aug. 8Sept. 12Oct. 10Nov. 16

0.00.22.36.98

1.071.201.06.93.28.93

+.27.01.04.86.98

Dec. 11, 1950Jan. 8, 1951Feb. 12Mar. 14Apr. 11May 9June 16July 18Aug. 15Sept. 19Oct. 8Nov. 20Dec. 17Jan. 16, 1952Feb. 14

1.031.001.301.15Dry

1.35.35

+.19.07

1.001.091.341.811.691.79

Mar. 17, 1952Apr. 21May 20June 16July 14Aug. 14Sept. 18July 6, 1953Aug. 7Sept. 9Oct. 8Nov. 10Dec. 10Jan. 7, 1954Feb. 2

DryDryDryDry

1.781.871.531.48.98.68

1.882.93.13.74.2

A6-2-5bbl

Aug. 9, 1949Oct. 25Jan. 11, 1950Feb. 8

1.704.20DryDry

Mar. 8, 1950Apr. 6May 17June 9

DryDry

3.723.91

July 11, 1950Sept. 11Oct. 10

3.123.924.09

A6-2-5bb2

Aug. 9, 1949Sept. 29Oct. 25Dec. 12Jan. 11, 1950Feb. 8Mar. 8Apr. 6May 17June 9July 11Aug. 8Sept. 12Oct. 10Nov. 16Dec. 11

5,005.926.05DryDryDryDry

5.705.475.735.355.395.906.046.296.34

Jan. 8, 1951Feb. 12Mar. 14Apr. 11May 9June 16July 18Aug. 15Sept. 19Oct. 8Nov. 19Dec. 17Jan. 16, 1952Feb. 14Apr. 21

6.406.626.576.065.455.755.015.125.856.116.356.376.576.615.72


6.005.765.235.546.456.536.58DryDryDryDryDry

4.994.445.03

A6-2-5bb3

Aug. Sept. Oct. Dec.

9, 1949292512

3.734.284.334.62

Jan. 11, 1950Mar. 8Apr. 6May 17

4.954.594.273.84

June July Aug. Sept.

9, 195011

812

4.104.043.724.19

TABLE 4 251




A6-2-5bb3 Continued.


4.404.524.584.655.114.814.293.744.073.393.73

Sept. 19, 1951Oct. 8Nov. 19Dec. 17Apr. 21, 1952May 20June 17July 15Aug. 13Sept. 18

4.184.464.745.013.974.264.033.863.894.71


5.085.245.365.545.415.465.423.582.823.31

A6-2-5cc

Aug. 3, 194925

Sept. 30Oct. 24Dec. 7Jan. 11, 1950

2.843.243.673.673.983.97


3.993.303.103.262.39


2.532.683.303.893.75

A6-2-8abl


6.557.808.408.699.419.96

10.459.649.439.357.365.607.347.527.788.90


9.179.237.87

10.339.548.325.737.166.608.489.009.09

10.4811.0510.9810.91


9.648.985.955.726.349.029.519.499.59

10.3010.4210.7011.138.937.368.09

A6-2-8ba

Aug. 8, 1949Sept. 29Oct. 26Dec. 12Jan. 11, 1950Feb. 8Mar. 8Apr. 6May 17June 9July 11Aug. 8Sept. 12Oct. 10Nov. 16Dec. 11Jan. 8, 1951Feb. 12

1.681.942.272.542.803.152.832.272.521.411.221.491.741.971.992.092.442.81

Mar. 14, 1951Apr. 11May 9June 16July 18Aug. 15Sept. 19Oct. 8Nov. 19Dec. 17Feb. 14, 1952Mar. 17Apr. 21May 20June 17July 15Aug. 13

2.201.881.581.041.511.061.792.152.581.733.123.012.211.941.411.801.30

Sept. 18, 1952Oct. 22Nov. 21Dec. 19Jan. 23, 1953Feb. 19Mar. 21Apr. 21May 20July 6Aug. 7Sept. 9Oct. 8Nov. 10Dec. 10Jan. 7, 1954Feb. 2

2.402.582.452.622.622.612.692.832.023.53.81.61.62.02.33.14.5





A6-2-8db


4.124.765.305.345.686.05


6.355.865.795.753.51


3.493.954.794.894.69

A6-2-9ba3

Aug. 8, 1949Sept. 29Oct. 25Dec. 12Jan. 11, 1950 Feb. 11Mar. 8Apr, 6May 17June 9

2.976.035.05DryDry DryDryDryDry

2.60

July 11, 1950Aug. 8Sept. 12Oct. 11Nov. 16 Dec. 11Jan. 8, 1951Feb. 12Mar. 14

0.462.513.905.395.65 6.907.077.116.99

Apr. 11, 1951May 9June 16July 18Aug. 15 Sept. 19Oct. 8Nov. 19Dec. 17

DryDry

2.261.232.50

26.46DryDryDry

A6-2-9bbl

Aug. 8, 1949Sept. 29Oct. 25Dec. 12May 17, 1950

7.10DryDryDryDry


Dry2.054.094.40

Dec. 11, 1950June 16, 1951July 18Aug. 15

5.9.22.761.843.63

A6-2-9bb2

Aug. 8, 1949Sept. 29Oct. 25Dec. 12

7.228.459.02

10.00

Apr. 6, 1950May 17June 9

10.3210.157.14

July 11, 1950Aug. 8Sept. 12

4.985.897.69

A6-2-9dd


16.8519,9522.0224.3527.4028,10


28.2828.1029.1525.8418.63


11.1415.1815.9619.9421.56

A6-2-16aa

July 14, 1949Aug. 9

29Sept. 29Oct. 24Dec. 7Jan. 11, 1950Feb. 8Mar. 8Apr. 6May 10June 9

15,6216.2517.8219.7221,6424.3325.3025.5026.0127,0126.4621,92

July 11, 1950Aug. 8Sept. 12Oct. 10Nov. 16Dec. 13Jan. 10, 1951Feb. 14Mar. 16Apr. 11May 9June 15

15.8514.5714.4618.2221.2322.3423.1723.7723.2926.4926.0317.91


15.0613.9314.0719.3522.8724.4224.8825.0926.6527.0523.6217.76

&Drain ditch installed nearby.

TABLE 4 253


Date Water II level II Date Water It


A6-2-16aa Continued

JulyAug.Sept.Oct.Nov.

14, 195213182121

16.0314.3714.7616.5321.06 |

Dec.Jan.Feb.Mar.

19,23,1919

19521953

23.1823.9824.0925.98

Apr.MayJuneJuly

20, 1953191816

26.1026.6618.4014.46

A6-2-16db

July 14. 1949Aug. 29Sept. 29Oct. 24Dec. 7Jan. 11, 1950Feb. 8

10.1510.6511.6012.3813.5613.7914.36

Mar. 8, 1950Apr. 6May 10June 9July 11Aug. 8Sept. 12

14.5414.9514.9112.059.949.198.05

Oct. 10. 1950Nov. 16Dec. 13Jan. 10, 1951Feb. 14Mar. 16

11.0712.5112.9913.8314.2914.73

A6-2-22ab

JulyAug.Sept.Oct.Dec.Jan.

13, 1949292924

711, 1950

19.4022.9427.0028.6331.1733.56

Feb.Mar.Apr.MayJune

8, 195086

109

34.2234.5436.4536.9831.25

JulyAug.Sept.Oct.Nov.

11, 19508

121016

21.6418.4623.3827.4830.24

A6-2-22bbl

July 13, 1949Aug. 9

26Sept. 29Oct. 24Dec. 7Jan. 11. 1950

23.1521.9522.5024.2425.7727.7428.62

Feb. 8, 1950Mar. 8Apr. 6May 10June 9July 11Aug. 8

28.9929.3229.9330.2829.0124.6320.85

Sept. 12, 1950Oct. 10Nov. 16Dec. 13Jan. 10, 1951Feb. 14Mar. 16

20.6623.9726.8827.3128.1828.8929.39

A6-2-27bbl

July 13, 1949Aug. 26Sept. 29Oct. 24

10.6411.1811.4012.24

Dec. 7, 1949Jan. 11, 1950Feb. 8Mar. 8

12.7612.0912.4213.20

Apr. 6, 1950May 10June 6

13.5313.9912.49

A6-2-27cc

JulyAug.

12, 26

1949 22.54 | 22.80 | [ Sept.

Oct.29, 23

1949 22.88 24.14

Dec. Jan.

7, 11,

1949 1950

23.96 22.66

A6r.2-34adl

July 12, 1949Aug. 26Sept. 29Oct. 24Dec. 7Jan. 11, 1950Feb. 8Mar. 8Apr. 6May 10June 6

42.8542.5543.3444.2546.0046.8946.5147.2948.0348.2246.07


42.9341.9141.6443.3945.1846.4747.3048.2148.9348.7147.68

June i!5, 1951July 18Aug. 15Sept. 19Oct. 8Nov. 19Dec. 17Jan. 16, 1952Feb. 14Mar. 17Apr. 21

44.3643.4742.0143.2344.4545.6346.7946.3547.6048.1848.42



Date Water || level || Date Water II

level I] Date Water level

A6-2-34cd

Apr. 30, 1949June 24July 29Aug. 26Sept. 29Oct. 24

6.825.706.124.556.636.61

Dec. 7, 1949Mar. 8, 1950Apr. 6May 10June 6

7.558.199.649.435.71


4.193.935.626.297.09

A6-2-34dc

Apr. 30, 1949June 30July 28Aug. 29Sept. 29Oct. 24Dec. 7Jan. 11, 1950

39.5035.8636.4536.2537.0837.6438.9139.64

Feb. 8, 1950Mar. 8Apr. 6May 10June 6July 11Aug. 8Sept. 12

38.6539,6840.4240.6738.7736.1935.7236.32

Oct. 10, 1950Nov. 15Dec. 13Jan. 10, 1951Feb. 14Mar. 16Apr. 13May 9

37.1738.5639.2939.9240.2441.1140.9140.51

A6-2-34dd

Apr.JuneJuly

29, 19492929

55.3051.2551.12

Aug.Sept.

26, 194926

51.0252.00

Oct.Dec.

24, 19497

52.7654.09

A7-l-24ddl

Mar. 19, 1952Apr. 22May 20June 16July 14Aug. 14

4.784.792.112.623.635.42

Sept. 18, 1952Oct. 22Nov. 22Dec. 17Jan. 22, 1953Feb. 19

6.056.186.076.196,266.42

Mar. 19, 1953Apr. 21May 19June 18July 16

6.516.716.632.084.50

A7-l-24dd2

Aug. 3, 194925

Sept. 30Oct. 24Dec. 7Jan. 11, 1950Feb. 8Mar. 8Apr. 6May 10

5.306.006.126.006.054.733.303.875.145.38

June 9, 1950July 11Aug. 8Sept. 12Oct. 10Nov. 13Dec. 11Jan. 8, 1951Feb. 12Mar. 14

2.383.054.835.795.675.725.915.985.454.94

Apr, 11, 1951May 9June 16July 18Aug. 15Sept. 19Oct. 8Nov. 19Dec. 17

4.884.692.544.555.696.056.126.086.28

A7-l-25ad

Sept. 30, 1949 15.30 1 Oct. 24, 1949 15.81 Dec. 7, 1949 16.38

A7-2-4aa

Aug.Sept.Oct.Nov.Dec.Jan.Feb.Mar.

9, 19507

1114129, 1951

1315

15.4217.4217.7017.5717.5815.9217.5017.61

Apr.MayJuneJulyAug.Sept.Oct.Nov.

12, 19511016181620

920

17.6517.5717.4914.7113.3615.8117.5317.17

Dec.Jan.Feb.Mar.Apr.MayJuneJuly

18, 195118, 1952151922211715

17.5217.3817.4817.3017.2717.3016.3917.63

TABLE 4 255


Date Water II level II Date Water II

level | Date Water level

A7-2-4aa Continued

Aug. 14, 1952Sept. 19Oct. 21Nov. 22

14.3117.2917.4817.60

Dec. 17, 1952Jan. 23, 1953Feb. 20Mar. 19

17.8517.8617.8117.83

Apr. 20, 1953May 21June 19July 17

17.7817.2815.9615.99

A7-2-4bal

June 26, 1950July 18Aug. 9Sept. 7Oct. 11Nov. 14Dec. 12Jan. 8, 1951Feb. 12Mar. 14Apr. 11May 9June 16

9.979.87

10.2610.1513.6215.5216.6817.6518.2418.7618.7618.9716.33

July 18, 1951Aug. 15Sept. 21Oct. 9Nov. 19Dec. 18Jan. 17, 1952Feb. 15Mar. 19Apr. 22May 21June 17July 15

9.8411.2913.0014.0315.9917.1817.3917.0118.0518.1115.9713.8011.33

Aug. 13, 1952Sept. 19Oct. 22Nov. 22Dec. 17Jan. 23, 1953Feb. 20Mar. 21Apr. 20May 21June 18July 17

10.9312.7414.4215.8016.7517.8818.5719.2119.8517.1111.3310.36

A7-2-5abl

JuneJuly

19, 18

1950 3.35 1 3.61 | I Aug.

Sept.10,

71950 4.98 1

4.68 |Oct. 11. 1950 6.18

A7-2-5bdl

June 26, 1950July 18Aug. 10Sept. 7Oct. 11Nov. 14Dec. 11Jan. 8, 1951Feb. 12Mar. 14Apr. 11May 9

1.912.022.112.712.965.996.386.576.707.117.477.21


5.413.432.884.495.635.946.236.316.597.046.406.30

June 17, 1952July 15Aug. 13Oct. 21Nov. 22Dec. 17Jan. 23, 1953Feb. 20Mar. 21Apr. 20May 21June 18

5.994.482.245.156.006.326.607.028.108.406.504.09

A7-2-5dcl


3.021.794.244.165,677.067.948.688.418.789.289.28

June 16, 1951July 18Aug. 15Sept. 21Oct. 9Dec. 18Mar. 19, 1952Apr. 22May 21June 17July 15Aug. 13

7.593.891.465.566.228.397.757.517.936.794.382.14


5.546.587.298.208.869.48

10.0810.508.585.663.52


Table 4. Measurements of the water level in observation Tce//s Continued



A7-2-9ab

Aug. 9, 1950Sept. 5Oct. 11Nov. 14Dec. 12Jan. 9, 1951

13.0413.42

Dry13.4613.30

Dry

Feb. 13, 1951Mar. 15Apr. 12May 10June 16July 18

DryDryDryDry

13.6013.29

Aug. 15. 1951Sept. 20Oct. 9Nov. 20Dec. 18

13.2113.30

DryDryDry

A7-2-9ba3


9.069.229.259.249.219.219.159.199.219.189.559.15


9.309.289.238.969.249.309.289.319.249.267.067.15


8.639.189.229.539.329.469.369.329.299.206.219.10

A7-2-10bb


40.1535.2537.4331.3035.0436.7638.7940.1941.7542.2542.3243.0341.91


34.6732.4233.4034.5637.5839.3340.5441.2841.7241.9941.3139.6135.38


32.7132.7035.0837.4038.6440.5441.6242.5443.0640.9839.3634.40

A7-2-17aa


9.269.459.529.489.458.73


9.389.43DryDry9.109.40

Aug. 15, 1951Sept. 20Oct. 9Nov. 20Dec. 18

9.489.509.459.459.46

A7-2-l7ab3

May 22, 1950June 15July 12Aug. 9Sept. 7Oct. 11Nov. 13Dec. 11Jan. 8, 1951Feb. 12Mar. 14Apr. 11May 9

13.018.676.007.178.199.29

10.6411.7512.5011.7712.0812.7112.52


9.837.265.898.419.49

10.9412.1910.3411.2112.1811.7910.81

June 17, 1952July 15Aug. 13Sept. 19Oct. 21Nov. 22Dec. 17Feb. 20, 1953Mar. 19Apr. 20May 21June 18

9.616.826.388.119.66

10.9211.7212.9413.8314.1812.088.86

TABLE 4 257

Table 4.i Measurements of the water level in observation wells Continued

Date Water H level | Date Water 1

level 1 Date Water level

A7-2-17bd

Aug. 11, 1949Sept. 30Oct. 24Dec. 12Jan. 11, 1950Feb. 8Mar. 8Apr. 6

5.707.858.98

10.639.55

10.0610.8011.94

May 7, 1950June 15July 12Aug. 9Sept. 12Oct. 11Nov. 13

11.367.424.935.826.257.908.07

Dec. 11, 1950Jan. 8, 1951Feb. 12Mar. 14Apr. 11May 9June 16

10.5111.2410.4311.6211.3611.498.26

A7-2-17cd2


6.717.30

10.2011.9313.1313.9813.5313,5214.2714.529.387.09


5.769.49

10.7212.5013.7012.0312.4013.8413.5812.357.407.18


5.568.04

10.7812.5313.1714.1814.8215.2615.6512.48

6.936.87

A7-2-17dbl

Apr, June

29, 30

1949 10.04 1 8.10

July Aug.

14, 4

1949 6.96 1 6.68 §

Aug. 25, 1949 7.60

A7-2-17dc

Aug.Sept.Oct.Nov.Dec.Jan.

9, 19505

1113118, 1951

9.409.509.609.669.69Dry

Feb.Mar.Apr.MayJuneJuly

12, 19511411

91618

DryDryDryDry

9.199.32

Aug.Sept.Oct.Nov.Dec.

15, 195120

92018

7.489.599.509.459.60

A7-2-20ab3

Aug, 9, 1950Sept. 5Oct, 11Nov. 13Dec, 11Jan. 8, 1951

8.548,73

12.9415.2616,41

Pry

Feb. 12, 1951Mar. 14Ap. 11M*y 9June 16July 17

DryDryDryDry

12.888.53

Aug. 15, 1951Sept. 20Oct. 9Nov. 20Dec, 17

7.0311.7713.5915.81

Dry

A7-2-20ac


5.435.88

10.2312,4713.7915,02

Feb. 12, 1951Mar, 14Apr. 11May 9June 16July 18

14.9514.95

DryDry

8.845.74


4.849.29

10.8913.1014.49


Table 4. Measurements of the water level in observation weWs Continued

Date Water jl level || Date Water II


A7-2-20bcl


4.164.625.516.496.937.29


5.733.817.267.034.694.20


4.115.405.916.797.73

A7-2-20bc2

Aug.

Sept.Oct.Dec.

4, 194925302512

6.306.658.629.22

10.85

Jan.Feb.Mar.Apr.

11, 1950886

9.8210.3310.9511.96

MayJuneJulyAug.

17, 195016129

10.925.814.845.63

A7-2-20bd2


5.536.479.78

11.4212.4913.2312.7512.4113.2113.397.946.14

Aug. 15, 1951Sept. 20Oct. 9Nov. 20Dec. 17Jan. 17. 1952Feb. 15Mar. 19Apr. 22May 21June 17July 15

4.869.11

10.3211.8012.9411.3911.9212.9512.6712.436.206.12


6.906.58

10.2811.6112.4813.3513.8814.3014.4911.456.104.77

A7-2-20cb


7.468.19

11.1012.5813.5014.1813.6413.0113.8813.939.117.68


7.0610.4811.5712.8813.8212.2712.7114.6413.3412.998.197.73


6.958.78

11.4912.6513.4214.0914.5914.9515.1112.707.487.21

A7-2-21cc

Aug. 5, 1949 25

10.30 11.85

Sept. 30, 1949 16.24 Oct. 24, 1949 19.95

A7-2-29ab

Aug. 29, 1949Sept. 30Oct. 24June 15, 1950July 12Aug. 8Sept. 12Oct. 11

8.9911.21

Dry10.417.506.428.86Dry

Nov. 13, 1950Dec. 11Jan. 8, 1951Feb. 12Mar. 14Apr. 11May 9

DryDryDryDryDryDryDry

June 16, 1951July 18Aug. 15Sept. 19Oct. 8Nov. 19Dec. 17

10.737.016.23DryDryDryDry

TABLE 4 259

Table 4. -Measurements of the water level in observation wells Continued

Date Water level Date.'

Water level

A7-2-29bbl

Date Water level

Aug. 26, 1949^ 3.48|| Sept. 30,1949^ 3.98 [| Mar. 8. 1950 [ Dry

A7-2-29bb2


6.637.059.76

11.1711.9412.49


12.1311.4312.0812.288.566.15


6.309.15DryDryDry

A7-2-29cal

Aug. 4, 194925

Sept. 30Oct. 24Apr. 6, 1950May 10June 15July 12Aug. 8Sept. 12Oct. 11Nov. 13Dec. 11Jan. 8, 1951

6.937.109.10

11.5013.3513.65

8.315.646.087.06

10.5710.9312.4212.54

Feb. 12, 1951Mar. 14Apr. 11May 9June 16July 18Aug. 15Sept. 19Oct. 8Nov. 20Dec. 17Mar. 19, 1952Apr. 22May 21

14.2513.8913.7012.2612.434.016.33

10.0111.2512.5513.2713.7813.6913.30


9.625.044.918.64

10.4812.0213.0113.6913.7814.1014.8113.609.30

A7-2-30ac3

Aug. 4, 194925

Sept. 29Oct. 24Dec. 7Jan. 11, 1950

4.204.424.274.354.682.88


3.273.994.384.513.25


2.833.594.004.174.48

A7-2-30ac4

Sept. 30, 1949Oct. 25Dec. 7Jan. 11, 1950Feb. 8Mar. 8Apr. 6May 10June 9July 11Aug. 8Sept. 12Oct. 10Nov. 13Dec. 11Jan. 8, 1951

5.125.265.604.134.444.905.305.374.203.604.214.855.125.415.875.84

Feb. 12, 1951Mar. 14Apr. 11May 9June 16July 18Aug. 15Sept. 19Oct. 8Nov. 19Dec. 17Jan. 16, 1952Feb. 14Mar. 19Apr. 22

0.214.555.144.913.994.434.696.265.365.485.844.014.565.244.56


3.993.944.214.325.205.535.575.796.046.036.136.204.932.694.29





A7-2-30ac5

Aug. 8, 1950Sept. 5Oct. 10Nov. 13Dec. 11Jan. 8, 1951Feb. 12Mar. 14Apr. 11May 9June 16

2.683.163.333.563.464.04

.07

.753.333.172.21

July 18, 1951Aug. 15Sept. 19Oct. 9Nov. 19Dec. 17Apr. 22, 1952May 20June 16July 14Aug. 14

2.682.943.403.533.704.062.762.182.192.442.65


3.453.713.824.024.314.464.384.483.38

.712.51

A7-2-30ad2


3.974.307.428.529.119.449.348.808.999.084.522.67


4.087.037.888.649.168.188.389.128.948.486.243.85


1.966.447.768.589.109.609.82

10.0210.236.055.722.47

A7-2-30bd


3.554.143.373.483.633.591.91.36

2.532.472.20

July 18, 1951Aug. 15Sept. 19Oct. 9Nov. 19Dec. 17Apr. 22, 1952May 20June 16July 14Aug. 14

3.484.173.853.673.594.072.101.421.743.004.13


4.104.063.'813.813.984.224.214.353.84.91

3.32

A7-2-30cb


4.595.124.664.644.494.79

.662.963.303,443.384.52


5.184.984.884.684.892.742.153.343.232.492.794.01


4.945.205.074.864.894.925.075.085.254.751.314.22

TABLE 4 261




A7-2-30dcl

Aug. 9, 1949Sept. 30Oct. 25Feb. 8, 1950Mar. 8Apr. 6

3.123.504.041.373.464.06


2.982.211.661.813.564.28

Nov. 13, 1950Dec. 11Jan. 8, 1951Feb. 12Mar. 14Apr. 11

4.894.704.364.224.594.46

A7-2-30dc2


4.154.855.525.795.275.634.935.535.325.124.624.70


4.795.305.445.765.785.285.235.715.435.175.544.72


4.565.645.945.876.166.026.126.186.135.264.624.74

A7-2-31bb

Aug. 8, 1950Sept. 5Oct. 10Nov. 13Dec. 11Jan. 8, 1951Feb. 12Mar, 14Apr. 11May 9June 16July 18

4.054.234.504.414.294.231.282.973.043.363.814.20


4.224.414.454.494.553.764.033.833.253.063.924.38


4.924.714.684.664.774.864.914.664.804.363.734.25

A7-2-31bc


2.493.043.063.163.243.252.793.082.482.362.232.20


2.682.973.073.183.302.192.502.692.502.412.212.41


3.733.313.363.373.503.583.603.273.433.051.832.61

A7-2-31bdl

Aug. 3, 1949Sept. 30Oct. 25Dec. 12Mar. 8, 1950Apr. 6May 10June 9

6.707.047.207.287.037.157.026.52

July 11, 1950Aug. 8Sept. 12Oct. 10Nov. 13Jan. 8, 1951Feb. 12Mar. 14

5.836.437.057.307.467.607.356.68

Apr. 11, 1951May 9June 16July 18Aug. 15Sept. 19Oct. 8Nov. 19

7.116.856.196.506.727.167.337.58





A7 -2 -Slbdl Continued

Dec. 17, 1951Jan. 16, 1952Feb. 14Mar. 19Apr. 21May 20June 16

7.757.557.557.557.206.647.31

July 15, 1952Aug. 14Sept. 18Oct. 22Nov. 21Dec. 19Jan. 22, 1953

6.576.727.507.477.877.727.79


8.007.967.797.247.206.46

A7-2-31bd8

Aug. 3, 1949Sept. 30Oct. 25Dec. 12Jan. 11, 1950Feb. 8Mar. 8Apr. 6May 10June 9July 11Aug. 8Sept. 12Oct. 10Nov. 13

6.326.546.706.656.976.826.526.586.475.995.475.846.596.856.95

Mar. 14, 1951Apr. 17May 9June 16July 18Aug. 15Sept. 19Oct. 8Nov. 19Dec. 17Jan. 16, 1952Feb. 14Mar. 19Apr. 21May 20

6.826.756.435.936.006.106.706.836.937.136.366.646.716.636.31

June 16, 1952July 15Aug. 14Sept. 18Oct. 22Nov. 21Dec. 19Jan. 22, 1953Feb. 19Mar. 21Apr. 21May 19June 18July 16

5.966.136.146.987.077.157.377.507.547.467.396.715.915.99

A7-2-31cb

Aug. 3, 194925

Sept. 30Aug. 8, 1950Sept. 12Oct. 10Nov. 13

7.107.477.426.797.497.627.74


7.988.027.507.737.257.01


5.916.417.017.427.717.90

A7-2-31dd

Aug. 9, 1949Sept. 29Oct. 24Dec. 12Jan. 11, 1950Feb. 8Mar. 8Apr. 6May 17June 9July 11Aug. 8Sept. 12Oct. 10Nov. 13Dec. 11

2.553.803.833.803.933.853.703.693.583.933.853.883.723.903.973.96

Jan. 8, 1951Feb. 12Mar. 14Apr. 11May 9June 16July 18Aug. 15Sept. 19Oct. 8Nov. 19Dec. 17Jan. 16, 1952Feb. 14Mar. 19Apr. 21

3.983.973.953.883.733.713.653.553.463.563.563.603.583.643.72

.90


1.021.131.161.301.051.321.401.461.511.581.581.67

.751.781.82

A7-2-32ab

Aug. 9, 1949Sept. 29Oct. 25Dec. 12Jan. 11, 1950

4.126.007.027.968.22


7.416.676.787.125.26


2.812.874.746.357.67

TABLE 4 263


Date Water II level || Date Water

level i Date Water level

A7-2-32ab Continued

Dec. 11, 1950Jan. 8, 1951Feb. 12Mar. 14Apr. 11May 9June 16July 18Aug. 15Sept. 19Oct. 8Nov. 19Dec. 17

8.368.839.228.728.678.535.924.843.896.717.428.278.98

Jan. 16, 1952Feb. 14Apr. 21May 20June 16July 14Aug. 13Sept. 18Oct. 22Nov. 21Dec. 19Jan. 23, 1953

9.229.198.878.765.713.664.666.407.248.298.919.01

Feb. 19. 1953Mar. 21Apr. 21May 18July 6Aug. 7Sept. 7Oct. 8Nov. 10Dec. 10Jan. 7, 1954Feb. 2

9.9010.0010.255.314.44.15.55.97.28.37.46.6

A7-2-32ba2

Aug. 9, 1949Sept. 29Oct. 25Dec. 12Jan. 11, 1950Feb. 11Mar. 8Apr. 6May 17June 9July 11Aug. 8Sept. 12Oct. 10Nov. 13Dec. 11Jan. 8, 1951Feb. 12

2.303.473.704.484.623.123.183.283.443.821.662.214.004.134.264.254.334.36

Mar. 14, 1951Apr. 11May 9June 16July 18Aug. 15Sept. 19Oct. 8Nov. 20Dec. 17Jan. 16, 1952Feb. 14Mar. 17Apr. 21May 20June 16July 14Aug. 13

4.383.184.084.193.193.303.463.593.783.823.894.263.053.203.313.423.012.71

Sept. 18, 1952Oct. 22Nov. 21Dec. 19Jan. 23, 1953Feb. 19Mar. 21Apr. 21May 18June 10July 6Sept. 9Oct. 10Nov. 10Dec. 10Jan. 7, 1954Feb. 2

3.143.283.403.493.543.623.913.743.823.024.13.13.23.23.54.15.1

A7-2-32bb

Aug. 9, 1949Sept. 29Oct. 25Dec. 12Jan. 11, 1950Feb. 8Mar. 8Apr. 6May 17June 9

4.755.805.966.20DryDry

6.306.156.024.20

July 11, 1950Aug. 8Sept. 12Oct. 10Nov. 13Dec. 11Jan. 8, 1951Feb. 12Mar. 14

1.962.185.436.346.84DryDryDryDry


DryDry

3.964.583.506.18DryDryDry

A7-2-32cb

Aug. 9, 1949Sept. 29Oct. 25Dec. 12Jan. 11. 1950Feb. 11Mar. 8Apr. 6May 17June 9July 11Aug. 8Sept. 12

2.553.764.184.685.065.415.124.514.093.143.112.393,97

Oct. 10, 1950Nov. 13Dec. 11Jan. 8, 1951Feb. 12Mar. 14Apr. 11May 9June 16July 18Aug. 15Sept. 19Oct. 8

4.284.664,844.99S.345.385.034.414.533.612.654;314.67

Nov. 20, 1951Dec. 17Jan. 16, 1952Feb. 14Mar. 17Apr. 21May 21June 16July 14Aug. 13Sept. 18Oct. 22Nov. 21

5.175.485.525.385.744.614.332,403.383.334*615.295.58

394090 O - 56 - 7




! level Date Water level

A7 -2-32cb Continued

Dec.Jan.Feb.Mar.Apr.

19, 195223, 1953191921

5.636.116.026.096.13

MayJuneJulySept.Oct.

19, 195310698

3.001.902.904.04.9

1 Nov.Dec.Jan.Feb.

1

10, 1953107, 19542

4.96.16.06.0

A7-2-32da

Sept. 23, 1949Oct. 25Dec. 12Jan. 11, 1950Feb. 11Mar. 8Apr, 6May 17

5.305.856.616.956.675.805.535.71


1.993.232.494.225.486.126.68

Jan. 8, 1951Feb. 12Mar. 14Apr. 11May 9June 16July 18

6.967.577.466.826.29.91

3.21

A7-2-33cd2

Aug. 1, 1949Sept. 30Oct. 25Dec. 12Jan. 11, 1950Feb. 11Mar. 8Apr. 6May 17

2.951.922.403.303.303.063.103.524.14

June 9, 1950July 11Aug. 8Sept. 12Oct. 10Nov. 16Dec. 11Jan. 8, 1951Feb. 12

3.943.123.312.262.202.292.423.183.17


3.493.813.943.212.485.496.467.397.84

A8-2-3dcl

July 5, 1950 18

26.49 26.51

Aug. 10, 1950 22.82 Sept. 7, 1950 24.36

A8-2-6ac


8.8610.5512.2012.7412.5212.7212.0613.6214.2913.8912.71

8.45

July 20, 1951Aug. 17Sept. 21Oct. 9Nov. 19Dec. 18Jan. 17, 1952Feb. 15Mar. 19Apr. 22June 17July 15

9.3611.1611.4611.5211.8311.2211.6712.3113.0411.609.109.38


10.1011.3012.2212.2912.0510.5412.8010.2411.0310.905.85

A8-2-7aal

July 7, 195018

Aug. 10Sept. 7Oct. 11Nov. 14Dec. 11Jan. 8, 1951Feb. 12Mar. 14

25.1324.5625.6127.2427.6027.5828.0628.6929.4529.77

Apr. 11, 1951May 9June 16July 20Aug. 17Sept. 21Oct. 9Nov. 19Dec. 18Jaa. 17, 1952

29.8429.6027.7526.6527.0926.1526.6927.6328.4128.51

Feb. 15, 1952Mar. 19Apr. 22June 17July 15Aug. 13Sept. 19Oct. 21Nov. 22Dec. 17

28.8129.2129.6628.0126.5927.6828.3428.2128.3828.50

TABLE 4 265




A8-2-7aal Continued

Jan. 22, 1953 Feb. 20 Mar. 21

29.07 1 29.21 29.74

Apr. 20, 1953 May 21

29.92 29.71

June 18, 1953 July 17

26.31 21.92

A8-2-8ca

July 7, 195018

Aug. 10Sept. 7Oct. 11Nov. 14Dec. 11Jan. 8, 1951Feb. 12Mar. 14Apr. 11May 9June 16

68.6568.0367.5366.7667.3868.9772.5474.9877.4778.4479.2477.4875.04


69.5471.8167.7168.2373.1778.6578.3278.5178.6079.9677.7069.98


70.8068.3969.7071.2372.8179.4379.6078.1478.9377.3068.6267.98

A8-2-9bc

July 5, 1950 18

5,48 5.29

Aug. 10, 1950 4.63 Sept. 7, 1950 5.93

A8-2-10aa

July 6, 195018

Aug. 10Sept. 11Oct. 11Nov. 14Dec. 11Jan. 8, 1951Feb. 12Mar. 14Apr. 11May 9

40.0140.4337.0739.2141.6043.0644.2545.4647.6248.9450.3150.03

June 16, 1951July 20Aug. 17Sept. 21Oct. 9Nov. 19Dec. 18Jan. 17, 1952Feb. 15Mar. 19Apr. 22June 17

45.0136.6438.8541.0042.0943.6844.6245.0645.9847.3548.6246.72


38.9439.3138.5839.6540.2040.5442.4643.8044.4045.3244.8036.89

A8-2-14bb

June 30, 1950 91.57 || July 18, 1950 89.23

A8-2-20cdl

June 26, 1950 July 18

1.76 2.79

June 27, 1950 July 18 Aug. 10 Sept. 7 Oct. 11 Nov. 14 Dec. 11 Jan. 8, 1951

1.87 .75

2.43 2.53 2.55 4.69 5.25 5.83

Aug. 10, 1950 Sept. 7

2.93 2.94

A8-2-21ca

Feb. 12, 1951 Mar. 14 Apr. 11 May 9 June 16 July 19 Aug. 17 Sept. 21

6.73 7.06 6.20 5.91 4.42 2.53 3.21 3.03

Aug. 10, 1950

Oct. 11, 1950 Nov. 14

90.31

2.63 3.87

Oct. 9, 1951 Nov. 19 Dec. 18 Feb. 15, 1952 Mar. 19 Apr. 22 June 17 Aug. 13

3.91 4.60 4.73 4.43 5.54 4.76 2.48 2.86


Table 4. Measurements of the wetter level in observation wells Continued

Date Water II level (I Date Water ||

level 1 Date Water level

A8-2-21ca Continued

Sept. 19, 1952Oct. 21Nov. 22Dec. 17

4.554.684.835.46

Jan. 23, 1953Feb. 20Mar. 21

5.725.806.14

Apr. 20, 1953May 21June 18

6.385.802.36

A8-2-23ccl

June 27, 1950July 18Aug. 10Sept. 1Oct. 11Nov. 14Dec. 11Jan. 8. 1951Feb. 12Mar. 14Apr. 15May 9

9.918.598.969.649.679.349.469.069.309.679.679.49

June 16, 1951July 20Aug. 17Sept. 21Oct. 9Nov. 19Dec. 18Jan. 17, 1952Feb. 15Mar. 19Apr. 22June 17

7.369.168.448.458.969.189.65

10.4310.2910.209.819.18

July 15, 1952Aug. 13Oct. 22Nov. 22Dec. 17Jan. 23, 1953Feb. 20Mar. 21Apr. 20May 21June 18

9.249.42

10.429.81

10.1010.4110.3010.6010.519.735.57

A8-2-28cd


15.4913.0212.6713.4615.5517.1718.1118.9519.9220.1219.9319.6615.82


10.8311.7414.4415.4317.4418.4318.8119.4819.1618.8818.3316.70


10.4713.0214.6015.8016.8217.18-19.0319.8819.0819.8418.4114.89

A8-2-29dcl


2.612.462.863.083.694.495.325.345.545.995.645.134.48


1.812.613.494.034.665.525.115.395.445.014.644.322.64


2.343.703.864.525.025.615.706.156.755.154.162.21

A8-2-32aa


5.445.565.696.177.428.419.03

Jan. 8, 1951Feb. 12Mar. 14Apr. 11May 9June 16July 20

9.429.72

10.299.829.768.224.58

Aug. 17, 1951Sept. 21Oct. 9Nov. 19Dec. 18Jan. 17, 1952Feb. 15

5.607.117.668.629.479.469.51

TABLE 4 267


Date Water II level 1 Date Water


A8-2-32aa Continued

Mar. 19. 1952Apr. 22May 21June 17July 15Aug. 13

9.099.167.937.175.605.40

Sept. 19, 1952Oct. 22Nov. 22Dec. 17Jan. 23, 1953

7.227.958.569.159.59


9.6910.3210.519.127.21

A8-2-32dbl


4.213.964.834.675.846.707.358.207.968.468.317.24

June 16, 1951July 20Aug. 17Sept. 21Oct. 9Nov. 19Feb. 15, 1952Mar. 19Apr. 22May 21June 17

6.793.944.485.776.187.027.418.037.377.096.32

July 15, 1952Aug. 13Sept. 19Oct. 22Nov. 22Dec. 17Jan. 23, 1953Feb. 20Mar. 21May 21June 18

4.564.165.856.306.807.407.898.028.617.185.68

A9-2-19da2


2.382.293.222.451.782.87


3.503.132.574.893.561.01


3.713.194.584.134.264.48

A9-2-20db


4.095,146.115.807.096.31


6.887.047.978.886.504.72


4.115.886.736.306.346.41

A9-2-31da


35.3037.5239.2140.0340.6941.1241.5442.4442.9343.2642.7338.13


36.5437.4139.3537.8639.3438.8639.9140.5141.7340.6838.7034.92


37.3038.0738.8940.1242.0142.6642.7137.0037.3136.6334.29

394090 O - 56 - 8





A9-2-33cd

July 7, 195018

Aug. 10Sept. 7Oct. 11Nov. 14Dec. 11

48.2947.0446.8346.3346.7249.5956.68


57.3447.0147.4348.6547.8153.42


50.7346.8543.9045.1342.1044.22

RECORD OF WELLS AND SPRINGS

(Wel

l n

o.:

See

text

for

des

crip

tion

of

wel

l-nu

mbe

ring

sys

tem

.T

ype

of w

ell:

B

, bo

red;

D

, dr

iven

; D

D,

dug

and

drill

ed;

Dr,

dr

illed

; D

u, d

ug;

Sp,

spri

ng.

Dep

th o

f w

ell:

M

easu

red

dept

hs a

re g

iven

in

feet

and

ten

ths

bel

ow m

eas

ur

ing

poin

t;

repo

rted

de

pths

ar

e gi

ven

in

fe

et b

elow

lan

d su

rfac

e.T

ype

of c

asin

g:

C,

conc

rete

; M

, m

ason

ry;

P,

iron

or

stee

l pi

pe;

W,

woo

d.G

eolo

gic

sour

ce:

Al,

allu

vium

; M

lp,

Lod

gepo

le l

imes

tone

; M

m,

lim

esto

ne

of M

adis

on g

roup

; T

g,

Ter

tiar

y de

posi

ts.

Met

hod

of l

ift:

Typ

e of

pum

p:

C,

cent

rifu

gal;

Cy,

cyl

inde

r; F

, na

tura

l fl

ow;

HR

, h

y

drau

lic r

am;

J,

jet;

N,

none

; P

, pi

tche

r;

PP,

reci

proc

atin

g pi

ston

pu

mp.

T

ype

of p

ower

: E

, el

ectr

ic m

otor

; G

, ga

soli

ne

engi

ne;

H,

hand

ope

r-

Tab

le 5

. R

ecor

d of

wel

ls a

nd s

prin

gsat

ed;

W,

win

d.U

se o

f w

ater

: D

, do

mes

tic;

I,

irri

gati

on;

In,

indu

stri

al;

N,

none

; O

, ob

se

rvat

ion

of w

ater

-lev

el f

luct

uati

ons

by U

. S.

G

eolo

gica

l Su

rvey

; S

, st

ock.

Mea

suri

ng p

oint

: B

co,

bott

om o

f co

ver;

L,

land

sur

face

; T

ea,

top

of c

as

ing;

T

co,

top

of c

over

; T

cp,

top

of c

over

in

pit;

Tcu

, to

p of

cur

b; T

p,

top

of p

itch

er p

ump;

T

pb,

top

of p

ump

base

; T

pc,

top

of

pipe

abo

ve

casi

ng;

Tpf

, to

p of

pum

p pl

atfo

rm;

Tpp

, to

p of

2-i

nch

pla

nk o

n fl

oor

of p

orch

; T

tp,

top

of 2

-in

ch d

iam

eter

pip

e in

pit

; TV

S, t

op o

f va

lve

seat

in

pitc

her

pum

p.R

emar

ks:

A,

adeq

uate

sup

ply;

C

a, w

ater

sam

ple

coll

ecte

d f

or c

hem

ical

an

alys

is;

I,

inad

equa

te

supp

ly;

O,

obse

rvat

ion

wel

l of

Soi

l C

onse

rv.

Ser

vice

, U

. S.

Dep

t. A

gric

ultu

re]

to

-a O

Wel

l no

.

A4-l

-lba

-2ab

-2

bal

-2

ba2

-2ba

3

-2b

dl

-2bd

2 -2

cal

-2ca

2 -2

ca3

-2d

bl

-2db

2 -2

dd

l -2

dd2

-2dd

3

Ow

ner

or

tena

nt

P. W

illi

ams.

...........

W.

Sh

erlo

ck..

....

....

.......do..................

......do..................

F.

Kit

to..

....

....

....

...

J. K

itto

....

....

....

....

.......do..................

W.

Kit

to................

......do..................

P. W

illi

ams.

...........

......do..................

......do..................

Typ

e of

w

ell

Du

Du

Du

Du

Dr

Dr

Dr

Du

Du

Du

Du

Du

Dr

Dr

Dr

Dep

th

of w

ell

(fee

t) 9.1

10.4

15

.7

20

100 91

87

.1

21

18

28.5

21.2

21

25

20

.2

24.6

Dia

met

er

of w

ell

(inc

hes)

60x36

18

24

15 6 6 6 24

48

36 36

36 6 6 6

Typ

e of

ca

s

ing W

P P P P P P P M

M M

M

P P P

Geo

lo

gic

sour

ce

Al

Al

Al

Al

Al

Al

Al

Al

Al

Al

Al

Al

Al

Al

Al

Met

hod

of

lift

Cy,

W

N

Cy.W

.H

Cy,

E

J,E N

J,

E

Cy,

W

J.E

J,

E

Cy

, W

J.

E

Cy,

H

Cy.

H

Cy.

E

Use

of

w

ater

S, O

O

N

S D O

D

, S

I D

D.S

.O

S D

D

D

S

Mea

suri

ng p

oint

De

sc

rip

tion

Tpf

T

cu

Tpf

Tpf

Tcu

T

cu L Tpf

Tpf

Tpf

T

pf

Tpf

Dis

tanc

e ab

ove

or

belo

w (

-)

land

sur

fa

ce (

feet

)

1.0 .0

.2 .5 .5

.5 .0

.9 .0 1.4

2.4

2.2

Hei

ght

abov

e m

ean

sea

level

(f

eet)

4,01

7.27

4,0

48.3

6

4.0

49.4

1

4,0

48.5

4

4,0

51.2

1

4,0

54.4

4

4,0

66.0

4

4,0

53.2

9

4,0

54.2

2

4,0

54.7

8

4.0

53.9

0

Dep

th t

o w

ater

le

vel

be

low

m

easu

r

ing

poin

t (f

eet)

2.55

7.

58

5.55

5.82

4.65

8.

50

6.50

22

.70

8.10

12.8

3 13

.92

13.5

5

Dat

e of

m

easu

re

men

t

6-30

-49

5-

2-49

6-3

0-4

9

6-3

0-4

9

6-30

-49

6-2

9-4

9

6-3

0-4

9

5-

2-49

6-

3-49

6-29

-49

6-2

9-4

9

6-2

9-4

9

Rem

arks

A A

A A A

A.C

a

A A

A

A

-lOaa

-lOcb

-llab

-12a

a-12bd

-12d

c-13cc

-14c

c-16da

-22cb

-27ab

A4-2

-4ab

-4bc

-Sac

-5bb

-5bc

-5bd

-5cc

-6aa

-6cc

-6cd

-6dd

-8bbl

-8bb2

-lObb

-16aa

-35cc

A5-l

-4cc

-Sad

-8bc

-8bd

-8ca

-8cdl

-8cd

2-9

dc

......do..................

T.

Wil

liam

s...........

W.

Kit

to...............

T.

Wil

liam

s...........

U.

S.

Geo

l. S

urve

y..

......do....

...............

......do..

.................

....

..d

o..

....

....

....

....

.

....

..d

o..

....

....

....

....

.

......do..

....

....

....

....

.U

. S

. G

eol.

Sur

vey.

. ......do..

.................

Mil

ler

& H

anse

n.......

W.

Ho

ssfe

ld..

....

....

..

......do....

....

....

....

...

T.

McM

ull

an..........

......do....

....

....

....

...

T.

Wil

liam

s...

....

....

.

R.

Har

ris.

...............

T.

Wil

liam

s...

....

....

.R

ader

burg

Gra

de

C.

Eden

fiel

d...........

F.

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Tab

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Dr

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Dr

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Dep

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4 1 1 1 1 1 1 1 1 1 1 36 3 1.25

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36 4 1 3

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P P P M M P M

M P P P

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Tg

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Tg

Tg

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Al

Al

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Al

Al

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Al

Al

Al

Al

Al

Al

Al

Al

Al

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P,H

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INDEX

Page Abstract..... ........ ........ ................ . 17 1-172Acknowledgments......... ...... ................. 174Agriculture........................................ 183AUuvium...................,..189, 199, 214, 223,

227, 228-229, 230 Amsden formation................. 189, 195, 203Analyses, chemical............... .223-224, 225Antelope Springs...........................217, 223

Beaver Creek.............................,.181, 224Bedford............................................. 175Bedford Spring..... ..............46-47, 216-217,

223, 225, 228 Belt series............... 191. 192-193, 203, 205Bench gravel...................................... 199Benchland.....................l87f 199, 207, 231Big Belt Mountains,..............................185Big Spring...................l75, 182. 209, 213.

215-216, 223, 225 Big Spring Ditch..................................l82Broadwater Canal.......................... 181, 182Brule

Cambrian rocks..... ........................ 193-194Canyon Ferry Dam............... 173, 180, 185,

201, 232 Canyon Ferry stock.............................. 201Chadron formation.... ................... .197, 202Chemical quality of die water...222-229, 232 Climate..........................*........,. 176-180Coal....................................l84, 196-197Colorado shale...........,...189, 196, 200. 206Conclusions......................... .........230-232Confederate Gulch.......................,175, 224Cretaceous rocks................................. 196Crow Creek..................... .....181, 224, 230Crow Creek area.......... ....173, 182, 185-187,

209, 211, 214, 231, 232 Crow Peak......................................... 185

Deep Creek..........................l81, 220, 224Devonian rocks................................... 195Diamond City..................................... 175Diatoxnaceous earth............................. 197

Drainage..................................... 180-181

Dry Creek anticline...................... 202, 219Dry Creek shale.................... 190, 194, 226

Earthquakes................ ....204-205, 213, 220Elkhorn Peak...................................... 185Elkhorn Range.................................... 185Ellis group......................................... 196Empire shale............................... 191, 192Evapotranspiration...... ...................... ...215

Faults....................Flathead quartdte....,

.....................203-204....184, 190, 193, 194,

200, 203, 206

Page Folds.......................................... 201-202Fossils, vertebrate................. ........ 197-198

Geologic history, summary.. .......... ..205-208Geology..................... 173, 188-208; pL 19Geomorphology.. ...... ..................... 185-187Gold..........................w.......175, 183-184Greyson Creek.................................... 181Greyson shale....................... ....... 191, 192Grist mill........................... ............... 175Ground water............................... 208-230

changes in storage..... ................ 209-211discharge............... ............... ....215-219effects of earthquakes..... ................... 213movement............................... 211, 231recharge.. ............................... ..20 8-209use.... .......................... ............219-220waterlogging...................... 213-214, 231

Gurnett Creek.. ................................ ...224Gurnett stock.... ............................ ......201

Hassel................ ............................... 176Helena limestone......................... 191, 1S3

History of the area................. ...... ..175-176

Igneous rocks... ............................. 199-201Indian Creek fault..... .......................... 203Irish Ditch......................................... 182Iron Mask mine. .................................. 184Iron ore...... .................................... ...184Irrigation.... ................... 173, 181-182, 230

Jacobson, Edward................................ 198Jefferson limestone......... 190, 195, 200, 206Jurassic rocks.. ................................ ....196

Kay, LeRoy, cited................«..... 197, 202Kimpton Spring... ................ .........217, 225Kbotenai formation......... 189, 196, 200, 206

Lead....... ................................ ..........184Lewis and Clark Expedition....................l75limestone Hills... ............. ......201-202, 203Literature cited... ...................... ....232-233Location of area....... ........................... 172Lodgepole limestone.............. 189, 195, 206Lombard overthrust........ ....... ............... 203Lone Mountain.................................... 199

Madison group..........................H. 189, 195Marble............... ............................... 184Meagher limestone... ...... 184, 190, 194, 206Mining..... ...................................183-184Miocene deposits...........................l97-198Mission Canyon limestone.. .....189, 195, 203

Missouri River.......... 172, 180-181, 224, 230Montana Ditch Co.. .......................... ...181Morrison formation....................... 189, 1%Mount Baldy... ................................ ....185

289

290 INDEX

Page Mount Edith....................................... 185Movement.........................................211

Newland limestone....................... 191, 192

Oil test well.....,.................................198Oligocene formations.................... 197, 202

P«kshaleM..«......................190, 194, 206Pennsylvanian rocte............................. 195Permian rocks.....................................195Phospfaoria formation.........189, 195, 203,206Pilgrim limestone.............190, 194, 203,206Plunket Spring...........l75, 213, 216, 223, 225Precambrian rocks......................... 192-193Precipitation................................ 176-180Pre-Tertiaryrocks................223, 225, 226Previous investigations..........................174Purpose of investigation.................. 173-174

Quadrant formation..........189, 195, 203, 206Ouartrite........................................... 184Quaternary deposits........................198-199

Radersburg.........................................175Railroads...........................................184Ray Creek......................................... 224Recharge.....................................20 8-209

Sawtooth formation.................189, 196, 206Scope of investigation.................... 173-174Seepage into streams............................215Sills................................................. 200Sixmile Creek.................................... 220Spokane Hills...............................l85, 203Spokane shale.......................191, 192, 200Springs........................................215-218

record of.................................. 270-287

State Water ConservationCommission....................... 181-182

Stocks.....................................«.200, 201.Stratigraphy.................................189-199

Cambrian rocks................................193Cretaceous rocls.............................. 196Devonian rt>cks................................ 195Jurassic rocks...................................196Mississippian rocks............................195Pennsylvanian rocks......................... 195Permian rocks..................................195Precambrian rocks............................ 192Quaternary deposits.........................«198Tertiary deposits.............................. 196

Structure, geologic........................201-205Summary.....................................230-232Surface water.............................. 224, 229

Temperature...................................... 180Tertiary deposits.....l89, 196-198, 203, 207,

223, 225-228, 230; pi. 19 Three Forks shale........... 190, 195, 200, 206Toston.............................................. 220Toston beds.......................................197Townsend................................... 176, 220Transportation.................................... 184

Vegetation.. .183

Warm Spring-Creek Canal..................... 182Waterlogging.........................213-214, 231Well-numbering system..................,MW. 176Wells.........................210, 218-220; pL 20

measurement of water level in...... 236-268record of................................. 270-287

Wolsey shale.......................M.190t 194,206

Yankee Ditch..................................... 182

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