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Geology and Ground-Water
Resources of the
Gallatin Valley
Gallatin County
Montana
By O. M. HACKETT, F. N. VISHER, R. G. McMURTREY, and W. L. STEINHILBER
With a section on SURFACE-WATER RESOURCES
By FRANK STERMITZ and F. C. BONER
And a section on CHEMICAL QUALITY OF THE WATER
By R. A. KRIEGER
GEOLOGICAL SURVEY WATER-SUPPLY PAPER 1482
Prepared as part of the program of the Department of the Interior for develop ment of the Missouri River basin
UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON :1960
UNITED STATES DEPARTMENT OF THE INTERIOR
FRED A. SEATON, Secretary
GEOLOGICAL SURVEY
Thomas B. Nolan, Director
The U.S. Geological Survey Library catalog card for this publication appears after page 282.
For sale by the Superintendent of Documents, U.S. Government Printing Office Washington 25, D.C.
CONTENTS
Page
Abstract _- _ __ _ _ _ - 1Introduction . 4
Purpose and scope of investigation . . 4Personnel and acknowledgments 4Previous geologic and hydrologic investigations 6Methods of investigation 8Well-numbering system 9
Geography- .......- 11Location and extent of the area 11Topography and drainage 12Climate . 14History _._.._.-_._._--_.____..._.._.. _.._.__.-___.._ ..-- 20Agriculture and industry . . . 20Transportation 23Mineral resources 25
Geology----. ------ .__ _ .. .... _ .. 25Sedimentary rocks...----- 25
Precambrianrocks _ - . .. 26Rocks of Paleozoic age 27
Cambrian system 28Devonian, Mississippian, and Pennsylvanian systems. 29Permian system _ . ___ - 30
Rocks of Mesozoic age 30Jurassic system--...----- . 31Cretaceous system . 31
Rocks of Mesozoic and Cenozoic age ... 32Cretaceous and Tertiary systems . 32
Rocks of Cenozoic age- .. ...- . 32Tertiary system. 32
Subsurface unit. ........ . 34Unitl___...__...._..._.._..._.__.............._........._._._..._... 35Unit 2. - __---__ 38Undifferentiated Tertiary strata 39
Tertiary and Quaternary systems 39Older alluvium .... . . ________._ ___ _ 39
Quaternary system .._ ___ 42Younger alluvium -. . _ _ 42
Terrace gravels in the Camp Creek Hills. 42Alluvial-fan deposits 42Steam-channel deposits. 43
Loess--- _ 45Colluvium. . - . .... 46
ill
IV CONTENTS
Page
Geology ContinuedIgneous rocks____________ ____________ -_-_____ - - -_ 46Structure - - _ _____ _ _- -- - - . -- 46
Horseshoe Hills _____________________ ____-__ _ _- 47Bridger Range_______________ __ _ ... .... __ _ _ 48Gallatin and Madison Ranges __ _ _ ___ - 49Gallatin Valley_.__-............_......_....._._- -... - - - - 50Effect of faults on the flow of water into and out
of the Gallatin Valley .._ __...._.._ ___.. - -. -- - 55Summary of Cenozoic history . 56
Water resources. __ __ _ ....... 57Surface water, by Frank Stermitz and F. C. Boner __ -. 58
Streams-- - - . - -- - -- - ----- 58Gallatin River_________ __ _ _.____ ______ __________.__ 58East Gallatin River__ ____ ___ - -- - 92Streams from the Gallatin Range ___ _ __-_ 92Streams from the Bridger Range __ __ _ __ . 94Other streams. .___ .____ 95
Estimates of surface-water inflow to Gallatin Valley . 97Utilization.. _ ....___ ..___.__..._ -. .. 99
Ground water _____ ___.___._ ___ _ ________ __ __ _._ __.__ 100Definition of terms _ ___ - . 100Determinations of aquifer properties 102Aquifer properties as they affect the specific capacity of a well 103Recharge____ _-- _ __ _ -_ _._ __- 107Discharge _._....__.. _____.__..... ...._...._.._... ._ ........._._ 109Configuration of the water table . _ 118Changes in storage _ _______ _ .._ _ ______ .. _ _ 119Water-level fluctuations caused by earthquakes and
other disturbances, - __.___ ___ _. 128Water-resources inventory, water years 1952 and 1953 128
Evaluation ____.___ _...._........... __._.......... ......_. . .___ .. .... 128Analysis__________________________________________ __________ ___________________________... 132
Water-resources inventory, water years 1935 through 1951 . 134Hydrologic units within the Gallatin Valley 136
Valley floor ..........._............................___.........____........ ._ _ ..........___..__.. 136Gateway subarea ___________ _ _______________ 136Belgrade subarea ______ _____________ _____________ __ _ ___ ___ 140Central Park subarea _ _____ ___________..___..._____... -.. .... 146Manhattan subarea __________________________________ ______.............___.___..._....... 149Upper East Gallatin subarea __ _ . 151
Bozeman fan ---__---- ___-_-________ _ _______________ _________________________________ 153Camp Creek Hills ______ -........ ___...__.. . ._ __________ . ...._.. __________ 157Valley fringe_____ ___________________________________________________________________________________ 158
Dry Creek subarea _____________________________ ____________________ 158Spring Hill subarea___________________ _____________ __......... .___....___............_ 158South Bridger subarea _______________________________________ 159Fort Ellis subarea _____________ ____________ ___ 159South Gallatin subarea __________ __ __ .__ __._ .._______. 159
Chemical quality of the water, by R. A. Krieger__ __ _ _ ______________ 160Geologic source and significance of the ions. _____ __ _ _____ ______ 160
CONTENTS V
Page
Chemical quality of the water, by R. A. Krieger ContinuedConcentration and nature of dissolved constituents 166Chemical quality in relation to hydrology 167Suitability of the water for irrigation . 168Suitability of the water for domestic use ______ _ ___. 175
Conclusion _ _ - _ _ - _ _ 176Selected references __ _ _____ _ __ _ 179Basic data 183Index - - ---- ---- ------- .-_- 277
ILLUSTRATIONS
[Plates in plate volume]
PLATE 1. Topographic map of the Gallatin Valley, Mont., showing location of wells, test holes, stream-gaging stations, and precipitation stations.
2. Map of the Gallatin Valley showing areal geology.3. Hydrograph of the discharge of Dry Creek at Andrus ranch, near
Manhattan, water years 1952 and 1953.4. Graphs showing daily amount of ground water consumed by a
cottonwood grove in the Gallatin Valley and of factors affecting ground-water consumption.
5. Map of the Gallatin Valley showing contour of the water table about April 1 and August 1,1953.
6. Map of the Gallatin Valley showing depth to water.7. Map of the Gallatin Valley showing the difference in position of
the water table, April 1 and August 1,1953.8. Monthly inventory of the surface-water resources of the Gallatin
Valley.9. Hydrographs of the water level in wells Al-4-25dc, Dl-4-6ddc2,
-9bal, -9ba2, -25aa2, -25aa3, and D2-4-13cc.10. Maps showing chemical characteristics of the ground water in the
Gallatin Valley.11. Map showing chemical characteristics of the surface water in the
Gallatin Valley.
Page
FIGURE 1. Well-numbering system ___.__ ____ 102. Map of the Gallatin Valley showing the principal topo
graphic features, drainage, and hydrologic subdivisions 113. Map of the Gallatin Valley showing the location of precipi
tation stations and the distribution of precipitation in 1952 _________________________________________________________ 18
4. Precipitation at Bozeman _. 195. Map of the Gallatin Valley showing the location of irrigated
land, 1952 ______ ______.____ _____________.___ 246. Map showing the relation of the Gallatin Valley to the Three
Forks basin _ ____ ____ ________________ 26
VI CONTENTS
Page
FIGURE 7. Local unconformity between units 1 and 2 of the Tertiary strata in the bluffs along the Madison River in the SE 1/^ NEU sec. 3, T. 1 S., R. 2 E ______ 36
8. Older alluvium in the Gallatin Valley ___ ___._________________ 419. Younger alluvium in the Gallatin Valley __ ______ _____________________ 44
10. Loess mantling upper Tertiary or Pleistocene gravel in theSW^SW^ sec. 26, T. 1 S., R. 3 E _____ 45
11. Small normal faults in the Tertiary strata in the SW^SE 1sec. 7, T. 2 S., R. 6 E __________ 51
12. Diagrammatic section showing vestiges of the monoclinalfold in Tertiary strata in the Camp Creek Hills _ ____________ 52
13. Diagram showing alternative hypotheses for the formationof the Belgrade trough ______________ _____ _ 54
14. Hydrologic cycle __________________________ _______________________ 5715. Map of the Gallatin Valley showing location of stream-
gaging stations _________________________________________________ 5916. Hydrographs of the discharge of the Gallatin River near
Gallatin Gateway and at Logan, water years 1952 and 1953 _____ _____ ____ ___________________________________ 89
17. Hydrographs of monthly surface-water inflow to, and out flow from, the Gallatin Valley, water years 1951-53 _________ 93
18. Hydrographs of annual surface-water inflow to, and outflowfrom, the Gallatin Valley, 1931-53_______________. ___ ._ 94
19. Hydrograph of the discharge of Middle Cottonwood Creeknear Bozeman, water years 1952 and 1953 _ ____ ___... 96
20. Graph showing theoretical drawdown in an "ideal" pumpedwell ______________________________ ____________________________________ 106
21. Hydrograph of the water level in well AR-3-33da showingthe effect of recharge from infiltrating irrigation water___ __ 108
22. Hydrograph of the water level in well D2-5-16aal showing the effect of recharge from infiltrating snowmelt and streamflow _____ __________________________________________ ____ 109
23. Hydrograph of the water level in well D2-5-16aal showing the effect of recharge from infiltrating precipitation and streamflow ___________________________________________________.___ 109
24. Cottonwood grove in the SW^SE 1 sec. 22, T. 1 N., R. 4 E _ 11225. Specimen hydrograph of the water level in well Al-4-22dcl__ 11226. Graphs for period July 1951 through September 1953, show
ing discharge of Gallatin River near Gallatin Gateway, total diversions from Gallatin River between Gallatin Gateway and Central Park, total monthly precipitation and average monthly temperature at Belgrade, and monthly cumulative departure from the volume of satu rated material as of the end of June 1952 _____________________________ 119
27. Graph used in computing average specific yield of theground-water reservoir in the Gallatin Valley _________________ 124
28. Graph showing estimated cumulative departure, 1934-53, from the volume of saturated material as of the end of June 1952 ______ __________________ _________________________ 125
CONTENTS VII
Page
FIGURE 29. Rating curve used in estimating midwinter cumulative de partures from volume of saturated material as of the end of June 1952 ______________ 127
30. Hydrographs of the water level in well A-4-25dc showingthe effect of earthquakes and passing trains ,. .. 129
31. Geologic section near Logan _ __ _ . _ 13132. Diagrammatic sections of the Gateway subarea showing two
possible interpretations of subsurface geologic relation ships -,__ _ ___ ____ ...... __ _ 137
33. Graphs showing the cumulative departure from the volume of saturated material'as of the end of June 1952 in the Gateway, Belgrade, Central Park, and Manhattan sub- areas and in the Bozeman fan ___..._ ...__ _ _ 138
34. Diagrammatic section of the Gateway subarea showing the theoretical changes in position of the water table that would result from increased consumptive use of ground water _______ . _______ _ __ _______ ______ __ 140
35. Diagrammatic section of the northern part of the Belgrade subarea showing changes in position of the water table that would result from increased consumptive use of ground water ..._______ ._______ _______ 145
36. Hydrographs of the water level in -wells Al-4-5da andAl-4-22dcl _____ _ - 147
37. Hydrographs of the flow of the principal streams rising inthe Central Park subarea 148
38. Hydrograph of the water level in well A2-3-33da. - 15239. Hydrographs of the water level in wells Dl-5-34cc2, D2-5-
14ac, -16aal, and -22ccd__..__ ..._-.__. _ _ __ 15640. Graph showing classification of ground and surface waters
of the Gallatin Valley for irrigation 174
TABLES
Page
TABLE 1. Daily temperatures at three stations in the Gallatin Valley,May 1952 through January 1954 15
2. Annual precipitation at Bozeman, 1869-1953 . 193. Annual precipitation at Belgrade, 1941-53 204. Monthly precipitation at 18 stations in the Gallatin Valley,
1952-53 . _....... __...__. ._.. _... ..._.._.. ..._.. _...._-.... - 215. Monthly volume of precipitation on the Gallatin Valley in
water years 1952 and 1953 236. Descriptions of stream-gaging stations in the Gallatin
Valley .____-_-_____.-- 607. Monthly and annual runoff of streams in the Gallatin
Valley _.......-_........ .___...... ___... -_....___...._.......... ._... __.. 698. Occasional measurements of the discharge of streams, ditches,
and springs in the Gallatin Valley 809. Differences in monthly and annual runoff at gaging stations
on the Gallatin River during water years 1952 and 1953.- 90
Vili CONTENTS
Page
TABLE 10. Estimated annual inflow to the Gallatin Valley during wateryears 1931 through 1951...._. -_- -_ __ 97
11. Estimated monthly inflow to the Gallatin Valley, exclusive of the Gallatin River, during period November through Feb ruary of water years 1931 through 1951.. ... 98
12. Summary of aquifer-test data 10413. Inflow to, and outflow from, the Central Park subarea. ___ 11114. Daily consumption of ground water by cottonwood grove. 11315. Daily precipitation near cottonwood grove 11416. Wind velocity near cottonwood grove 11517. Daily evaporation from a class-A pan near cottonwood grove- 11618. Estimated ground-water discharge from the Gallatin Valley.. 11719. Monthly changes in volume of saturated material in the
Gallatin Valley . ._..._._.__ ._. ...__ .._.. .._.._._._ _....._ 12120. Cumulative monthly departures from volume of saturated
material as of the end of June 1952 _.. _ 12221. Monthly changes in volume of ground water stored in the
Gallatin Valley _ _ _.__________._._._ 12322. Estimated cumulative departures from volume of saturated
material as of the end of June 1952..._ ... ____ ...... 12623. Monthly and annual changes in surface-water supply of the
Gallatin Valley, water years 1952 and 1953 13024. Estimated annual changes in surface-water supply of the
Gallatin Valley, water years 1935 through 1951 13525. Monthly losses in flow of the Gallatin River between Cameron
Bridge and Central Park _. 14326. Monthly gains and losses in flow of the East Gallatin River
between Lux Siding and Penwell Bridge 14427. Chemical analyses of ground water in the Gallatin Valley 16228. Chemical analyses of surface water in the Gallatin Valley 16429. Changes in water quality in a downslope direction in the
Bozeman fan ___ ____ __ _ - 16730. Annual changes in total mineralization of ground water from
shallow wells ___ ___ ... 16831. Chemical properties relating to suitability of ground water
for irrigation in the Gallatin Valley . . . 17032. Chemical properties relating to suitability of surface water
for irrigation in the Gallatin Valley . 17233. Logs of wells and test holes. ......... .. ____ 18434. Water-level measurements by tape 20435. Water-level measurements from recorder chart 22936. Record of wells and springs-.---------. 244
GEOLOGY AND GROUND-WATER RESOURCES OF THE GALLATIN VALLEY, GALLATIN COUNTY, MONTANA
By 0. M. HACKETT, F. N. VISHER, R. G. MCMURTREY and W. L. STEINHILBER
ABSTRACT
The Gallatin Valley, an intermontane basin in southwestern Montana, has an area of about 540 square miles and is drained by the Gallatin River and its tributaries. Although much of the valley is semiarid, annual precipitation may average more than 20 inches near the Bridger and Gallatin Ranges, which border the valley on the east and south. Agriculture is the leading occupation. Much of the central part of the valley is irrigated, but most of the higher land along the margins of the valley is dry farmed. The extent to which the agricultural economy of the valley ultimately may be developed depends on the degree to which the valley's water resources are utilized.
The Three Forks structural basin, in which the Gallatin Valley is located, was formed as the result of crustal movements in early Tertiary time. Sub sequently, the basin was filled to a depth of 4,000 feet or more with volcanic ash and with sand, silt, and clay eroded from the surrounding highlands. As the result of renewed crustal unrest in late Tertiary or early Quaternary time, the Tertiary strata were tilted eastward; where exposed in the Camp Creek Hills, in the western part of the Gallatin Valley, they form a homocline that dips 1° to 5° to the east. A major east-trending fold in the Tertiary strata in the northern part of the Camp Creek Hills is believed by the authors to mark a subjacent fault, referred to in the present report as the Central Park fault.
The Tertiary strata are divisible into three units, of which the lowest is known only from subsurface data. The subsurface unit probably is of early Oligocene age and is inferred by the authors to be at least 2,400 feet thick. From test drilling, it is known to consist, in part, of blue-green sandstone, claystone, and siltstone, and to contain a few beds of bentonite(?) and lignite. The lower of the exposed units, unit 1, probably includes strata of late Oligocene and early Miocene age and is about 900 feet thick in the Camp Creek Hills. Predominantly of lacustrine origin, this unit is composed largely of well-stratified volcanic ash, tuffaceous marl, siltstone, and sandstone and contains a few beds of limestone. Unit 2, probably of late Miocene and Pliocene age, is predominantly of fluvial and colluvial origin and is a little more than 400 feet thick in most places in the Camp Creek Hills. It consists of poorly stratified to massive, buff to tan, variously consolidated tuffaceous siltstone, claystone, sandstone, and conglomerate, and contains a few beds of gray ash. Whether the strata of Tertiary age that skirt the mountain ranges on the east and south sides of the Gallatin Valley are equivalent in age to, or younger than, those of the Camp Creek Hills could not be determined by the authors.
2 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Post-Tertiary crustal movement, probably along the postulated Central Park fault, created a deep east-trending trough in the Tertiary strata be tween the Camp Creek Hills and the Bridger Range. Alluvium deposited by the Gallatin River and its tributaries during Quaternary time not only filled this trough but mantled the Tertiary strata throughout the lower part of the Gallatin Valley. Also, broad fans of alluvium were deposited on the lower slopes of the Bridger and Gallatin Ranges by streams heading in the mountains. The alluvium consists of cobbles and gravel intermixed with sand, silt, and clay.
The Gallatin River is the source of irrigation water for about three-fourths of the irrigated land in the valley. During the 2 periods of record (1889-92 and 1930-52) the annual flow into the Gallatin Valley, as measured near Gallatin Gateway, averaged 536,000 acre-feet. During the 1952 water year (October 1, 1951, through September 30, 1952) the discharge of the Gallatin River at Gallatin Gateway was 715,000 acre-feet, or about 73 percent of the total surface-water inflow to the valley (976,000 acre-feet). In the 1953 water year the discharge of the Gallatin River at Gallatin Gateway was 518,000 acre-feet, or about 70 percent of the total inflow to the valley (744,000 acre-feet). Nearly all the other inflow to the valley was contributed by streams draining the Gallatin and Bridger Ranges.
Although much ground water is available in the Gallatin Valley, this resource is largely undeveloped. The principal aquifer is the alluvium be neath the valley floor. This aquifer is characterized by generally high coefficients of transmissibility 100,000 to 300,000 gpd (gallons per day) per foot and in many places would yield ample water for irrigation. The adjacent alluvial fans generally yield sufficient water for only stock and domestic use, but the more extensive fans probably would yield supplies sufficient for some irrigation. Low to moderate coefficients of transmissibility (7,000 to 65,000 gpd per foot) characterize the alluvial fans. The Tertiary strata have relatively low coefficients of transmissibility (generally less than 6,000 gpd per foot) and yield sufficient water for only stock and domestic use.
The ground-water reservoir is recharged principally by infiltrating irri gation water. Influent seepage from streams, particularly during the period of high runoff in the spring, is another important means of recharge. Ground water is discharged by seepage to the streams at the lower end of the valley and by evapotranspiration. The discharge of ground water as surface flow from the valley is estimated to be about 240,000 acre-feet per year. Recharge to the ground-water reservoir exceeds this amount by the unknown volume of ground water consumed through evapotranspiration.
Along the valley sides, ground water moves toward the valley floor, and in the Bozeman fan and beneath the valley floor it moves generally northward. In most of the area between the Gallatin and East Gallatin Rivers the water table is within 30 feet of the land surface throughout the year, and within much of this area it is within 10 feet of the surface.
Data indicate an increase of ground water in storage during the late spring and early summer months, and a decrease in storage during the rest of the year. Using a computed value of 15 percent for the specific yield, the writers calculated that ground-water storage increased by about 150,000 acre-feet during the period March through July in the 1952 water year and that it decreased by about 132,000 acre-feet during the other months of that year. In the 1953 water year, ground-water storage increased by 149,000
ABSTRACT 3
acre-feet during the period April through July and decreased by 167,000 acre-feet during the other months.
An inventory of the water resources in the Gallatin Valley shows that during the 1952 water year a total of 1,484,000 acre-feet of water entered the valley (976,000 acre-feet as surface water and 508,000 acre-feet as pre cipitation). Of the total, a net of 17,500 acre-feet was added to ground- water storage. During the same period, 437,000 acre-feet was used con sumptively, and 1,030,000 acre-feet of water left the valley as surface flow. In the 1953 water year 1,103,000 acre-feet of water entered the valley (744,000 acre-feet as surface water and 359,000 acre-feet as precipitation). During the same period, 405,000 acre-feet was used consumptively, and 716,000 acre-feet left the valley as surface water. Of the total (1,121,000 acre-feet), 17,900 acre-feet was withdrawn from ground-water storage.
In this report the Gallatin Valley is subdivided into areas and subareas according to geologic and hydrologic characteristics. Each area and subarea is discussed in regard to its potential for development of ground water for large-scale use.
Theoretically, about 20,000 acre-feet of ground water per year could be pumped in the Gateway subarea and at least 100,000 acre-feet per year could be pumped in the Belgrade subarea without reducing the amount of ground water in storage. Ground water from the Belgrade subarea could be conveyed by ditches to the Manhattan subarea for irrigation.
In some places on the Bozeman fan, a supplemental supply of water for irrigation could be obtained from underground sources, but elsewhere on the fan the supply of ground water is sufficient only for domestic and stock needs.
Ground water for irrigation is not available in the Camp Creek Hills nor in the Dry Creek, South Bridger, Fort Ellis, and South Gallatin subareas. Available data indicate that the Upper East Gallatin and the Spring Hill subareas do not have large ground-water supplies, but additional informa tion would be necessary before an accurate evaluation could be made.
If ground water were used to increase irrigation in the valley, the reduction in outflow from the valley would approximate the volume of water used con sumptively. Maximum irrigation would involve (a) use of surface water for irrigation from the beginning of the irrigation season to the period of surface-water shortage; (b) artificial recharge of the ground-water reser voir in the Gateway and Belgrade subareas by spreading surplus surface water before and during the irrigation season; (c) use of ground water during the period of surface-water shortage for irrigation in the Gateway, Belgrade, Central Park, and Manhattan subareas, and the use of surface water in the remaining irrigated parts of the Gallatin Valley.
Calcium and bicarbonate are the principal dissolved constituents in ground water from deposits of Quaternary age in the Gallatin Valley. Generally, the water has a mineralization of about 150 to 400 ppm of dissolved solids, is hard, and contains iron in excess of 0.3 ppm. The chemical quality of water from the alluvium underlying the valley floor does not vary from place to place nor with depth; it resembles the quality of water from Quaternary deposits in the Bozeman fan and the valley-fringe area. However, water from the Tertiary strata does vary in quality from place to place as well as with depth. Sodium is a principal dissolved constituent in some water from Tertiary strata. In the northern part of the valley floor, water that entered a deep test hole from Tertiary strata and Precambrian rocks was of the
4 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
sodium chloride bicarbonate type and was more highly mineralized than water from wells tapping deposits of Quaternary or Tertiary age.
Water in streams in the lower Gallatin River drainage basin also is of the calcium bicarbonate type. At Logan, the only outlet for water from the basin, the maximum concentration of dissolved solids in the Gallatin River was 258 ppm in water samples collected at intervals throughout the 1952 water year.
Ground water in the Quaternary deposits and surface water are rated as excellent for irrigation because salinity, percent sodium, residual sodium carbonate, and boron are low. Most of the water from the Tertiary strata also is rated as excellent for irrigation, though salinity, percent sodium, residual sodium carbonate, and boron generally are greater than in water from the Quaternary deposits.
INTRODUCTION
PURPOSE AND SCOPE OF INVESTIGATION
Through the Montana State College, the U.S. Soil Conserva tion Service, and local organizations, such as the Gallatin Valley Water Users' Association, the residents of the Gallatin Valley urged that a detailed study be made of the water resources of their valley. Plans for such a study materialized in the fall of1950 when, at the request of the U.S. Bureau of Reclamation, the U.S. Geological Survey agreed to evaluate the total water resources of the Gallatin Valley. The study was begun in April1951 and completed in June 1954.
In making this study it was necessary to ascertain (a) the amount of water entering and leaving the valley; (b) the occur rence and availability of ground water; (c) the source, rate, and quantity of ground-water recharge; (d) the manner, rate, and quantity of ground-water discharge; (e) the seasonal, annual, and long-term changes in ground-water storage; (f) the direction of ground-water movement; (g) the chemical quality and the variations in quality of the water; and (h) the location of those parts of the valley where ground water could be utilized as a source of irrigation supply.
PERSONNEL AND ACKNOWLEDGMENTS
The investigation was under the direct supervision of F. A. Swenson, district geologist of the Ground Water Branch of the Geological Survey. Frank Stermitz, district engineer of the Sur face Water Branch, supervised the collection of streamflow data. P. C. Benedict, regional engineer of the Quality of Water Branch, supervised the chemical-quality phase of the investigation.
INTRODUCTION O
In addition to the authors, several others of the Geological Sur vey participated in the study. M. D. Allison, geologist, and A. J. Rosier, hydraulic engineer, assisted with the fieldwork, and E. R. Jochens, chemist, initiated the quality-of-water studies. C. E. Erdmann, of the Conservation Division, and G. D. Robinson, of the Geologic Division, were especially helpful in the geologic phases of the investigation. The names "Camp Creek Hills" and "Salesville fault" were suggested by P. F. Fix.
An experimental geophysical investigation was made for* the Geological Survey by Dart Wantland, Roxy Root, and R. D. Casey, of the Geophysical Section of the Engineering Geology Branch, U.S. Bureau of Reclamation.
The cooperation and assistance of the following agencies and organizations contributed to the progress of the investigation: U.S. Weather Bureau, U.S. Bureau of Reclamation, U.S. Soil Con servation Service, Montana State College at Bozeman, State En gineer's Office, Gallatin Valley Water Users' Association, Gallatin County Agent's Office, Gallatin County Commissioners, and of ficials of the city of Bozeman and the villages of Belgrade and Manhattan.
The writers are particularly indebted to the residents of the valley who gave information, permitted access to land and use of wells, and acted as observers at precipitation and stream-gag ing stations. Valuable information was furnished by Harry and Bert VanDyken and P. T. Marsh, well drillers, and by the Mon tana Power Co. and the Gallatin Gateway Oil Co.
Unpublished maps of adjacent areas were made available by E. S. Perry, of the Montana School of Mines, and W. J. McMannis. Dr. McMannis, who had prepared his map in partial fulfillment of the requirements for the degree of doctor of philosophy at Princeton University, gave his permission for the inclusion of his representation of bedrock relationships along the west flank of the Bridger Range on the geologic map prepared for this report.
Special thanks are due O. W. Monson, of the Agricultural En gineering Department at Montana State College, for his counsel and active assistance throughout the investigation. Others who assisted are C. C. Bradley and E. R. Dodge, of the Montana State College staff, and A. R. Codd, of the U.S. Soil Conservation Serv ice. During the 1953 field season, several valuable field con sultations were held with Peter Verrall, who then was mapping the geology of the Horseshoe Hills in partial fulfillment of the requirements for the degree of doctor of philosophy at Princeton University.
6 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
PREVIOUS GEOLOGIC AND HYDBOLOGIC INVESTIGATIONS
Peale (1896) mapped and described the general geology of the 60-minute Three Forks quadrangle, which includes the Gal- latin Valley. He was the first geologist to describe the Tertiary strata of this area, naming them the Bozeman lake beds.
Iddings and Weed (1894) described the general geology of an area adjoining the Gallatin Valley on the east.
Douglass1 discussed the relationships and extent of the Tertiary lake basins in western Montana. He included a generalized strati- graphic description of the Tertiary strata in the Madison Valley, which is adjacent to the Gallatin Valley, and dated these strata as Oligocene and Miocene on the basis of vertebrate fossils. Douglass (1903, 1909) also published additional descriptions of vertebrate fossils from the Tertiary strata in several western Montana lake basins, including the Three Forks basin of which the Gallatin Valley is a part.
Later, the age and stratigraphic relationships of the Tertiary strata in the Three Forks basin were determined more accu rately by other investigators. Reports by Wood (1933, 1938), Wood and others (1941), Schultz and Falkenbach (1940, 1941, 1949), and Dorr (1956) are especially significant.
Pardee (1925) published a comprehensive review of the litera ture pertaining to the Tertiary geology of western Montana. Later (1950) he summarized the results of many years of study in a general account of the geology and Cenozoic history of west ern Montana. His discussion of the stratigraphy, history, and structure of the Tertiary strata is of particular interest.
A description of physiographic features in the Gallatin Valley and adjacent areas is included in a comprehensive report by Alden (1953) on the physiography and glacial geology of western Montana. Detailed investigations of areas adjacent to, or in cluding parts of, the Gallatin Valley have been made by Berry (1943), Skeels (1939), Klemme, 2 and McMannis (1955). Each of the reports on these studies contains a geologic map and a de tailed description of the stratigraphy and structural geology. Fix3 described the geologic structure of the Gallatin Valley with particular regard to regional structural relationships.
Several papers that deal with the regional stratigraphy of Mon tana include extensive reference to the Paleozoic section in the
1 Douglass, Earl, 1899, The Neocene lake beds of western Montana and description of some new vertebrates from the Loup Fork: Unpublished master of science thesis, Univ. Montana, 27 p.
2 Klemme, H. D., 1949, Geology of the Sixteen Mile Creek area, Montana: Unpublished doctor of philosophy dissertation, Princeton Univ., 197 p.
3 Fix, P. F., 1940, Structure of Gallatin Valley, Montana: Unpublished doctor of philosophy dissertation, Univ. Colorado, 68 p.
INTRODUCTION 7
Horseshoe Hills along the north margin of the Gallatin Valley. Notable among these are papers on the Cambrian section by Deiss (1936), Berry (1943), Lochman (1950), and Hanson (1952) and on the Devonian section by Sloss and Laird (1946). The Precambrian rocks near Gallatin Gateway at the southern end of the valley are described in detail by Clabaugh (1952), with special reference to the occurrence of corundum.
Reed (1951) briefly described the mines and mineral resources of Gallatin County.
Murdock (1926) described irrigation and drainage in the Gal latin Valley as they existed before 1922. He discussed methods of relieving water shortages in the valley and the drainage of wet areas and also called attention to excessive water loss by seep age and evaporation. Murdock suggested that use of ground water for irrigation not only would provide additional water where needed but also would assist in the drainage of waterlogged land. His paper includes some data on ground-water levels in the valley.
A report by the U.S. Soil Conservation Service (1948) con tains preliminary hydrologic information on the Gallatin Valley; it also proposes a program for a future hydrologic investigation. In a later report for the Soil Conservation Service, Long (1950) presented the results of a drainage investigation in the Central Park subarea at the north end of the valley. In addition to water- level data, logs of observation wells, and a water-table contour map, Long's report contains recommendations concerning drain age procedure.
Debler and Robertson (1937), in a report prepared for the Bureau of Reclamation, described reservoir sites on streams that enter.the Gallatin Valley. The report includes preliminary de signs and estimated costs of dams, an economic survey of the valley, and a partial land classification.
The Montana State Engineer's Office (1953a, b) published two reports on the water resources of Gallatin County. The first report presented the history of land and water use in irrigated areas and the second, detailed maps showing irrigated areas and sources of water supply.
In 1952 and 1953 the Bureau of Reclamation measured all water diverted by canals in the valley and the return surface flow from irrigation. The results were not yet available as of 1954. The Bureau also classified the land and made estimates of water shortages in the valley.
8 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
The soils of the Gallatin Valley were mapped and described by DeYoung and Smith (1936). The history of the Gallatin Valley, its settlements and institutions, is described in a publication by the Montana Institute of the Arts (1951).
METHODS OF INVESTIGATION
A rather comprehensive stream-gaging program was conducted by personnel of the Surface Water Branch of the Geological Sur vey to determine, within reasonable limits, the surface-water flow into, and out of, the valley during the time of the study. (See pi. 1.) The Gallatin River was gaged where it enters and leaves the valley and at three intermediate points. Gaging stations were maintained also on the 10 principal tributaries. Five of the gaging stations were among those regularly main tained by the Geological Survey; the others were established for this study. To serve as a basis for estimating the discharge of the numerous other streams having a fairly sustained flow of 1 cfs (cubic foot per second) or more, monthly discharge measure ments and some miscellaneous gage readings were obtained. All streams contributing an appreciable amount of water to the valley were measured at least twice. Also, monthly measure ments were made of the large spring-fed streams that rise within the valley.
To obtain a record of the distribution of precipitation in the valley, 14 rain gages were installed in addition to the 4 perma nent gages maintained by the Weather Bureau. (See pi. 1.) These additional stations were established with the cooperation and assistance of the Weather Bureau and were operated through out 1952 and 1953. Eleven of the stations were serviced daily by volunteer observers from among the ranchers of the valley, and 3 accumulation gages were serviced monthly by personnel of the Geological Survey. The daily maximum and minimum tempera tures also were recorded at three of the stations.
More than two-thirds of the wells and springs in the Gallatin Valley were inventoried and all available pertinent data were compiled (table 36). The well locations are'shown on plate 1. Measurement of the water level in 123 wells was made monthly (table 34), and water-stage recorders were installed in 12 wells in order to record water-level fluctuations in detail (table 35).
Reconnaissance mapping of the principal geologic units ex posed in the valley proper was begun in 1952 and completed the following year. The mapping was done on aerial photographs and adjusted to Geological Survey 15-minute topographic quad rangles by means of a sketchmaster. The final geologic map
INTRODUCTION V
(pl. 2), which was compiled from these sheets, includes not only the valley proper but also a marginal belt which was mapped to show the relationship of the valley fill to the consolidated rocks of the mountain flanks. The geology along the east margin of the valley was taken from a map of the Bridger Range by McMan- nis (1955).
Twenty test holes, ranging in depth from 25 to 1,000 feet and totaling 5,966 feet, were drilled under contract during the period 1951-53; their locations are shown on plate 1. Test drilling was the primary source of subsurface geologic data and provided much valuable information on the occurrence of ground water.
During the planning of the investigation, subsurface explora tion by geophysical methods was proposed. It was thought that the seismic (refraction) method would locate the contact between the valley fill and the consolidated rocks of the basement com plex and that resistivity surveying would determine the bound aries of the permeable water-bearing beds within the valley fill. Experiments using both methods were made in the summer and fall of 1951 (Wantland, 1951a, b). The seismic work proved to be of little value, however, partly because adequate control was lacking and partly because the method was poorly suited for depth determinations of the order needed. The resistivity work likewise proved to be of little value, probably because the geologic setting was so complicated. If adequate control had been avail able for verification of the results, geophysical methods of ex ploration probably would have proved worth while.
The hydrologic properties of water-bearing materials were de termined by means of "single-well" pumping tests. Because this type of test can be made with ease, economy, and speed, it was possible to make about 100 such tests. In addition, "multiple- well" pumping tests were made at 4 sites. These latter tests served as a check on the results obtained from the single-well tests.
One hundred and three samples of water for chemical analysis were collected from selected wells, springs, test holes, and streams in all parts of the valley. The analytical results were used in rating the suitability of the water for irrigation and other uses, in correlating water quality with geologic source of the water, and in determining more fully the relationship between surface water and ground water.
WELL-NUMBERING SYSTEM
All wells referred to in this report were assigned numbers in dicating their location within the system of land subdivision of
508919 O-60 2
10 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
the U.S. Bureau of Land Management. (See fig-. 1.) The first letter (capital) of the number indicates the quadrant of the principal meridian and base-line system in which the well is lo^ cated; the letters beg-in with A in the northeast quadrant and proceed counterclockwise. The first numeral of the number de notes the township; the second, the rang-e; and the third, the section in which the well is situated. Lowercased letters follow ing- the section number indicate, respectively, the quarter section, the quarter-quarter section, and the quarter-quarter-quarter sec tion. These subdivisions of the section are designated a, b, c, and d and are assigned in counterclockwise direction, beginning-
R.I W. R. IE. R.8E.
B
C
z <acc.LU-S:
BASE
A
LINE
D
\\\
T. 4 N.
3
2
T.1 N.
T. 1 S.
2
R. 4E.
Well Al-4-16da^
Sec 16
6
7
18
19
30
31
5
8
17
20
29
32
4
9
163
21
28
33
3
10/
/ 15
22
27
34
2[/
11
14
23
26
35
1
12
13
24
25
36
T.1 N.
c I d --
FIGURE 1. Well-numbering system.
GEOGRAPHY 11
in the northeast quarter. If two or more wells are situated in the same tract, they are distinguished by numerals following the lowercased letters.
Springs, test holes, and precipitation stations also were as signed numbers according to the same system.
GEOGRAPHY
LOCATION AND EXTENT OF THE AREA
The Gallatin Valley is an intermontane basin in the Rocky Mountains of southwestern Montana. (See fig. 2.) It lies almost entirely within Gallatin County, is about 25 miles long and 20 miles wide, and has an area of about 540 square miles. A large
FIGURE 2._Map of the Gallatin Valley showing the principal topographic features, drainage,and hydrologic subdivisions.
12 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
tributary valley, that of Dry Creek, projects to the northeast from the main valley. The Bridger and Gallatin Ranges flank the valley on the east and south, the Horseshoe Hills form the north ern boundary, and the topographic divide between the Gallatin and Madison Rivers bounds the valley on the west.
TOPOGRAPHY AND DBAINAGE
Gallatin Canyon, at the upper end of the valley, is the prin cipal inlet for surface water to the valley, and a gorge at Logan, at the lower end, is the only outlet.
The principal part of the Gallatin Valley is bounded on the west by the Gallatin River and on the north and east by the East Gal latin River, Bozeman Creek, and Sourdough Creek.4 It is shaped, in plan view, like a giant powderhorn having for its large end the southern border of the valley and for its apex the northwest ern end of the valley. The land surface gradient of this part of the valley ranges from about 100 feet per mile at the extreme southern, or upper, end to less than 40 feet per mile near the northwestern, or lower, end. From a centrally located axis, this part of the valley slopes toward the Gallatin and East Gallatin Rivers at either side. Its surface is comparatively smooth, and it has little relief except for Goochs Ridge, which extends north ward into the valley between Middle (Hyalite) 5 and South Cotton wood Creeks. The altitude ranges from about 5,400 feet at the upper end of the valley to about 4,100 feet at the lower end.
Adjacent to the floor of the valley on the west are the Camp Creek Hills, remnants of a relatively high partly dissected sur face or group of surfaces that sloped northeastward from the top of the bluffs along the Madison River toward the valley floor. The Camp Creek Hills taper from a maximum width of about 10 miles in their central part to a width of about 2 miles at their northern end. In the southern part of the valley their boundary with the valley floor is marked by a sharp east-facing escarp ment; in the northern part of the valley the escarpment is replaced by a colluvial slope that grades into the Manhattan ter race. The western and southern parts of the Camp Creek Hills area are flat to rolling, but the eastern and northern parts are broken by many draws and small canyons.
* According to a decision by the Board on Geographic Names dated Sept. 5, 1957, Bozeman Creek is formed by the junction of Sourdough and Spring Creeks and flows northward to the East Gallatin River. Sourdough Creek heads in Mystic Lake and flows northwesterly about 10 miles to join Spring Creek and form Bozeman Creek. Locally, however, the names "Sourdough Creek" and "Bozeman Creek" are applied to the entire stretch from Mystic Lake to the East Gallatin River. In this report, therefore, the entire stretch will be referred to as Sourdough (Bozeman) Creek.
5 According to a decision of the Board on Geographic Names dated Nov. 7, 1928, "Hyalite" is the official name of this creek, but, locally, it is also known as Middle Creek. In this report, it is referrred to as Middle (Hyalite) Creek.
GEOGRAPHY 13
The south and east sides of the Gallatin Valley are bordered by coalescing alluvial fans that slope rather steeply from the Gal latin and Bridger Ranges. The Gallatin Range averages about 9,000 to 10,000 feet in crest altitude. Between Middle (Hyalite) and Sourdough (Bozeman) Creeks a broad alluvial fan, the "Boze- man fan," extends out from this range and merges with the valley floor. The Bridger Range is linear and its crest trends north at an average altitude of 8,500 to 9,000 feet. The fans extending from the base of this range either terminate in an escarpment along the East Gallatin River or merge with the river alluvium.
On the north side of the valley is a sharp cliff cut by the Gal latin and East Gallatin Rivers where they impinge on the Horse shoe Hills, a series of northeast-trending ridges that rise about 1,000 feet above the valley floor.
An extension of the valley, the Dry Creek subarea, lies between the Horseshoe Hills and the Bridger Range. This subarea is rolling and cut by draws; it is continuous with, but somewhat wider than, the slopes bounding the southern part of the valley floor (fig. 2), and is considerably higher than the valley floor. Alluvial fans from the Bridger Range extend into the eastern part of the Dry Creek subarea.
The Fort Ellis subarea extends southeastward from Bozeman. Its surface, which also stands above the valley floor, is rolling and somewhat dissected. Alluvial fans from the Gallatin Range border this subarea on the south.
The Gallatin Valley is drained and watered by the Gallatin River and its tributaries. The Gallatin River rises in the north west corner of Yellowstone National Park and flows northward through the Gallatin Canyon between the Gallatin and Madison Ranges. About 80 miles below its source the river enters the Gallatin Valley at a point known as the Gateway. It then arcs gently north-northwestward through the valley for a distance of about 28 miles. At Logan it passes through a small gorge and leaves the valley. Three miles downstream it joins the Madison and Jefferson Rivers to form the Missouri River. The few inter mittent streams that head in the Camp Creek Hills drain directly into the Gallatin River.
The East Gallatin River is the main tributary of the Gallatin River. It rises about 10 miles east of Bozeman near Bozeman Pass, enters the valley about 5 miles east of Bozeman, and arcs northwestward to its confluence with the Gallatin River north of Manhattan. The entire east side of the valley, most of the south
14 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
and north sides, and most of the valley floor are drained by tributaries of the East Gallatin River. Therefore, despite its short length, the East Gallatin River becomes a major stream before it joins the Gallatin River.
Numerous short perennial streams of high gradient enter the valley from the Gallatin and Bridger Ranges. A relatively few small intermittent streams form in the Camp Creek Hills or enter the valley from the Horseshoe Hills. Several small spring-fed streams rise within the valley; most of these discharge into the East Gallatin River.
CLIMATE
The climate of the Gallatin Valley is characterized by long cold winters and short cool summers. Much of the valley is semiarid.
Extreme daily and seasonal fluctuations in temperature are common. The mean annual temperature at Bozeman is 42.0°F, the highest recorded temperature is 112°F, and the lowest re corded is 53 °F below zero. The growing season at Bozeman is about 119 days; that in the lower part of the valley is shorter by several days to a few weeks, probably owing to downvalley move ment of cool air. The average date of the last killing frost at Bozeman is May 22, and that of the first killing frost is Septem ber 18. Departures from this average are common, killing frosts having been recorded in all months of the growing season. The maximum and minimum daily temperatures recorded at three stations near Manhattan, near Menard, and at Anceney dur ing the period May 1952 through January 1954 are given in table 1.
Precipitation in the Gallatin Valley is unevenly distributed. (See fig. 3.) The northern, central, and western parts of the valley receive much less precipitation than do the parts of the valley near the Bridger and Gallatin Ranges.
The average annual precipitation at Bozeman during the en tire period of record, 1869-1953, is 18.16 inches. However, be cause the record before 1895 is fragmentary, the average of 17.81 inches for the period 1895-1953 probably is more nearly repre sentative. (See fig. 4.) As shown by the graph of average monthly precipitation, nearly two-thirds of the precipitation at Bozeman falls during the period April to September. The pre cipitation in May and June amounts to about one-third of the annual precipitation. A secondary maximum, much less than that in the spring, usually occurs in September. The amount of precipitation from year to year, however, is characterized by
TABL
E 1
. D
aily
tem
pera
ture
s at
thr
ee s
tati
ons
in t
he G
alla
tin
Val
ley,
May
195
2 th
roug
h Ja
nuar
y 19
54[H
, h
igh
; L
, lo
w]
Day
1952
May
H
L
June
HL
July
HL
Aug
.
HL
Sep
t.
HL
0<
H
,t. L
Nov
.
HL
Dec
.
HL
1953
Jan
.
HL
Feb
.
HL
Mar
.
HL
Apr
.
HL
May
HL
Ju
H
ne L
July
HL
Aug
.
HL
Sep
t.
HL
Ost
.
HL
Nov
.
HL
Dec
.
H
L
1954
Jan.
H
L
Sta
tion
A2-
3-34
bd
(n
ear
Man
hat
tan
)
1....
.2..
...
3...
..
4...
. .
5...
..
6...
..7.
...
. 8..
...
9...
..
10.... .
11.... .
12. ....
13..
...
14 ...
..
15. ..
..
16..
...
17.... .
18..
...
19..
...
20..
. ..
21.
....
22
...
..23
...
..24
...
..25..
...
26..
...
27..
...
28.....
29.
....
30..
...
31..
...
70 72 65
71
6? 64
64
66 66 75 74
67 62
59
61
64
69
59
64
48
60 71 77 73 63 74
78
70
65 72
'32
'41 '45
'35
40 34 35 44 43
71 79 81
79
87
86 78
77
86 76 82 76 7?,
85
81
73 74
80
74
77
71
69 76 65 59 64
68
82
84
75
42
42 52 45 44
39 54
33 54
29 36
52
46
34
33
44
39
44
34 27 50 45 42 48
39
42
41
7? 7? 86
86
86 77 76
86
90 91
86 66 72 79
87
85
81
79
73
82
71
75 Qfl
85 88 84
88
88
87
93
90
39 40 37 40
40
40 31
34 40 41
54 52
49 38
39
41
37
36
49
42
55
37 38 53 35 39
44
47
37
39
39
86 87 85
82
87
88 89
82
86 74
75 84
89 86
87
84
85
89
86
85
89
96 94 97 89 82
77
84
76
64
64
51 55 53 46
41
48 52 44
48 50 47 40
41 40
38
35
35
35
39
38
36
37 45 41 48 36
37
33
30
39
30
69 84 90
87
81
84 84
84
89 72
76 72
61 70
83
86
87
85
72
74
73
80 82 86 85 89
81
76
85 77
29 28 33
44
44
36 39
38
32 35 46 34 39 19
23
26
32
33
37
31
30
?,4
25 28 26 25
32
32 28
29
76 83 68
61
64
70 79
80
88 70
74 73 60 54
65
65
68
67
72
71
67
70 73 70 65 62
60
65
68
62
57
?,5
25 33
24
24 19 16 22
19 31
23 32
23 18
14
32
18
18
21
17
19
23 17 20 17 15
14
12
11
41
18
56 47 50
66
52
50 58
46
48 53
60 51
51 44
44
36
38 40
43 40
34 28 30 26 24 20
20
17
12 8
?,6
12 5 8 19
17 12
24 22 4 17 11
14 10
29
28
26
20
19
11
11
-1 19 18 -7 -4 -4
-19
-19
-17
25 39 44
35
36
4? 44
38
37 44 41 39
43 37
38
41
30
30
29
31
30
31 27 16 11 15
15
34
41
32
33
-11 ,5 12 3 8 7 7 7 8 13
13 24 24 15 8 14
10
11
16 7 13
-1 9
-?,0
-21
-14
-14
-16 5 16
47
40
34
18 40
48 55 52
57 60
50 38
38
45
42 41
48
50
45
48 52 60 55 38
38 45
48
47
62
12
25
16 -9 10
20
49 38 24 49
34 19
28
40 7 25
29
33
37
32 99 ?,3
34 17
17
17
34
32
37
48 62
53
42
43 55
34
35 38
33 39
35 38
38
38
39
32
28
29
35
41 32 29 38 50 49
41
35 43 32
33 17 28 23
30
18 2 321 9 6
21
15
15
21 4 4 3 8 7
-63 3 31
23
97 34 45 47
45 52
51
56 64
53 52
44 40
51
54
41
46
58
48
44
44 45 66 59 54
68 72
59
57
54
10 -2 -14 27
30
18 19
19
19 23
3?,
27
29 27
17
22
16
16
27
26
21
23 23 17 25 17
26
26
35
15
29
46 58
50
48
45 42
38 4?,
42
44 45
48 41
52
46
40
48
62
70
73
75 58 57 67 78
72
62
46
53
15 8 23
32
33 32
16
19 20
14 23 24 22
27
29
27
13
14
32
33
28 35 31 23 32
46
41
33 28
51 51 60
68
78
83 77
55 5?,
48
40 41
48 58
66
70
66
72
66
58
61
57 66 60 59 65
70
64
57
65
76
31 34 18
20 22
25 31
24
35 31 ?,4
22
27 23
24
25
34
35
47
38
33
32 28 39 38 37
37
50
46
42
35
76 75 48
59
60
67 65
64 75 83
83 75
79 74
74
80
80
76
69
64
77
81 80 65 66 73 78
81
84
90
37 45 43 41
38
41 47
40
34 49
41 40
35 48
42
45
35
39
43
42
30
38 37 36 28 29
34
40
39
39
78 84 86
88
84
87 86
90
92 96
95 98
100 99
90
80
90
94
92
83
84
9?,
93 89 80 90
93
97
93
97
92
55 35 39
37
42
36 39
42 45 42
46 47
49 50
51
37
34
38
40
42
33
34 4.9
38 4?,
42
46
42 47
44 47
89 83 85
88
85
92 96
89
84 75
80 94
91 87
93
91
90
92
95
98
88
90 90 90 81 88
84 74
79
87
87
46 49 43
45
39 4?,
44
43
41 52
37 36 59 49
41
40
44
40
40
41
41
43 4?,
41 29 30
36
44
36
35
37
88 66 64 72
82
87 83
8i
85 87
89 92 87 84
88
83
76
75
81
77
79
84 76 68 78 80
79
78
80
85
42 41 35 29
31
31 33
31 44 31
31 31
33 32
29
39
41
30
41
26
24
37 32 34 21 24
32
31
21
26
77 58 6i
69 72
81 79
82
84 85 7?,
71 77 75
71
70
74
75
71
61
51
50 49 5'?
56 49
66
70
72
62
67
36 34 16
20
19
24 23
23 28 25
2ft
24 29 21
26
25
24
27
32
18
31
26 16 18 25 20
21
19
22
29
37
64 58 53 57
61
56 54
58
55 57
68 67
63 58
67
63
57
33
28
26
39
43 47 4ft
46 50
48
44
45
43
2ft
39 10
11
26
23 16
11
14 16
23 25
24 20
26
34
30 22 0 2
20 25 27 34 26 32 20 22
25 22
4?,
39 37
38 42
45 33
32 47 43
37 49
44 33 45
35
44
39
47
50
36
33 3?,
34 35 42
36
50
45
52
50
27 H 5 12
20 28 0 2 2?,
20 6
25 21 10
20
10 9 8 20
32
27
20 3 11 6 18
22
12 9 16
44 41 41
43
57 5?,
56
46
38 46
31 30
30 39
20 2 11
34
28
-3 5
44 40 11 13 30
38
46
43 42
31 17 25
12
39 22 28
23
201 1 3 10 17
-17
-18
-6
-22
-21
-44
-34 281
-11
-19
-13 10
35
35
TAB
LE 1
. D
aily
tem
per
atu
res
at
thre
e st
ati
ons
in t
he G
alla
tin
Val
ley,
May
195
2 th
roug
h Ja
nuary
19
54
Con
tinu
ed
Day
1952
M
H
ay L
Ju
H
ne L
July
HL
Aug
.
H
L
Sep
t.
HL
Oct
.
HL
Nov
.
HL
Dec
.
HL
1953
Jan.
HL
Feb
.
HL
Mar
.
HL
Apr
.
HL
May
HL
Jun
e
HL
July
HL
Aug
.
HL
Sep
t.
HL
Oct
.
HL
Nov
.
HL
D
H
3C. L
1954
Ja
H
n. L
Sta
tion
A3-
5-18
da (
nea
r M
enar
d)
1...
..2. ...
.3. .
. .
.
5...
. .
6...
..
7.....
8. .
...
9. ....
10..
.. .
11
....
.12. ..
..13..
...
14..
...
15.. ...
16..
. ..
17..
...
18..
...
1 Q
20.....
21.
....
22..
...
23 .....
24 ...
..25
.....
26 ...
..
27...
..28..
. ..
29 .....
30..
...
31.....
70 62 64 62 60
54
54 64
69 70 64
62 48 5? 58 59 64 62 47 56
67 73 69 65
73 60 60
72
54 37 33 35 35
40
33 28
51 40 47
36 32,
35 32 37 38 32 35
34 3fi
43 36
37 44 29
35
72,
77 77 76 86 82 74
76
82 75 82 77 82
67 68 70 75 73 73 68 58
71 58 59 61
63 80 82
71
44 40 46 47 45 49 46 44
54 55
34 30 42
46 40 35 39 49 38 48 39
33 41 39 41
46 43 54
44
68 72,
82,
87 82,
62,
73 84
88 86 77 66 68
74 84 80 76 76 68 75 64 73 88 83 83 78
83 82,
84
87 89
38 39 44 57 50 46 33
53
56 54
51 48 46
40 48 46 42,
43 49 46 52,
36
45 41 39 45
50 43 46
43 49
82,
81 80 83 87 78 79
82
68 71
78 84 83
79 80 81 84 81 86 91 90 92,
84 80 73 79 75
66 57
54 59 51 44 51 51 46
46
47 47
43 44 46
40 39 41 42,
44 46 48 48
47 52,
40 43
42,
37
40 36
64 74 85 84 77 82,
81
80
83 70 76 68 80
66 79 76 78 78 68 69 76 78
79 80 81 83
83 71 79
81
32,
34 45 44 48 42,
41
40 38 40 48 38 36 2,7
32,
34 35 43 49 32,
32,
34 38 36 37 39
37 36 36
39
70 76 64 57 68 75
76
79 67
69 68 44
57 56 54 62 72,
70 65 61 67
68 68 60 63
63 64 58
56 49
36 32,
34 2,7
32,
28
30 2,9
35
31 30 28 2,5
28 31 34 33 27 2,9
28 2,5
24
23 22,
24
39 31
43 41 43 58 52,
47 52
45 45 52
54 53 47
45 59 33 33 35 3Q 40 34 24
24 2,4
2,1 17
18 18 25 2,9
2,6
17 19 2,8
2,7
2,3
21
21 4 18 9Q 2,5
22
26 33 25 2,5
OQ 16 7 1 16 4 2,-5 -7 -11 -8
36 35 36 38 41 40 38
33
33 36
36 42,
42
43 45 45 33 2,6
98 36 32 34
25 18 19 21
35 33 37
39 35
15 18 14 12,
2,2,
14
22
13 16
11 2,8
32 2,2,
20 26 18 2,2,
14 14 19 8 9 -6 -8 -7 __ Q 14 10
10 7
33 30 42,
38 34 2,7
36
41
50 49 44 40 40 38 40 42,
41 36
46 47 45 42
31 41 43
40 53
9 4 2,8
19 14-1
3 26
23
35 31 38 35 19 30 32,
31 31 30 2,9
17
30 32,
30 19 2,1 24
26 35
50 48 52,
48 36 40 45
37 29 29
2,9
34 38
37 35 32,
31 2,8
24 26 35
30 2,8
32,
46
43 2,7
35 36 36 OQ 22,
2,8
15
25
2,3 5 19 15 8 19 2,0
18 2 0 3 8 10 -7 10 22 18
2,0
2,2,
2,0
97 42,
40 41
45
50 46
54 44 43 45 33 38 46 39 36
37 57 53 46
60 63 52 51 44
8 8 2,4
2,6
18
23
18 19
18 30 25
8 18 2,8
31 1Q 19
2,5
2,0
30 21
2,3
36 29
2,3
33
Q7
40 51 50 43 37 35
34
33 31 37
38.
42 07 47 43 36 AC.
CO 69 65 70
55 CO 71
67 53 42 48
20 2,8
on QQ 31 28
24
2,0
18
on 2,8
28 O1 32,
32,
24 2,0
21 on 34 36
37 37 37 37
43 34 31 31
47 48 62,
75 79 71 50
48
42,
38 3Q 48 57
61 65 63 67 58 CO 56 51
62 64
70 66 67
61 70
34 33 2,8
3f)
32 37 29
33 2,8
28
2,0
2,5
26 28 2,8
33 36 45 37 31 30
30 36 33 43 JO 42 41 3Q 37
74 72 45 55 55 56 60 58 72 85
83 80 76 79 70 79 76 73 70 59 73 78
76 ^Q 63 69 79 76 83 86
40 44 40 38 3Q 42,
41
43
35 48 4.^
45 45 V7 42,
43 45 38 44 37
9Q 38
41 33 2,8
30 42,
38 4K
76 80 76 83
88
88 89 S.Q
95 96
94 S.4
82 85 ss 91 78 80 90 93 78 87
93 SQ 90
91 89
38 36 41 64
43 46 45 48 50 54 64 54 39 36 43 40 37 3Q
51 41 43 48
47 48
84 72,
80 75 7Q 86 93
88
82 67
78 89 90
86 88 88 85 8QQQ
Q3 85 85
86 81 85 81 73 75
OA
49 52,
41 48 40 42,
46 49
41 48
34 42,
43 44 44 43 43 42,
^3
46 44
36 29 36 38 3Q 36
36
84 68 59 67 77 83 86
62 82,
83
87 84 80 85 85 82,
69 71 76 64 79 79
69 62,
73 74 77 75 63 80
44 40 31 97
31 33 37
39
36 36
42 43 38 33 47 43 30 42,
2,8
31 40
36 3Q 2,7
26
38 34 25
34
72 52,
58 69 72,
71 74 78
79 80
70 69 74 72 70 64 69 70 60 58 44 45 48
59 67 67
54
42,
31 16 2,4
2,3
31 28
30
40 34
37 2,8
29
33 33 37 33 30 36 2,0
30 27 22
30 2,5
29
2,4
41
65 54 52 57 57 45
57
57 59
63 63 51
53 54 9Q 2,4
Ofi
35 39
42,
3Q 45 43
42,
43
47
31 2,0
12,
2,7
18
16
19 20 2,7
2,9
28 9Q 26 2,0
_o 10 2,0
32
30 2,4
2,2,
29
2,8
2,0
31
26
33 32,
34 3^ 38 28
25
43 37
32,
34 32
41 40 36 43 42,
43 43 34 23
30 31 33 39
32,
42,
32
32,
43
Ofi
15 17 1 9 26 3 4 14 22 6 in 10
19 in 9 15 11 21 32 15 6 6 12 13
13 25 14
12 26
43 47 49 49
40
30 31 24 24 24
35 0 28 30 22 28 30 42
39 13 18 26
35 4* 38
46 41
10 32 32 22
28
14 8 0 5 5
-14 -7 -12 1 9
-36
97 14
10-1
2-18 10
12 31 32 20
i-IO OJ h--OJ OCOCOOOC5-
eotf-tf-cooicoenco- co en onf en as en en coco o- os » * en to i-1 m coen-
- CO >fr. O to CO COco- ciientf-co-
tOOOOOOOOOOOOOOO- 0000<IO50000<IOOOO-->l tO M 00 CO CO Qi
O CO QUO CO I Oa CO K) OOP-
OOOOOOOOOO W ^11 w W
~3 C5 ~J ~3 00 00 "COCOOO5 to WQ
oo en to oo co en c
to >f to i-1 to to to to to to co co co to to i-1 to to co to co to to to to to to co to co COi-'OO5 i-'COi-'COOS COOOtOOS0105O5 tft'tocooarf^-ootoT en rf»> rf»" en rf»> en i *" CO 00 O5 00 00 ooooMCocooa
-1 CO O5 CO O O5 I-1 ~J C
cowcotoco- acoOi-'Oao > co co to co co co scOOOCOMOsen
^t-1 *.tooo toco>to to to i-1 to co co co
-~IOOtOOOOOaOiCnOtOK)Oi-
co to co co to to co to to to to co co to t COi-'lMOi>fCOrf^tOO3O5tOO3lOi-'
00 Oi CO 00 CO
to co co tf- eo to co i,5VI lOOS^-O
..*-enMoovi- onftf iMCneni-'OS' encooo
JOOOOOOMO5O5O5S 3 10 Oi i-1 O O to W l.
OOOOO500COOO<IOOCOOO^IOOOOOO.coooaiaicoenoooii-'coooo«-^iHi rt* H^tOCOO)
CO CO tf.tf.tf". CO CO en Cn Oi Cn O5 t
500COCOOOOO<IOOMOO
o oa to co oo gjJ<I<IMO5MOO<IO5M<l OOOOMOOOOOOOOO D 00 O5 tf *« O O ^ tOCOCO- IO O5 00 0^- CO rf* to to CO
CO K)^ --* * ^ I tocoi-" I CO to to to CO CO CO en en en tf». >*-. CO t
tototocoi I (-i-1OOOOCni-'OSCOtt'ttOCnCOO^OSOi
LI
18 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
FIGURE 3. Map of the Gallatin Valley showing the location of precipitation stations and the dis tribution of precipitation in 1952.
many departures from average. The precipitation trends dur ing the period 1895-1953 are indicated by the graph showing the cumulative departure from average; above-average precipita-
GEOGRAPHY 19
i 20T?
/o
_ _ _. /7-*f- ^/
/ / / / S /
/ / / / / >
/ / ' / s
* V A
////' / / / / '/ y/ ' / /s// s // / / /'
VERAGEM8.I6
/ / / r
////
/ / / / / // /
/ r /
fBf ' ''*"'''''Witi % 1
v\
w^ sp;; f \''////< 7/; \ '#$%'"'*'>/, '*,////"S"j //////''" / /''''<.'A'A>t.'''''<t't //i " '
V '^'^
'// 'ii
CUMULATIVE DEPARTURE FROM AVERAGE PRECIPITATION, 1895-1953
AVERAGE-17.81
FIGURE 4. Precipitation at Bozeman. From records of the U.S. Weather Bureau.
tion is represented by a rising line and below-average precipita tion by a falling line.
The annual precipitation for the period of record at Bozeman and at Belgrade is given in tables 2 and 3, respectively; the monthly precipitation during the period 1952-53 for all stations is given in table 4.
The monthly volume of precipitation on the Gallatin Valley, excluding the Dry Creek subarea, during water years 1952 and
TABLE 2. Annual precipitation at Bozeman, 1869-1953[From records of the U.S. Weather Bureau]
Year
1869 .........1870 .........1871 .........1872.........1873 .........1874.........1875 .........1876.........1877 .........1878 .........1879 .........1880 .........1881 .........1882 .........1883 .........1884 .........1885 .........1886. ........1887.........1888. ........1889 .........1890. ........
Inches
19.54
19.7419.41
15.6621.5021.0830.1617.5519.6816.4822.0232.63
Year
1891 .......1 CQO
1893 .......1894.. .....1895 .......1896.......1897 .......1898. ......1899 .......1900... ....1901. ......1902 .......1903..... . .1904...... .1905.......1906. ......1907 .......1908. ......1909 .......1910... ....1911. ......
Inches
18.1615.4717.4217.2013.4414.18
17.6416.1914.7316.8817.2324.4722.3418.7418.14
Year
1912... ....1Q1 Q
1914... ....
1916. ......1917... ....1918.......1919... ....1920 .......1921. ......1922 .......1923 .......1924... ....1925 .......
1927 .......1928...1929 .......1930 .......1931. ......1932 .......
Inches
21.6518.67
25.0021.1915.6818.8911.0219.2515.1917.7415.2720.9419.4019.8221.8419.1815.7714.1715.2917.34
Year
1933 .......1QQ4.
1935 .......1936..... ..1937 .......1938.... ...1939 .......1940 .......1941.......1942 .......1943 .......1944.. .....1945. ......1946.......1947 .......1948.......1949 .......1950 .......1951... ....1952 .......1953 .......
Inches
15.8910.5415.4612.7817.9920.3514.0318.6322.8717.2417.1820.9319.5318.5824.5419.5017.1118.1920.2019.5716.40
20 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
TABLE 3. Annual precipitation at Belgrade, 1941-53[From records of the U.S. Weather Bureau]
Year
1941....... ..1942 .........1943.........1944
Inches
17.1012.3813.5014.89
Year
1945 .......1946 .......1947 .......
Inches
12.6512.1218.35
Year
1948 .......19491950. ......
Inches
19 7013.5715.11
1
Year
1951. ......1952.... .. .1953... ....
Inches
13.8113.8312.04
1953 was computed by multiplying the monthly precipitation at each station by an area that was determined by the Theissen method of weighting (Theissen, 1911, p. 1082-1084) and then totaling the products thus obtained. (See table 5.) Because sev eral of the stations were not in operation during the period Oc tober through December 1951, estimates of precipitation at these stations were made on the basis of measured precipitation at other stations in the valley.
HISTORY
The Lewis and Clark expedition visited the Gallatin Valley in 1805. The settlement of the valley was not begun, however, until the mining communities, established as a result of the discovery of gold in the early 1860's, created a demand for agricultural products. The first irrigation ditch was dug in 1864, and the arrival of the Northern Pacific Railway in 1883 gave added im petus to the settlement of the valley.
The population of Gallatin County in 1950 was 21,902, and most of the people lived in the valley. In addition to being the leading trading center, Bozeman is the county seat and the site of the Montana State College. Its population in 1950 was 11,325. Belgrade and Manhattan also are important trading centers.
AGRICULTURE AND INDUSTRY
Farming and livestock raising are the principal occupations in the Gallatin Valley. Most of the cropland on the valley floor, the Bozeman fan, and the Manhattan terrace is irrigated, as are about one-third of the Camp Creek Hills and scattered tracts in the eastern and northern parts of the valley. (See fig. 5.) Ac cording to data compiled by the Montana State Engineer's office (1953a, p. 27-30), 107,261 acres was irrigated in 1952. Irrigation water is diverted from the Gallatin River, the East Gallatin River, and their tributaries. Because the growing season is short, only small grains, forage crops, and vegetables such as peas and po tatoes are grown. Most of the remaining area is dry farmed, wheat being the main crop. In general, individual dry farms are
TABL
E 4.
Mon
thly
pre
cipi
tati
on a
t 18
sta
tion
s in
the
Gal
lati
n V
alle
y, 1
952-
58
Sta
tion a
nd
ob
serv
er
Al-
3-1
6bb,
Pau
l B
ieri
ng. ..
....
....
Al-
6-1
6bd,
C.
W.
Cra
mer
. ..
....
...
A2-2
-9aa
, U
.S.
Wea
ther
Bure
au,
Tri
den
t ..
....
....
....
....
....
..
A2-5
-14bb,
U.S
. G
eol.
Su
rvey
. ..
...
A3-5
-18da,
Del
mer
Mo
ore
...
....
..
Dl-
2-1
3aa
, U
.S.
Geo
l. S
urv
ey. ..
...
Dl-
3-1
4ab
, H
. I.
Vis
ser.
...........
Dl-
4-2
2da,
Geo
rge
Nutt
er.
........
Dl-
5-6
cd,
U.S
. W
eath
er B
ure
au,
D2-3
-21ad
, N
ick
Dan
ho
f . ..
....
...
D2
-4-1
3cc
, L
. B
. C
lary
. ..
....
....
.
Alt
itu
de
(fee
t)
4,3
10
5,0
40
4,0
36
4,1
67
4,3
05
5,6
00
5,0
53
4,8
40
4,4
70
4,5
50
4,4
50
4,7
55
4,7
35
4,9
10
Yea
r
f 19
52
\ 19
53
/ 19
52
\ 19
53
/ 19
52
\ 19
53
/ 19
52
\ 19
53
/ 19
52
\ 19
53
/ 19
52
\ 19
53
/ 19
52
\ 19
53
/ 19
52
1 19
53
/ 19
52
\ 19
53
/ 19
52
\ 19
53
/ 19
52
\ 19
53
/ 19
52
\ 19
53
/ 19
52
\ 19
53
/ 19
52
\ 19
53
Pre
cip
itat
ion
, in
in
ches
Jan.
0.3
7
.49
1.3
2
.81
.43
.48
1 .4
8 .6
3
.58
.70
.84
.62
.90
.73
1 .5
1 .3
5
.41
.78
.94
.45
.92
.55
.62
.28
.93
.36
.68
.38
Feb
.
0.3
8
.86
1.5
3
1.7
7
.32
.73
.34
.80
.40
1.0
2
.58
1.5
1
.80
1.3
0
.36
.89
1 .2
8 .7
4
.66
.78
.65
1.0
0
.44
1.2
4
.90
1.0
5
.63
.90
Mar
.
1.0
5
.28
2.1
4
.73
.97
.37
1.1
3
.43
1.1
5
.32
1.0
4
.59
1.2
0
.38
.76
.39
.50
.40
.86
.69
1.0
8
.67
.83
.53
1,1
3
1.1
1
.94
.83
Ap
r.
0.7
8
1.2
0
1.2
0
2.4
1
.77
1.2
3
.53
1.3
0
.52
1.2
2
.93
1.8
3
.50
1.2
8
.85
1.9
3
.56
1.5
6
.85
1.8
9
.80
1.6
3
1.21
1.7
3
1.4
3
1.7
1
1.4
4
1.7
4
May
3.8
7
2.0
1
6.2
1
5.7
0
4.2
2
2.2
3
4.0
42.2
6
3.9
5
2.5
4
4.9
9
3.6
3
5.1
4
2.7
7
4.5
9
2.4
3
3.9
1
2.4
7
4.2
5
1.6
0
4.4
7
2.4
6
5.3
8
2.2
8
4.9
6
2.3
1
4.5
3
2.2
0
Jun
e
1.4
4
2.0
7
2.8
5
4.9
9
2.1
7
2.3
8
1.3
2
2.5
6
.35
2.8
2
1.3
7
3.9
3
1.5
8
2.9
2
1.6
1
2.6
9
1.4
2
2.4
0
1.0
4
2.1
1
1.6
5
2.9
5
1.9
3
2.1
8
1.6
1
2.9
8
1.9
7
2.3
9
July
1.7
4
.09
2.2
6
.30
1.8
7
.10
1.8
8
.15
1.8
6
.17
1.9
8
.27
2.6
1
.39
1.7
7
.13
1.8
4
.17
1.3
0
.39
2.1
4
.23
1.8
6
.46
1 1.5
0
.59
1.4
2
.37
Aug
.
0.8
6
.33
1.0
2
.90
.63
.91
.46
.37
1.0
1
.79
1.2
9
1.0
5
.54
.88
.83
.83
.52
.72
.26
.21
.50
.32
1.0
2
.44
.83
Tra
ce
1.2
3
.22
Sep
t.
0.1
3
.28
.90
1.2
7
.23
.27
.21
.45
.44
.50
.52
.65
.38
.41
.45
.51
.37
.55
.54
.44
.36
.72
.61
.58
.48
.68
.59
.66
Ost
.
Tra
ce
.40
.37
.69
.01
.38
Tra
ce
.39
.13
.58
.24
.40
.04
.39
.07
.36
.00
.47
.05
.52
.12
.54
.05
.56
.10
.74
.07
.47
Nov.
0.8
4
.54
1.4
1
.99
.69
.50
.63
.46
.92
.43
1.0
1
.61
.77
.60
.65
.46
.60
.31
.52
.40
.70
.65
.77
.89
.83
.81
.84
.55
Dec
.
0.2
6
1 .1
8
.89
.93
.14
.22
.24
.23
.40
.41
.44
.70
.40
.5
8
.36
.16
.40
.05
.43
.11
.44
.32
.28
.19
.32
.51
.28
.29
To
tal
11
.72
8.7
3
22
.10
2
1.4
9
12
.45
9.8
0
11
.26
1
0.0
3
11
.71
1
1.5
0
15
.23
1
5.7
9
14
.86
1
2.6
3
12
.81
1
1.1
3
10
.81
1
0.6
2
11
.70
9.5
9
13
.83
1
2.0
4
15
.00
1
1.3
6
15
.02
1
2.8
5
14
.62
1
1.0
0
TAB
LE 4
. M
onth
ly p
reci
pit
ati
on a
t 18
sta
tion
s in
the
Gal
lati
n V
alle
y, 1
95
2-5
3 C
onti
nued
Sta
tio
n a
nd
obse
rver
D2
-5~
l3ab
, U
.S.
Wea
ther
Bure
au,
D4-4
-28,
U.S
. W
eath
er B
ure
au,
Alt
itude
(fee
t)
4,8
56
5,0
90
5,0
15
5,4
25
Yea
r
/ 19
52
\ 19
53
/ 19
52
\ 19
53
/ 19
52
\ 19
53
/ 19
52
\ 19
53
Pre
cip
itat
ion
, in
in
ches
Jan.
1.2
4
.65
1.1
0
.90
2.0
1.2
7
1.4
4
.60
Feb
.
1.1
9
1.0
5
1.1
5
1.2
8
1.1
5
1.2
1
1.1
7
1.8
2
Mar
.
1.5
9
1.0
4
1.5
4
1.3
3
1.2
8
1.2
0
1.81
1
.29
Apr.
1.9
9
2.0
5
1.8
0
1.8
2
2.4
4
2.4
1
2.5
2
1.4
8
May
6.6
3
3.2
3
5.7
3
3.3
3
6.2
32.4
2
6.5
5
2.6
2
June
2.0
2
3.1
3
1.7
8
3.8
8
2.1
2
2.8
4
2.0
3
3.8
4
July
1.2
8
.63
1,2
5
.51
1.'4
5 .7
2
2.2
9
.62
Aug
.
1.1
6
.42
1.1
2
.84
1.3
2
.08
1.8
6
.64
Sep
t.
.56
1.0
0
.42
1.3
7
.66
.78
.79
1.4
8
Oct
.
.21
1.3
9
.26
.83
.16
1.0
4
.54
.41
Nov
.
1.2
9
1.1
3
1.2
9
1.0
5
1.0
2
.80
1.2
0
1.4
9
Dec
.
.41
.68
.46
1.1
2
.26
.51
.52
1.3
0
To
tal
19
.57
1
6.4
0
17
.90
1
8.2
6
20
.10
1
4.2
8
22
.72
1
7.5
9
to
to g o
f
o .9 O in 8 8 H
yi O
lEst
imat
ed.
O
2
1-3
GEOGRAPHY 23
TABLE 5. Monthly volume of precipitation on the Gallatin Valley in water years 1952 and 1953, in thousands of acre-feet
Month
November .................................December .................................
February ..................................March ....................................
May. .....................................
July. .....................................August ....................................September .................................
Total ...............................
Water year
1952
77.0 11.2 33.6 26.3 20.9 33.3 35.3
135.2 46.8 48.8 26.1 13.8
508.3
1953
3.5 25.7 11.1 15.5 30.3 20.8 50.5 76.0 82.3 10.5 13.1 20.1
359.4
much larger than irrigated farms, but their total area in the val ley is smaller.
Throughout most of the valley, livestock is raised in conjunc tion with the growing of crops. Many of the cattle are sold for beef, but dairy herds also are important sources of income, and some sheep, hogs, and horses are raised.
Industry has a minor but important place in the development of the valley. Logging, an important activity in earlier years, has been resumed recently in the adjacent mountainous regions, and the new sawmill at Belgrade is the largest single industrial plant in the valley. Flour mills, livestock-commission yards, apiaries, a seed company, and a cheese factory are the other chief indus trial enterprises. The headquarters for the Gallatin National Forest are at Bozeman, and a federally owned fish hatchery is situated at the mouth of Bridger Canyon, about 3 miles northeast of Bozeman. During the summer the tourist trade is important; many dude ranches are near the valley, and Yellowstone Na tional Park is only a few hours' drive from Bozeman.
TBANSPOBTATION
The Gallatin Valley is served by the main line of the Northern Pacific Railway and by a branch line of the Chicago, Milwaukee, St. Paul and Pacific Railroad. A transcontinental highway, U.S. 10, passes through Bozeman, Belgrade, Manhattan, and Logan; U.S. 191 connects Bozeman with points to the south. An ade quate system of secondary roads covers the area. Gallatin Field,
26 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
EXPLANATION
FIGURE 6. Map showing the relation of the Gallatin Valley to the Three Forks basin.
peripheral mountains. In summarizing the age, lithology, thick ness, and relationships of the Precambrian, Paleozoic, and Meso- zoic rocks, the writers have drawn freely on reports by Peale (1896), Berry (1943), Deiss (1936), Gardner and others (1945), Sloss and Laird (1946), Lochman (1950), Sloss and Moritz (1951), Hanson (1952), and McMannis (1955).
PRECAMBRIAN ROCKS
Precambrian metamorphic and sedimentary rocks are the old est rocks exposed in the valley. The metamorphic rocks, called
GEOLOGY 27
Archean gneiss by Peale (1896, p. 3), are principally varieties of gneiss, though schist, quartzite, and, locally, marble also are present. Outcrops of metamorphic rocks at the south end of the Camp Creek Hills are thought by Clabaugh (1952, p. 61) to belong to the Pony series (Tansley and Schafer, 1933) of pre- Beltian age. Gneissic rocks are exposed along the base of the southern part of the Bridger Range, along much of the base of the Gallatin Range, and in the southern and southwestern parts of the Camp Creek Hills. Test holes D2-4-9bc and Dl-3-36bc, drilled north of the Precambrian outcrop in the Camp Creek Hills, pen etrated the Tertiary strata; the former was bottomed in Pre cambrian gneiss and the latter in what was thought to be weathered Precambrian gneiss. (See table 33.) Possibly the gneissic rocks underlie the Tertiary strata in most places in the southern part of the valley.
The Precambrian sedimentary rocks belong to the Belt series, which has not been subdivided into formations in the Gallatin Valley area. They consist mostly of arkosic sandstone and con glomerate, graywacke conglomerate, and slate; most of these rocks are dark colored, but some in the vicinity of Dry Creek are bright colored. The Belt series is exposed along the base of the Horseshoe Hills, along Dry Creek, and along the base of the northern part of the Bridger Range. The maximum exposed thickness is about 6,000 feet. Within the valley proper these rocks crop out along the south side of the Gallatin River in the stretch 11/2 to 3 miles east of Logan. Test hole A2-3-33da was bottomed in strata of the Belt series. (See table 33.) The Belt series is believed by the authors to underlie the Tertiary strata in the northern part of the valley.
The Precambrian rocks in the valley are not considered .a po tential source of ground water; generally they are too far below the surface to be economically accessible to wells. The two test holes drilled to the gneissic rocks yielded small quantities of wa ter, some of which may have been derived from weathered bed rock. Small quantities of water also may be present in fractures in the gneiss and in rocks of the Belt series.
ROCKS OF PALJBOZOIC AGE
Marine rocks of Cambrian, Devonian, Mississippian, Pennsyl- vanian, and possibly Permian age are present in the Gallatin Valley and vicinity. These Paleozoic rocks crop out along the flanks of the Horseshoe Hills and the Gallatin and Bridger Ranges. They also locally underlie Tertiary and Quaternary de-
28 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
posits in the vicinity of Logan and in the Camp Creek Hills west of Gallatin Gateway.
No wells within the valley derive water from the Paleozoic rocks.
CAMBRIAN SYSTEM
The Cambrian system is represented by the Flathead quartzite, Wolsey shale, Meagher limestone, and Park shale, all of Middle Cambrian age, and the Pilgrim limestone and Snowy Range formation of Late Cambrian age. An unconformity separates the Cambrian rocks from the underlying Precambrian rocks, and there is a disconformity between the Cambrian rocks and the overlying Devonian system. Within the Cambrian system the contacts between formations are conformable and gradational.
The Flathead quartzite is a resistant, ridge-forming forma tion composed principally of pink and reddish-brown quartzite and sandstone. The average thickness of the Flathead is about 130 feet; however, in the Gallatin Range the Flathead thins to less than 100 feet.
The Wolsey shale, which overlies the Flathead quartzite, is a greenish-gray, black, and purple micaceous shale, interbedded in its lower part with quartzite and sandstone and in its upper part with limestone. Worm casts in the sandy layers charac terize the basal part. The Wolsey weathers readily, and, where steeply dipping, usually forms a troughlike depression between outcrops of the Flathead quartzite and the Meagher limestone. The thickness of the Wolsey shale differs considerably from place to place but averages about 200 feet.
The Meagher limestone is a massive-appearing cliff-forming gray to brown limestone, interbedded with shale near its base. Parts of this formation are mottled. The Meagher limestone has a relatively uniform thickness of about 350 feet.
The Park shale is mostly green, brown, and maroon fissile shale, containing limestone layers in its basal part. Like the Wolsey shale, it weathers more readily than the immediately underlying and overlying formations. Its average thickness is about 200 feet.
The Pilgrim limestone is similar in general appearance to the Meagher limestone. It is a massive-appearing cliff-forming gray to brown limestone containing many layers of dark, mottled oolite and limestone conglomerate. It is about 400 feet thick. The term Maurice limestone also has been applied to this forma tion in the vicinity of the Gallatin Valley (Lochman, 1950, p. 2205).
GEOLOGY 29
Overlying the Pilgrim limestone is a mappable unit consisting, in its lower part, of strata of Late Cambrian age and, in its upper part, of strata of Devonian age. Sloss and Laird (1946) were the first to recognize the age of these strata and the pres ence of an erosional surface at the top of the Cambrian. Loch- man (1950, p. 2212-2213) applied the term Snowy Range for mation to the Late Cambrian strata, and Emmons and Calkins (1913) applied the term May wood formation to the Devonian. Lochman described the Snowy Range formation as follows:
Within the Snowy Range formation two members can be recognized: the lower Dry Creek shale member of interbedded shales and calcareous sand stone * * * and the upper Sage pebble-conglomerate member of intercalated shales and limestone pebble conglomerates with a dense columnar limestone near the base * * *
The thickness of the Snowy Range formation was not ascertained, but it is known to vary considerably because the Sage pebble- conglomerate member was subjected to deep erosion before the overlying Maywood formation was deposited. However, the com bined thickness of the Snowy Range and Maywood formations ranges from a little less than 100 to slightly more than 250 feet. Hanson (1952, p. 17-18) identified Lochman's Snowy Range for mation as the Red Lion formation of Emmons and Calkins (1913).
DEVONIAN, MISSISSIPPIAN, AND PENNSYLVANIA^ SYSTEMS
The Maywood formation of Devonian age consists of red shale and gray to yellow silty dolomite and limestone. Because it was deposited on the eroded surface of the Sage pebble-conglomerate member (Lochman, 1950, p. 2212) of the Snowy Range forma tion, it varies considerably in thickness but, combined with the Snowy Range formation, is nowhere much more than 250 feet thick.
The Jefferson limestone, also of Devonian age, rests conform ably on the Maywood formation. It consists of gray and dark- brown limestone and dolomite and is characterized by a pet roliferous odor when freshly broken. It forms massive-appearing cliffs which are distinguishable by their dark color from the other limestone cliffs within the area. The thickness of the for mation averages about 550 feet.
The Three Forks shale of Late Devonian and Mississippian age conformably overlies the Jefferson limestone and, in gen eral, is divisible info three units a basal unit of varicolored shale and limestone capped with ledge-forming gray and yellow limestone; a central unit of green and purple shale; and an upper unit of gray limestone, yellow sandy limestone, and calcareous sandstone. Berry (1943, p. 14-15) applied the term Sappington
30 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
sandstone to the sandy limestone of the upper unit and con sidered it to be of Mississippian age. Sloss and Laird (1946) be lieved the Sappington to be of Devonian age and designated it as a local member of the Three Forks shale. The age of the Sappington is now considered to be Late Devonian and Mississip pian. The average thickness of the Three Forks as a whole is about 200 feet.
The Madison group of Mississippian age lies unconformably on the Three Forks shale and includes the Lodgepole limestone, which is a well-laminated gray and yellow to brown limestone, and the Mission Canyon limestone, which is a massive light-gray limestone. The Madison group was not differentiated in this study. The thickness of the Madison in the vicinity of Gallatin Valley ranges from about 1,200 to 1,500 feet or more.
The Big Snowy group, which overlies the Madison group and underlies the Amsden formation in the Bridger Range (McMan- nis, 1955) was not recognized in the area mapped for this report.
The Amsden formation, in part of Mississippian age and in part of Pennsylvanian age, rests disconformably on the Madison group. The Amsden consists of a lower unit of red siltstone and limestone, which weathers readily, and an upper unit of light- yellow to gray dolomite which is interlayered with quartzite near the contact with the overlying Quadrant quartzite. The Amsden formation is about 400 feet thick in the Horseshoe Hills and about 200 feet thick in the Gallatin Range southeast of Bozeman.
The Quadrant quartzite of Pennsylvanian age is conforma ble to, and gradational with, the Amsden formation and consists almost wholly of white and pink to light-yellow massive quartzite or quartzitic sandstone. Dolomite, similar to that of the Amsden formation, generally is present at the base of the Quadrant, and in some places layers of brown chert are in the upper part. This formation is a prominent cliff former. It ranges in thickness from about 75 to 150 feet.
PERMIAN SYSTEM
Although the Phosphoria formation was not recognized among the Paleozoic rocks exposed in the area, it may be represented by layers of chert and quartzite on top of the Quadrant quartzite in the Dry Creek subarea. The Phosphoria is present in the Horseshoe Hills west of the Dry Creek subarea.
ROCKS OF MESOZOIC AGE
Rocks of Jurassic and Cretaceous age crop out along the north west margin of the Dry Creek subarea and east and southeast
GEOLOGY 31
of the Fort Ellis subarea. They are not a source of ground wa ter in the Gallatin Valley.
JURASSIC SYSTEM
The Jurassic system is represented by the marine Ellis group of Middle and Late Jurassic age and the continental Morrison formation of Late Jurassic age.
The Ellis group comprises the Sawtooth, Rierdon, and Swift formations but was mapped as a unit in this study. From a thickness of more than 300 feet southeast of Bozeman, the Ellis group thins northward to a thickness of about 20 feet near Menard. The Sawtooth formation rests disconformably on the Quadrant and is predominantly a gray to brown shale and lime stone. It is the least conspicuous formation of the Ellis group in the Gallatin Valley. The Rierdon formation, conformable to the Sawtooth, is composed of distinctive brown oolitic limestone interbedded with shale. The Swift formation, separated by a dis- conformity from the Rierdon, is a glauconitic and calcareous brown sandstone and generally is conglomeratic at its base. This formation was not recognized in the vicinity of Menard, but where present elsewhere in the area it forms prominent cliffs.
The Morrison formation rests conformably on the Ellis group. It consists of varicolored red, brown, purple, and gray siltstone and shale interbedded with brown to yellow sandstone. In some places a few feet of coal and carbonaceous shale are present in the upper part of the unit. Because the Morrison weathers rap idly where exposed, its presence generally is marked by a red soil-covered slope below the more resistant basal unit of the overlying Kootenai formation. The thickness of the Morrison ranges from about 100 to 400 feet.
CRETACEOUS SYSTEM
The Cretaceous system is represented by the continental Kootenai formation, the marine Colorado shale, and the conti nental Livingston formation.
The Kootenai formation consists of three units. The basal unit is resistant quartzitic sandstone that generally is conglom eratic in its lower part. The middle unit is nonresistant red to purple shale, siltstone, and claystone; it includes also a bed of massive pinkish-gray limestone in the area southeast of the Fort Ellis subarea. The upper unit is a resistant, locally quartzitic sandstone; in the vicinity of Menard and in the Fort Ellis sub- area, this unit contains a thin notably fossiliferous limestone bed near its top. The thickness of the Kootenai formation ranges
32 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
from about 400 to 700 feet. At least locally, the con tact of the Kootenai with the underlying Morrison formation is a disconformity.
Only the lower part of the Colorado shale is exposed in the area. In the vicinity of Menard it consists only of black and gray shale and thin beds of rusty-colored sandstone, but in the area southeast of the Fort Ellis subarea it also contains massive green ish-gray sandstone.
ROCKS OF MESOZOIC AND CENOZOIC AGE
CRETACEOUS AND TERTIARY SYSTEMS
The Livingston formation of Late Cretaceous and Paleozoic age crops out at the extreme north end of the Dry Creek sub- area and also southeast of Bridger Canyon. It consists prin cipally of andesitic tuff and volcanic conglomerate.
ROCKS OF CENOZOIC AGE
The Cenozoic rocks constitute the valley fill and are the pri mary source of ground water in the Gallatin Valley.
TERTIARY SYSTEM
Continental deposits of Tertiary age in the Three Forks struc tural basin were named Bozeman lake beds by Peale (1896, p. 3). However, the term "lake beds" now is considered to be a mis nomer, because only part of the Tertiary section is of lacustrine origin. In this report, therefore, the deposits are referred to simply as Tertiary strata.
The Tertiary strata crop out in the Camp Creek Hills, the Dry Creek subarea, the Fort Ellis subarea, and along Goochs Ridge; except locally, they underlie the alluvium and alluvial fans throughout the valley. Where exposed along the margins of the Gallatin Valley, most of the strata of Tertiary age are moder ately well cemented fanglomerate, consisting of poorly sorted locally derived rock fragments in a matrix of clay or calcareous silt and sand. Toward the center of the basin the Tertiary strata are finer grained and consist principally of tuffaceous siltstone and fine-grained tuffaceous sandstone, which in places are inter- bedded with marl, pure ash, crossbedded sandstone, and con glomerate. Most of the Tertiary strata are poorly consolidated, but some are well consolidated.
The complete thickness of the Tertiary strata is not exposed in the basin. Test holes A2-3-33da, Dl-3-36bc, and D2-4-9bc, which bottomed in Precambrian rock, were drilled through 245, 836, and 515 feet of Tertiary strata, respectively. Other evidence,
GEOLOGY 33
however, indicates that the Tertiary strata are much thicker in the deepest part of the structural basin. Peale (1896, p. 3) estimated the maximum thickness of the Tertiary in the Galla- tin Valley to be between 2,000 and 2,500 feet by assuming that the beds exposed in the bluffs overlooking the Madison River are older than the beds east of Bozeman and that the gentle east ward dip of the beds is not disturbed by faulting. A test hole drilled by the Montana Power Co. in the Madison Valley pene trated 1,182 feet of Tertiary strata older than the 1,300 feet of Tertiary strata exposed in the bluffs overlooking the Madison River; also, an oil test (Tom Tice 1, drilled by Ben Ryan) in the Madison Valley reportedly penetrated claystone and siltstone, probably of Tertiary age, at a depth of 2,000 feet. This addi tional subsurface information increases the estimated maximum thickness of the Tertiary strata in the Gallatin Valley to at least 4,000 feet.
Available subsurface information and exposures near Anceney indicate that the Tertiary strata rest on a surface of moderate relief. This surface probably was produced by erosion and modi fied by Tertiary and post-Tertiary faulting.
Peale (1896, p. 3) assigned a Neocene age to his Bozeman lake beds. Subsequently, Douglass (1903, p. 146-155) correlated the beds in the lower part of the bluffs on the east side of the Madison River with the White River formation of Oligocene age, and the beds in the upper part, which he called the Madison Val ley beds, with the Loup Fork beds of late Miocene age. The term Loup Fork beds has long since been discarded as having "vague significance" (Wood and others, 1941, p. 24), and the age assigned by Douglass to the Tertiary strata has been corrected and more closely defined by later investigators. Schultz and Falkenbach (1949, p. 80-83), who have studied oreodonts col lected from Douglass' upper unit in the Madison Valley, consider this unit to include strata of both late Miocene and Pliocene ages. On the basis of a collection of vertebrate fossils from the same unit in the vicinity of Anceney, Dorr (1956, p. 73), con siders the upper unit to be mostly of latest Miocene age. The age of Douglass' lower unit is less well established. The strata underlying the Madison Valley beds of Douglass (1903) at the base of the bluffs east of the Madison River have been termed the Leuciscus turneri beds and assigned a late Miocene age by Wood (1938, p. 291-292). On the other hand, the Tertiary strata in the bluffs west of the Madison River, in the Three Forks quad rangle, are reported by G. D. Robinson (written communication,
34 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
1956) to be of early Oligocene age, and, as the eastward dip of these beds carries them below the strata east of the river, possibly the lowermost beds exposed east of the river also are of early Oligocene age. However, since fossil evidence is lacking-, it cannot be stated definitely that deposits of unquestionable late Oligocene and early Miocene age are present.
The Tertiary strata of the Gallatin Valley are here divided into three units, of which the lowest is present only in the sub surface. The other two crop out at the surface. The lower of the exposed units, unit 1, is predominantly lacustrine and cor responds lithologically to Douglass' White River beds. The upper, unit 2, is predominantly fluvial and colluvial and corresponds lithologically to Douglass' Madison Valley beds. In the Horse shoe Hills north of the Gallatin River, units 1 and 2 cannot be distinguished from each other and are referred to as undifferen- tiated Tertiary strata.
Many wells, particularly in the Camp Creek Hills and near the margins of the Gallatin Valley, derive water from strata of Tertiary age. Most of these wells tap predominantly fine-grained material that yields water slowly. A few, however, tap lenses of well-sorted sand and gravel that yield water freely. A large spring near Manhattan (A2-3-32db) derives water, at least in part, from fractures in the Tertiary strata.
SUBSURFACE UNIT
Test hole Al-2-29adc, drilled by the Montana Power Co., penetrated mainly gray sandstone, green and gray-green clay- stone, and siltstone in the lower half of the hole. The claystone is interbedded with a few thin beds of lignite. As cores from test hole Al-2-29adc indicated that the coarse sandstone grades upward into claystone, which is in sharp contact with the sand stone in a similar succession above, these deposits seem to be cyclic, at least in part. In the upper half of the hole, mainly sandstone containing some clayey layers and thin beds of ben- tonite(?) was penetrated. (See table 33 for log of test hole Al- 2-29adc.) The authors believe that the uppermost bed pene trated by the test hole is stratigraphically 140 to 150 feet lower than the lowermost bed of unit 1, which is exposed in the bluffs on the east side of the Madison River in sec. 28, T. 1 N, R. 4 E. This interval may include the bentonitic beds that crop out west of the Madison River.
In the midthirties an oil test near test hole Al-2-29adc was drilled to a depth of a little more than 2,600 feet. The rocks
GEOLOGY 35
that were penetrated between the depths of 2,000 and 2,400 feet were reported to consist principally of conglomerate and vari colored shale, and a few coal layers were present between depths of 2,000 and 2,100 feet. From this it seems likely that the oil test was still in Tertiary strata at 2,400 feet.
The rocks penetrated by these deep test holes are stratigraphi- cally lower than the rocks exposed in the bluffs along the Madison River and may be equivalent, in part, to beds of early Oligocene age that crop out in the Three Forks quadrangle west of the river. If the subsurface Tertiary strata extend into the Gallatin Valley and dip eastward, as do the exposed Tertiary strata in the Camp Creek Hills, they have not been reached by any of the test holes drilled in the central part of the Gallatin Valley.
UNIT 1
The full thickness of unit 1 crops out 5 to 6 miles south of Logan, in the basal part of the bluffs along the Madison River. Southward, the lower part of the unit is below river level, but the uppermost part crops out in the gullies that are cut into the covered slope at the base of the bluffs. Northward, only the upper part of the unit is exposed near the base of the bluffs. A part of unit 1 crops out for a distance of about 2 miles south of U.S. Highway 10 near Logan. Elsewhere in the valley the upper part of unit 1 is exposed along the upper reaches of Godfrey Creek, along Camp Creek north of Anceney, and in the Dry Creek sub- area west of Menard.
Unit 1 is composed principally of well-stratified volcanic ash, tuffaceous marl and siltstone, tuffaceous fine- to medium-grained sandstone, and a few beds of limestone that stand out as re sistant ledges where exposed to erosion. In some places con glomerate and poorly sorted crossbedded sandstone also are pres ent. Unit 1 is predominantly white, cream, and light gray. Ripplemarks on the sandstone, the presence of limestone layers, the even stratification of the beds, and the presence of ostracodes throughout the unit indicate that unit 1 was deposited in a lacustrine environment. Several of the limestone beds contain gastropods of those seen by the writers, the best preserved were those north of the old McCrea ranch, about 2y% miles west of Menard. Douglass (1903) reported finding fish fossils in beds which are considered by the writers to be the upper part of unit 1 and which probably correspond to the Leuciscus turneri beds of Wood.
36 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
The base of unit 1 has been set arbitrarily at the base of the lowest bed exposed where the Madison River has cut through an anticline in the Tertiary strata, about 5 to 6 miles south of Logan. The contact between units 1 and 2 is marked by a local uncon formity which is discernible in the bluffs along the Madison River. (See fig. 7.) Near the margins of the Three Forks basin,
FIGURE 7. Local unconformity between units 1 and 2 of the Tertiary strata in the bluffs along the Madison River in the SE%NE14 sec. 3, T. 1 S., R. 2 E. Photograph taken at same place as that taken by Douglass (1903, p. 200) who considered the unconformity to be the contact of the White River beds with the Loup Fork beds.
unit 1 contains a larger proportion of detrital material and is less well stratified than in the central part of the basin; its contact with unit 2 is gradational. For mapping, the contact in the marginal areas of the basin was placed at the top of the uppermost ostracode-bearing bed.
Near the south end of the bluffs along the Madison River and in the vicinity of Anceney, unit 1 rests on Precambrian gneissic rock. In the Horseshoe Hills, west of Menard, unit 1 rests on Paleozoic and Mesozoic rocks and contains a much larger propor tion of limestone than elsewhere.
GEOLOGY 37
Section of unit 1, measured in the bluffs along the Madison River
[Beds 1 through 5 measured on the north slope of a prominent bluff in the SE^NW^ sec. 34, T. 1 N., R. 2 E., beginning at unconformity at top of unit 1; beds 6 through 16 measured in the NW%NE14 sec. 27, T. 1 N., R. 2 E. Bed 5 is common to both exposures]
Thickness Bed Description (feet)
1. Ash, sandy, silty, gray; interbedded with prominent thin white marl beds containing many ostracodes and with layers, 3 to 12 in. thick, of fine-grained loosely cemented tuffaceous sandstone; ash contains numerous dark minerals .. . .... .. . _ 199
2. Sandstone, very coarse grained and pebbly, crossbedded,ferruginous; contains abundant dark minerals. - 3
3. Siltstone, gray-white, tuffaceous in places; interbedded with numerous thin layers of white ash and several beds of light-gray fine-grained calcareous sandstone averaging 1 in. in thickness; sandstone beds stand out as resistant bands on the weathered slope 177
4. Ash, thinbedded, gray-white; interbedded with a few thinbeds of siltstone; ash contains ostracodes 21
5. Limestone, argillaceous, gray; weathers to chocolate- brown; forms a hard, resistant ledge that is useful as a marker horizon .._.. _. 10
6. Ash, calcareous, sandy, massive, gray; weathers to brown; interbedded with layers of white to gray pure ash that are as much as 4 in. thick... __.. ....._... _ 59
7. Sandstone, medium-grained, calcareous, light-brown.. 14%8. Siltstone, calcareous, brown Vz9. Sandstone, pebbly, poorly sorted, calcareous, massive, dark-
brown; partly crossbedded; contains a few lenses of conglomerate 18
10. Siltstone, tuffaceous, calcareous, thinbedded; contains afew thin lenses of sandstone . 12
11. Sandstone, poorly sorted, ferruginous, massive, loosely con solidated, light gray-brown____ 4
12. Marl, tuffaceous, white; interbedded with calcareous whiteash; marl contains ostracodes 11
13. Limestone, coquinalike, conglomeratic, massive, gray-white; weathers to grayish brown; contains thin beds of white ash - . . _ 2%
14. Siltstone, tuffaceous, cream-colored; interbedded with fine grained loosely cemented massive light-gray sandstone.... 78
15. Covered. Probably tuffaceous siltstone interbedded withpure ash . 250(?)
16. Grit, pebbly, poorly sorted, blocky, well-cemented, light- brown to gray; consists principally of quartz, feldspar, mica, and fragments of volcanic and gneissic rock 62
Total .._ .......... .-__-..--._.- _ 921%
38 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
UNIT 2
Unit 2 is exposed throughout the Camp Creek Hills, in much of the Dry Creek subarea, in draws cutting the alluvial fans along the Bridger Range north of Bozeman, on the north and south sides of the East Gallatin River east of Bozeman, and along Goochs Ridge.
Unit 2 is highly variable in composition but consists principally of poorly stratified massive buff to tan partly calcareous vari ously consolidated tuffaceous siltstone, claystone, sandstone, and conglomerate; it contains a few beds of gray pure ash and small lenses of marl and limestone. Although it is predominantly of fluvial and colluvial origin, the beds of marl and limestone indi cate that some of the deposition occurred in ponds or small lakes. A bed of conglomerate and buff siltstone at the base of unit 2 projects as a ledge from the bluffs along the Madison River. About 100 feet above the base of unit 2 a distinctive bed of conglomerate, locally well cemented, is present in the northern part of the Camp Creek Hills. West of Manhattan, where erosion has removed the overlying material from this bed, it forms a continuous northeastward slope from the bluffs along the Madison River to the floor of the Gallatin Valley. Along the east and south east margins of the valley, unit 2 grades into, and interfingers with, fanglomerates which extend out from the adjacent high lands. Vertebrate fossils collected from this unit have been de scribed by Douglass (1903), Schultz and Falkenbach (1940, 1941), and Dorr (1956).
Section of unit 2, measured in the bluffs along the Madison River
[Beds 1 through 7 measured at head of large draw in the SW^NW^ sec. 2, T. 1 S., R. 2 E., be ginning at base of a 32-ft layer of boulders, cobbles, and coarse gravel, which caps the bluffs ; beds 8 through 15 measured on south-facing escarpment in the NE^NW 1 sec. 26, T. 1 N., R. 2 E. Bed 8 is common to both exposures]
Thickness Bed Description (feet)
1. Siltstone, sandy, tuffaceous, calcareous, cream to buff; interbedded with several beds of gray ash, 1 to 2 ft thick, and a few beds of massive buff claystone ___ _ _ 66
2. Covered. Probably tuffaceous siltstone- _ _ - 433. Claystone and siltstone, massive, buff; interbedded with
several very thin layers of gray ash _ 294. Siltstone interbedded with claystone, cream-colored; con
tains a few sand-size particles.. - 275. Sandstone, tuffaceous, very loosely cemented, green-gray;
composed of fine to medium quartz grains, glass shards, and very fine grains of magnetite . \Vz
6. Sandstone, very fine grained, tuffaceous, layer of ash one- fourth inch thick at base; grades downward into tuffa ceous siltstone interbedded with claystone 13
GEOLOGY 39
Section of unit 2 measured in the bluffs along the Madison River Continued
Thickness Bed Description (feet)
7. Covered. Probably tuffaceous sandstone interbedded withlayers of gray ash __. - - - - 12
8. Conglomerate, sandy, calcareous, gray; interfingers with coarse, pebbly sandstone. Angular to rounded cobbles and pebbles of the conglomerate are composed of gneiss, volcanic rocks, and quartz; the fine-grained constituents of the conglomerate are predominantly quartz, dark min erals, and garnet 32
9. Siltstone, sandy, tuffaceous, calcareous, buff; grades down ward into fine-grained tuffaceous sandstone _. 29
10. Sandstone, coarse-grained, tan; contains well-rounded peb bles near top; interbedded with, and grading into, fine grained tan sandstone 44
11. Siltstone, buff; grades downward into sandy siltstone .. 912. Sandstone, whitish-tan; grades downward from coarse- to
fine-grained sandstone __ _ . 1313. Ash, massive, gray-white; contains coarse shards ________ ____ 1014. Conglomerate and coarse sandstone, tan 4%15. Conglomerate of subrounded gravel in calcareous silt
matrix; interfingers with brown siltstone and sandstone; forms a prominent persistent vertical ledge which is use ful as a marker horizon; numerous bone fragments near basal part. (Probably same bed from which Douglass collected vertebrate fossils.) 40
Unconformity at top of unit 1.
Total _ _ _______ _ _ _ 373
UNDIPFEBENTIATED TERTIARY STRATA
Tertiary strata, which could not be differentiated into units 1 and 2, are exposed in the Horseshoe Hills as small outliers of lime-cemented fanglomerate resting unconformably on Precam- brian and Paleozoic rocks. The fanglomerate consists of frag ments of locally derived Paleozoic limestone. West of Nixon Gulch the fanglomerate grades upward into cliff-forming cream- colored limestone containing gastropod fossils. From a distance this limestone resembles limestone of Paleozoic age. The fan- glomerate either is horizontal or dips very slightly southward toward the valley. The stratigraphic position of these Tertiary strata relative to units 1 and 2 is unknown.
TERTIARY AND QUATERNARY SYSTEMS
OLDER ALLUVIUM
A high benchlike fringe of alluvial-fan and stream-channel deposits skirts the Bridger and Gallatin Ranges. In the Dry Creek
40 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
and Fort Ellis subareas the surface of these deposits slopes to ward, and merges with, the surface of older Tertiary strata, but elsewhere the sloping surface of these deposits terminates in an escarpment. In places, these deposits are deeply eroded.
The alluvial fans of this unit are composed of locally derived poorly sorted rock fragments in a matrix of sand, silt, and clay. Some of these deposits, which are lime cemented and variously consolidated, are referred to as fanglomerate. The rock frag ments forming the fans that skirt the Gallatin Range generally are more rounded than those in the fans skirting the Bridger Range. The gneissic fragments in the fans are deeply weath ered. Fanglomerate does not crop out along the Gallatin Range, but the overall thickness (possibly as much as 150 feet) of un- consolidated material there is so much greater than it is next to the Bridger Range as to suggest that fanglomerate may be present but is mantled by later deposits. The stream-channel al luvium consists of rounded cobbles. The contrast between stream- channel and alluvial-fan deposits is illustrated in figure 8.
As no fossils were found in any of these deposits, it was not possible to determine their age from paleontologic evidence. How ever, from their physiographic relationship to the deposits that underlie the floor of the Gallatin Valley, they are believed by the writers to be of either late Tertiary or early Pleistocene age, or both. It seems more likely that deposition of rock debris along the mountain front probably was more or less continuous from Tertiary into Quaternary time. Both the Bridger and Gallatin Ranges were glaciated, and it is likely that the coarse materials in these deposits were derived from the glaciers.
The fanglomerate along the front of the Bridger Range in the Pass Creek area of the Dry Creek subarea is tilted, but the un- differentiated Tertiary and Quaternary deposits elsewhere re tain their valleyward primary dip.
The Tertiary strata exposed in the bluffs overlooking the Madi son River are mantled by a veneer, 10 to 30 feet thick, of mod erately well sorted well-rounded cobbles predominantly of quartz- ite. Pardee (1950, p. 403) suggested that these deposits represent deposition during the same cycle of erosion that formed the Flaxville plain of Alden (1932). If this is correct, these deposits may be of Pliocene or early Pleistocene age. These deposits were not mapped for this study.
Sufficient water for stock and domestic use generally can be obtained from the older alluvium.
GEOLOGY 41
FIGURE 8. Older alluvium in the Gallatin Valley. A. Stream-channel deposits in the SE cor. of the SW»4NE% sec. 18, T. 3 S., R. 5 E. B. Alluvial-fan deposits in the NE cor. of the
sec. 14, T. 1 S., R. 5 E.
508919 O-60 4
42 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
QUATERNARY SYSTEM
YOUNGER ALLUVIUM
Terrace gravels In the Camp Creek Hills
Deposits of probable Pleistocene age, derived from the destruc tion of higher lying gravel deposits and fanglomerate, are pres ent at the surface in parts of the Camp Creek Hills. These de posits range in thickness from 10 to 40 feet, but they were not mapped for this study.
Remnants of a terrace formed by the Gallatin River are pres ent along the east margin of the Camp Creek Hills. In the SE cor. of sec, 10, T. 2 S., R. 4 E., west of Sheds Bridge, the terrace is about 140 feet above river level, and in sec. 16, T. 1 N., R. 3 E., southwest of Manhattan, the terrace is about 140 to 160 feet above river level. The unconsolidated deposits underlying the terrace remnants are similar in composition to the alluvium along the Gallatin River. The entire thickness of the terrace deposits is not exposed, but west of Sheds Bridge it is at least 15 feet. These deposits were not mapped during this investigation.Alluvial-fan deposits
Alluvial fans, probably of late Pleistocene age, extend into the Gallatin Valley from the foot of the slopes of the bordering Gal latin and Bridger Ranges. The most extensive of these, the Boze- man and Spring Hill fans, were deposited by streams that cut into fans of older alluvium higher on the slope. Along the Bridger Range, north of the Spring Hill fan, several younger fans have been deposited on pediments previously formed on older fans.
The younger alluvial fans are composed of a heterogeneous mixture of coarse- and fine-grained sediments. The proportion of gravel, cobbles, and scattered boulders to the silt and clay is not uniform in each fan; in general, however, the coarser material is predominant near the head of the fan and the finer material near the margins. Scattered throughout the alluvial fans are stringers of moderately clean sand and gravel which were de posited by the distributaries that built the fan; lenses of clay and gravel also are scattered throughout the alluvial fans. Each fan is composed of locally derived rock.
The alluvial-fan deposits thin in a downslope direction. Well D2-5-22ccd, on the Bozeman fan, was drilled through 165 feet of fan alluvium before entering strata of probable Tertiary age. Well Dl-5-34cc2, 4 miles downslope from well D2-5-22ccd, was drilled through 131 feet of alluvial-fan deposits before entering Tertiary strata.
GEOLOGY 43
According to the degree of sorting and the amount of silt and clay present, the younger alluvial-fan deposits yield small to moderate quantities of water to wells. The stringers and lenses of gravel and sand are the source of most of the water.Stream-channel deposits
The alluvium along the Gallatin River and under the extensive alluvial plain between the Gallatin and East Gallatin Rivers con sists of cobbles and gravel intermixed with sand, clay, and silt. The upper 20 feet, as seen in gravel pits, is composed of clean and moderately well sorted cobbles and gravel. In the Central Park subarea, however, the upper 20 feet contains a higher pro portion of silt and clay. Test drilling indicates that below a depth of 20 feet the alluvium consists predominantly of cobbles and pebbles, but that varying proportions of sand, silt, and clay are mixed with the coarse material, and lenses of sand, silt, and clay are present. Most of the cobbles, pebbles, and sand grains are fragments of gneiss and dark volcanic rocks derived from the Gallatin and Madison Ranges. In general, the ratio of fine- to coarse-grained material increases in a downstream direction. The character of the alluvium in the Belgrade area is shown in figure 9.
Available evidence indicates that the alluvium of the Gallatin River rests on Tertiary strata except where the river enters and leaves the valley. Test drilling between Gallatin Gateway and Sheds Bridge (SE^4 sec. 10, T. 2 S., R. 4 E.) indicates that the alluvium is 70 to 80 feet thick. Northward from Sheds Bridge the alluvium thickens. The log of test hole Al-4-25dc, in the vicinity of Belgrade, indicates that the alluvium is at least 400 feet thick, and it is reported that an oil test (State well 1), a quarter of a mile north of Belgrade, was drilled through more than 800 feet of alluvium. Toward the north end of the valley, however, the alluvium is thinner. Test hole Al-4-15da2, about 4 miles north of Belgrade, penetrated 215 feet of alluvium before entering the underlying Tertiary strata. At the extreme north edge of the valley, test hole Al-4-5da penetrated 31 feet of ma terial known to be alluvium and 104 feet of material of question able Tertiary age before entering strata of known Tertiary age.
Except where silt and clay fills the voids between the coarse particles of sand and gravel, the alluvium yields copious amounts of water to wells. In the vicinity of Belgrade, at depths ranging from about 15 to 50 feet below the land surface, there is a layer of lime-cemented gravel which is a semiconfining layer for water in the underlying material.
44 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
FIGURE 9. Younger alluvium in the Gallatin Valley. Stream-channel deposits in thesec. 7, T. 1 S., R. 5 E.
The alluvium along the tributary streams entering the valley from the Bridger and Gallatin Ranges generally is composed of sand, gravel, and cobbles. The alluvium along the streams that head in the Bridger Range consists of fragments of Precambrian gneiss and arkose and of Paleozoic limestone and quartzite, but the alluvium along the streams that head in the Gallatin Range is similar in composition to the alluvium underlying the plain between the Gallatin and East Gallatin Rivers. The alluvium along these minor streams is probably no more than 20 or 30 feet thick, but in most places it yields water freely to wells.
Compared to the generally coarse alluvium of the Gallatin River and its tributaries from the mountains, the alluvium along the streams in the Camp Creek Hills, and to some extent along Dry Creek, is much finer grained because it was derived largely from fine-textured Tertiary strata. The yield of water from this ma terial is low.
The alluvium directly underlying the plain between the Galla tin and East Gallatin Rivers is thought to be of late Pleistocene age, whereas that along the present stream courses is of Recent age. The Gallatin River appears to be at grade in its course
GEOLOGY 45
through the valley and, therefore, is no longer aggrading the alluvial plain. The character, extent, and thickness of the al luvium underlying the plain between the rivers indicate that the alluvium was deposited concurrently with the glaeiation of the Gallatin and Madison Ranges.
LOESS
Buff calcareous silt, probably of eolian origin, mantles hills and slopes in many places in the Gallatin Valley. In some places it rests directly on Tertiary strata and in others on the terrace deposits or on the older or younger alluvial fans. Particle-size analyses show that 60 to 80 percent of the material is silt, 10 to 30 percent clay, and 3 to 15 percent sand. The few samples examined under the microscope were composed mostly of quartz grains, some mica, very little calcite and magnetite, and scat tered glass shards. The loess is massive and vertically jointed; where cut through, it stands in vertical walls. (See fig. 10.) Generally, it is thicker on hilltops than on slopes.
The eolian origin of these deposits is indicated by their compo sition and distribution. The glass shards indicate that the loess
FIGURE 10. Loess mantling upper Tertiary or Pleistocene gravel in theT. 1 S., R. 3 E.
sec. 26,
46 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
was derived at least in part from the Tertiary strata. Deposi tion probably began in late Pleistocene time and is still in prog ress in the Camp Creek Hills. The areal extent of the loess was not mapped during this study.
COLLUVIUM
Colluvium is the gravity-transported debris deposited at the foot of an escarpment or steep slope; as used in this report, the term also includes slope wash. The composition of colluvium de pends upon the composition of the type of material exposed in the escarpment or slope from which the colluvium is derived.
The largest deposit of colluvium in the Gallatin Valley borders the Camp Creek Hills near Manhattan. Much of this deposit is silt and clay intermixed with a small amount of sand and gravel; south of Manhattan, waterlogging has resulted where the water table intersects the surface of the colluvium. Most of the other deposits of colluvium consist of coarse material overlying the upper margin of alluvial fans. All the colluvial deposits in the Gallatin Valley are considered to be of Recent age. Their areal extent was not mapped for this study.
IGNEOUS BOCKS
Thick sills are intruded into the rocks of Cambrian age in many places in the Gallatin Valley area. One, described as syenitic rock by Peale (1896, p. 4), is in the middle unit of the Flathead quartzite in the Horseshoe Hills west of Nixon Gulch, but traced eastward its position gradually changes in the sec tion until it is near the base of the Wolsey shale in the vicinity of Dry Creek. Another thick sill lies near the contact of the Wolsey shale with the overlying Meagher limestone in the in- faulted block of Paleozoic rock west of Gallatin Gateway. Cla- baugh (1952, p. 67) described it as hornblende andesite por phyry. A sill whose petrologic classification was not determined is present in the Kootenai formation west of Menard. As the sills are broken by several transverse faults, intrusion must have occurred before the faulting took place.
A small body of basalt, considered by Peale to be of Miocene age, crops out in sec. 7, T. 3 S., R. 4 E., west of Gallatin Gateway.
STRUCTURE
The Gallatin Valley and the peripheral highland areas are characterized by diverse structural trends. Because the base ment complex of the valley is buried beneath thick deposits of
GEOLOGY 47
Cenozoic age, valley structure must be considered in relation to that of the surrounding highland areas.
HORSESHOE HILLS
The low Horseshoe Hills bound the floor of the Gallatin Valley on the north and the Dry Creek subarea on the west. The exposed strata range in age from Precambrian to Tertiary, except that strata of known Ordovician, Silurian, and Triassic ages are not represented. Outliers of Tertiary deposits unconformably overlie many of the older rocks.
The Horseshoe Hills are for the most part a group of tight northeast-trending folds, which are overturned slightly to the southeast. The strata that form the north margin of the floor of the Gallatin Valley are part of the southeastern limb of a syncline that is the southernmost fold in the group.
The rocks adjacent to the valley floor form a group of north east-plunging minor folds. Differential erosion of these folds has formed a series of zigzag ridges, the most prominent of which is underlain by the Madison group. This area has no extensive faults, though several small normal faults offset the Flathead quartzite, particularly in the troughs and at the crests of the minor folds.
At the west margin of the Dry Creek subarea, the older rocks are buried beneath Tertiary strata which fill the basin between the Horseshoe Hills and the Bridger Range. The rocks are tightly folded and extensively faulted. The principal faults appear to be normal, but south of Accola a small thrust cuts the Meagher limestone. Many of the minor normal faults and bedding-plane thrusts were not mapped for this study. The structural complex ity in this part of the Horseshoe Hills probably is due to the intersection of the major structural trends of the Horseshoe Hills and the Bridger Range.
The rocks in the southern part of the Horseshoe Hills are in contact with the alluvium of the Gallatin and East Gallatin Riv ers. Some of the pre-Tertiary rocks are exposed on the south side of the Gallatin River between sec. 33, T. 2 N., R. 3 E., and sec. 35, T. 2 N., R. 2 E. The river, in this locality, has cut a narrow channel across Precambrian and Paleozoic strata. The depth of this channel was determined by drilling two test holes (A2-2-35abl and A2-2-35ab2) in the narrow gorge near Logan. These test holes entered bedrock at depths of 22 and 23 feet, respectively.
Atwood (1916, p. 706) considered that the present course of the river at Logan was predetermined by its course during a
48 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
previous cycle of erosion. Tertiary outliers in the Horseshoe Hills strengthen the theory that the Tertiary deposits overlapped the frontal slopes of the Horseshoe Hills and that the Gallatin River was superimposed from its course over the Tertiary strata to its present position.
BRIDGER RANGE
The Bridger Range, a high linear mountain range which bounds the Gallatin Valley on the east, extends from Bridger Creek to the head of Dry Creek. The mountains are composed of rocks that range in age from Precambrian to Cretaceous, but strata of Ordovician, Silurian, Permian, and Triassic ages are not known to be present. The Paleozoic rocks overlie Precambrian meta- morphic rocks in the southern part of the Bridger Range and Precambrian rocks of the Belt series in the northern part (Mc- Mannis, 1955, p. 1393, 1416). The Paleozoic and Mesozoic rocks strike north-northwest, parallel to the axis of the range. They dip steeply to the east and in places are overturned to the east.
Several high-angle thrust faults transect the Bridger Range. Most of them have an eastward trend with local deviations to the southeast. McMannis (1955, p. 1416-1426) has shown the movement on these faults to be related to two phases of Lara- mide compression strike-slip movement by east-west compres sion and underthrusting by later south-southwest north-northeast compression.
One of these faults, the Pass fault, is of particular significance. The western segment of the fault is believed by McMannis (1955, p. 1391, 1421) to be the contact between the Precambrian gneiss on the south and the Precambrian Belt series on the north. The coarse arkosic nature of the Belt rocks near the fault led him to conclude that deposition of the Belt series in this locality was fault controlled that is, coarse arkosic material from the ris ing Archean block to the south was shed onto the subsiding northern block. He believed that later Laramide compression first caused strike-slip movement on this old fault, which was followed by underthrusting of the block of Archean-type rocks on the south.
Berry (1943, p. 7, 25) postulates a similar origin for the Belt series in the Jefferson River valley. According to Berry, the Belt rocks were deposited on the north side of a line of weakness along which thrust faulting (the Jefferson Canyon fault) later took place.
Peale (1893), Berry (1943), and McMannis (1955) are in es sential agreement that the shoreline during Belt time trended
GEOLOGY 49
eastward across the Gallatin Valley, and both Berry and McMan- nis postulated that the shoreline marks either a fault or a zone of weakness in the basement complex.
Normal faulting along the west side of the Bridger Range is believed to have elevated the range with respect to the valley. Pardee (1950, p. 380) and McMannis (1955, p. 1427, 1428) pre sented evidence for normal faulting. Pardee believed the mini mum relative downthrow along the fault system called the Bridger frontal fault system to be 3,000 feet.
GAI/LATIN AND MADISON RANGES
The Gallatin River canyon separates the Madison Range on the west from the Gallatin Range on the east. Structurally, however, the two ranges are segments of the same mountain unit. This unit bounds the Gallatin Valley on the south.
The mountains are composed of Precambrian gneiss and some infaulted blocks of Paleozoic and Mesozoic rocks. About 150 square miles are covered by andesitic lavas and breccias of prob able late Eocene or early Oligocene age (Horberg, 1940, p. 283). The thickness of these extrusive rocks has been estimated by Peale (1896, p. 4) to be about 2,000 feet. Several porphyritic intrusives cut the Mesozoic rocks in the southern part of the mountains.
The Precambrian rocks are dominantly hornblende gneiss and garnetiferous feldspar-rich gneiss. These are cut by numerous pegmatites, quartz stringers, and quartz veins. The rocks are tightly folded and severely crumpled in places, yet a general east-west trend is recognizable.
Of three principal faults cutting across the mountains, only the northernmost, the Salesville fault, is in the Gallatin Valley. This fault, striking N. 50°-55° W., can be traced from sec. 10, T. 3 S., R. 3 E., to sec. 20, T. 3 S., R. 4 E., where it disappears beneath the Tertiary strata. Precambrian gneiss is in contact with Cambrian and Devonian strata along the fault line. Peale (1896, p. 5) believes this fault to be the same one that appears east of the Gallatin River in the foothills of the Gallatin Range, where Carboniferous strata are in contact with Precambrian gneiss. It is a high-angle fault; the exact dip of the fault plane is undetermined.
A clear-cut boundary does not exist between the Madison Range and Gallatin Valley because the foothills of the mountain range grade into the floor of the valley and there is no evidence of faulting between the foothills and the valley. The elevation of the surface of the gneiss in test holes Dl-3-36bc and D2-4-9bc
50 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
is consistent with the projected slope on the gneissic surface in the Madison Range foothills. The Tertiary beds probably were deposited on a normal erosional surface developed on the gneiss.
Faulting may or may not be present along the front of the Gallatin Range. The available subsurface information is not suf ficient for a determination.
GALLATIN VALLEY
The Tertiary strata in the Gallatin Valley form a homocline that dips from 1° to 5° in a generally eastward direction toward the Bridger Range. Local deviations are numerous. In the northern Camp Creek Hills the beds dip northeastward. Near the contact of the Precambrian rocks and the Tertiary strata in the southern Camp Creek Hills, the dip of the Tertiary strata reflects the slope of the underlying bedrock surface.
Several of the faults that transect those parts of the Bridger and Gallatin Ranges adjacent to the valley undoubtedly also cross the valley, and the basement complex is probably broken into blocks, especially near the Bridger frontal fault zone. Several linear features in the valley, such as the east escarpment of Goochs Ridge and a similar escarpment about a mile west of Sheds Bridge, suggest the possibility of structural control by post-Tertiary faulting; however, no definite evidence to support this hypothesis was found.
Hot water issuing from the Bozeman Hot Springs and that found during the drilling of test holes D2-4-9bc and Dl-3-36bc, as well as the warm water produced by several wells in the south ern Camp Creek Hills, indicate deep circulation of water, possibly along faults in the basement complex.
Small normal faults in the Tertiary strata are seen through out the valley. Most of the observed faults are parallel to the general northward trend of the Bridger frontal fault system. The displacement along these faults generally is less than 1 foot; however, displacements of more than 20 feet have been noted and it seems likely that faults of even greater displace ment are present. Figure 11 shows small faults in the Tertiary strata on the east side of South Church Street near the city lim its of Bozeman. In the Camp Creek Hills, a gravel deposit is downf aulted against fine-grained Tertiary beds in the SW^SWi/4 sec. 26, T. 1 S., R. 3 E., along the south bank of the Lowline Canal. In an exposure along the Dry Creek road south of Menard, faults in the Tertiary strata are marked by layered clastic dikes. These small normal faults cut unit 2 and probably
GEOLOGY 51
FIGURE 11. Small normal faults in the Tertiary strata in the SW^4SE^4 sec. 7, T. 2 S., R. 6 E.
are due to post-Miocene readjustment of the Tertiary strata to the faulting along the Bridger frontal fault zone.
The only major structural element which is transverse to the Bridger frontal fault system and for which direct evidence was found in the Tertiary strata is an east-trending monoclinal fold crossing the northern part of the valley. This fold, involving both units 1 and 2 of the Tertiary strata, is believed by the authors to reflect a subjacent fault (shown on pi. 2 as the Central Park fault) in the basement complex. The surface of the es carpment above the bluffs along the Madison River is capped with gravel at this location. The gravel cap north of the fold (Ni/2 sec. 35, T. 1 S., R. 2 E.) has been elevated about 200 feet relative to the gravel cap south of the fold. The relationship of the gravel cap and the Tertiary strata is best seen on the north side of the flexure. The Tertiary strata here are truncated and the gravel bed is nonconformable, which indicates that some folding and erosion had taken place before deposition of the gravel. The fact that the gravel bed also is folded indicates re- occurring movement along this structure. As the flexure is traced eastward across the Camp Creek Hills the crest of the fold has
52 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
S.
FIGURE 12. Diagramatic section showing vestiges of the monoclinal fold in Tertiary stratain the Camp Creek Hills.
been eroded, and all that remains is a discontinuous ridge of south-dipping lime-cemented gravel. (See fig. 12.) This ridge arcs east-northeastward from the bluffs along the Madison River toward Central Park, but east of the Gallatin River the fold is concealed by alluvium.
Where covered by alluvium, the location of the fold has been determined from subsurface data. The drilling of test hole Al- 4-19cb was terminated in alluvium at a depth of 301 feet. Well Al-3-14dd, 1 mile northwest of Al-4-19cb, entered Tertiary strata at a depth of 30 feet. The fold therefore must pass be tween test hole Al-4-19cb and well Al-3-14dd. To the east, test hole Al-4-15da2 is believed to be approximately on the fold; this test hole entered Tertiary strata at 215 feet. South of test hole Al-4-15da2 the Tertiary strata are at a much greater depth, and north of the test hole they are at a much shallower depth. East of this test hole the fold cannot be traced. It may coin cide, however, with the south edge of unit 2 of the Tertiary strata at, and eastward from, the East Gallatin Cemetery (sees. 15-17, T. 1 N., R. 5 E.) and probably intersects the Bridger frontal fault zone in the vicinity of Spring Hill.
The postulated Central Park fault in the basement complex of the valley coincides approximately with the shoreline of the Belt sea, which shoreline was considered by Berry (1943) and Mc- Mannis (1955) to be fault controlled. If the high gravel-capped surface in the bluffs along the Madison River is of Pliocene or early Pleistocene age, as suggested by Pardee (1950, p. 403), then the folding of the Tertiary strata that accompanied move ment along the Central Park fault must have occurred at least as
GEOLOGY 53
recently as late Pliocene time, and perhaps as recently as Pleis tocene time. The south side of the Central Park fault is the downthrown side, though during deposition of the Belt series the north side was the downthrown side, a reversal of movement along the fault apparently having taken place. McMannis pre sented evidence of a similar reversal in the Bridger Range along what probably is a part of the same fault zone.
Elsewhere, also, the Pliocene (?) surface is broken by fault ing. A west-northwest-trending escarpment west of the point at which Elk Creek enters the Madison River (about 9 miles west of Anceney) marks a fault; the gravel-capped surface south of the escarpment is about 160 feet lower than the surface north of the escarpment, and the Tertiary strata exposed in the bluffs facing the Madison River are deformed where the fault line in tersects the bluffs. This break in the Pliocene (?) surface prob ably resulted from movement along the westward extension of the Salesville fault and would be another indication of relatively late movement along preexisting faults in the older rocks of the Three Forks basin.
Pleistocene sedimentation in the Belgrade subarea apparently was controlled by renewed movement along the Central Park fault. The relative downward movement of the Tertiary strata south of the fault has formed, in effect, a trough in which the coarse alluvium from the Gallatin River has been deposited. Whether actual ponding in this trough ever took place or whether the rate of deposition approximated the rate of subsidence is unknown. So far as could be determined from the test-hole sam ples, none of the test holes penetrated obviously layered sediments.
The anomalous position and extent of the Spring Hill fan in relation to contemporaneous fans that flank the Bridger Range at higher levels to the north and south suggest that depo sition of this fan also may have been controlled by the Central Park fault.
On the basis of the available test-hole data, the surface of the Tertiary beds below the Bozeman fan does not seem to slope northward at a sufficient angle to account for the great thick ness of gravel, in excess of 400 feet, penetrated by test hole Al-4-25dc north of Belgrade. Either the Tertiary strata are warped gently downward (fig. 13A) toward the Central Park fault, or a fault near the south margin of the Belgrade plain has dropped the Tertiary strata north of the fault so as to form, with the Central Park fault, a graben (fig. 13B). As no geologic evidence was found to support the presence of such a fault south
54 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
N.
GALLATIN RANGE
HORSESHOE HILLS
Central Park fault
N.
GALLATIN RANGE
HORSESHOE HILLS
B
EXPLANATION
Deposits of Tertiary age
Central Park fault
Alluvial-fan deposits of Quaternary age
Belt series (Precambrian)
FIGURE 13. Diagram showing alternative hypotheses for the formation of the Belgrade trough. A. By downwarping of the Tertiary strata northward toward the Central Park fault. B. By down dropping of block between the Central Park fault and a fault south of Belgrade.
of Belgrade, it seems more likely that the Tertiary strata south of the Central Park fault are merely downwarped.
There is no evidence of a post-Tertiary channel leaving the valley other than that at Logan. Bedrock underlies the alluvium at Logan at a depth of about 20 feet. The fact that the altitude of this bedrock threshold at the valley outlet is considerably higher than the altitude of the base of the alluvium in the Bel-
GEOLOGY 55
grade trough is considered by the writers to be conclusive evidence that the Belgrade trough is a structural feature.
EFFECT OF FAULTS ON THE FLOW OF WATER INTO AND OUT OF THEGALLATIN VALLEY
Although some water probably enters and leaves the valley through faults in the pre-Tertiary rocks, there is no evidence that any of these faults is a conduit for a significant amount of water in relation to the total inflow to, and outflow from, the valley. Locally, however, streams that enter the valley are known to gain a large part of their flow from fault zones.
Ross Creek in the Bridger Range and South Cottonwood Creek in the Gallatin Range are two streams known to gain part of their flow from fault zones. Ross Creek rises where a major fault zone transects limestone of the Madison group, and it picks up most of its flow from springs along the fault zone. Several years ago the Montana State College abandoned its snow-measurement course across the crest of the Bridger Range from Ross Creek because the measurements could not be correlated with stream- flow east of the Bridger Range. Much of the snow along the crest and on the east side of the range in the vicinity of Ross Peak undoubtedly percolates into the porous Paleozoic rocks, especially the fractured limestones, and is discharged into Ross Creek on the west side of the range. This accounts for the very high runoff (161 inches in 1952 and 178 inches in 1953) from the Ross Creek drainage basin, an area of 1.29 square miles.
A major fault crosses South Cottonwood Creek just above the site of the gaging station established for this study. Precam- brian metamorphic rock on the north side of the fault is in juxtaposition with limestone of the Madison group on the south side. In early October 1952, a discharge of 18.05 cfs was measured at the gaging station and a discharge of only 6.41 cfs was measured above the fault, 2% miles upstream from the station. Therefore, at that time, the amount of water entering the stream from the fault was nearly 12 cfs, or about two-thirds of the volume passing the gaging station.
Undoubtedly, other streams from the Bridger and Gallatin Ranges also gain flow from fault zones. For example, McMannis (1955, p. 1423) mentioned that Lyman Creek, which furnishes part of the water supply for Bozeman, is fed by a spring at the junction of two faults.
56 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
SUMMARY OF CENOZOIC HISTORY
The Cenozoic history of the Gallatin Valley accords, in general, with the regional history as described by Pardee (1950) and McMannis (1955).
After the deposition of Cretaceous sediments, tectonic activity related to the Laramide orogeny began. There seem to have been several phases of folding and faulting in the area, which culmi nated in late Paleocene time with major mountain building. Then followed a long period of erosion, during which sediments derived from surrounding mountain ranges and from contem porary vulcanism began to accumulate in basins which were probably formed by tectonic movements. Deposition continued into Oligocene time, and a few thousand feet of Tertiary sedi ments accumulated in the gradually sinking basins. At that time the area must have been characterized by gently sloping low lands separated by moderately low mountains. From middle Oligo cene to late Miocene time, in the vicinity of the Gallatin Valley at least, the drainage was exterior and erosion prevailed over deposition.
Renewed crustal movement and volcanic activity in late Mio cene time again interrupted the through drainage, and additional sediments were deposited in the basin. Faulting (along the Bridger frontal fault), beginning at this time and continuing in termittently through Pliocene and Pleistocene time, dropped the basin floor with respect to the Bridger Range, and tilted the Ter tiary strata eastward.
During a period of relative stability an extensive erosion sur face was developed, and the gravel cap at the top of the bluffs along the Madison River was formed. The truncation of east ward-dipping Tertiary strata by the surface upon which the gravel was deposited (p. 51) is evidence that the tilting of these strata began before the surface was formed. As the upper most part of the Tertiary section exposed along the bluffs in cludes deposits of early Pliocene age, the terrace surface may be of middle or late Pliocene or earliest Pleistocene age.
In early and middle Pleistocene time, the Madison River cut a deep valley across the middle of the Three Forks basin, and the Gallatin River was superimposed at Logan. The present size and the large-scale structural features of the Gallatin Valley thus were determined. Also in early or middle Pleistocene time, re newed movement along the Central Park fault raised the strata north of the fault with respect to those south of the fault. In the Belgrade area, the downthrown block formed a trough in which
WATER RESOURCES 57the alluvium of the Gallatin River began to accumulate. Concur rently, extensive alluvial fans were formed along the flanks of the Bridger and Gallatin Ranges, and the Camp Creek Hills were eroded and terraced.
During late Pleistocene time the then-existing alluvial fans were dissected and new fans were deposited; the Bozeman fan is one of these younger fans. Alluvium continued to accumulate in the Belgrade trough to a thickness of at least 400 feet.
Intermittent crustal movement in the Gallatin Valley area has continued to the present.
WATER RESOURCES
Ground water and surface water are components of a com plex dynamic system termed the hydrologic cycle. Therefore, if they are to be evaluated, they must be considered not only in rela tion to each other but also in relation to the other components of the system.
Meinzer (1942, p. 1) described the hydrologic cycle as
the circulation of the water from the sea, through the atmosphere, to the land; and thence, with numerous delays, back to the sea by overland and subter ranean routes, and in part, by way of the atmosphere * * *
The principal components of the hydrologic cycle are illus trated in figure 14. The cycle is very complex and the compo nents are closely related. Surface water may seep into the un derlying rock and become ground water, just as ground water
PRECIPITATION(Ram, snow, etc.)
FIGURE 14. Hydrologic cycle. Modified from U.S. Geological Survey Circular 114, figure la.
508919 O-60 5
58 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
may return to the earth's surface through springs and effluent seepage to become surface water. Transpiration and evaporation may take place at any point in the cycle where water is exposed to the air or available to plants. Water that is stored temporarily as soil moisture may move downward to the water table and be come ground water; also, ground water may move upward into the soil horizon when soil moisture becomes depleted.
The following sections describe the principal phases of the hydrologic cycle with which this report is concerned.
SUBFACE WATER
By FRANK STERMITZ and F. C. BONER
At the time the study of the water resources of the Gallatin Valley was begun, permanent stream-gaging stations already were in operation on the Gallatin River near Gallatin Gateway and at Logan, and also on the East Gallatin River and on Bridger and Middle (Hyalite) Creeks. Beginning in May 1951, as part of the Gallatin Valley study, a number of additional gaging stations were established so as to obtain more complete information on the flow of surface water into the valley and on the movement of surface water within the valley. Pertinent data for all the stream-gaging stations are given in table 6; the station locations are shown both in figure 15 and on plate 1. Runoff records for these stations are given in table 7. In addition, occasional measurements were made at various other sites in the valley. These measurements, together with descriptions of the sites, are given in table 8, and the locations of the sites are shown on plate 1.
The general pattern of runoff in the Gallatin Valley is typical of that throughout the Rocky Mountain region, where precipitation varies greatly with altitude and topography, and where the ra pidity of snowmelt varies widely with exposure, cover, and alti tude. Extensive diversion of surface water for irrigation and the resultant return flow affect all streams in their course across the valley. However, the year-to-year variation of surface outflow from the Gallatin Valley at Logan is not great. During the period August 1928 to September 1953, the highest annual runoff was 1,077,000 acre-feet in water year 1948 and the lowest was an estimated 328,200 acre-feet in water year 1934.
STREAMS
GALLATIN RIVER
In the 80-mile reach of the Gallatin River above the gaging station near Gallatin Gateway, the average gradient is about 40
WATER RESOURCES 59
EXPLANATION
STREAM-GAGING STATIONS
FIGURE 15. Map of the Gallatin Valley showing location of stream-gaging stations.
feet per mile, the width of the valley is generally less than 1 mile, and only a few tributary streams are longer than 15 miles. Irri gation, which is confined to scattered hay meadows in the tribu tary valleys, has no appreciable effect on the regimen of the river.
Above the gaging station near Gallatin Gateway, the Gallatin River drains an area of 828 square miles. The inflow to the Gal latin Valley at this station was gaged for the first time in August 1889, and, except for July 1893, gaging was continued through June 1894. Although the Gallatin River was gaged for several subsequent years, the point of gaging was downstream from points where two large diversions were made, and hence, the measurements did not represent the total flow of the river into
TABL
E 6
. D
escr
iptio
ns o
f str
eam
-gag
ing
stat
ions
in th
e G
alla
tin V
alle
y[G
agin
g st
atio
n:
P,
per
man
ent;
T,
tem
por
ary.
T
ype
of g
age:
R,
reco
rdin
g; S
, st
aff;
W,
wir
e w
eigh
t]
Gag
ing
stat
ion
Gal
lati
n R
iver
near
Gal
lati
nG
atew
ay (
P).
Wil
son
(Eas
tF
ork)
Cre
ekne
ar G
alla
tin
Gat
eway
.
Wes
t F
ork
of
Wil
son
Cre
ek,
near
Gal
lati
nG
atew
ay.
Big
Bea
r C
reek
ne
ar G
alla
tin
Gat
eway
.
Loc
atio
n
Des
crip
tion
NE
Ji s
ec.
18,
T.
4 S.
,R
.4E
. O
n le
ft b
ank,
0 . 2
5 m
ile
belo
w m
outh
of S
pani
sh C
reek
and
8 m
iles
sout
hwes
t of
Gal
lati
n G
atew
ay.
SW
M s
ec. 3
6, T
. 3
S.,
R.
4 E
. 1
mil
e ab
ove
con
flue
nce
wit
h W
est
For
kan
d 4
. 5 m
iles
sout
h of
Gal
lati
n G
atew
ay.
NE
M s
ec.
2, T
. 4
S.,
R.
4 E
. 1
mil
e ab
ove
con
flue
nce
wit
h E
ast
For
kan
d 4.5
m
iles
sout
hof
Gal
lati
n G
atew
ay.
SW
Jise
c.2
9,
T.
3 S
., R
.5
E.
Abo
ve
mai
ndi
vers
ion
cana
l, 2
mil
esab
ove
conf
luen
ce
wit
hL
ittl
e B
ear
Cre
ekan
d 4
. 5 m
iles
sout
hea
st o
f G
alla
tin
Gat
ew
ay.
Lat
itu
de
45°3
0'
45°3
1'25
"
45°3
1'05
"
45°3
2'35
"
Lon
gitu
de
111°
16'
lll°
10
'20
"
in-i
i'35'
111°0
8'2
5"
Dra
in
age
area
(squar
e m
iles
)
82
8 5.3
3
3.8
1
13.2
Gag
e
Type
R S*
Alt
itud
eof
datu
m
(fee
t)
1 5
,16
7.7
Max
imum
dis
char
ge
Date
June 6
,19
52
Cu
bic
feet
per
seco
nd
6,9
10
Gag
e heig
ht
(fee
t)
5.7
1
Min
imum
dis
char
ge
Date
Jan.
19,
1935
Cubic
feet
p
er
seco
nd
117
Gag
e h
eig
ht
(fee
t)
0.6
8
Rem
ark
s
Month
ly
runoff
d
eriv
edfr
om
measu
rem
ents
at
ab
ou
t m
on
thly
in
terv
als
an
d c
om
par
iso
n o
f h
y-
dro
gra
phs.
M
easu
re
ments
pri
or
to co
nti
n
uo
us
reco
rd:
Aug.
2,19
51,
3.4
cf
s;
Sept.
12
,19
51,
2.6
cfs
.
Month
ly r
unoff
der
ived
fr
om
mea
sure
men
ts a
tab
ou
t m
on
thly
in
terv
als
and c
om
par
iso
n o
f h
y-
dro
gra
phs.
M
easu
re
men
ts p
rior
to c
on
tin
uous
reco
rd:
Au
g.
2,19
51,
2.1
cfs
; S
ept.
12
,19
51,
2.0
cfs
.
Month
ly r
unoff
der
ived
fr
om
mea
sure
men
ts a
tab
ou
t m
on
thly
in
terv
als
an
d c
om
par
iso
n o
f hy-
dro
gra
ph
s, s
up
ple
men
ted
by w
eekly
or
dail
y g
age
read
ings.
M
easu
rem
ents
pri
or
to c
onti
nuous
rec
ord
: A
ug
. 2,
1951,
7.9
cfs;
Sep
t. 1
2,
1951
,6
.1 c
fs.
.
o 03 8 H
Lit
tle
Bea
r C
reek
ne
ar G
alla
tin
Gat
eway
.
Sou
th C
otto
n-
woo
d C
reek
ne
ar G
alla
tin
Gat
eway
(T
).
Gal
lati
n R
iver
at
Axt
ell
Bri
dge
near
Gal
lati
n G
atew
ay (
T).
Fis
h C
reek
nea
r G
alla
tin
Gat
eway
.
Yel
low
Dog
C
reek
nea
r B
elgr
ade.
God
frey
Cre
ek
near
Bel
grad
e.
NW
Ji s
ec.
31,
T.
3 S.
, R
. 5
E.
1.5
mil
es a
bove
m
outh
and
4.5
mil
es
sout
heas
t of
Gal
lati
n G
atew
ay.
NE
Ji s
ec. 3
4, T
. 3
S.,
R.
5 E
. O
n le
ft b
ank,
15
ft
belo
w W
ortm
an
ranc
h br
idge
and
6.5
m
iles
sou
thea
st o
f G
alla
tin
Gat
eway
.
NW
Ji s
ec.
35,
T.
2 S.
, R
. 4
E.
Nea
r ce
nter
of
span
on
dow
nstr
eam
si
de o
f br
idge
, 2
mil
es
nort
h of
Gal
lati
n G
atew
ay a
nd 2
0 m
iles
ab
ove
conf
luen
ce w
ith
Eas
t G
alla
tin
Riv
er.
Cen
ter
of n
ort
h l
ine,
se
c. 3
4, T
. 2
S.,
R.
4 E
. A
bout
0.5
mil
e ab
ove
mou
th a
nd
2.5
m
iles
no
rth
of
Gal
la
tin G
atew
ay.
SW
Ji s
ec.
5, T
. 2
S.,
R.
4 E
. 20
0 ft
bel
ow
conf
luen
ce o
f 2
fork
s an
d 7.5
mil
es s
outh
w
est
of B
elgr
ade.
NW
Ji s
ec.
24,
T.
1 S.
, R
. 3
E.
At
coun
ty
road
bri
dge,
25
ft
abov
e ir
riga
tion
can
al,
0.5
mil
e so
uth
of
Chu
rch
Hil
l, an
d 6.5
m
iles
so
uthw
est
of
Bel
grad
e.
45C3
2'20
» 11
1°09
'45
45°3
2'20
"
45°3
7'
45°3
7'40
"
45°4
2'10
"
45°4
5'
111
005'
15"
3.87
22.5 6.85
S *
R W S S
1 5,689.5
1 4,815.7
June
5,
1952
1952
283
2.52
6.90
Mar.
22,
26,
1952
Jan. 24,
26,
1952
9.2
220
.73
Mon
thly
run
off
deri
ved
from
mea
sure
men
ts a
t ab
out
mon
thly
int
erva
ls
and
com
pari
son
of h
y-
drog
raph
s, s
uppl
emen
t
ed b
y w
eekl
y or
dai
ly
gage
rea
ding
s.
Mea
sure
m
ents
pri
or t
o co
ntin
uo
us r
ecor
d:
Aug
. 2,
19
51,
2.1
cfs;
Sep
t. 1
2,
1951
, 1.
6 cf
s.
Mon
thly
run
off
deri
ved
from
mea
sure
men
ts a
t m
onth
ly i
nter
vals
an
d
com
pari
son
of h
ydro
- gr
aphs
, su
pple
men
ted
by w
eekl
y or
dai
ly g
age
read
ings
.
Do.
See
fo
otn
ote
s at
end
of t
able
.
TABL
E 6
. D
escr
ipti
ons
of s
trea
m-g
agin
g st
atio
ns i
n th
e G
alla
tin
Va
lley C
onti
nued
to
Gag
ing
stat
ion
Godfr
ey C
reek
nea
r B
elgra
de
Conti
nued
.
Bak
er C
reek
nea
r M
anh
atta
n
Gal
lati
n R
iver
at
Cam
ero
n
Bri
dge
nea
r B
elgr
ade
(T).
Gal
lati
n R
iver
at
Cen
tral
Par
k
nea
r M
anh
at
tan
(T
).
Rid
gle
y C
reek
nea
r M
an
hat
tan.
Lo
cati
on
Des
crip
tion
Aft
er J
un
e 10
, 19
52:
SW
M s
ec.
36,
T.
1 S
., R
. 3
E.
At
coun
ty r
oad
bri
dg
e, 1
mil
e n
ort
h o
f L
ittl
e H
ol
lan
d S
choo
l an
d 8
.5
mil
es s
outh
wes
t of
B
elgr
ade.
NW
M s
ec.
12,
T.
1 N
.,
R.
3 E
. A
t co
un
ty
road
bri
dge,
0.3
mil
e ab
ov
e m
ou
th a
nd
1 .
5 m
iles
eas
t of
Man
hat
tan.
NW
M s
ec.
22,
T.
1 S
., R
. 4
E.
Nea
r ce
nte
r of
sp
an o
n dow
n
stre
am s
ide
of b
ridge,
3
mil
es s
ou
thw
est
of
Bel
gra
de
and
12
mil
es
abo
ve
conf
luen
ce
wit
h E
ast
Gal
lati
n
Riv
er.
NE
M s
ec.
19,
T.
1 N
., R
. 4
E.
Nea
r ri
ght
ban
k o
n d
ow
nst
ream
si
de o
f ra
ilro
ad b
ridge,
3
mil
es s
ou
thea
st o
f M
anhat
tan a
nd
5
mil
es a
bove
con
flue
nce
wit
h E
ast
Gal
lati
n
Riv
er.
SW
M s
ec.
7, T
. 1
N.,
R.
4 E
. A
t co
unty
road
bri
dge
abov
e m
outh
an
d 2
mil
es e
ast
of
Man
hat
tan
.
Lat
itu
de
45°4
2'05
"
45°5
1'35
"
45°4
5'
45°4
9'
45°5
1'00
"
Lo
ng
itu
de
nns'
so"
111°
17'5
5"
111°
13'
111°
16'
Iiri
6'5
5"
Dra
in
age
area
(squar
e m
iles
)
6.3
2
Gag
e
Type
S<
S5
w S S <
Alt
itude
of d
atum
(f
eet)
« 4,
496.
1
6 4,
291.
4
Max
imum
dis
char
ge
Dat
e
Jun
e 14
, 19
53
Jun
e 18
, 19
53
Cu
bic
fe
et
per
se
cond
9,1
10
4,9
70
Gag
e hei
ght
(fee
t)
7.0
0
5.2
2
Min
imum
dis
char
ge
Dat
e
Oct
. 8,
19
53
Aug
. 2,
19
51
Cubic
fe
et
per
se
con
d
27 4.8
Gag
e hei
ght
(fee
t)
1.8
7
.92
Rem
ark
s
Month
ly r
un
off
der
ived
fr
om m
easu
rem
ents
at
month
ly i
nte
rval
s an
d
com
par
iso
n o
f hydro
- g
rap
hs,
su
pp
lem
ente
d
by w
eekl
y or
dai
ly g
age
read
ings.
Do.
Do
.
I O < > «- o
Cam
p C
reek
nea
r B
elg
rad
e.
Ran
dal
l C
reek
nea
r M
an
hat
tan.
Rock
y C
reek
(E
ast
Gal
lati
n
Riv
er)
nea
r B
oze
man
(T
).
Bea
r C
reek
nea
r B
oze
man
(T
).
So
urd
ou
gh
(B
oze
man
) C
reek
nea
r B
oze
man
(T
).
Eas
t G
alla
tin
R
iver
at
Bo
zem
an (
P).
Bri
dg
er C
reek
nea
r B
oze
man
(P
).
EM
sec
. 28
, T
. 1
S.,
R.
3 E
. A
t co
unty
ro
ad
bri
dge
at
Arn
old
rai
l
road
sid
ing,
9.5
mil
es
south
wes
t of
Bel
gra
de
and 1
0 m
iles
ab
ov
e m
outh
.
i se
c. 2
, T
. 1
N.,
R.
3 E
. A
t co
un
ty r
oad
b
rid
ge,
1 m
ile
east
of
Man
hat
tan a
nd 1
.5
mil
es a
bo
ve
mouth
.
sec.
24,
T.
2 S
., R
. 6
E.
On
right
ban
k,
0 . 3
mil
e d
ow
nst
ream
fr
om h
igh
way
bri
dge
and 6
mil
es s
ou
thea
st
of B
oze
man
.
sec.
36,
T.
2 S
., R
. 6
E.
On
left
ban
k,
3 m
iles
ab
ov
e m
ou
th
and
6 m
iles
south
east
of
Bo
zem
an.
sec.
17,
T.
3 S
., R
. 6
E.
On
left
ban
k,
0.2
5 m
ile
abo
ve
Bo
zem
an s
ettl
ing b
a
sin
and
7 m
iles
so
uth
of
Bo
zem
an.
4 se
c. 3
1, T
. 1
S.,
R.
6 E
. O
n le
ft b
ank,
100
ft a
bo
ve
hig
hw
ay
bri
dge,
500
ft
belo
w
mouth
of
Sourd
ough
Cre
ek,
0.5
mil
e ab
ov
e m
ou
th o
f B
ridger
C
reek
and 0
.5 m
ile
nort
h o
f B
ozem
an.
45°4
2'55
"
45°5
1'40
"
45°3
8'35
"
45°3
7'35
"
45°3
4'40
"
45°4
2'05
"
sec.
34,
T.
1 S
.,"R
. 6"
E.
On
rig
ht
ban
k,
3 m
iles
ab
ov
e m
ou
th a
nd
3 m
iles
nort
hea
st o
f B
oze
man
.
45°4
2'30
"
HI'
21
'15
"
110°
55'3
5"
110
055'
45"
111°
01'4
0*
110°
58'0
0ff
34.5
S
'
49.5
17.6
28.0
149 62.2
« 5,044.1
« 5, 1
83.4
1 5, 351.0
« 4,701.6
June
3,
1953
....do..
June 4,
1953
...do...
June
3,
1953
608
450
040
O^o
1,240
902
4.65
3.40
2.41
6.09
4.90
Nov. 7
,1952
Feb. 9
,10,
19-
25,
1953
;Mar. 3
,4, 1953
Feb.
23,
24,
1953
Dec. 9
,1944
Mar.
23,
1953
7.9
1.1
5 12
.9
1.88 .31
Do.
Do
.
Mea
sure
men
t p
rio
r to
co
n
tin
uo
us
reco
rd:
Sep
t.
11,
1951
, 15.1
cfs
; S
ept.
21
, 19
51,
14.0
cf
s.
Mea
sure
men
ts p
rio
r to
co
nti
nu
ou
s re
cord
: S
ept.
11,
195
1, 3
.6 c
fs.
8 M
Ul
See
foot
not
es a
t en
d of
tab
le.
CO
TABL
E 6.
Des
crip
tion
s of
str
eam
-gag
ing
stat
ions
in
the
Gal
lati
n V
all
ey C
onti
nued
Gag
ing
stat
ion
Lym
an C
reek
near
Boz
eman
.
Chu
rn C
reek
nea
rB
ozem
an.
Dee
r C
reek
nea
rB
ozem
an.
Eas
t G
alla
tin
Riv
er n
ear
Bel
grad
e.
Mid
dle
Cot
ton-
woo
d C
reek
Loc
atio
n
Des
crip
tion
NW
Ji s
ec.
28,
T.
1 S.
,R
. 6E
. A
bout
0.2
5m
ile
abov
e ci
ty o
fB
ozem
an d
iver
sion
and
abou
t 1
. 5 m
iles
abov
e m
outh
.
SW
Ji s
ec.
30,
T.
1 S.
, R
.6
E.
Abo
ut 2
mile
sab
ove
mou
th a
nd 2
mil
es n
ort
h o
fB
ozem
aa.
NW
J£ s
ec.
30,
T.
1 S.
,R
. 6
E.
At
coun
tyro
ad,
1 m
ile a
bove
mou
th a
nd 3
mile
sn
ort
h o
f B
ozem
an.
SE
Ji s
ec.
4, T
. 1
S.,
R.
5 E
. A
t S
pain
rai
lro
ad s
idin
g an
d 3
mile
sea
st o
f B
elgr
ade.
SW
M s
ec.
9, T
. 1
S.,
R.
6 E
. O
n le
ft b
ank,
Lat
itude
45°4
3'30
ff
4504
5'50
"
Lon
gitu
de
110°
59'3
0"
110°
59'5
0"
Dra
in
age
area
(squ
are
mil
es)
175 4.3
5
Gag
e
Typ
e
S 5
R
Alt
itud
eof
dat
um(f
eet)
65,2
86.5
Max
imum
dis
char
ge
Dat
e
June
4,
1953
Cub
icfe
etpe
rse
cond 12
0
Gag
ehe
ight
(fee
t)
2.3
2
Min
imum
dis
char
ge
Dat
e
Cub
icfe
etpe
rse
cond
Gag
ehe
ight
(fee
t)
Rem
arks
Mon
thly
run
off
deri
ved
from
mea
sure
men
ts a
tm
onth
ly i
nter
vals
and
com
pari
son
of h
ydro
-gr
aphs
.
Mon
thly
run
off
deri
ved
from
mea
sure
men
ts a
tm
onth
ly i
nter
vals
and
com
pari
son
of h
ydro
-gr
aphs
. M
easu
rem
ents
prio
r to
con
tinu
ous
rec
ord:
S
ept.
13,
195
1,0
.5 c
fs;
Aug
. 27
, 19
52,
0.6
cfs
.
Mon
thly
run
off
deri
ved
from
mea
sure
men
ts a
tm
onth
ly i
nter
vals
and
com
pari
son
of h
ydro
-gr
aphs
.
Mon
thly
run
off
deri
ved
from
mea
sure
men
ts a
tm
onth
ly i
nter
vals
and
com
pari
son
of h
ydro
-gr
aphs
, su
pple
men
ted
by w
eekl
y or
dai
ly g
age
read
ings
. M
easu
re
men
ts p
rior
to
cont
in
uous
rec
ord:
Ju
ly 1
2,19
51,
75.0
cfs
; A
ug.
3,19
51,
25.2
cfs
; S
ept.
5,
1951
, 52
.4 c
fs.
O o M
oa
O C3 g M
GO e r g ^ S o
near
Boz
eman
(T).
Mid
dle
(Hya
lite
) C
reek
at
Hya
li
te r
ange
r st
atio
n ne
ar
Boz
eman
(P
).
Mid
dle
(Hya
lite
) C
reek
nea
r B
elgr
ade.
Bos
twic
k C
reek
ne
ar B
elgr
ade.
Tho
mps
on C
reek
ne
ar B
elgr
ade.
Ben
Har
t C
reek
ne
ar B
elgr
ade.
Ros
s C
reek
nea
r B
elgr
ade
(T).
100
ft f
rom
For
est
Ser
vice
tra
il,
0 . 8
mil
e fr
om e
nd o
f co
unty
ro
ad,
and
5.5
mile
s no
rthe
ast
of B
ozem
an.
sec.
23,
T.
3 S.
, R
. 5
E.
On
righ
t ba
nk,
7.5
mile
s so
uth
of
Boz
eman
and
20
mile
s ab
ove
mou
th.
SE
M s
ec.
32,
T.
1 N
., R
. 5
E.
At
rail
road
br
idge
, 0.5
mil
e ab
ove
mou
th a
nd 2
. 5 m
iles
no
rthe
ast
of B
elgr
ade.
[EM
sec
. 6,
T.
1 S.
, R
. 6E
. 0.2
5 m
ile a
bove
di
vers
ion
dam
and
7
mil
es e
ast
of B
elgr
ade.
SE
M s
ec.
13,
T.
1 N
., R
. 4
E.
0.5
mile
abo
ve
mou
th a
nd 4
mile
s no
rth
of B
elgr
ade.
EM
sec
. 11
, T
. 1
N.,
R.
4 E
. 0
.5 m
ile
abov
e m
outh
and
5
mile
s nort
h o
f B
el
grad
e. sec.
16,
T.
1 N
., R
. 6
E.
On
left
ban
k,
5 ft
abo
ve c
ount
y ro
ad b
ridg
e an
d 10
m
iles
nort
heas
t of
B
elgr
ade.
45°3
4'
45°4
7'15
"
45°4
7'00
"
45°4
9'55
"
45°5
1'00
"
45°5
0'30
"
111
C07'
40»
111°
09'3
5"
110°
59'2
5*
48.4
5.04
1.29
R S«
S S*
R
'5,5
39.6
«5,1
94.9
June
14,
18
98
June
3,
1953
; Ju
ly 5
, 6,
1953
956
34
9 2. 1
0
1.86
Feb
. 2,
19
39
Mar
. 21
-25,
19
52
.4
9.2
» 1.
16F
low
reg
ulat
ed b
y M
iddl
e C
reek
Res
ervo
ir s
ince
M
arch
195
1.
Mon
thly
run
off
deri
ved
from
mea
sure
men
ts a
t m
onth
ly i
nter
vals
and
co
mpa
riso
n of
hyd
ro-
grap
hs.
Mea
sure
men
t pr
ior
to c
onti
nuou
s re
c
ord:
Oct
. 8,
195
2, 5
3.5
cf
s.
Mon
thly
run
off
deri
ved
from
mea
sure
men
ts a
t m
onth
ly i
nte
rval
s an
d
com
pari
son
of h
ydro
- gr
aphs
, su
pple
men
ted
by w
eekl
y or
dai
ly g
age
read
ings
. M
easu
rem
ent
prio
r to
co
ntin
uous
re
c
ord:
S
ept.
14
, 19
51,
1.7
cfs
.
Mon
thly
run
off
deri
ved
from
mea
sure
men
ts a
t m
onth
ly i
nte
rval
s an
d
com
pari
son
of h
ydro
- gr
aphs
, su
pple
men
ted
by w
eekl
y or
dai
ly g
age
read
ings
.
Do.
See
foot
note
s at
end
of t
able
.cn
TABL
E 6.
Des
crip
tion
s of
str
eam
-gag
ing
stat
ions
in
the
Gal
lati
n V
all
ey C
onti
nued
Gag
ing
stat
ion
Tru
man
Cre
ekne
ar B
elgr
ade.
Ree
se C
reek
nea
rB
elgr
ade
(T).
Bea
r C
reek
nea
rB
elgr
ade.
Fos
ter
Cre
ekne
ar B
elgr
ade.
Dry
Cre
ek a
tA
ndru
s ra
nch
near
Man
h
atta
n (
T).
Loc
atio
n
Des
crip
tion
SW
M s
ec.
21,
T.
1 N
.,R
. 6
E.
100
ft a
bove
aban
done
d di
vers
ion
ditc
h an
d 9
. 5 m
iles
nort
heas
t of
Bel
grad
e.
NE
Ji s
ec.
10,
T.
1 N
.,R
. 5
E.
On
left
up
stre
am a
bu
tmen
t of
coun
ty b
ridg
e, 7
mile
sno
rthe
ast
of B
elgr
ade.
SE
J£ s
ec.
7, T
. 1
N.,
R.
5 E
. A
t co
unty
road
bri
dge,
300
ft
abov
e m
outh
and
5m
iles
nort
h of
Bel
gr
ade.
NE
Ji s
ec.
12,
T.
1 N
.,R
. 4
E.
At
coun
ty
road
bri
dge,
5 . 5
mile
sno
rth
of B
elgr
ade.
SE
J£ s
ec.
23,
T.
2 N
.,R
. 4
E.
On
righ
tdo
wns
trea
m a
butm
ent
of c
ount
y br
idge
, 0.2
5m
ile
abov
e m
outh
of
Rey
nold
s C
reek
and
8 m
iles
nor
thea
st o
fM
anhat
tan.
Lat
itud
e
45°4
9'25
*
45°5
1'35
*
45°5
1'00
*
45°5
4'35
*
Lon
gitu
de
110°
59'1
0*
111°
04'5
0*
111°
08'5
5*
111
010'
55*
Dra
in
age
area
(squ
are
mile
s) 2.94
22.0
4.3
0
96.4
Gag
e
Typ
e
R S 10
R
Alt
itud
eof
dat
um(f
eet)
64,5
05.2
«4, 4
45.0
Max
imum
dis
char
ge
Dat
e
June
3,
1953
Apr
. 7,
1952
Cub
icfe
etpe
rse
cond 17
5
309
Gag
ehe
ight
(fee
t)
3.5
5
4.0
3
Min
imum
dis
char
ge
Dat
e
July
31,
1951
Cub
icfe
etpe
rse
cond 4.0
Gag
ehe
ight
(fee
t)
1.93
Rem
arks
Mon
thly
run
off
derv
ied
from
mea
sure
men
ts a
tm
onth
ly i
nter
vals
and
com
pari
son
of h
ydro
-gr
aphs
. M
easu
rem
ent
prio
r to
con
tinu
ous
rec
ord:
S
ept.
14,
195
1,1
. 1 c
fs.
Mon
thly
run
off
deri
ved
from
mea
sure
men
ts a
tm
onth
ly i
nter
vals
and
com
pari
son
of h
ydro
-gr
aphs
, su
pple
men
ted
by w
eekl
y or
dai
ly g
age
read
ings
. M
easu
rem
ent
prio
r to
con
tinu
ous
rec
ord:
S
ept.
14,
195
1,2.7
cfs
.
Mon
thly
run
off
deri
ved
from
mea
sure
men
ts a
t ab
out
mon
thly
inte
rval
san
d co
mpa
riso
n of
hy-
drog
raph
s.
Oi
g
o
f
o o CJ $
WATER RESOURCES 67
*Ul -ikllls11 i:&*i ft i:^| ft Sis« Sfl-g'sJ^ -c«-s-oibsg2| . Si'^gS-S -Sl'^gl-SSge£j3 to fT* <» 3 t, !H?) "72 !n3t43t;3iM S§ Ig^'C^o IS^-C" o^ e .i>g §3g|^>. §sgS"'^.8|.^§ ^1 S 111^ - xIMfi|5^fl) p1 r *Y 43 PJ tr flj M -. >Y 43 5 rj G) M wsl ^sg^^^^d | ^gg^M^^g^w sQ e2j3e2>>g M ci gja e 8 >.g'i:^t-jj"<! Oui^lSTJJSh OCJc3«T3j3t.O.O'-i
« 2 200
t-
oo"^us
3^
IM
w w
a'->o
PS a
R. 4 E. 0.1 mile above mouth and 8 miles northeast of
Manhattan.
vB
a §§ sS|SJ$
or
_^s . s Si
onthly runoff derived from measurements a'
about monthly interv and comparison of hy irographs, supplemen oy weekly or daily ga
readings.
2
02 o-
1C 1C O O T»I IM T)< 1Ci-i IM ro ro
t * * *IO O O "^S*1 ^ r1 r1« Xi M JqlO U5 10 U5
lO 10 1O 1O^ ^ ^ ^
r a-afe°3 .«<», rlcJS*. ro>o,^
Sllllii Sffl 3fP sl3iS-|i >l||j >11|| SI «;«*«!
vt f o o R a> 6 -» VJ, O-3-w V(i 3OT) oi >* 5 3^ oS ^.J O«-J3 2JS O C3 jt/^i-O'S * "^^i OO 0 ^ "-^.J fi O C "ejuOn-d o 15 SO e^: H ^ ^ * 02 02 !5 !5j hV CQ
^S §&i «£ £§ £§g |2 g ^ o§ og gO553JS ^§ is os d os£
& 02 6 5
oCO
oCO
s1C
SEM sec. 31, T. 2 N., R. 4 E. At county road bridge, 1 .5 miles
above mouth and 3 . 5
miles northeast of
Manhattan.
3 ,£ a
a \, °*
3 S Jn
TABL
E 6
. D
escr
ipti
ons
of
stre
am
-gagin
g s
tati
ons
in t
he G
alla
tin
Vall
ey C
onti
nued
Gag
ing
stat
ion
Gal
lati
n R
iver
at
Log
an (
P).
Loc
atio
n
Des
crip
tion
NE
M s
ec.
35,
T.
2 N
.,R
. 2
E.
On
righ
tba
nk a
t br
idge
, 0.5
mil
e w
est
of L
ogan
and
5 m
iles
abov
eco
nflu
ence
wit
h Je
ffe
rson
and
Mad
ison
Riv
ers.
Lat
itud
e
45°5
3'
Lon
gitu
de
111°
26'
Dra
in
age
area
(squ
are
mile
s)
1,80
5
Gag
e
Typ
e
R
Alt
itud
eof
dat
um(f
eet)
'4,0
82.3
Max
imum
dis
char
ge
Dat
e
June
5,
1948
Cub
icfe
etpe
rse
cond
7,87
0
Gag
ehe
ight
(fee
t)
8.4
0
Min
imum
dis
char
ge
Dat
e
July
19,
1939
Cub
icfe
etpe
rse
cond
130
Gag
ehe
ight
(fee
t.)
2.0
4
Rem
arks
O O Kj
O M1
Dat
um o
f 19
29,
sup
ple
men
tary
ad
just
men
t of
194
0.2
Aft
er A
pr.
8,
1952
.
3 A
fter
Mar
. 31
, 19
52.
4 A
fter
Ju
ne
9, 1
952.
-
Aft
er A
pr.
16,
195
2.
6 D
atum
of
1929
, u
nad
just
ed.
? A
fter
Apr.
5,
1952
. 8
Aft
er J
une
10,
1952
.
9 S
ite
and d
atum
th
en i
n us
e.10
Aft
er A
pr.
1,
1952
.11
Aft
er A
pr.
30,
195
2.
w CO e S: H
TABL
E 7.
Mon
thly
and
ann
ual
runo
ff, i
n ac
re-f
eet,
of s
trea
ms
in t
he G
alla
tin
Val
ley
[An
nu
al
run
off
val
ues
roun
ded
acco
rdin
g to
sta
ndar
d
pra
ctic
e of
U
.S.
Geo
logi
cal
Sur
vey.
V
alue
s in
ita
lics
wer
e us
ed i
n co
mputi
ng m
easu
red
trib
uta
ry i
nflo
w(t
able
23
)]
Wat
er y
ear
lO
ct.
Nov
.D
ec.
Jan
.F
eb.
Mar
.A
pr.
May
Jun
eJu
lyA
ug.
Sep
t.A
nnua
l
Gal
lati
n R
iver
nea
r G
alla
tin G
atew
ay
1 tt&O
1890. .................
1891
....
....
....
....
..18
92..
... ..
....
....
...
1893
....
....
....
....
..1894....... ..
....
....
.
1930
. .................
1931
....
....
....
....
..19
32..
....
....
....
....
1933 ...
....
....
....
...
1934
....
....
....
....
..
1935 ..................
1936
....
.. ............
10^7
1938
....
....
....
....
..1939 ...
....
....
....
...
1940..................
1941
....
....
....
....
..
1943
...
....
....
....
...
1944
....
....
....
....
..
1945..................
1946
....
....
....
....
..19
47..
....
....
....
....
1948. .................
1QJ.Q
1950. .................
1951
. .................
1952. .................
1953 ...
....
....
....
...
1954. .................
24,700
36,300
36,1
0045
,700
35 ,400
31,700
14,600
22,600
19,370
16,3
50
18,050
17,890
25,9
70
20,560
21,710
32,540
21 ,920
25,8
70
24,500
27,410
24 ,940
32,370
28,9
10
24,2
9028
,690
27,7
5024
,690
21 ,220
23,800
30,100
29,800
35,000
27,3
00
20,800
18,300
19,300
17,850
14,8
0016,060
14,6
9015,900
19,780
16,350
16,450
23,610
20,280
22,1
80
20,040
21 ,740
19,400
24 , 13
023
,040
21,0
0024,580
22,5
5019,460
17,910
24,600
25,000
26,700
33,8
0024
,600
18,400
17,900
16,400
17,830
13,180
14,800
14,0
6014
,740
17,080
14,380
15,8
8019,460
17,320
19,110
16,840
16,740
17,630
22,5
6019,540
17,060
19,890
18,020
19,000
16,330
19,700
24,6
0026,400
28,800
20,3
00
12,300
16,700
17,500
18,200
13,380
14,360
14,630
14,350
17,120
14,000
15,250
16,780
16,240
17,860
17,750
17,410
15,340
21 ,480
18,490
14,540
15,280
17,400
18,590
17,800
22,2
0024,700
23,900
18,9
00
17,700
15,900
14,700
15,790
12,2
4012,960
13,190
12,680
14,980
13,040
13,3
9015,330
14,780
16,490
15,310
15,920
13,100
19,470
15,680
14,510
15,440
15,550
15,180
19,700
27,700
24,6
0023
, 10
019,100
20,3
0016,300
15,900
18,150
12,6
4013,820
13,4
3013,960
19,410
14,490
15,290
16,210
17,230
16,860
16,4
6018,400
16,170
17,760
17,260
17,000
17,310
17,300
17,120
27,400
29,800
26,800
27,500
33,6
00
29,900
20,900
22,700
34,160
18,7
2034,810
15,660
22 , 17
033,770
22,7
5018,710
40 0
8044,640
21,080
17,820
47,5
4024
,740
26,520
35,980
24,830
26,1
0044
,310
20,3
70
129,000
117,
000
91,500
87,000
180,
000
89,800
117,
000
55,3
0062,820
54,9
90127 ,000
92,3
6084,430
125,
200
121 ,000
82 ,360
86,170
92,1
90
67,110
106,
700
154,
900
153 ,000
135,
000
116,
000
186,
800
53,680
157,
000
150,
000
264,000
232 ,000
239,000
125 ,000
105,000
227,000
181 ,000
38,2
90
158,000
107,700
187,
600
89,9
70
134,
500
91,2
60177
000
238
! 600
160,
600
155,
300
158,
800
193,600
224,
300
120,
400
179,
900
207,
700
183,600
85,4
0094,300
156,000
279,900
285
,400
59 ,30
029,200
71,3
0051
,100
21 ,200
59,3
2031 ,890
45 , 19
075
,810
50,6
90
45,000
37,0
1091,610
124,
400
76,250
96,3
7069
,600
113,100
78,0
1048,840
112,600
70,620
85,420
87,7
70
26,200
46,800
46,8
0058
,900
38,2
00246,800
38,8
0018,200
30,6
0029
,000
16,570
26,2
4024
,520
23,0
9032,910
26,660
26,040
26,2
1033
,020
41,210
33,6
70
37,2
8030
,830
42,630
44,260
28,1
40
45,1
5039
,170
42,540
33,890
26,8
0036 , 10
034
,700
43,7
0034
,900
2 36
, 100
26,5
0013,900
24,500
24,3
0015,370
20,2
6019
,010
18,110
23,0
9021 ,440
22 ,050
32,3
0024,120
27,290
28,180
28,4
3026,290
32,0
7030
,160
24,600
31,1
7026,910
29,210
24,3
10
612 ,0
00638,000
809,000
2690
,000
2 766 ,0
00
407,
666
591 ,0
00470,000
295,
600
420,
100
418,000
390,
200
515,
500
462,100
464,
200
385,
800
575,
900
690
, 100
530,300
513,
200
557,400
667,
600
694 ,0
0051
5,90
0
562 ,3
0052
0,20
0714,600
517,
700
t-3
H 50 19 02 o
c!
50
O
H
02 OS
C
O
See
foot
note
s at
end
of t
able
.
TABL
E 7.
M
onth
ly a
nd a
nnua
l ru
noff
, in
acr
e-fe
et,
of s
trea
ms
in t
he G
alla
tin
Val
ley C
onti
nued
Wat
er y
ear
1O
ct.
Nov
.D
ec.
Jan
.F
eb.
Mar
.A
pr.
May
June
July
Aug
.S
ept.
Ann
ual
O M
Wil
son
(Eas
t F
ork
) C
reek
nea
r G
alla
tin G
atew
ay
Q 0
1952
....
....
....
...
...
19
53
..................
160
148
134
113
128
107
117
115
101 83
101
130
206
117
1,07
0 20
92,
080
1,05
048
0 43
723
8 18
216
3 14
6
0
4,98
0 M$
2,
840
* O 0
Wes
t F
ork
of
Wil
son
Cre
ek n
ear
Gal
lati
n G
atew
ay
Cj
V.
19
52
..................
1953
..... .............
99
123
101
101
103 92
93
9877
72
75
105
160 95
767
165
1,01
0 65
930
1 28
318
4 12
312
5 953,
100
L
2,01
0 5j
Big
Bea
r C
reek
nea
r G
alla
tin G
atew
ay
j|j
19
52
..................
19
53
....
....
....
....
..19
54. .................
292
291
497
280
253
548
264
230
407
228
226
184
163
160
172
686
241
3,93
0 87
14,
900
3,33
01
,240
1
,130
514
476
357
340
73
13,0
40
J£
7,72
0 Q a O
L
ittl
e B
ear
Cre
ek n
ear
Gal
lati
n G
atew
ay
M
CO
1952...............
...
1953.................
.1954
....
....
....
...
...
99
107
107
81
85
105
73 78
86
69
7358
61
56
5919
4 6086
7 17
379
9 58
639
7 26
219
6 12
513
5 11
63,
020
5
1 ,7
80
C-H > H
Sou
th C
otto
nwoo
d C
reek
nea
r G
alla
tin G
atew
ay
H
1951....... ...........
19
52
..................
19
53
....
....
....
....
..1,
130
1,10
091
4 89
181
9 86
577
2 75
068
2 66
264
2 70
61,
340
736
6,29
0 1,
580
4,52
0 9,
120
7,86
0
3,10
0 3,
270
4,30
0
1,55
0 1,
700
1,52
0
1,21
0 1,
220
1,08
0
J27
,900
£
22,0
50
EJ ^
Gal
lati
n R
iver
at
Axte
ll B
ridg
e, n
ear
Gal
lati
n G
atew
ay
g
19
50
..................
1951
...
....
....
....
...
171,
000
95.1
3084
,170
55
.060
32,3
30
37.6
8026
,750
26
,700
H
WATER RESOURCES 71
o in
oo mo IN in
INi-C
oo *OS IN OS
COIN
|2
88t^to os os
mooIN
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m m mos os o>
jO
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£
or-»00
to
t- toCOCO
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oS
co in m IN cot-
CN
c
in
§
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'
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IN t^ IN INin in
* to into
to -H oo m m m
m mos®
Yellow Dog Creek near Belgrade
8os
COINcoos
t^toCO 1
SI
S33
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2
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IN CN
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m mos os
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O IN
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m mIN IN
<N CO <NCO IN IN
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Baker Creek near Manhattan
§tos
2g00 OS
m^t<
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°,°.t^co co coCO CN
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10 *o 10 10 10O5 O5 O5 O5 O5
TABL
E 7
. M
onth
ly a
nd a
nnua
l ru
noff
, in
acr
e-fe
et,
of s
trea
ms
in t
he G
alla
tin
Va
lley C
onti
nued
Wat
er y
ear
1O
ct.
Nov
.D
ec.
Jan
.F
eb.
Mar
.A
pr.
May
Jun
eJu
lyA
ug.
Sep
t.A
nnua
l
ra
Gal
lati
n R
iver
at
Cen
tral
Par
k,
nea
r M
anhat
tan
£-1 O
1950
. .................
1951
..... .............
19
52
....
....
....
....
..1953
..... .............
19
54
....
....
....
....
..
13 ,7
40
4,92
0 5,
580
19,9
30
14 ,4
20
10,8
90
16,0
70
20,5
60
17,9
10
15,7
50
20,2
4014
,750
15
,700
16,3
70
17,7
6046
,100
18
,290
166,
400
18,6
40
111,
100
43,8
10
121,
200
140,
100
41,9
90
2,49
0 29
,340
35
,920
1,22
0 6,
830
3,48
0 1,
530
4,17
0 10
,710
7,
100
2,51
0
3
476,2
66
Q31
0,60
0 o * d
Rid
gley
Cre
ek n
ear
Man
hat
tan
<;
s-~
19
52
..................
1953
..................
1954... ...............
413
237
113
393
276
154
393
234
195
313
262
276
239
307
274
385
240
325
236
119 84
258
145
115 79
301 79
3,59
8 hr
t 2
,390
JO M
Cam
p C
reek
nea
r B
elgr
ade
£H
1952....... ...........
19
53
....
....
....
....
..19
54
..................
296
271 74
149
189 71
87
103 74
67
116
58
107
65
145
3,13
0 17
136
1 15
831
1 36
331
7 31
020
0 14
732
3 83
O
5 ,3
64
H
2,16
0 &
..........
Q F
Ran
dal
l C
reek
nea
r M
anh
atta
n
E~]
>J
19
52
..................
19
53
..................
19
54
....
....
....
....
..ie
915
384
11
7
397 46
11
9
234 41
234 34
484 36
1,05
0 13
963
9 11
71,
380
104
65
8935
3 16
549
2 95
»-H
^
1 , 1
20
<H F
Roc
ky C
reek
(E
ast
Gal
lati
n R
iver
) n
ear
Boz
eman
^
1952
. .................
1953
..................
754
710
750
600
690
592
608
593
574
555
654
848
8,14
0 2,
010
9,99
0 5,
990
3,23
0 8,
270
1,47
0 1,
550
867
912
742
785
is,
28,4
70
O
23,4
20
2, H
WATER RESOURCES 73
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508919 O-60 6
TABL
E 7.
M
onth
ly a
nd a
nnua
l ru
noff
, in
acr
e-fe
et,
of s
trea
ms
in t
he G
alla
tin
Val
ley C
onti
nued
Wat
er y
ear
*O
ct.
Nov
.D
ec.
Jan
.F
eb.
Mar
.A
pr.
May
June
July
Aug
.Se
pt.
Ann
ual
O raL
yman
Cre
ek n
ear
Boz
eman
2 0
19
52
....
....
....
....
..19
53
..................
234
246
196
208
184
184
173
166
149
150
179
172
349
149
627
248
714
762
545
479
397
394
274
345
4,02
0 i-4
3,
500
" 2 oC
hurn
Cre
ek n
ear
Boz
eman
d
1953
9432
657
6824
F ^ f D
eer
Cre
ek n
ear
Boz
eman
2 td
1953..................
4510
914
66
s 02 C?
Eas
t G
alla
tin
Riv
er n
ear
Bel
grad
e ^ ^
1952..................
1953..................
1954
4,28
0 2,
640
2,35
0
3,78
0 2,
520
2,52
0
3,53
0 2,
590
2,57
0
2,64
0 2,
780
2,97
0 2,
040
3,11
0 3,
270
22,5
30
5,77
042
,800
16
,630
17,1
20
33,4
507,
200
5,16
03,
690
2,52
03,
490
2,45
011
7,10
0 02
81
,820
" >-
i rM
iddl
e C
otto
nwoo
d C
reek
nea
r B
ozem
an
9> i-3 i i
1Q
K1
1952..................
1953..................
79
4469
45
63
4055
40
52
2870
52
939
241
1,46
0 97
3
353
368
1,55
0
134
137
182
83
79
70
71
54
42
2
3,42
0 ^
3,31
0 p W
M
iddl
e (H
yali
te)
Cre
ek a
t H
yali
te R
ange
r S
tati
on,
near
Boz
eman
^ t>
1895..................
1896..................
1897..................
3,13
6 2.
337
2,73
722,4
60
2 1,
845
2 1,
438
2 1
,537
1,96
45,
903
17,2
5610
,084
3,56
6 2,
705
2,97
5 2,
380
025
3,44
5 ^
ISO
ft
18
99
..................
19
00
....
....
....
....
..19
01 ...
....
....
....
...
19
02
....
....
....
....
..19
03
....
....
....
....
..19
04
..................
1004
.19
35
..................
19
36
..................
1937...................
1938
. .................
19
39
....
....
....
....
..
1940
. .................
1941
...
....
....
....
...
19
42
..................
1943............. ..
...
19
44
....
....
....
....
..
19
45
....
....
....
....
..19
46
....
....
....
....
..19
47
....
....
....
....
..19
48. .................
1949........... .......
19
50
..................
19
51
... ...............
19
52
..................
19
53
..................
19
54
....
....
....
....
..
2 4
,544
2,98
72
2,95
1
2,58
0
1,17
01,
310
1,30
01,
350
1,78
0
1,47
01,
610
3,26
01,
830
1,83
0
2,30
02,
080
2,06
02,
780
2,51
0
2,03
02,
060
2,19
01
,750
1,76
0
23,8
68
2,32
0
i,6io
1,10
01,
130
1,04
01,
460
1,11
01,
170
2,07
01,
590
1,74
0
1,50
01,
790
1,90
01,
940
2,23
0
1,51
01,
810
1,61
088
11,
080
23,6
89
2 1
,840 70
81,
060
1,03
086
11,
350
1,02
01,
070
1,90
01,
270
1,26
0
1,17
01,
610
1,37
01,
860
1,84
0
1,39
01,
740
1,37
070
086
3
2 3,
074
599
837
891
899
1,17
0
1,12
01,
270
1,51
01,
200
1,12
0
1,10
01,
410
1,04
01,
810
1,21
0
1,12
01,
500
1,09
081
5
2 3, 0
55 637
690
696
742
833
750
1,06
01,
010
1,16
01,
100
1,10
01,
410
916
1,06
01,
250
1,16
099
21,
060
845
24,6
12
764
906
873
980
1,07
0
841
1,22
01,
230
1,06
01,
060
1,02
01,
480
994
1,48
092
0
1,16
065
31,
150
1 ,0
30
2 4,
844
2 5,3
55
1,10
03,
900
1,24
02,
100
2,57
0
1,87
01,
900
4,0
50
4,0
50
1,30
0
1,28
04,
680
2,28
07,
290
3,12
0
1,81
01,
360
3,24
01
,480
10,8
8329,2
85
2 9
,039
6,59
07,
270
8,46
08,
170
8,59
0
10,4
406,
790
7,3
40
7,77
08,
060
8,33
06,
920
12,6
4017
,860
8,71
0
6,09
06,
880
17,2
805,
450
24,1
5929
,982
2 16
,066
15 ,0
55
13,9
105,
280
9,4
30
10,9
807,
770
12,0
207,
370
10,8
3014
, 19
013
,970
11,9
909,
200
14,2
8015
,830
9,8
30
12,1
707,
330
13,3
4013
,740
13 ,5
8920
,559
5,47
2
7,13
3
7,23
01,
880
3,2
80
3,98
04
,71
0
4,1
60
2,78
08,
040
8,26
07
,63
0
9,2
50
5,61
09
,86
06,
390
4,18
0
7,68
06,
120
6,36
08
,54
0
4,5
62
6,38
3
3,3
82
4,5
64
2,52
01,
530
1,57
02,
260
2,08
0
2,07
01,
820
2,74
02,
820
2,75
0
2,78
02,
950
3,76
04
,59
02,
130
3,3
80
4,0
70
4,0
00
5,36
0
4,45
73,4
14
2,85
6
2,49
9
22,3
80
2964
1,47
01,
260
1,43
01,
520
1,65
0
1,68
03
,430
1,96
01,
860
2,67
0
2,18
02,
290
3,31
03,
030
2,17
0
2,33
01,
980
2,77
02,
330
29
7,8
20
37,7
1027
,020
31,3
3034
,880
35,0
30
38,5
5031
,49
045
,940
47 ,0
6044
,490
44,0
0041
,43
054
,410
65 ,9
2040
,100
41 ,
830
3 36
, 500
M9
,46
0342,9
20
3 H
M
SO SO
M
tn
O c| s M
tn
Mid
dle
(Hya
lite
) C
reek
nea
r B
elgr
ade
1952
..................
974
339
258
688
7,160
15,3
008,
090
7,360
4,68
34,
760
Bos
twic
k C
reek
nea
r B
elgr
ade
19
52
..................
19
53
....
....
....
....
..19
54 ..................
ol
85 86
95 77 57
89 41 26
79 6669 50
83 6546
493
068
670
41,
660
315
424
165
137
107
101
3,2
00
3,5
20
See
foo
tno
tes
at e
nd o
f ta
ble.
76 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
"3
§ *3
a02
M
3
>>
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e
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Bea
r C
reek
nea
r B
elgr
ade
1952..
....
....
... ..
...
1953
....
....
....
....
..18
8 18
918
1
186
163
195
152
167
193
196
246
166
210
184
245
432
230
212
163
186
204
224
117
200
161
182
162
2,5
10
2,2
60
Post
er C
reek
near
Bel
gra
de
19
53
....
....
....
....
..23
3216
1512
Dry
Cre
ek a
t A
ndru
s ra
nch
, n
ear
Man
hat
tan
's-
Rey
nold
s C
reek
near
Man
hat
tan
fr
jer
l
1953
..................
6865
7489
6777
6076
127
9292
9598
2 g
CQ O
Dry
Cre
ek a
t B
row
nel
l ra
nch
, near
Man
hat
tan
^ »
1951... ...............
508
402
332
458
O H
Sto
ry C
reek
near
Man
hat
tan
1952... ...............
1953
..................
1954
..................
1,4
80
1
,12
0
1,0
00
1,2
90
1
,18
0
922
1,2
90
1
,11
077
8
1,0
70
1
,06
080
579
783
1 93
61
,33
0
845
1,7
00
776
674
900
984
664
1,0
60
1
,07
01
,29
0
1,1
80
13
,80
0
11
,64
0
Cow
an C
reek
near
Man
hat
tan
195
2..
....
....
....
....
1953
..................
195
4..
....
....
....
....
541
581
562
512
526
568
415
500
555
430
586
442
477
480
491
662
499
635
342
409
650
309
584
403
200
476
419
5,7
14
5,8
60
See
footn
ote
s at
end
of
tab
le.
TABL
E 7
. M
onth
ly a
nd a
nnua
l ru
noff
, in
acr
e-fe
et,
of s
trea
ms
in t
he G
alla
tin
Vall
ey C
onti
nued
Wat
er y
ear
1O
ct.
Nov
.D
ec.
Jan.
Feb
.M
ar.
Apr
.M
ayJu
ne
July
Aug
.S
ept.
Ann
ual
Gib
son
Cre
ek n
ear
Man
hat
tan
1952..
................
1953
....
. ..
....
....
...
1954..
...........
1,08
01,
110
1,05
0
952
1,13
01,
110
1,020
1,11
01,
040
795
1,11
057
591
065
91,
010
942
889
946
1,09
0833
1,05
0758
753
1,08
084
51,05
01,02
010,690
12,030
Bu
llru
n C
reek
nea
r M
anh
atta
n
1952..
................
1953..
................
1954
....
....
....
....
..
829
534
532
873
637
936
922
741
1,08
0
954
746
827
706
805
869
1,85
080
72,
230
631
833
926
1,06
028
620
836
9686
367
12,080
7,620
Gal
lati
n R
iver
at
Log
an
1893
. .................
18
94
....
....
....
....
..1895.................
.18
96. ..
....
....
....
...
18
97
..................
1898
. .................
1899.................
.19
00. .................
1901
...
....
....
....
...
19
02
..................
19
03
....
....
....
....
..1904.................
.19
05
..................
1906.......... ........
19
28
....
....
....
....
..19
29 ..................
19
30
..................
19
31
....
....
....
....
..19
32
....
....
....
....
..
2 36
, 900
M3,0
00
43,2
0041
,80
0
37 ,9
0051
,300
2 34
,900
07
ofln
oo
j.nn
36,3
0043
,800
45,4
00on
7f>
n
54,7
0041
,600
55,2
0024
.900
229,
800
24
4,6
00
42,4
00
40,1
0042
,100
242,
800
41 ,
700
qo
ann
40 ,4
0041
,70
044
,000
36,7
00
52,8
00
32.7
00
2 27
, 700
249,
200
37,5
0043
,300
39,7
0049
,200
249,
200
38,9
0036
,900
36,9
0036
,900
50,7
002
36 9
00
44,9
0045
,100
40,1
0034
.400
2 24
, 600
49,2
0041
,800
43,0
00
43,0
0024
3,00
055
,300
23
6,9
00
32,6
00
43,0
0028
,400
45,6
00
40,3
0033
,200
38,1
0025
,800
2 25
,000
44,4
0038
,100
36 ,
100
38,9
00233,3
00
55,5
00233,3
00
30,6
00
44,4
0030
,100
36,1
00
28,9
0043
,000
30,0
0031
.100
2 35
, 000
48,8
0043
,000
40,0
00
42,8
0023
9,20
061
,500
2 36
,900
41 ,
700
48,5
0029
,400
35,7
00
48,9
0042
,700
47,5
0040
,600
2 49
,300
69,1
0042
,400
58,9
00
61,2
0027
6,30
067
,900
2 46
, 10
036
,600
51 ,9
0069
,600
32,9
00
53,1
1063
,700
51,7
0044
,300
2176
,000
148,
000
67,5
0023
2,00
0
133,
000
2121
,000
192,
000
2289
,000
133,
000
93,2
0017
0,00
058
,700
101
,000
76,9
00
71 ,
900
117,
000
2256
,000
151,
000
268,
000
173
,000
296,
000
2325
,000
134,
000
2122
,000
165,
000
210,
000
232
,000
132,
000
168,
000
57,7
00
88,1
0015
9,00
0
267,6
00
64,6
0075
,000
42,7
00
57 ,4
0021
05,0
0020
,200
2 17
,600
53,4
00
72,6
0079
,300
31,7
00
46,7
0022
,100
11 ,
600
37,8
00
227,7
00
29,5
0042
,900
27,5
00
22,8
002
41 ,
900
21 ,
000
2 11
,600
25,2
00
22,6
0022
,000
13,8
00
229,5
00
19,5
0032
, 10
0
14 ,4
0018
,400
223,8
00
2 31
,50
043
,000
40,6
0030
,800
43,9
002
30 ,3
0028
,800
224,0
00
23,7
00
24,8
0032
,400
16,6
00
41,3
0029
,700
36,2
00
18,0
0026
,700
2787
,000
2784
,000
782,
000
810,
000
857,
000
2958
,000
2763
,000
2 73
5 ,0
0064
6,00
0
725
,000
816,
000
543
,000
688,
000
539
,000
511,
000
593,
000
H
1 Q°.^
l
1QQ4.
1935 ...
....
....
....
...
1 Q°.f
l
1937
....
....
....
....
..1QQQ
1939
...
....
....
....
...
1940
....
....
....
....
..19
41 ...
....
....
....
...
1942..................
1943
....
....
....
....
..1944 ...
....
....
....
...
1945
....
....
....
....
..1946.. ...
....
....
....
.1947 ..................
1948. .................
1949....... ...........
1950
....
....
....
....
..19
51..
....
....
....
....
1952
....
....
....
....
..19
53 ..................
1954
....
....
....
....
..
39,0
002 39
,970
20,4
9025,180
23 , 14
024,480
40,5
00
34,9
0033
,450
60,580
43,2
8041
,950
49 , 13
049
,010
51,540
65,4
0051,960
49,3
6058
,680
55,520
37,8
4035
,990
49,0
002 45, 820
19,500
36,5
1028,920
26,6
3050
,620
35,6
0035,760
53,340
49 , 10
049
,940
46,9
3049
,560
53,7
1061 ,76
056
,230
49,2
4054
,420
55,900
47,9
0043
,030
37,5
002 40
, 580
28,5
4036
,520
30,6
8034
,590
45 , 18
0
39 ,860
39,9
9052
,490
42,6
9049
,700
44,3
8045 ,720
48,4
8055
,960
51,2
10
42,4
1051
,370
47,6
6049
,990
48,0
30
38,700
2 39, 970
27,6
7033
,830
25,1
9033
,540
40,1
40
33 ,990
38,010
40,2
7041
,010
41,0
00
46,9
3043,170
44,4
5054,020
44 050
35 ,780
39,6
1042
,620
cn 9flft
25,8
0035
,570
27,5
4022
, 14
036,370
31,0
5024,490
34,210
33,5
1038
,780
40,6
5036
,080
40,5
0039
,420
40,9
5051,250
35,790
40,8
0044
,710
39,1
80
39,6
0038
,950
34,0
2046
,670
35 , 14
034
,620
53,0
80
45,2
0043
,360
46,5
0064,960
42,6
8055,430
51,1
7054
, 12
0CQ non
47,9
1053
,270
43,6
3047
,560
42 ,300
25,5
30
37,4
9059
,250
47,3
4046
,520
58,7
90
57,9
8042
,740
96 ,970
82 ,470
4.Q
14.O
39,6
6081 ,770
67,2
2090
,870
77 QHH
57,5
6062 ,49
0118,600
47,8
70
76,9
002 10,760
43,9
6012
4 ,400
80,440
116,
300
97,3
50
132 ,400
65,0
10128,500
131
600
75,8
3012
2,60
0166,200
226 ,700
144
000
75,7
00155,300
279,100
flQ oon
137 ,000
16,660
103,
200
41,1
5084
,030
163,000
80,6
30
117,
600
58,400
193 ,300
252,
000
184,
600
148,500
114,300
228,
500
262 ,900
i n^i
tifift
151,
000
78,0
90197,200
011
7ftn
2 14
,800
9,96
0
19,190
10,480
19,750
58,300
24,3
40
18,650
20,220
51 ,680
81,700
7Q
fi4.
H
70,9
6038
,030
84,740
65 ,460
oo fi
in
75,2
8028
,580
70,220
55,870
2 16,600
10,2
90
14,3
5013 ,750
15,9
4019
,840
18,340
20,0
9021 ,960
21 ,470
32,3
5023,160
25,5
7026,790
33,6
2047
,670
23,860
40,5
7038
,420
35,8
30on
r;*7
n
2 27
, 400
14 , 19
0
19,6
9019
,360
20,9
8020
,900
25,8
10
26,3
8048
,290
36,3
1037
,730
Af\
Qi ft
36,0
8043
,650
57,5
6040
,600
38,1
20
44,0
1049
,670
44,4
6033
,410
2 545 ,0
002 32
8, 200
395,
600
447,900
609,800
559 ,3
00
596,400
480,
700
820,200
899,500
711,
100
667,
200
709,400
928
, 100
1,077,000
mQAfi
709,
600
714,
600
1,030,000
716,200
1 Y
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O
80 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
TABLE 8. Occasional measurements of the discharge of streams, ditches, and springs in the Gallatin Valley
DateDischarge
(cfs)Temperature
DateDischarge
(cfs)Temperature
Jack Creek, tributary of Gallatin River[Measured in SE 1 sec. 9, T. 4 S., R. 4 E., about 1.75 miles above mouth and 6.5 miles south of
Gallatin Gateway]
Aug. 26, 1952....... 0.2 45 Aug. 28, 1953...... 0.2
[Measured inYankee Creek, tributary of Gallatin River
sec. 3, T. 4 S., R. 4 E., about 2 miles above mouth and 5.5 miles south of Gallatin Gateway]
Aug.
[Mea
June June July Aug. Sept. Oct. Nov. Dec. Jan.
[Mea
Oct.
26, 1952...... . 0. 5 48 Aug. 28, 1953... ... 0.
Wilson Creek, tributary of Gallatin Riversured in NW^ sec. 35, T. 3 S., R. 4 E., about 0.25 mile below mouth of
miles south of Gallatin Gateway]
3, 12, 16, 12, 10, 14, 11, 17, 20,
sur
3,
1952.......1952.......1952.... .. .1952.......1952.... ...1952..1952.......1952.......1953.......
ed in SE%
1952... ....
55.48. 7. 3. 2. 2. 4. 3. 4.
sec. 32
68 0 2 3 8 6 9 0
45 56 58 53 42 37 32 35
Big Bear Creek, tribi, T. 3 S., R. 5 E., a
southeast of Ga
5.2 .......... 42
Feb. 24, 1953... ...Mar. 18, 1953.... ..Apr. 15, 1953......May 25, 1953......June 18, 1953..... .July 21, 1953.. .... Aug. 10, 1953......Sept. 17, 1953..... .
3.4. 3. 5.
29. 4. 1. 2.
9,
West Fork and 3.5
8 8 9 9 3 6 8 3
32 3340 44 47 54 58 51
itary of Wilson Creekbout 1 mile above gaging station and 5.5 miles llatin Gateway]
Big Bear Creek, tributary of Wilson Creek[Measured in NE*4 sec. 32, T. 3 S., R. 5 E., about 0.5 mile above gaging station and 5 miles
southeast of Gallatin Gateway]
Oct. 3, 1952....... 3.6 42
South Cottonwood Creek, tributary of Gallatin River[Measured in NE*4 sec. 12, T. 4 S., R. 5 E., 2.75 miles above gaging station and 9.5 miles south
east of Gallatin Gateway]
Oct. 3,1952....... ..... .6.4 41
Spain-Ferris ditch 4, diversion from Spain-Ferris ditch 5[Measured in SW^NW^A sec. 7, T. 1 S., R. 5 E., at U.S. Highway 10 and 0.85 mile southeast of
Belgrade]
July 7, 1953.... ...Aug. 5, 1953.. .....
7.47.5
Sept. 1, 1953.... ..Sept. 28, 1953... . . .
3.73.2
Spain-Ferris ditch 5, diversion from Spain-Ferris ditch 1[Measured in NW%NW*4 sec. 7, T. 1 S., R. 5 E., at U.S. Highway 10 and 0.8 mile southeast of
Belgrade]
July 7, 1953.. .....Aug. 5, 1953.......
5.61.0
Sept. 1, 1953... ....Sept. 28, 1953... ...
0.4.1
WATER RESOURCES 81
TABLE 8. Occasional measurements of the discharge of streams, ditches, and springs in the Gallatin Valley Continued
DateDischarge
(cfs)Temperature
DateDischarge
(cfs)Temperature
Spain-Ferris ditch 3, diversion from Spain-Ferris ditch 1[Measured in SW14SW14 sec. 5, T. 1 S., R. 5 E., 1.6 miles east of Belgrade]
Aug. 5,1953....... 2.1 .............. Sept. 1,1953...... 0.4
Spain-Ferris ditch 2, diversion from Spain-Ferris ditch 1[Measured in SE^SW1 sec. 5, T. 1 S., R. 5 E., 2 miles east of Belgrade,]
July 7,1953....... 0.4 .............. Sept. 1,1953...... 0.1Aug. 5, 1953....... .3
Spain-Ferris ditch 1, diversion from Gallatin River in NW% sec. 14, T. 2 S., R. 4 E.[Measured in SW^SE^ sec. 5, T. 1 S., R. 5 E., 2.1 miles east of Belgrade]
July 7,1953....... 5.0 .............. Sept. 1,1953...... 8.6Aug. 5,1953....... 4.2 .............. Sept. 28, 1953...... 6.5
Gallatin River[Measured in SE% sec. 10, T. 2 S., R. 4 E., 250 ft below Sheds Bridge and 7.5 miles west of
Bozeman]
Apr. 2, 1952...... . 305
Mammoth ditch, diversion from Gallatin River[Measured in NW^SW^ sec. 1, T. 1 S., R. 4 E., at U.S. Highway 10 and 0.4 mile northwest of
Belgrade]
July 7,1953....... 10.3 .............. Sept. 1,1953...... 2.2Aug. 5,1953....... 10.3 .............. Sept. 28, 1953. .
J. S. Hoffman ditch 2, diversion from J. S. Hoffman ditch 1[Measured in NE^NE^ sec. 33, T. 1 N., R. 4 E., at U.S. Highway 10 and 2.9 miles northwest of
Belgrade]
July 7,1953....... 3.9 .............. Sept. 1,1953...... 1.7Aug. 5,1953....... 2.1 .............. Sept. 28, 1953..... . 1.0
J. S. Hoffman ditch 1, diversion from J. B. Weaver ditch 1 in NE%, sec. 22, T. 1 S., R. 4 E.[Measured in NE^SE^i sec. 34, T. 1 N., R. 4 E., at U.S. Highway 10 and 1.7 miles northwest of
Belgrade]
July 7,1953....... 6.5 .............. Sept. 1,1953...... 1.Aug. 5,1953....... 3.8 .............. Sept. 28, 1953...... 1.5
J. B. Weaver ditch 2, diversion from J. B. Weaver ditch 1[Measured in SE^SE^ sec. 34, T. 1 N., R. 4 E., at U.S. Highway 10 and 1.65 miles northwest of
Belgrade]
July 7,1953....... 2.5 .............. Sept. 1,1953...... 0.2Aug. 5,1953....... 4.3 .............. Sept. 28, 1953...... 1.2
82 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
TABLE 8. Occasional measurements of the discharge of streams, ditches, and springs in the Gallatin Valley Continued
DateDischarge
(efs)Temperature
DateDischarge
(cfs)Temperature
J. B. Weaver ditch 1, diversion from Gallatin River in NE% sec. 22, T. 1 S., R. 4 E.[Measured in NW^NE^i sec. 2, T. 1 S., R. 4 E., at U.S. Highway 10 and 0.9 mile northwest of
Belgrade]
July 7,1953....... 22.0 .............. Sept. 1,1953...... 6.4Aug. 5,1953....... 16.8 .............. Sept. 28, 1953...... 3.6
Stone-Weaver ditch 2, diversion from Stone-Weaver ditch 1[Measured in SE^NW1! sec. 34, T. 1 N., R. 4 E., at U.S. Highway 10 and 2.3 miles northwest of
Belgrade]
Sept. 1,1953....... 0.2 .............. Sept. 28, 1953...... 0.3
Stone-Weaver ditch 1, diversion from Gallatin River in NWVi sec. 22, T. 1 S., R. 4 E.[Measured in SE%NW% sec. 84, T. 1 N., R. 4 E., at U.S. Highway 10 and 2.4 miles northwest of
Belgrade]
July 7,1953....... 4.6 .............. Sept. 1,1953...... 1.Aug. 5, 1953....... 2.1 .............. Sept. 28, 1953...... 1.3
Barnes ditch, diversion from D. N. Hoffman ditch in SWV4 sec. 28, T. 1 N., R. 4 E.[Measured in SE%SW% sec. 28, T. 1 N., R. 4 E., at U.S. Highway 10 and 3.3 miles northwest of
Belgrade]
July 7,1953....... 4.8 .............. Sept. 1,1953...... 0.7Aug. 5,1953....... 2.6 .............. Sept. 28, 1953...... .4
Gallatin River[Measured in SW*4 sec. 4, T. 1 S., R. 4 E., 200 ft below county road bridge and 3 miles west of
Belgrade]
Apr. 2,1952....... 276 ..........
Smith drain (continuation of Upper Creamery ditch), diversion from Gallatin River insec. 4, T. 1 S., R. 4 E.
[Measured in SW%SW% sec. 20, T. 1 N., R. 4 E., at U.S. Highway 10 and 4.9 miles northwest ofBelgrade]
July 7,1953....... 5.1 .............. Sept. 1,1953...... 6.7Aug. 5,1953....... 5.9 .............. Sept. 28, 1953...... 6.5
Lower Creamery ditch, diversion from Gallatin River in SW}4SE*4 sec. 19, T. 1 N., R. 4 E.[Measured in NE%SE% sec. 19, T. 1 N., R. 4 E., at U.S. Highway 10 and 5.4 miles northwest of
Belgrade]
July 7,1953....... 17.6 .............. Sept. 1,1953...... 2.1Aug. 5,1953....... 14.0 .............. Sept. 28, 1953...... 3.5
Gallatin River[Measured in SE% sec. 1, T. 1 N., R. 3 E., 50 ft below county road bridge and 1.75 miles east of
Manhattan]
Sept. 20, 1951....... 182 51
WATER RESOURCES 83
TABLE 8. Occasional measurements of the discharge of streams, ditches, and springs in the Gallatin Valley Continued
DateDischarge
(cfs)Temperature (°F) Date
Discharge (cfs)
Temperature <°F)
Camp Creek, tributary of Gallatin River[Measured in NE% sec. 4, T. 2 S., R. 3 E., at Vincent School, 50 ft below county road bridge and
10.5 miles northwest of Gallatin Gateway]
Sept. 20, 1951. 0.5 49
[Measured inCamp Creek, tributary of Gallatin River
4 sec. 2, T. 1 S., R. 3 E., at Buell railroad siding, 50 ft above county road bridge and 4.75 miles south of Manhattan]
Sept. 20, 1951 ....... 16.3 51
Gallatin River[Measured in NW% sec. 1, T. 1 N., R. 3 E., 300 ft above railroad bridge and 1.5 miles northeast
of Manhattan]
Apr. 2, 1952. 425
Pitcher Creek, tributary of Rocky Creek (East Gallatin River)[Measured in SW^ sec. 13, T. 2 S., R. 6 E., 0.4 mile above mouth and 5 miles east of Bozeman]
Sept. 13, 1951...Aug. 27, 1952.......
0.2.3
4549
Aug. 26, 1953 ...... 0.3
Kelly Creek, tributary of East Gallatin River[Measured in SE*4 sec. 11, T. 2 S., R. 6 E., 1.25 miles above mouth and 4.5 miles east of Bozeman]
Sept. 13, 1951.......Aug. 27, 1952.......
0.4.8
4349
Aug. 26, 1953...... 0.6
Limestone Creek, tributary of Sourdough (Bozeman) Creek[Measured in NE*4 sec. 4, T. 3 S., R. 6 E., at abandoned farm 2.25 miles above mouth and 5.5 miles
southeast of Bozeman ]
Sept. 12, 1951.......Aug. 26, 1952.......
0.7.7
4152
Aug. 26, 1953...... 0.5
Nichols Creek, tributary of Limestone Creek[Measured in SE^ sec. 5, T. 3 S., R. 6 E., 1.5 miles above mouth and 5.5 miles south of Bozeman]
Sept. 12, 1951.......Aug. 26, 1952. ......
0.2.2
4151
Aug. 26, 1953...... 0.2
East Gallatin River, tributary of Gallatin River[Measured in NE% sec. 36, T. 1 S., R. 5 E., 10 feet below county road bridge and 2 miles north of
Bozeman]
Apr. 3,1952....... 73.5
84 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
TABLE 8. Occasional measurements of the discharge of streams, ditches, and springs in the Gallatin Valley Continued
DateDischarge
(cfs)Temperature
DateDischarge
(cfs)Temperature
East GaUatin River, tributary of Gallatin River[Measured in NW% sec. 23. T. 1 S., R. 5 E., 4.0 miles northwest of Bozeman]
Apr. 3. 1952. 79.2
Deer Creek, tributary of East Gallatin River[Measured in SW% sec. 20, T. 1 S., R. 6 E., 1.5 miles above mouth and 3 miles northeast of
Bozeman]
Aug. 27, 1952. 0.1
Sypes Creek, tributary of East Gallatin River[Measured in SE*4 sec. 17, T. 1 S., R. 6 E., 3.5 miles above mouth and 4.5 miles northeast of
Bozeman]
Sept. 13, 1951. Aug. 27, 1952.
0.5 .1
4651
Aug. 26, 1953. 0.1
West branch of East Gallatin River, diversion from East GaUatin River in SW/4, sec. 14, T. 1 S., R. 5 E., and tributary of East GaUatin River in SW% sec. 32, T. 1 N., R. 5 E.
[Measured in SW^SW 1 sec. 4, T. 1 S., R. 5 E., 2.6 miles east of Belgrade]
July 7,1953....... 16.2 .............. Sept. 1,1953...... 7.6Aug. 5,1953....... 7.8 .............. Sept. 28, 1953...... 4.0
Arnold-Toohey ditch, diversion from East GaUatin River in SW% sec. 10, T. 1 S., R. 5 E.[Measured in SE^4SW% sec. 4, T. 1 S., R. 5 E., 3.1 miles east of Belgrade]
July 7,1953....... 1.4 .............. Sept. 1,1953...... 2.0Aug. 5,1953....... 3.9
Middle Cottonwood Creek, tributary of East Gallatin River[Measured in NW}4 sec. 10, T. 1 S., R. 6 E., 1.1 miles above gaging station and 6 miles northeast
of Bozeman]
Oct. 2, 1952.. ..... 0.6 48
Middle Cottonwood Creek, tributary of East Gallatin River[Measured in SE^ sec. 9, T. 1 S., R. 6 E., 0.5 mile above gaging station and 6 miles northeast of
Bozeman]
Oct. 2, 1952....... 0.8 48
Watts Creek, tributary of Middle Cottonwood Creek[Measured in NE^NW^i sec. 9, T. 1 S., R. 6 E., 1 mile above mouth and 6 miles northeast of
Bozeman]
Oct. 2, 1952....... 0.04 46
WATER RESOURCES 85
TABLE 8. Occasional measurements of the discharge of streams, ditches, and springs in the Gallatin Valley Continued
DateDischarge
fcfs)Temperature(°F) Date
Discharge (cfs)
Temperature (°F)
Watts Creek, tributary of Middle Cottonwood Creek
Bozeman ]
Aug. 27, Oct. 2,
1952.......1952.......
0.1 .1
46 46
Aug. 26, 1953..... . 0.1
Middle (Hyalite) Creek, tributary of East Gallatin River[Measured in NE% sec. 17, T. 1 S., R. 5 E., at U.S. Highway 10 and 2.5 miles southeast of
Belgrade]
Nov. 25, 1952...... . 4.9 Dec. 5,1952...... 0.6
Aakjer Creek, tributary of Middle (Hyalite) Creek [Measured in SE*4 sec. 17, T. 1 S., K. 5 E., at U.S. Highway 10 and 3 miles southeast of Belgrade]
Sept. 20, 1951. Nov. 25, 1952.
17.7 3.1
48.5 Dec. 5, 1952. 0.5
[Measured inMiddle (Hyalite) Creek, tributary of East Gallatin River
sec. 5, T. 1 S., R. 5 E., 0.5 mile above mouth of West Branch of East Gallatin River and 2.4 miles east of Belgrade]
July 7, 1953. Aug. 5, 1953.
46.927.5
Sept. 1, 1953... ...Sept. 28, 1953..
48.245.7
Schafer Creek, tributary of Bostwick Creek[Measured in SE^4 sec. 5, T. 1 S., R. 6 E., 3 miles above mouth and 6 miles northeast of Bozeman]
Sept. 14, 1951.......Aug. 27, 1952... ....
0.2 .1
4553
Aug. 26, 1953. 0.1
East Gallatin River, tributary of Gallatin River[Measured in NE*4 sec. 19, T. 1 N., R. 5 E., 250 ft below county road bridge and 3.5 miles north
east of Belgrade]
Apr. 3, 1952. 141
[Measured inEast Gallatin River, tributary of Gallatin River
sec. 2, T. 1 N., R. 4 E., 300 ft above county road bridge and mouth of Smith Creek and 6 miles north of Belgrade]
Apr. 3, 1952....... 221
Jones Creek, tributary of Ross Creek[Measured in NE*4 sec. 21, T. 1 N., R. 6 E., 1.5 miles above mouth and 10 miles northeast of
Belgrade]
Aug. 28, 1952....... 0.2 41 Aug. 28, 1953...... 0.1
86 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
TABLE 8. Occasional measurements of the discharge of streams, ditches, and springs in the Gallatin Valley Continued
DateDischarge
(cfs)Temperature(°F)
«
DateDischarge
(cfs)Temperature (°F)
Dry Fork Creek, tributary of Ross Creek[Measured in SE*4 sec. 4, T. 1 N., R. 6 E., 2 miles above mouth and 11 miles northeast of
Belgrade]
Oct. 2, 1952... 0.3 41
Dry Fork Creek, tributary of Ross Creek[Measured in NW% sec. 9, T. 1 N., R. 6 E., 1.5 miles above mouth and 10.5 miles northeast of
Belgrade]
Oct. 2,1952....... 0.6 41
Dry Fork Creek, tributary of Ross Creek[Measured in SW^ sec. 9, T. 1 N., R. 6 E., 1 mile above mouth and 10 miles northeast of Belgrade]
Sept. 14, 1951.......Aue. 28. 1952.......
O a
.44545 Aue. 28. 1953......
0.1.8
41
North Cottonwood Creek, tributary of Reese Creek[Measured in NE% sec, 18, T. 2 N., R. 6 E., 7 miles above mouth and 12.5 miles northeast of
Belgrade]
0 0 40
North Cottonwood Creek, tributary of Reese Creek[Measured in NW}£ sec. 18, T. 2 N., R. 6 E., 6 miles above mouth and 12 miles northeast of
Belgrade]
Oct. 1, 1952....... 1.5 40
North Cottonwood Creek, tributary of Reese Creek[Measured in SW*4 sec. 13, T. 2 N., R. 5 E., 5 miles above mouth and 11.5 miles northeast of
Belgrade]
Oct. 25, 1951.......Aug. 28, 1952..... ..
0.81.3
3545
Oct. 1,1952......Aug. 28, 1953..... .
0.41.5
40
Bright ditch, diversion from Reese Creek in SW/4 sec. 8, T. 1 N., R. 5 E.[Measured in SE% sec. 7, T. 1 N., R. 5 E., 0.1 mile above mouth and 5.5 miles north of Belgrade]
Apr. 30, 1953..... ..June 23, 1953.... ...July 22, 1953.......
0.9.4
2.9
4962
Aug. 11, 1953......Sept. 4, 1953......Sept. 30, 1953......
2.31.6.3
58
Reese Creek, tributary of Smith Creek[Measured in NE% sec. 18, T. 1 N., R. 5 E., 0.25 mile above mouth, 0.5 mile below Bright ditch
diversion, 3.25 miles below gaging station and 4.5 miles north of Belgrade]
Apr. 30, 1953.......
July 22, 1953.......
14.095.4199
515564
Aug. 11, 1953..... .Sept. 4, 1953..... .Sept. 30, 1953..... .
11.89 K
14.0
55
WATER RESOURCES 87
TABLE 8. Occasional measurements of the discharge of streams, ditches, and springs in the Gallatin Valley Continued
DateDischarge
(cfs)Temperature
DateDischarge
(cfs)Temperature
Foster Creek, tributary of Smith Creek[Measured in NE% sec. 29, T. 2 N., R. 5 E., at county road bridge and 8.5 miles north of Belgrade]
Oct. 25, 1951. 0.6 40 Aug. 28, 1952. 0.4 53
Spring 4, tributary of Dry Creek[Measured in NW^NW% sec. 14, T. 3 N. ( R. 4 E., 12.5 miles northeast of Manhattan]
Aug. 27, 1953....... 0.004
Spring 6, tributary of Dry Creek[Measured in NW%NE*4 sec. 22, T. 3 N., R. 4 E., 11.5 miles northeast of Manhattan]
Aug. 27, 1953....... 0.04
Spring 5, tributary of Dry Creek[Measured in NE^SW% sec. 15, T. 3 N., R. 4 E., 12 miles northeast of Manhattan]
Aug. 27, 1953....... 0.02
Spring 7, tributary of Dry Creek[Measured in NW%NE% sec. 21, T. 3 N., R. 4 E., 11 miles northeast of Manhattan]
Aug. 27, 1953....... 0.04
Spring 8, tributary to Dry Creek[Measured in SW&SE^i sec. 28, T. 3 N., R. 4 E., 9.5 miles northeast of Manhattan]
Aug. 27, 1953....... 0.1
Spring 9, tributary to Dry Creek[Measured in NE%SE% sec. 34, T. 3 N., R. 4 E., 9.5 miles northeast of Manhattan]
Aug. 27, 1953....... 0.02 ..............
Dry Creek, tributary of East Gallatin River[Measured in NE% sec. 3, T. 1 N., R. 4 E., 100 ft below county road bridge and 6 miles east of
Manhattan]
Dec. 4,1952....... 17.0 ..............
East Gallatin River, tributary of Gallatin River[Measured in SE 1 sec. 32, T. 2 N., R. 4 E., 100 ft below county road bridge and 4 miles north
east of Manhattan]
Sept. 20, 1951....... 351 50 Apr. 3, 1952...... 393
88 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
TABLE 8. Occasional measurements of the discharge of streams, ditches, and springs in the Gallatin Valley Continued
DateDischarge
(cfs)Temperature (°F) Date
Dischargefcfs)
Temperature(°F)
East Gallatin River, tributary of Gallatin River[Measured in NE% sec. 36, T. 2 N., R. 3 E., 200 ft below mouth of Bullrun Creek and 3 miles
northeast of Manhattan ]
Nov. 25. 1952. ...... 314 Dec. 4,1952...... 301
Gallatin River[Measured in SE% sec. 27, T. 2 N., R 3 E., 500 ft below county road bridge and 2.5 miles north
of Manhattan]
Mar. 27, 1952....... 755
Spring 1, tributary of Gallatin River[Measured in NW% sec. 33, T. 2 N., R. 3 E., 2.5 miles northwest of Manhattan]
Aug. 29, 1952. ......Mar. 5,1953.......
10.7.06
KA
33Apr. 24, 1953...... 0.00
Spring 2, tributary of Gallatin River[Measured in NE% sec. 32, T. 2 N., R. 3 E., 2.75 miles northwest of Manhattan]
Aug. 29, 1952.......Mar. 5, 1953.......
22.69.0
5353
Anr 94. IQ^ 8.318.6
55
[Measured inSpring 3, tributary of Gallatin River
sec. 32, T. 2 N., R. 3 E., at abandoned fish hatchery 2.75 miles northwest of Manhattan]
July 22, 1952... ....Aug. 29, 1952. ......Mar. 5, 1953. ......
8.314.54.9
5252
Apr. 24, 1953......Aug. 12, 1953......
3.711.7
52
the Gallatin Valley. Gaging at the Gallatin Gateway station was resumed in June 1930. The average discharge for the 25 water years of complete record during the period 1889 to 1952 was 758 cfs and the median, 725 cfs. The mean discharge of 1,116 cfs in water year 1892 was the highest during the period of record, and 984 cfs during water year 1952 was the second high est. The lowest was in water year 1934, when the mean discharge was 409 cfs.
The general pattern of inflow at the Gallatin Gateway gaging station is fairly well illustrated by the hydrographs for water years 1952 and 1953. (See fig. 16.) From the beginning of the water year through March the gradual recession of streamflow is affected occasionally by rain, severe cold, or minor snowmelt. A rising trend beginning in April and culminating in a peak in
WATER RESOURCES 89
FIGURE 16. Hydrographs of the discharge of the Gallatin River near Gallatin Gateway and at Logan, water years 1952 and 1953.
late May or early June is caused by concurrent precipitation and snowmelt. The pronounced recession that follows is affected slightly by occasional rains. The rise to a secondary peak on May 4,1952, was somewhat unusual.
In the reach of the Gallatin River from the gaging station near Gallatin Gateway to the gaging station at Logan, the pattern of flow is modified by extensive diversions for irrigation; losses to, and gains from, the ground-water reservoir; and, to a lesser extent, runoff from within the valley. Comparison of the flow at the several gaging stations on the Gallatin River during water years 1952 and 1953 illustrates the usual downstream depletion during the irrigation season and other losses. (See table 9.) A rather consistent loss between the gaging stations at Cameron Bridge and Central Park is accounted for, at least in part, by discharge into Baker Creek and other distributary channels of the river originating between these two stations. In years of
508919 O-60 7
TABL
E 9
. D
iffer
ence
s in
mon
thly
and
ann
ual
runo
ff a
t ga
ging
sta
tion
s on
the
Gal
latin
Riv
er,
in t
hous
ands
of
acre
-fee
t, du
ring
wat
er y
ears
195
2 an
d 19
58
Gag
ing
stat
ion
Oct
.N
ov.
Dec
.Ja
n.
Feb
.M
ar.
Apr
.M
ayJu
neJu
lyA
ug.
Sep
t.A
nnua
l
Water year 1952
Gai
n (+
) or
los
s ( )
in f
low
. ....
Gai
n ( +
) or
los
s ( )
in f
low
. ....
At
Cen
tral
Par
k. ..
....
.............
Gai
n ( +
) or
los
s ( )
in f
low
. ....
Gai
n (+
) or
los
s (
) in
flo
w..
. . .
Tot
al g
ain
( +)
or l
oss
( )
in f
low
be
twee
n G
alla
tin
Gat
eway
an
d
Gai
n in
flo
w d
ue t
o tr
ibuta
ry i
nflo
w. .
. N
et g
ain
( +)
or l
oss
( )
in f
low
due
to
cha
nges
in
tota
l w
ater
sto
rage
27.7
526
.38
-1.3
7
26.3
820
.12
-6.2
6
20.1
213
.74
-6.3
8
13.7
455
.52
+4
1.7
8
+27.7
710
.19
+1
7.5
8
22.5
524
.31
+1.7
6
24.3
125
.12
+ .8
1
25.1
219
.93
-5.1
9
19.9
355
.90
+35.9
7
+3
3.3
58.
77
+24.5
8
18.0
219
.44
+1.4
2
19.4
419
.95
+ .5
1
19.9
516
.07
-3.8
8
16.0
747
.66
+31.5
9
+2
9.6
47.
87
+21.7
7
17.4
019
.58
+2.1
8
19.5
820
.75
+1
.17
20.7
515
.75
-5.0
0
15.7
542
.62
+2
6.8
7
+25.2
27.
01
+18.2
1
15.5
516
.66
+1
.11
16.6
617
.71
+1
.05
17.7
114
.75
-2.9
6
14.7
539.1
8+
24.4
3
+23.6
36.
32
+17.3
1
17.3
018
.37
+1.0
7
18.3
718
.46
+ .0
9
18.4
616
.37
-2.0
9
16.3
743
.63
+27.2
6
+26.3
36.
66
+19.6
7
44.3
148
.91
+4
.60
48.9
145
.86
-3.0
5
45.8
646
.10
+ .2
4
46.1
011
8.60
+7
2.5
0
+7
4.2
937
.49
+36.8
0
186.
8021
5.70
+28.9
0
215.
7021
3.20
-2.5
0
213.
2016
6.40
-46
.80
166.
4027
9 . 1
0+
11
2.7
0
+92.3
073
.10
+19.2
0
207.
7019
7.70
-10
.00
197.
7020
1.50
+3.8
0
201.
5012
1.20
-80
.30
121.
2019
7.20
+7
6.0
0
-10
.50
54
.64
-65
.14
85.4
274
.99
-10
.43
74.9
938
.04
-36
.95
38
.04
29.3
4-8
.70
29.3
470
.22
+4
0.8
8
-15
.20
23.4
1
-38
.61
4.9
^4
34.2
4-8
.30
34.2
411
.89
-22
.35
11.8
93.4
8-8
.41
3.4
83
5.8
3+
32.3
5
-6.7
114
.45
-21
.16
9Q
91
24.2
5-4
.96
24.2
512
.23
-12.0
2
12.2
37.1
0-5
.13
7.1
044.4
6+
37.3
6
+1
5.2
511
.67
+3
.58
714.
5579fl
*\
%
+5.9
8
Ton
V
I64
4.83
-75.7
0
644.
8347
0.23
-174.6
0
4.7f
) 91
1,0
29.9
2+
55
9.6
9
+315.3
726
1.58
+53.7
9
Water year 19
53
At
Axt
ell
Bri
dge.
..................
At
Cen
tral
Par
k. ........
...........
Gai
n (+
) or
los
s ( )
in f
low
. ....
24.6
921
.53
-3.1
6
21.5
37.5
8-1
3.9
5
7.5
84.9
2-2
.66
19.4
621
.60
+2.1
4
21.6
017
.19
-4.4
1
17.1
914
.42
-2.7
7
19.0
021
.27
+2.2
7
21.2
723
.66
+2.3
9
23.6
620
.56
-3.1
0
18.5
920
.65
+2
.06
20.6
522
.50
+1
.85
22.5
020
.24
-2.2
6
15.1
817
.14
+1
.96
17.1
418
.58
-U1
A4.
18.5
815
.70
-2.8
8
17.1
218
.70
+1
.58
18.7
019
.79
+1.0
9
19.7
917
.76
-2.0
3
20.3
722
.12
+1
.75
22.1
220
.55
-1.5
7
20.5
518
.29
-2.2
6
53.6
848
.45
-5.2
3
48.4
528
.60
-19
.85
28.6
018
.64
-9.9
6
183.
6019
6.70
+ 1
3.10
196.
7016
4.70
-32.0
0
164.
7014
0 . 1
0-2
4.6
0
87.7
777
.41
-10
.36
77.4
135
.83
-41
.58
35.8
335
.92
+ .0
9
33.8
929
.99
-3.9
0
29.9
98.9
8-2
1.0
1
8.9
81.
53-7
.45
24.3
119
.50
-4.8
1
19.5
06.
77-1
2.7
3
6.77
2.51
-4.2
6
517.
66
-2.6
0
515.
0637
4.73
-14
0.3
3
374.
7331
0.59
-
64.1
4
Ul o M
Ul g F £ o
WATER RESOURCES 91
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J?laflow due to tr n (+) or loss ( changes in toti bin the Gallat
2a« atOr?
92 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
low runoff the streambed at a few points between Cameron Bridge and Central Park is dry during much of the latter half of the irrigation season. The greater diversion for irrigation from the reach of river between the Axtell and the Cameron Bridges does not fully account for the apparent loss between these points. The loss is particularly evident in the 1953 water year and throughout the period of record, June through September, in the 1950 and 1951 water years.
The discharge of the Gallatin River at Logan for water years 1952 and 1953 (fig. 16) is typical of the outflow from the valley. Flow generally increases during October and continues to in crease until the weather becomes severely cold. Flow during the winter usually decreases until snowmelt from the valley and foot hills produces a rise in March or early April. A brief recession in flow generally precedes a rise in flow that results from snow- melt at higher elevations. Peak flow occurs in May or June concurrently with the peak flow at Gallatin Gateway, but often is somewhat lower in spite of the nearly synchronized peak flows of intervening tributaries. The discharge at Logan then de creases rapidly to a low in late July or early August. The rise in late August, which continues into the next water year, probably is the result of increasing ground-water discharge and decreas ing evapotranspiration.
The average discharge of the Gallatin River at Logan for the years of complete record is 957 cfs. The median yearly discharge is 984 cfs.
Comparison of the hydrographs of the discharge of the Galla tin River near Gallatin Gateway and at Logan shows the relation of the monthly (fig. 17) and annual (fig. 18) runoff at these points. It is interesting to note the divergence between the two hydrographs after the drought years of the 1930's.
EAST GALLATIN RIVER
The East Gallatin River is a relatively short stream, but, be cause of its many tributaries, its flow increases rapidlyHn its course through the valley. Its tributaries include most of the streams from the Gallatin and Bridger Ranges and many spring- fed streams rising within the valley. Some of the streams that rise in the mountainous areas either sink into their alluvial fans or are diverted before reaching the East Gallatin River, but they contribute to the flow of the river through some of the shorter spring-fed streams that rise on the lower slopes of the fans.
WATER RESOURCES 93
300,000
250,000
200,000
150,000
100,000
Inflow near Gallatin Gateway plus trib utary inflow
1950 1951 1952 1953
FIGURE 17. Hydrographs of monthly surface-water inflow to, and outflow from, the GallatinValley, water years 1951-53.
STREAMS FROM THE GALLATIN RANGE
The principal streams that rise in the Gallatin Range and that make a major contribution to the water supply of the valley are Wilson, Big Bear, South Cottonwood, Middle (Hyalite), Sour dough (Bozeman), and Bear Creeks. Their yield per square mile of drainage area is high, averaging approximately the same as
94 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
1,250,000
1,000,000
750POO
500,000
250,000
Inflow near Gallatin Gateway pi us trib utary inflow
1928 1930 1935 1940 1945 1950 1955
FIGURE 18. Hydrographs of annual surface-water inflow to, and outflow from, the Gallatin Valley; estimated for period 1931-61, measured for period 1952-53.
that of the Gallatin River above Gallatin Gateway. Their com bined flow during water year 1952 was nearly 132,000 acre-feet, or about half the measured tributary inflow to the Gallatin River within the valley.
STREAMS FROM THE BRIDGER RANGE
Bridger Creek, which drains a considerable part of the east slope as well as the narrow south edge of the Bridger Range, is a principal tributary of the East Gallatin River. Some water for irrigation is diverted from it before it enters the Gallatin Valley. Streams draining the west slope of the Bridger Range are fairly short and are characterized by more rapid snow runoff than are the streams draining the Gallatin Range. Ross Creek evidently receives a large part of its flow from outside its surface drainage area, presumably from an underground source. Although the surficial drainage area above the gaging station is only 1.29 square miles, the runoff was 161 inches in water year 1952 and 178 inches in water year 1953. Furthermore, the runoff pattern
WATER RESOURCES 95
lags behind the precipitation pattern. The other principal streams entering the Gallatin Valley from the Bridger Range are Reese, Middle Cottonwood, and Bear Creeks. The discharge of Middle Cottonwood Creek near Bozeman (fig. 19) is typical of runoff from the Bridger Range.
Insofar as their contribution to the surface-water supply of the valley is concerned, the streams draining the west slope of the Bridger Range are relatively unimportant because the flow of most of them either sinks into their alluvial fans or is di verted completely before reaching the East Gallatin River. These streams are important locally, however, as they are the only source of irrigation supply for some of the higher lying cropland.
Dry Creek, although it rises in the Bridger Range, is similar in its flow characteristics to streams rising in the foothills. (See pi. 3.) During water year 1952 the high flow occurred in early April and was followed by a lesser peak in late May. Thereafter the flow receded rapidly to a low point in mid-August. The slight rise to a firm flow of 17 to 19 cfs probably reflects inflow from springs or return flow from upstream irrigation.
OTHER STREAMS
The few streams rising in the Horseshoe Hills are intermittent and contribute little to the water supply of the Gallatin Valley. Streams rising in the Camp Creek Hills, which rim the west side of the Gallatin Valley, are similar in their flow characteristics to those 'rising in the Horseshoe Hills. Heavy rains or rapid snowmelt in the early spring produces appreciable runoff for a short time, but at other times the flow is negligible in the upper reaches of these streams. Many of them are perennial in their lower courses, however, because they receive return flow from irrigation. Ridgley, Bullrun, Gibson, Ben Hart, and Thompson Creeks are typical of streams rising in the lower part of the Gal latin Valley. The flow of these streams is derived largely from ground-water discharge and, in many places, is diverted for irrigation.
A complex system of diversion for irrigation has greatly modi fied the natural drainage pattern. Long-continued diversion dur ing all seasons of the year has given many canals the appearance of natural stream channels, and many of the old channels have lost their identity as stream courses. A multiplicity and confu sion of stream names has resulted. Stream names in this report are those commonly used in the area, though they may differ from the names used in water-right filings.
96 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
i33d oiano NI ' ON003S d3d 133d 01900 NI
WATER RESOURCES 97ESTIMATES OF SURFACE-WATER INFLOW TO GALLATIN VALLEY
Except for the runoff from a total of 44 square miles in water year 1952 and 39 square miles in water year 1953, all the runoff from the 1,265-square-mile area draining into the Gallatin Val ley was gaged with reasonable completeness during the 2 years this study was in progress. The ungaged area consisted of scat tered small wedge-shaped tracts along the east and northeast margins of the valley; the runoff from this ungaged area was estimated to be 400 acre-feet per square mile, or 17,600 acre-feet in water year 1952 and 15,600 acre-feet in water year 1953. Mis cellaneous measurements and occasional gage readings that were made in water year 1953 on a few small streams and springs indicated that this estimated runoff was approximately correct.
For use in computing annual ground-water discharge during the period 1934-51, estimates of annual tributary inflow to the Gallatin Valley were made for the 21-year period preceding this study (table 10); estimates were also made of the monthly tribu tary inflow for the months November through February of each water year during the same period (table 11). Both the annual and monthly estimates of tributary inflow were based primarily on the relationship of the flow of individual streams or groups of streams to the total tributary inflow during water years 1952 and 1953. The discharge of the Gallatin River near Gallatin
TABLE 10. Estimated annual inflow to the Gallatin Valley, in thousands of acre-feet, during water years 1931 through 1951
Water year
1931............ ...............1932...........................1933... ........................1934................. ..........1935...........................1936..... ......................1937...........................1938.... .......................1939........... ................1940...........................1941............... ............1942....... ....................1943...........................1944...........................1945...........................1946 ...........................1947...........................1948...........................1949 ...........................1950...........................1951...........................
Gaged inflow near Gallatin
Gateway
407591470296420418390516462464386576690530513557668694516562520
Estimated tributary
inflow
160200190120150150170200180180160240240200200200280350180200210
Estimated total inflow
567791660416570568560716642644546816930730713757948
1,044696762730
98 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
TABLE 11. Estimated monthly inflow to the Gallatin Valley, exclusive of the Gallatin River, during period November through February of water years 1931 through 1951, in thousands of acre-feet
Water year
1931.....................1932.....................1933.....................1934.....................1935.....................1936.....................1937.....................1938.....................1939.....................1940.....................1941.....................1942.....................1943.....................1944.....................1945.....................1946.....................1947.....................1948.......... ...........1949.....................1950.....................1951.....................
November
87876666856
12898
1011121089
December
77775665755
1277689
12879
January
57774555556866677
11768
February
766645554446656666777
Gateway, precipitation records, and the results of snow surveys in the Middle (Hyalite) Creek basin also were used in making the estimates. The general uniformity of the numerical relationships of the individual months and those for the water year, particu larly for water years 1940 through 1951, made the results seem reasonable.
The accuracy of the estimates of tributary inflow to the Galla tin Valley varies inversely with the extent of the ungaged area. The estimates for water years 1931 through 1934, when records for the Gallatin River near Gallatin Gateway and precipitation records were the only basis, are considered to be accurate within 30 percent. The estimates for water years 1935 through 1939, when the flow of Middle (Hyalite) Creek also was measured, are considered to be accurate within 25 percent. Establishment of a gaging station on the East Gallatin River at Bozeman in Sep tember 1939 again decreased the area from which runoff was not measured, and the estimates for water years 1940 through 1945 are considered to be accurate within about 20 percent. The collection of records on Bridger Creek near Bozeman, begin ning in January 1946, may have improved further the accuracy of these estimates of tributary inflow for the water years 1946 through 1951.
WATER RESOURCES 99
The estimates of tributary inflow for individual months No vember through February (table 11) are considered to be accu rate within the following percentages: For water years 1931 through 1939, 40 percent; water years 1940 through 1945, 30 percent; water years 1946 through 1951, 25 percent. However, the estimates of total tributary inflow during the period No vember through February of each water year may be accurate within about 20 percent.
Values for total surface-water inflow to the Gallatin Valley dur ing water years 1931 through 1951 are shown in table 10 and figure 18. Because gaged discharges generally are considered to be accurate within 15 percent for individual months and within 10 percent for annual values, the values for total annual sur face-water inflow (gaged plus estimated) probably are reliable within 15 percent.
UTILIZATION
Surface water is the principal source of irrigation supply in the Gallatin Valley. According to data collected by the Montana State Engineer (1953a, p. 27-30), 107,261 acres was under ir rigation in 1952. A total of 72,433 acres received water from the Gallatin River, and 10,594 acres received water from tributaries of the Gallatin River, exclusive of the East Gallatin. A total of 3,424 acres received water from the East Gallatin, and 20,810 acres received water from its tributaries. Water shortages dur ing the last half of the irrigation season are reported in nearly all years for farms having the later water rights. These short ages are aggravated during extremely dry years. The only exist ing storage facilities, except for municipal storage, are Middle Creek Reservoir, which can store about 8,000 acre-feet, and Mystic Lake, which can store about 1,100 acre-feet.
The city of Bozeman is supplied with water from Sourdough (Bozeman) Creek, which rises in the Gallatin Range, and from Lyman Creek, a short, partly spring-fed stream, which rises in the Bridger Range. Storage facilities are provided by Mystic Lake near the head of Sourdough (Bozeman) Creek, and by two reservoirs, one on Sourdough (Bozeman) Creek and one on Ly man Creek.
Sportsmen consider the streams of the Gallatin Valley to be ex cellent for trout fishing. The spring-fed streams in the north end of the valley provide a nesting place for ducks; also, because these streams remain relatively free of ice, many ducks winter in the area.
100 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
GROUND WATER
DEFINITION OF TERMS
Below a certain level within the earth the porous rocks gen erally are saturated with water under hydrostatic pressure. This water is known as ground water > and the water-bearing rocks (formations, groups of formations, or parts of formations) that will yield sufficient water to be a source of supply are referred to as aquifers. Aquifers are recharged chiefly by the infiltration of precipitation and by influent (losing) streams, and they dis charge mostly through seeps and springs into effluent (gaining) streams. In some places water is withdrawn from the aquifers by pumping from wells and, where the water table is shallow, by vegetation having roots that penetrate to the zone of saturation or to the capillary fringe that extends above it.
Where ground water is unconfined, its upper surface is re ferred to as the water table and the water is said to occur under water-table conditions. Meinzer (1923b, p. 22, 32) defined the water table as the upper surface of a zone of saturation except where that surface is formed by an impermeable body. In gen eral, the water table is not a level surface, but conforms, in subdued relief, to the irregularities of the overlying land sur face; also, it fluctuates in response to changes in the ratio of ground-water recharge to discharge.
Where a zone of saturation is bounded above by a bed of rela tively impermeable material and the water is confined under sufficient hydrostatic pressure to rise above the base of that con fining bed, the aquifer is termed "artesian" and the confining bed is referred to as an aquiclude. The imaginary plane to which artesian water will rise in nonpumped wells is called a pressure- head-indicating surface, or piezometric surface, and may be either below or above the land surface. Like the water table, the piezo metric surface is not a level surface, but, unlike the water table, it fluctuates not only with changes in the ratio of recharge to discharge but also with changes in pressure conditions within the aquifer.
Meinzer (1942, p. 390) stated:
The two properties of a rock material that most largely determine the be havior of its contained water and its productiveness as a water-bearing formation are its specific yield and its permeability. Both of these properties are determined by the character of the interstices and the resultant effects of molecular attraction. The specific yield relates to the storage capacity of the rocks; the permeability relates to their capacity to transmit water.
The specific yield of a water-bearing formation, as defined by Meinzer (1923b, p. 28), is the ratio of (1) the volume of water
WATER RESOURCES 101
that a saturated aquifer will yield by gravity to (2) the volume of the aquifer. It is, therefore, a measure of the quantity of water that a saturated aquifer will yield when drained by gravity. Un der water-table conditions, the specific yield is practically equal to the coefficient of storage, which is a property of the aquifer that may be determined by making pumping tests. Unlike the term "specific yield," however, the coefficient of storage applies to both water-table and artesian aquifers and is defined as the volume of water (measured outside the aquifer) that an aquifer releases from, or takes into, storage per unit surface area of the aquifer per unit change in the component of head normal to that surface. For a water-table aquifer, the water released from stor age is attributed largely to gravity drainage or refilling of the zone through which the water table moves and only in small part to compressibility of the water and aquifer material in the satu rated zone. For an artesian aquifer, however, the water released from storage is attributed solely to compressibility of the water and aquifer material in the saturated zone.
The standard coefficient of permeability of a water-bearing formation, as used by the Geological Survey, is the rate of flow of water at 60 °F, in gallons per day, through a cross section of 1 square foot, under a hydraulic gradient of 100 percent (1 foot per foot). A related coefficient, which has been called the field coefficient of permeability, was defined by Meinzer (1942, p. 452) asthe rate of flow of water, in gallons a day, under prevailing conditions, through each foot of thickness of a given aquifer in a width of 1 mile, for each foot per mile of hydraulic gradient.
The capacity of an aquifer to transmit water is termed "trans- missibility." The coefficient of transmissibility, which for many purposes is a more useful unit than the field coefficient of perme ability, was defined by Theis (1935, p. 520) and commonly is expressed by the Geological Survey as the number of gallons of water per day, at the prevailing water temperature, that is trans mitted through each mile strip extending the full saturated thickness of the aquifer under a hydraulic gradient of 1 foot per mile.
The specific capacity of a well is its rate of discharge per unit of drawdown. The term is applied only to wells in which the drawdown varies approximately as the discharge. In such wells the specific capacity can be determined by dividing the discharge of the well, generally in gallons per minute (gpm) by the water- level drawdown, generally measured in feet.
102 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
DETERMINATIONS OF AQUIFER PROPERTIES
An aquifer test, or so-called "pumping test," is a field method whereby the main hydrologic properties of an aquifer can be de termined. The coefficient of transmissibility of an aquifer can be computed from a test using a single pumped well ("single-well" test), whereas the coefficients of both transmissibility and stor age can be computed from a test using a single pumped well and one or more observation wells ("multiple-well" test). If, in addition to the coefficient of transmissibility, the saturated thickness of the aquifer is known, the average coefficient of permeability of the water-bearing material can be computed.
Because a single-well test can be made without installing ob servation wells, this type of test was the principal method used in the determination of transmissibility coefficients in the Gal- latin Valley. Altogether, about 100 such tests were made and the coefficient of transmissibility at 37 sites was computed (more than one test was made at several of the sites). As a check on the values thus obtained, tests involving the use of 3 or 4 obser vation wells in addition to the pumped well were made at 4 sites. These multiple-well tests served also as a random sampling of the coefficients of storage. The results of both types of tests are summarized in table 12.
The coefficient of transmissibility of known Tertiary strata was determined at six scattered points within the valley. Five of the values ranged from 300 to 6,000 gpd per foot but one was 17,000 gpd per foot. The results of two other tests indicated inconclu sively that lenses of unconsolidated sand and gravel within the Tertiary strata may have considerably higher coefficients of transmissibility. One of these, a test on well Al-3-33dd, gave a value of 26,000 gpd per foot, but it was not known whether all or only part of the water was withdrawn from Tertiary strata. The other, a test of a sand layer between the depths of 249 and 260 feet in test hole Al-4-15da2, indicated a coefficient of transmissibility between 30,000 and 40,000 gpd per foot, but a more exact computation could not be made. Examination of ex posed Tertiary strata and computations of the coefficient of per meability for the tests at sites Dl-3-36bc, Dl-4-25aa2, and D2-4- 9bc have led to the conclusion that the Tertiary strata generally would yield sufficient water for domestic use and the watering of livestock but not for irrigation or other large-scale uses.
The coefficient of transmissibility of the Bozeman alluvial fan was determined at 6 sites and that of the Spring Hill fan at 2 sites. The wide range in values, 7,000 to 65,000 gpd per foot, indi-
WATER RESOURCES 103
cates that the alluvial-fan deposits generally will yield ample water for domestic and livestock use but that only locally will it yield sufficient water for irrigation or other large-scale uses.
The coefficient of transmissibility of the alluvium of the Gal- latin and East Gallatin Rivers was determined at 24 sites; it ranges from 38,000 to 670,000 gpd per foot and averages about 200,000 gpd per foot. A test made on a well (Al-5-10ba) tap ping both the alluvium along Reese Creek and the underlying Tertiary strata yielded a transmissibility value of 24,000 gpd per foot.AQUIFER PROPERTIES AS THEY AFFECT THE StPECIFIC CAPACITY
OF A WELL,
The specific capacity of a well depends not only on the water- yielding properties of the aquifer but also on the type and con struction of the well. Theoretically, therefore, if a well has been designed and constructed perfectly (an "ideal" well), its specific capacity can be determined from known aquifer properties.
To illustrate this point, a graph has been prepared to show the theoretical drawdown in an ideal well that taps an aquifer of known characteristics. (See fig. 20.) In this graph, the co efficient of transmissibility (T) is plotted along the abscissa and the drawdown (s), for a pumping period (t) of 12 hours, is plotted along the ordinate. Three lines representing different values for the coefficient of storage (S) are plotted on the graph, each for a well having a radius (r) of 1 foot and yielding at a rate (Q) of 500 gpm. Thus, for example, at the end of a 12-hour pumping period an ideal well yielding 500 gpm and tapping an aquifer having T = 100,000 gpd per foot would have a draw down of about 7.1 feet if S = 0.05, a drawdown of about 8.4 feet if S = 0.005, and a drawdown of about 9.7 feet if S = 0.0005. Similarly, after a 12-hour pumping period an ideal well yielding 500 gpm and tapping an aquifer having T = 50,000 gpd per foot would have a drawdown of about 13.5 feet if S = 0.05, about 16 feet if S = 0.005, and about 18.5 feet if S = 0.0005.
In reality, actual drawdown exceeds theoretical drawdown even in the best designed and constructed wells and may be several times the theoretical drawdown in poorly designed and constructed wells.
The 4 multiple-well tests gave values ranging from 0.001 to 0.06 for the storage coefficient of the alluvial deposits in the Gal latin Valley. The smaller values (0.001 and 0.006) indicate that in at least a part of the areas "sampled" by the tests the water is confined. It is believed that the average coefficient of storage of
TABL
E 1
2.
Sum
mar
y of
aqu
ifer
-tes
t dat
a
Wel
l or
te
st h
ole
Aq
uif
er
Dep
th
of w
ell
at t
ime
of t
est
(fee
t)
Yie
ld
(gpm
)L
ength
of
test
(m
inute
s)
Coe
ffic
ient
of
tr
ansm
is-
sibil
ity (
T)
(gpd
per
fo
ot)
Coe
ffic
ient
of
sto
rage
(S)
Thic
knes
s of
aq
uif
er
(fee
t)
Fie
ld
coef
fici
ent
of p
erm
ea
bil
ity
(P
f)
(gpd
per
sq
uar
e fo
ot)
Rem
ark
s
Gat
eway
sub
area
D2-4
-26dc .........
D3-4
-llb
db........
All
uviu
m ..........
.....d
o...........
25.9
18.5
64 7160
10
0380,0
00
17
0,0
00
!85
'2,0
00
Bel
gra
de
subar
ea
5-2
8db2 ........
Dl-
4-l
cb. .........
Idc
2d
d..
....
....
9cb ..........
15ab
.........
25aa
2 ........
Dl-
5-5
ad
.. .
.......
Qfr
l
30cb
.........
D2-4
-lld
c. ..
....
..14
ada2
...
....
14bb
.........
....
.do..
....
....
......d
o...........
....
.do..
....
....
...
...d
o..
....
. ..
.......d
o...........
....
.do
....
...
....
Ter
tiar
y s
trat
a ..
..
All
uv
ium
. ........
.....d
o...........
....
.do..
....
....
.....
.do..
....
....
......d
o...........
....
.do..
....
....
.
24
118
110
107
178 30
30.5
22
5 25.6
25
12.5
65
50
11
.1
74
265
224
520 62
250
220
2 12
5 24
68
260
280 48
28
100 10
20
0 25
0 13
30
60
8,7
60 30
30
60
10
0 30
75
280,0
00
58,0
00
670,0
00
240,0
00
13
0,0
00
1
40
,00
0
94
,00
0
17,0
00
13
0,0
00
50,0
00
290,0
00
270,0
00
260,0
00
70,0
00
74 11 58
230
4,5
00
4,5
00
Flo
w t
est
of a
qu
ifer
bet
wee
n
dep
ths
of 1
49 a
nd 2
23 f
t.
Cen
tral
Par
k s
ubar
ea
Al-
4-5
da..
.........
5dd. .........
6b
c..
....
....
.19
cb .........
22
dc4
...
[Ter
tiar
y s
trata
. . .
.
.....d
o...........
. ....do...........
.....d
o...... .
....
35 207 18
39.3
f
81
\ 18
0 27
240 16
32
55
31
0
220
30 40
100 60
10
200
10
0,0
00
3,7
00
11
0,00
0 38,0
00
480,0
00
18
0,0
00
480,0
00
0.0
06
.05
26
25
>25
89
63
4,0
00
U.O
OO
1
1,5
00
5
,50
0
2,9
00
Ober
vat
ion w
ells
at
25,
50,
and 1
00 f
t fr
om
pu
mp
ed
wel
l.
Flo
w t
est
of a
qu
ifer
bet
wee
n
dep
ths
of 1
17 a
nd 1
80 f
t.
Obse
rvat
ion w
ells
at
200,
27
0, a
nd
300
ft
fro
m
pum
ped
wel
l.
& o
WATER RESOURCES 105
inOS
c< *
t£1c
1o
o8
09
c cc
§gococ
Si09
oo tc h-h-
fc;
Alluvium. ........
a«
2
pumped
1"K
2
11
; c c cc P"T-*
s
cs
tch.CT
4
> cH T-
c o cc
i
tc tc
4
&i-?5C*HC>
;I
8"o"-o
t!u u£ **
.9o32iiio
o
to
§O
oooo oooo oooo oooo
s Tf CD CS CDOiO CO CS O CD
OOOO OOOOiO
s^sa SSag
<N N TJ<
WifflCOO OtOO5"5
<N 3 IN '"'rH
3 t; 3 o |g 3 c ">.*'>T .55 >T
Dl-5-26da. ........
)*O 58 C9 ( 1 ^H ^4 W5 t^"? rt ~*
iQ
4
4 .u11C»
1 i
9
Camp Creek Hills
oo
^
§ 00 oo
tO tO i-l
000
^
O5P3O
Tertiary (?) strata.. Tertiary strata. . . .
Al-3-33dd ......... Dl-3-36bc. ........
r»S>_d-flhn.
I
to
t-.
S
Alluvium and
Tertiary strata.
«3
ing Hill subai
o.OS
oo§§
oo
22
to
Alluvium. ........ .....do...........
t-d
||
508919 O-60 8
106 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
100
yi O
, i O
o o
a:o 5
X\\
\
Theoretical drawdown when: 5=0.05, 0.005, or 0.0005 r=l footC?=500 gallons per minute f=l2 hours T=ranges from 10,000 to 1,000,000
gallons per day per foot
\\\
110,000 100,000 1,000,000
COEFFJCIENT OF TRANSMISSIBILITY T, IN GALLONS PER DAY PER FOOT
FIGURE 20. Graph showing theoretical drawdown in an "ideal" pumped well.
the alluvium in the Gallatin Valley would be about 0.05 after 12 hours of pumping and at the end of many weeks of pumping it would be much larger.
When it is considered that the maximum saturated thickness of the alluvial-fan deposits is 80 to 100 feet, that the coefficient of transmissibility ranges from 7,000 to 65,000 gpd per foot, and that the coefficient of storage is about 0.05, or higher, it can readily be seen that the drawdown in wells pumped at a high rate would be great except where the coefficient of transmis sibility is relatively high. However, the drawdown in wells tap ping the alluvium of the Gallatin and East Gallatin Rivers would rarely be excessive, even if the actual drawdown were two or three times the theoretical drawdown, because the coefficient of transmissibility of that aquifer generally is greater than 100,000 gpd per foot.
WATER RESOURCES 107
RECHARGE
The ground-water reservoir underlying the Gallatin Valley is recharged principally by infiltrating stream and irrigation water and only in small part by direct infiltration of precipitation and snowmelt.
In at least part of their course across the valley, Middle (Hyalite) Creek and the Gallatin and East Gallatin Rivers are influent during part or all of the year and are a source of con siderable recharge to the underlying and adjacent alluvium. The monthly loss from the Gallatin River between gaging stations at Cameron Bridge, near Belgrade, and Central Park, near Man hattan, for example, is estimated to have averaged at least 3,000 acre-feet per month during the 1953 water year. Smaller streams, where they emerge from the Bridger and Gallatin Ranges, lose much, if not all, of their flow by seepage into their alluvial fans.
In the irrigated parts of the valley, seepage from the many irrigation canals and laterals is the chief source of recharge to the ground-water reservoir. Infiltration of applied irrigation wa ter, another source of recharge, is appreciable where the soil is highly permeable. The effect of application of irrigation water is illustrated by the hydrograph of the water level in well A2- 3-33da, which was drilled into the alluvium near the outer edge of the Manhattan terrace. (See fig. 21.) Irrigation of fields upgradient from the well caused a rapid and substantial rise of the water level; when water was no longer applied, the water level in the well fell rapidly. Of the surface water that entered the valley during the 1952 and 1953 irrigation seasons, between 300,000 and 400,000 acre-feet is estimated to have been diverted for irrigation each season. Probably at least half this amount infiltrated to the water table.
The amount of recharge from precipitation depends on the volume, duration, intensity, and seasonal distribution of the pre cipitation, the slope of the land surface, the permeability and moisture-holding capacity of the soil, the consumptive use through evapotranspiration, and the capacity of the ground-wa ter reservoir to store additional water.
Parts of the Gallatin Valley receive a substantial amount of re charge from direct precipitation and snowmelt during the spring. Recharge from infiltrating snowmelt and from increased stream- flow due to snowmelt is illustrated by the hydrograph of the water level in well D2-5-16aal, which is on the Bozeman fan. (See fig. 22.) Daytime rises in temperature caused meltfhg of
108 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
18 19 20 21 22 23 24 25AUGUST 1952
FIGURE 21. Hydrograph of the water level in well A2-3-33da showing the effect of recharge from infiltrating irrigation water.
snow and consequent increases in streamflow, and nighttime cooler temperatures either slowed or stopped the snowmelt and reduced the streamflow. The highest daily water level lagged about 4 to 5 hours behind the highest daily temperature. In the higher part of the Bozeman fan, in particular, the water level in wells rises in response to precipitation. Recharge from direct infiltration of precipitation and to increased streamflow due to precipitation is illustrated by figure 23, which is a hydrograph of well D2-5-16aal during a period of substantial rainfall. Re^ charge from precipitation is greater in this part of the valley than elsewhere because of a combination of favorable factors: the volume of precipitation is greater than in the lower part of the valley, moisture requirements are less than in nonirrigated
WATER RESOURCES 109
MARCH 1952 APRIL 1952
FIGURE 22. Hydrograph of the water level in well D2-5-16aal showing the effect of recharge from infiltrating snowmelt and streamflow.
parts of the valley, spring snowmelt immediately precedes or coincides with the period of heaviest rainfall, and the soil gen erally is highly permeable.
DISCHARGE
Ground water is discharged by wells, springs, evaporation, transpiration, and effluent seepage into streams and drains.
Almost all the ground water pumped from wells in the Gallatin Valley is used for watering livestock and for domestic supply.
SEPTEMBER 1951
FIGURE 23. Hydrograph of the water level in well D2-5-16aal showing the effect of recharge from infiltrating precipitation and streamflow.
110 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Only one municipal supply, that for the town of Belgrade, is provided by wells. Total pumpage in the valley is minute com pared to the total volume of ground water and, therefore, is rela tively unimportant as a discharge factor. However, if irrigation or industrial use of ground water is increased materially in the future, discharge by pumping from wells then would become an important factor.
Evaporation of ground water occurs wherever the water table is near the land surface. Transpiration of ground water by phreatophytes (plants whose roots penetrate to the capillary fringe or to the zone of saturation) is another method of dis charge. Evapotranspiration (evaporation plus transpiration) is large along stream courses and in poorly drained areas. In the Gallatin Valley the principal areas of ground-water discharge by evapotranspiration, aside from land bordering the stream courses, are an extensive waterlogged area north of Central Park between the Gallatin and East Gallatin Rivers, a small area just south of Manhattan along the road to Amsterdam, and the shallow drain- ageways on the Bozeman fan.
An attempt was made in the fall of 1952 and during the 1953 growing season to determine the amount of ground water dis charged by evapotranspiration from a large part of the Central Park plain. Inflow to, and outflow from, a part of the plain were measured (table 13) and ground-water inflow was estimated. However, other variables were such that a reliable determination could not be made.
The amount of ground water consumed during the 1953 grow ing season by a typical grove of cottonwood trees 175 feet long and 150 feet wide (fig. 24) was measured by a method devised by White (1932, p. 61).
This method is based on the formulaq = y (24r ± s)
in whichq = the quantity of ground water withdrawn by transpiration and evap
oration during a 24-hour period, in inches;y = the specific yield of the material in which the water table fluctuated
during the same 24-hour period;r = the hourly rate of water-table rise during a 4-hour period of dark
ness when ground-water withdrawals by transpiration and evap oration were negligible, in inches;
ands = the net fall or rise of the water table during the same 24-hour period,
in inches.Well Al-4-22dcl, which is 9.1 feet deep and 36 inches in di
ameter, is near the middle of the cottonwood grove. A Stevens type-F weekly recording gage with a 12-inch float was installed
WATER RESOURCES 111
TABLE 13. Inflow to, and outflow from, the Central Park subarea[Asterisk (*) indicates preliminary data supplied by U.S. Bureau of Reclamation]
Stream or irrigation diversion
Amount of flow (cubic feet per second)
Fall 1952
July 7, 1953
Aug. 5, 1953
Sept. 1, 1953
Sept. 28, 1953
Inflow to area
Spain-Ferris ditches: No. 4. ......................No. 5........................No. 3 .......................No. 2........................No. 1 .......................
Mammoth ditch. .................J. S. Hoffman ditches:
No. 2........................No. 1 .......................
J. B. Weaver ditches: No. 2.. .....................No. 1........................
Stone-Weaver ditches: No. 2........................No. 1........................
Barnes ditch, diversion from D. N.
West branch of East Gallatin River.
Middle (Hyalite) Creek. ...........East Gallatin River near Belgrade . .East Gallatin River at Penwell
Bridge
Bear Creek ......................
Spring Branch Creek. .............Trout Creek. ....................Smith Creek near East Gallatin
Total......................
*54.3
*17.0*.7
*10.0
*41 Q
123.9
7.45.6
.45.0
10.3
3.96.5
2.522.0
4.6
4.816.21.4
46.9*115.0
*36.0*.4
*1.1*26.0
*.6*12.0
*27.7
356.3
7.51.02.1
.34.2
10.3
2.13.8
4.316.8
2.1
2.67.83.9
27.5*52.0
*12.0*.2
*2.3*18.0
*.5*7.7
*10.9
199.9
3,. 7.4.4.1
8.62.2
1.71.9
.26.4
.21.6
.77.62.0
48.2*36.0
*11.0* 2
*2.6*21.0
*.6*8.8
*18.8
184.9
3.2.1
6.5.9
1.01.5
1.23.6
.31.3
.44.0
45.7*38.0
*11.0*.2
*2.8*22.0*1.0
*10.9
*20.0
175.6
Outflow from area
East Gallatin River below mouth of Bullrun Creek.............. 301 *414.1 *271.2 *352.0 *345.6
Difference
177.1 57.8 71.3 167.1 170.0
112 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
FIGURE 24. Cottonwood grove in the sec. 22, T. 1 N., R. 4 E.
on this well to obtain smooth records of diurnal water-level fluctuations. (See fig. 25.) The values of r and s in the formula were determined from these records, and an aquifer test made on test hole Al-4-22dc4, also in the grove, gave a value of 0.05 for the storage coefficient used as y in the formula. The daily
8 9 IO II 12 13 AUGUST 1953
FIGURE 25. Specimen hydrograph of the water level in well Al-4-22dcl.
WATER RESOURCES 113
consumption of ground water by the cotton wood grove (trans piration), as computed from the formula, is given in table 14 and shown graphically on plate 4. Consumption for the season totaled about 2 feet. The consumption would be greater if, as may be true, the storage coefficient is higher than the 0.05 indi cated by the test.
TABLE 14. Daily consumption of ground water, in inches, by cottonwoodgrove
Day
1. ...................2. ...................3....................4....................5....................6.. ..................7.. ..................8....................9. ...................
10. ...................11. ...................12....................13. ...................14.. ..................15....................16. ...................17... .................18....................19. ...................20....................21. ...................22 ....................23 ....................24. ...................25 ....................26 ....................27....................28....................29. ...................30....................31.. ..................
June
0)0)0)0)0)0)C 1)C 1 )0.04
.12
.10
.04
.12
.15
.06
.14
.16
.12
.10
.01
.07
.11
.11
.06
.06
.12
.12
.12
.16C 1)
July
(')
0)0.16
.20
.21
.21
.20
.19
.25
.25
.25
.25
.25
.25C 1)C 1)
.29
.25
.24
.28
.23
.25
.26
.27
.28
.25
.31
.28
.28
.25
.21
1953
August
0.28fJQ
1Q1Q
.24
.25
.25
.25
.25
.101Q
.27
.200)
.24
.20
.25
.17
.24
.230)C 1 )0)0)0)0)C 1)C 1)
.14
.16
.23
September
0.22.08
0.13.16.15.17.18.19
0).16.13.18.15.14.14.14.18.21.11.09.08.08.13.17.13.15.14.08.18
October
0.11.01.04.07.06.10.07.06.07.06.06.03.06.05.05.04.09.03.07.07
0)«0)(')C 1)0)0)C 1)C 1 )0«
1 Not determined.
Precipitation, relative humidity, temperature, wind velocity, evaporation, and hours of sunshine are factors that affect the transpiration rate of vegetation. Records of all but the hours of sunshine were kept at, or near, the cottonwood grove during most of the 1953 growing season and are shown graphically on plate 4. The total length of daylight (that is, the theoretical number of hours of sunshine rather than the actual hours of sunshine) is shown also.
114 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Precipitation was measured by a recording rain gage near the grove (table 15). The CAA station, about 4 miles southeast of the grove, measured the relative humidity and both the maxi mum and minimum temperatures. An anemometer near the grove was used in measuring wind velocity (table 16) and a class-A evaporation pan was used in measuring evaporation (ta ble 17). Both the anemometer and evaporation pan were read daily by Mr. Holdiman, a local resident.
Temperature, more than any other factor, seems to have had the greatest effect on the withdrawal of ground water by the cottonwood grove. A high relative humidity, however, signifi cantly decreased the transpiration rate of the trees. If the wind velocity had been recorded for the daylight hours only, rather than for the entire day, possibly a better correlation between it and ground-water withdrawals would have been apparent. When precipitation was sufficient to wet the leaves of the trees,
TABLE 15. Daily precipitation, in inches, near cottonwood grove
Day
1. ...................2. ...................3. ...................4. ...................5. ...................6. ...................7.. ..................8. ...................9. ...................
10.. ..................11. ...................12. ...................13. ...................14. ...................15.. ..................16. ...................17....................18. ...................19. ...................20. ...................21 ....................22 ....................23........ ............24. ...................25. ...................26.. ..................27....................28. ...................29 ....................30.. ..................31. ...................
June
C 1)C 1)C 1)C 1)C 1)C 1)0.07
.02
.00
.03
.04
.21
.00
.06
.00
.00
.02
.02
.10
.40
.00
.00
.18
.00
.09
.00
.00
.00
.00
.00
July
0.00.00.00.00.00.00.00.00.00.00.00.00.00.00.14.00.00.00.00.00.00.0000
.00
.00
.00
.00
.00
.00
.00
.00
1953
August
0.00.08.00.07.00.00.00.00.04.04.00.00.00.00.00.00.00.00.00.00.00.00.00.00.00.00.00.00.00.00.00
Septembe r
0.00.50.00.00.00.00.00.00.00.00.00.00.00.00.00.00.00.00.00.00.00.08.00.00.00.00.00.00.00.00
October
0.00.20.00.00.00.00.00.00.00.00.00.00.00.00.00.00.00.00.00.10.30.00.00.00.00.00.00.00.00.00.00
i Not measured.
WATER RESOURCES 115
TABLE 16. Wind velocity, in miles per day, near cottonwood grove
Day
1.... ......2.. ........3..........4.. ........5. .........6........ ..7.. ........8..... .....9..........
10.... ......11. .........12.. ........13.. ........14. .........15..........16..........17..........18..........19 ..........20..........21..........22..........23..........24..........25..........26 ..........27..........28. .........29 ..........30..........31..........
May
0)0)C 1)0)C 1 )079.6
191.995.3
163.0155.4230.873.873.955.856.967.2
113.555.4
117.269.9
149.3136.5163.2136.3100.871.795.1
122.467.773.9
June
41.5130.4107.622.8
142 .439.069.380.343.261.062.650.1
116.489.535.884.569.1
102.258.5
130.8113.5225.580.3C 1 )0)0)
112.612.563.369.6
19
July
100.049.5M 755.157.14fi ^40.051.847.748.042.545.272.192.363.418.445.147.844.092.171.538.648.561.1
100.058.473.756.185.488.056.2
53
August
29.369.750.083.728.947.360.8
115.782.288.235.077.043.653.764.262.538.038.34Q ^51.947.453.664.6
149.141.879.436.171.737.729.344.5
September
40.514^ Q45.028.648.942.050.384.824.839.622.041 Q50.231.031.674.482.7
117.2194.319.137.070.567.256.0
150.096.755.4
106.941.4
126.4
October
54.7QR Qnc fl
0)26.744.440.342.344 751.647.037.017.379.015.826.943.8
112.80)
104.8118.519.320.127.534.123.021.139.353.260.445.1
1 Not recorded.
ground-water withdrawals virtually ceased. This is illustrated by the fact that during a light rain the water level in the well began to rise earlier in the day than usual, and rose at the same rate as at night. (See fig. 25.)
A reconnaissance of the Gallatin Valley indicated that a total of about 15,000 acres of land is covered by cottonwoods and wil lows. If the consumptive use of ground water by this type of vegetation is about 2 feet of water per year, as was computed for the typical stand of cottonwoods (fig. 24), then the total consumptive use of ground water by such vegetation in the Gal latin Valley is about 30,000 acre-feet per year. However, if the specific yield determination used in the computation for the typi cal grove is low by a factor of as much as 2 or 3, the real order of magnitude of evapotranspiration may be more nearly 60,000 or 90,000 acre-feet per year.
116 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
.TABLE 17. Daily evaporation, in inches, from a class-A pan near cottonwoodgrove
Day
1..........2..........3..........4..........5..........6. .........7..........8..........9..........
10..........11..........12..........13..........14..........15..........16..........17..........18..........19..........20..........21..........22..........23..........24..........25..........26..........27..........28..........29..........30..........31..........
May
0)(')
0)C 1)C 1 )(')
0.25.11
(')C 1 )(!)(!)(!)C 1)(')(!)(')C 1 )C 1 )(')C 1 )(')
0)«C 1)C 1)(!)0)C 1)C 1 )(!)
June
(')C 1)(')(')(')
«0)0)C 1)C 1 )
0)C 1 )
0)C 1)0)0)C 1 )0.24
.08
.17
.21
.35
.24C)(J)
«.10
(')
.26
.29
19
July
0.24.26.21
0)C 1)0)C 1 )C1)0)C 1 )
.28
.19
.22
.38
.28
.16
.18
.22
.220)0)C 1 )«C 1 )
.30
.24
.28
.28
.21
.31
.11
53
August
0.26.10.16.26.12.24.24.29.16.16.22.22.18.18.29.15.07.22.20.21.12.22.17.25.06.15.17.15.09.12.15
September
0.14.05.06.15.12.16.07.14.16.18.13.13.11.09.21.11.12.19.11.07.11.13.08.04.15.10.09.12.005.15
October
0.03.12.03.0.05.08.03.03.02.12.0.03.03.02.06.04.08.0.08
C 1 )C 1 )0)(!)( l)C1 )( l )(')(!)(!)(!)C 1 )
1 Not measured.
Ground water is discharged wherever the water table inter sects the land surface. In the Gallatin Valley, discharge by both spring flow and effluent seepage occurs where alluvial-fan de posits thin above relatively impermeable underlying material or where drains and stream courses intersect the water table. Much of the ground-water discharge occurs in the Central Park sub- area, north of' an east-west line drawn through Central Park. The Gallatin and East Gallatin Rivers are effluent north of this line, and many streams rise in the area,
Estimates were made of the annual discharge of ground water as surface water during the period March 1934 through February 1953. (See table 18.) These estimates are based on an analysis of records of streamflow in the Gallatin Valley.
Because nearly all the inflow to the valley during July and August is diverted for irrigation and very little of the diverted
WATER RESOURCES 117TABLE 18. Estimated ground-water discharge, in thousands of acre-feet,
from the Gallatin Valley
Year (March through
February)
(1)
1934-35 ......1935-36......1936-37 ......1937-38... . ..1938-39 ......1939-40. .....1940-41 ......1941-42... ...1942-43 ......1943-44. .....1944-45. .....1945-46.1946-47 ......1947-48......1948-49 ......1949-50.1950-51......1951-52 ......1952-53 ......
Measured discharge of
Gallatin River at Logan during August
(2)
10 14 14 16 20 18 20 22 21 32 23 26 27 34 48 24 41 38 36
Estimated average monthly
ground-water discharge
during summer
(3)
10 14 10 16 20 18 19 20 21 24 23 25 25 31 27 24 28 28 32
Average difference between monthly
inflow and outflow during period
November through February
(4)
8 12 11 12 17 17 16 18 19 16 21 19 22 24 20 18 20
1 20.5 1 22.2
Estimated average monthly ground- water discharge
During winter
(5)
11 15 11 15 20 18 18 18 19 19 21 19 22 23 20 18 21
1 20.5 1 22.2
For the year
(6)
10 14 10 16 20 18 18 19 20 22 22 22 24 27 24 21 25 24 27
Estimated annual ground- water
discharge
(7)
120 170 120 190 240 220 220 230 240 260 260 260 290 320 290 250 300 290 320
1 Measured.
water returns as waste surface water to the valley streams, the outflow from the valley during these months largely represents ground-water discharge. If, however, the records of streamflow and precipitation indicated that not all surface-water inflow was diverted or that precipitation within the valley or return of waste water contributed substantially to the outflow, the meas ured flow of the Gallatin River at Logan during August (column 2) was adjusted accordingly in estimating the average monthly ground-water discharge during the summer (column 3). The estimates of ground-water discharge probably err on the low side.
During the cold-weather months, November through Febru ary, when precipitation contributes little or no runoff and evapo- transpiration is of minor importance, the difference between in flow to, and outflow from, the valley consists largely of ground-water discharge. Differences between the inflow and out flow during the winter months were averaged (column 4) and then adjusted (column 5) on the basis of temperature and pre cipitation records.
The average of the monthly summer and winter ground-water discharges (column 6) was considered to represent the average monthly ground-water discharge for the year, and when multi plied by 12, was considered to represent the annual ground-
118 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
water discharge (column 7). The estimates of annual ground- water discharge range from 120,000 to 320,000 acre-feet and average about 240,000 acre-feet.
A different method of estimating ground-water discharge was used for the years March 1951 through February 1952 and March 1952 through February 1953. This method was based on a graph showing cumulative departure from the amount of ground water in storage on June 30, 1952. (See fig. 26.) The slope of the graph during the fall and winter months, when evapotrans- piration is at a minimum, was used to determine the average monthly rate of ground-water discharge as surface flow. By this method, the amount of ground water discharged from the valley for those years was computed to be about 280,000 and 300,000 acre-feet, respectively. These values compare well with the values obtained for the same years by the streamflow method.
CONFIGURATION OF THE WATER TABLE
The water table is an irregular sloping surface that conforms roughly to the topography of the land surface. The configura tion of the water table beneath a large part of the Gallatin Valley at the approximate low and high positions during 1953 (about April 1 and August 1, respectively) is shown by contour lines on plate 5. The configuration of the water table beneath the rest of the valley could not be shown because of the lack of sufficient data and because much of the ground water is confined.
Ground water moves in the direction of the hydraulic gradient, that is, at a right angle to the water-table contour lines. Along the sides of the Gallatin Valley, ground-water movement is to ward the valley floor, and within the valley it is in a general northward direction. The rate of movement is proportional to the slope (hydraulic gradient) and to the permeability of the material.
The depths to water (about April 1, 1953) in wells in the Gal latin Valley are shown on plate 6 by numbers adjacent to the well symbols. As shown by the pattern on the same plate, the depth to water is less than 10 feet throughout most of the valley floor and the lower part of the Bozeman fan. However, in some places in these parts of the valley, the depth to water is as much as 50 feet. In the Camp Creek Hills the depth to water ranges from about 1 foot to as much as 600 feet. Along the south and east fringes of the valley and in the Dry Creek subarea it ranges from a few feet to 170 feet.
FIGURE
26. Graph
s for
perio
d July
1951
throug
h Septemb
er 1953
, showi
ng discharge of
Gallatin
River
near Gallatin
Gateway, total
diversions
from
Gallatin River
between
Gallatin
Gateway
and
Central
Park,
total
monthly
precipitation and
average
monthly
temperature at
Belgrade,
and
monthly cumulative
departure from
the
volume
of
saturated
material as of
the
end
of
June
1952.
CHANGES
IN
STORAGE
The
water
table
rises
when
recharge exceed
s discha
rge and
falls
when
discharge exceeds
recharge.
Changes in
ground-wa
ter
storage within
the
valley are reflected
by
fluctuations of
the
THOU
SAND
S OF
AC
RE- F
EET
INCH
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120 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
water level in wells. The difference between any two measure ments of the water level in a well is a measure of the net amount of material that was saturated or drained in the vicinity of the well during- the period between the measurements.
In estimating- chang-es in ground-water storage for the valley as a whole, the valley was divided into hydrologic units (fig-. 2), each having- distinctive characteristics; the units were subdivided into polyg-onal areas, each having- an observation well within it. The boundaries of the polyg-onal areas were determined by the Theissen method (Theissen, 1911, p. 1082-1084). The chang-e in water level in each well, multiplied by the area of the polygon in which the well was situated, was considered to be the volume of material saturated or drained within the polyg-on during- the pe riod for which computed. The sum of the volumes for all the polyg-onal areas in a hydrologic unit was considered to be the total volume of material saturated or drained within the unit. In some instances, where observation wells were widely scattered and the polyg-onal areas were correspondingly large, the meas ured chang-es in water level were adjusted to conform more nearly to water-level changes in areas having- similar hy- drolog-ic characteristics and for which more adequate informa tion was available. Fortunately, observation-well coverag-e was adequate throughout the valley floor, where most of the change in storage takes place. The nonirrigated part of the Camp Creek Hills was not included in the computation because so little re charge is available to this area that the annual change in ground- water storage is insignificant.
The monthly changes in the volume of saturated material in the Gallatin Valley (excluding the Dry Creek subarea) for the period July 1951 through September 1953 are given in table 19, and the cumulative monthly departures from the volume of satu rated material as of the end of June 1952 are given in table 20. A graph of the monthly cumulative departure from the volume of saturated material as of the end of June 1952 in the Gallatin Valley is shown in figure 26, together with graphs of the dis charge of the Gallatin River at Gallatin Gateway, total diversions of water from the Gallatin River between Gallatin Gateway and Central Park, and precipitation and average temperature at Bel grade. The changes in the volume of ground water in storage (table 21) were computed by multiplying the changes in volume of saturated material by the average specific yield of the material (0.15).
TABL
E 1
9.
Alo
ntkl
y ch
ange
s in
vo
lum
e of
sa
tura
ted
mat
eria
l in
th
e -J
alla
tin
V'a
iiey
(exc
lusi
ve
oj D
ry
Jree
fc
suba
rea)
, in
thou
sand
s of
acr
e-fe
et[l
a, G
atew
ay s
ub
area
; Ib
, B
elgr
ade
sub
area
; Ic
, C
entr
al P
ark
su
bar
ea;
Id,
Man
hat
tan
sub
area
; le
, U
pp
er E
ast
Gal
lati
n su
bare
a; I
I, B
ozem
an f
an;
R,
rem
aind
erof
Gal
lati
n V
alle
y]
Are
a or
sub
area
Oct
.N
ov.
Dec
.Ja
n.
Feb
.M
ar.
Apr
.M
ayJu
ne
July
Aug
.S
ept.
.
Wat
er y
ear
1951
Id...................
II ...................
R. ..................
Tot
al ...
....
...
+ 1
1.0
+ 1
.5
-13.6
+ 1
8.9
+ 1
7.8
-15.4
-4
.0
+2.0
-7
.0
-24.4
-44.1
-6
.9
-15.9
-3
5.3
-1
02.2
Wat
er y
ear
1952
la..
....
....
....
....
.Ib...................
Ic...................
le..
....
....
....
....
.
Id...................
II ...................
R. ..
....
....
....
....
Tot
al ...
....
...
-106.2
-7.1
-10.4
-40.0
-163.9
-90.5
-6.2
-36
.9-3
1.6
-165.2
-102.9
-8.0
-11.0
-24.6
-146.5
-71
.3-7
.0-2
2.5
-19
.9-1
20.7
-54
.7-6
.3-2
4.4
-31
.3-1
16.7
+3
2.3
+ .6
+57.1
+20.0
+ 1
10.2
+ 1
38.0
-4.6
-i-4Q
^+
156
.4+
33
9.3
+2
13
.5+
27.2
+2
6.5
+45.5
+3
12
.7
+ 1
13.7
+ 1
7.5
+2
9.1
-.7
+ 1
59.6
-6.6
+31.5
-.2
-2.5
_1_
K
+ 1
1.5
+42.5
+ 7
6.7
-13.4
-22.9
-4.5
9
_1_
K
+23.6
-16
.1-8
0.9
1
1 Q
_ Q
4
Q
-6.9
-3.7
-4.0
-20.0
-6.6
-87.9
en
o
d g w cc
Wat
er y
ear
1953
la..
....
....
...
....
..Ib...................
Ic ...................
Id...................
le..
....
....
....
....
.II...................
R. ..
....
....
....
....
Tot
al ...
....
...
-14.4
-72.8
-6.7
-3.9
-2.9
-27
.8-7
5.1
-203.6
-13.4
-77.5
-3.4
-9.3
-2.1
-26
.7-4
7.3
-179.7
-10.7
-56.6
-7.5
-6.7
-2.9
-25.6
-34.2
-144.2
-8.4
-100.0
-2.2
-7.7
-2.9
-23
.1-3
2.7
-177.0
-3.8
-52.1
-3.0
-4.2
-4.2
-18
.6 5
Q Q
-125.8
-3.0
-44
.4+
1.3
-3.4
-4.3
-6.5
-6.1
66.4
-3.2
+9.5
+ .
6+
.1+
1.7
-1.4
_I_Q
n+
10.
3
+2
6.6
+ 1
44.7
+24.5
+29.0
+3
1.4
+ 1
7.1
+9
6.8
+3
70
.1
+5
5.8
+2
31
.6+
7.0
_1_7
Q
-16.8
-1-1
17
3
+93.3
+4
96
.1
1
0 Q
+ 7
2.3
-1.9
+ 1
0.6
-1-4
Q
+ 1
2.4
_1_O
Q
O
+ 1
15.6
Q
4
-17.8
-^2.2
-8.6
-2.6
-4.6
-27.3
-72.5
_ K
n
-67.5
-5.5
-5.0
-2.6
-27.8
-29.1
-14
2.5
TABL
E 2
0.
Cum
ulat
ive
mon
thly
dep
artu
res
from
vol
ume
of s
atur
ated
mat
eria
l in
the
Gal
lati
n V
alle
y (e
xclu
sive
of
Dry
Cre
eksu
bare
a) a
s of
the
end
of
June
195
2, i
n th
ousa
nds
of a
cre-
feet
[la.
Gat
eway
su
bar
ea;
Ib,
Bel
grad
e su
bar
ea;
Ic,
Cen
tral
Par
k su
bar
ea;
Id.
Man
hat
tan
sub
area
; le
, U
pp
er E
ast
Gal
lati
n su
bare
a; I
I, B
ozem
an f
an;
R,
rem
aind
erof
Gal
lati
n V
alle
y]
Are
a or
sub
area
Oct
.N
ov.
Dec
.Ja
n.
Feb
.M
ar.
Apr
.M
ayJu
ne
July
Aug
.S
ept.
Wat
er y
ear
1951
Id.................. .
II. ..................
R. ...................
Tot
al ..........
*.......
-23
.4
+3
.3
-29
.5
-50
.4
-100.0
-12.4
+
4.8
-4
3.1
-3
1.5
-8
2.2
-27.8
+
.8
-41.1
-3
8.5
-1
06.6
Wat
er y
ear
1952
la..
...
....
....
....
..Ib..................
.Ic
...
....
....
....
....
le. ..................
la.
Ib.
Ic.
le. .........
Id. ..................
II ...
....
....
....
....
R. ..................
Tot
al ..........
-71.9
-6.1
-57.0
-73.8
-208.8
-178.1
-13
.2-6
7.4
-114.0
-372.7
-268.6
-19.4
-104.3
-145.6
-537.9
-371.5
-27
.4-1
15.3
-170.2
-684.4
-442.8
-34.4
-137.8
- 1
90 .
1-8
05.1
-497.5
-40.7
-162.2
-221.4
-921.8
-465.2
-40
.1- 1
05 .
1-2
01.2
-811.6
-327.2
-44.7
-55.6
-44.8
-472.3
-113.7
-17.5
-29
.1+
.7
- 1
59 .
6
-6.6
+31.5
-.2
-2.5
_1_
K
+ 1
1.5
+4
2.5
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1953
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-46.3
-99.0
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-59.9
-55.2
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-59
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-86
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-70.4
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-29.2
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-112.2
-136.7
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-78
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-209.3
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-85.6
-429.6
-33.1
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-26
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-988.7
-88
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-978.4
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-8.0
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-115.6
-608.3
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WATER RESOURCES 123TABLE 21. Monthly changes in volume of ground water stored in the Gallatin
Valley, in thousands of acre-feet
Month
October ........................November ......................December .......................
February .......................March. .........................
May ............................
July............................
September ......................
1951
+2.67-3.67
-15.33
Water year
1952
-24.58-24.78-21.97-18.11-17.51+ 16.53+50.90+46.90+23.94+ 11.51-12.14-13.18
1953
-30.57-26.98-21.58-26.48-18.88-9.96+ 1.61
+55.51+74.49+ 17.30-10.92-21.40
This value for specific yield is the average ratio of net gain in surface flow to net loss in volume of saturated material during a period when all precipitation was stored as snow and no ground water was used consumptively. During such a period, the net gain in surface flow was due wholly to discharge of ground water. Figure 27 is the graph used in computing the average specific yield of the ground-water reservoir in the Gallatin Valley.
The average monthly water-level fluctuations in the Gallatin Valley are illustrated by the same graph that shows monthly cumulative departure from the volume of saturated material as of the end of June 1952. (See fig. 26.) Under the existing water regimen in the valley, the pattern of fluctuation is unlikely to change from year to year, though the magnitude of seasonal changes will vary with the volume and duration of recharge. The difference between the water level on about April 1 and Au gust 1, 1953 (the average lowest and highest positions, respec tively, during that year) is shown on plate 7. It may readily be seen that the maximum change in water level occurs in the central part of the Belgrade subarea, that significant changes occur in the Gateway subarea, at the upper end of the Bozeman fan, and in the Manhattan subarea, but that elsewhere in the valley the change is relatively insignificant.
A long-term record of water-level fluctuations is important be cause a progressive decline or rise of the water table over a period of several years could have a pronounced effect on water use and the agricultural economy of the Gallatin Valley. No meas urements of water-level fluctuations in the Gallatin Valley were made before the period of this investigation. However, the trend
124 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
UJ 90
U.
UJor o
U_ 80
O
0) 0
HOUSAN vi o
>" 60
O_J u_
WATER at
0
GAIN IN SURFACE-OJ 4* O O
Ul
Ul
> 20H
O 10
0 1C
Slope
/00c\
October
of lines equals 15 perc
//
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__ EXPL^
^February
Febru
//
/OJanuary
^NATION
Water year 1952
O Water year 1953
I/
)0 200 300 400 500 600 700 800 90
CUMULATIVE NET LOSS IN VOLUME OF SATURATED MATERIAL, IN THOUSANDS OF ACRE-FEET
FIGURE 27. Graph used in computing average specific yield of the ground-water reservoir inthe Gallatin Valley.
and magnitude of the annual water-level fluctuations during the 17-year period preceding this investigation were inferred by es timating the cumulative departure (at the beginning of August and at the end of December in each year of the period) from the volume of saturated material as of the end of June 1952. (See table 22 and fig. 28.)
The estimates for the end of December (column 2, table 22) were obtained by using the estimates of average winter ground- water discharge (column 5, table 18) and a rating curve based
1000
500
-50
0
-1000
-1500
0 E
ST
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OM
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1936
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1942
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1944
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1946
19
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1948
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1950
19
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1952
19
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UR
E 2
8.
Gra
ph s
how
ing
esti
mat
ed c
um
ula
tive
dep
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re,
1934
-53,
fro
m t
he v
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e of
sat
ura
ted
mat
eria
l as
of
the
end
of J
un
e 19
52.
to 01
126 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
TABLE 22. Estimated cumulative departures from volume of saturated 'ma terial as of the end of June 1952, in thousands of acre-feet
Year (March through
February)
(1)
1934-35......1935-36......1936-37......1937-38......1938-39......1939-40......1940-41 ......1941-42. .....1942-43......1943-44. .....1944-45......1945-46......1946-47......1947-48......1948-49. .....1949-40......1950-51 ......
Estimated cumulative departure, at end of December, from the volume of saturated
material as of the end of June 1952
(2)
-1,180-880
- 1 , 180-880 fi4fl-760 760-760-700-700-570-700-530-470 fi4fl-760-570
Estimated change in volume of saturated
material, August through December
(3)
-250-360-250-400-500-460-460-480-500-550-550-550-610-670-610-530-630
Estimated cumulative departure, at beginning of August, from volume
of saturated material as of the end of
June 1952
(4)
-930-520-930-480-140-300-300-280-200-150-20
-150+80
+200-30
-230+60
on the ratio of monthly ground-water discharge to the corre sponding cumulative departures from volume of saturated ma terial during the period November 1951 through February 1952 (fig. 29). The estimates for the beginning of August (column 4, table 22) were obtained by subtracting the estimated change in volume of saturated material, August through December (col umn 3, table 22), from the estimated cumulative departure at the end of December (column 2, table 22). The estimated change in volume of saturated material, August through December, was obtained by multiplying the estimated annual ground-water dis charge (column 7, table 18) by the ratio (2.1) of the volume of material drained during the period August through December 1951 (602,200 acre-feet) to the volume of ground water dis charged during the year March 1951 to February 1952 (290,000 acre-feet). The cumulative departure in volume of saturated material at the beginning of March (fig. 28) was approximated by extending the line that connects the August and December departures.
Figure 28 indicates that the lowest water level in the period 1934-53 was in 1935. The fluctuation in 1952 was the greatest annual fluctuation during the 19-year period and was about two- thirds of the difference between the lowest and highest water
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128 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
water development because of the decrease in ground-water stor age and the increase in depth to water that may result.
WATER-LEVEL FLUCTUATIONS CAUSED BY EARTHQUAKES AND OTHER DISTURBANCES
During this investigation several earthquakes caused fluctua tions of the water level in wells Al-4-25dc and D2-4-9bc, each of which was equipped with a water-level recording gage. The effect of two earthquakes, one in Siberia and the other in Mex ico, are illustrated by hydrographs of the water level in well Al-4-25dc. (See fig. 30.) The water level in this well was af fected also by the passing of trains on the freight line of the Northern Pacific Railway, about 150 feet from the well. Minor water-level fluctuations caused by the passing of automobiles and trucks- were recorded by the gage on well Al-4-5da, located about 20 feet from the county road.
WATER-RESOURCES INVENTORY, WATER YEARS 1952 AND 1953
EVALUATION
The hydrologic data collected in the Gallatin Valley during the 1952 and 1953 water years were used in making a monthly inventory of the total water resources of the valley. The Dry Creek subarea was not included in the inventory, however, be cause too few data on changes in ground-water storage were collected in that part of the valley. The results of the inventory are given in table 23 and are shown graphically on plate 8.
The Gallatin Valley is well suited for an inventory of this type because nearly all the components of the inventory could be measured with reasonable accuracy. Surface-water inflow to the valley was measured at gaging stations situated around the mar gin of the valley; precipitation was measured at stations scat tered throughout the valley; the net discharge from, and recharge to, the ground-water reservoir underlying the valley were com puted from measurements of the water level in numerous wells; and surface-water outflow was measured at Logan, the valley's only outlet.
Because the accretions to the surface-water supply of the val ley must balance the depletions, the difference between the meas ured accretions (surface-water inflow, precipitation, and net ground-water discharge) and the measured depletions (net ground-water recharge and surface-water outflow) is equal to the net difference between the unmeasured accretions and un measured depletions. The unmeasured accretions consist of sub surface inflow and snowmelt; the unmeasured depletions consist
2526
SE
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1953
27
28
29
OC
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ater
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to
TABL
E 2
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ater
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195
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53,
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tial
rec
ord
for
Chu
rn,
Dee
r,
and
Fos
ter
Cre
eks
in t
he
1953
wat
er y
ear.
WATER RESOURCES 131of subsurface outflow, evaporation, transpiration, storage as snow, and net increases in soil moisture. The inventory shows that the unmeasured accretions exceeded the unmeasured deple tions in only 2 months (March and April 1952) of the 2-year period.
Subsurface inflow and outflow are believed to be negligible. The only subsurface materials that conceivably might transmit a significant volume of water to, or from, the valley are the Tertiary strata that separate the Gallatin and Madison Valleys, the alluvium beneath the floor of the inlet and outlet canyons of the valley, and fractured rocks in the basement complex.
As the water table in the Camp Creek Hills stands above the water table in both the Madison and Gallatin Valleys, ground water cannot move out of the Gallatin Valley into the Madison Valley, nor can ground water move from the Madison Valley into the Gallatin Valley.
The thickness of the alluvium at the inlet gaging station is not definitely known but probably is about 40 feet. This thick ness is based on evidence that the alluvium probably is less than 20 feet thick at other places in the canyon and that it is about 80 feet thick at Gallatin Gateway, about 8 miles downstream from the gaging station. The width of the alluvial surface at the gaging station is about 0.1 mile, and the gradient of the stream is about 30 feet per mile. Therefore, if it is assumed that the coefficient of permeability is 10,000 gpd per square foot, the maximum underflow at the inlet gaging station would be only 1,300 acre-feet per year.
Two wells, A2-2-35abl and -35ab2, were drilled near the out let gaging station and penetrated, respectively, 22 and 23 feet of alluvium before entering limestone bedrock. (See fig. 31.) As
Gal/at in River _J^^.
(1) A2-2-35abl
(2) rA2-2-35ab2
- V°!h
Limestone of the Madison group
LOGAN
Vertical and horizontal scale
FIGURE 31. Geologic section near Logan.
132 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
these wells, drilled in September 1952, reached no water, appar ently all underflow at that time was restricted to the alluvium underlying1 the riverbed. At the time of spring1 runoff, however, more of the alluvium probably transmits underflow. Although the river crosses several limestone formations at Logan, the for mations are not known to be very cavernous in that vicinity, and loss of water into them is believed to be small. Underflow through the alluvium plus loss to the limestone formations is considered to be well within the error of measurements at the Logan gaging station.
Thermal water issuing from springs and flowing wells in the valley suggests that the basement rocks may be broken in places by joints or faults. Although water conceivably enters or leaves the valley through such conduits, no evidence indicates that any large amounts of water are conveyed by them. The difference between amounts of water entering and those leaving the valley through openings in the basement rocks probably is so small as to be of no importance.
In the cold-weather months the unmeasured depletions con sist largely of snow storage and evaporation of snowmelt, and in the warm-weather months largely of evapotranspiration and increases in the moisture content of the soil. Unmeasured accre tions consist largely of snowmelt that results in increased runoff.
ANALYSIS
During the period October 1951 through February 1952 ground- water recharge was slight, and, as ground-water discharge con tinued, there was a decrease in the volume of saturated material within the valley and a gain in surface-water flow. Most of the precipitation occurred as snow, much of which was discharged from the valley by evaporation. Surface-water outflow from the valley during this period consisted largely of water that entered the valley as surface-water inflow and of water discharged from the ground-water reservoir.
During March and April 1952 soil moisture was replenished and the ground-water reservoir received considerable recharge from melting snow and precipitation. Surface-water outflow from the valley still exceeded surface-water inflow, however, be cause precipitation and snowmelt added to the runoff.
In May 1952 the ground-water reservoir was replenished further, in part by the infiltration of surface water diverted for irrigation and in part by precipitation. Much water was con sumed by evapotranspiration. It was the month of greatest
WATER RESOURCES 133
accretion to the total water supply of the valley and also the month of greatest surface-water outflow from the valley.
During June and July 1952, ground-water storage continued to increase in spite of withdrawals by evapotranspiration and discharge as surface flow. Much of the surface-water inflow to the valley was diverted for irrigation, and part of the diverted water infiltrated to the zone of saturation. Nearly all the pre cipitation either evaporated or replenished soil moisture; little or none infiltrated to the water table and little or none left the valley as surface-water outflow. For the first time in the 2-year period, surface-water outflow was less than surface-water inflow.
In August 1952, despite continued recharge to the ground-wa ter reservoir, discharge of ground water exceeded recharge. As surface-water inflow to the valley was entirely consumed within the valley, surface-water outflow from the valley consisted wholly of pickup from the ground-water reservoir and con tinued to be less than surface-water inflow.
During the period September 1952 to March 1953 ground- water discharge exceeded recharge. Replenishment of soil moisture and evapotranspiration exceeded precipitation, the dif ference being largely accounted for by discharge from the ground- water reservoir. Surface-water outflow from the valley was greater than surface-water inflow throughout this period, the increase consisting almost wholly of ground-water discharge.
Beginning in April 1953 and continuing through the next July, the ground-water reservoir was filled to a level only slightly below that of July 1952. Apparently most of the recharge re sulted from the infiltration of rainfall and applied irrigation water. In contrast to the previous spring, direct recharge from melting snow was insignificant. Except during April, surface-water outflow from the valley was less than surface-water inflow.
In August and September 1953, discharge of ground water again exceeded recharge. Most of the precipitation and surface- water inflow to the valley were disposed of by evapotranspiration and the replenishment of soil moisture; surface-water outflow from the valley consisted almost wholly of ground water dis charged from storage.
Despite the constantly varying ratio of ground-water recharge to discharge, the volume of ground water in storage in the Gal- latin Valley at the end of the 2-year period almost exactly equaled the volume in storage at the beginning. Although precipitation, particularly as snowmelt, sometimes is significant as a source of recharge to the ground-water reservoir, surface-water inflow
134 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
to the valley, diverted for irrigation, is by far the principal source of recharge. Even though surface-water inflow was insuf ficient for existing irrigation requirements, surface-water outflow from the valley during the 2-year period was slightly greater than surface-water inflow.
WATER-RESOURCES INVENTORY, WATER YEARS 1935 THROUGH1951
Estimates of the annual changes in the surface-water supply of the valley for the 17 water years preceding the 2-year period of the monthly inventory are given in table 24. In this table, the estimates of surface-water inflow to the valley are those given in table 10, and the values for surface-water outflow are the measurements of the flow of the Gallatin River at Logan, as given in table 7.
The estimated values for precipitation were derived as follows: The ratio was determined between (a) total precipitation on the valley as measured in water years 1952 and 1953 (table 5) and (b) precipitation during those same years at the Bozeman and Belgrade stations of the U. S. Weather Bureau (tables 2 and 3). The annual precipitation by water years at the Boze man station during the period 1934-40 and the averaged annual precipitation by water years at the Bozeman and Belgrade sta tions for the period 1940-51 were multiplied by this ratio. The results probably are accurate within about 20 percent.
The values for the net gains from, or losses to the ground- water reservoir are the differences between successive October 1 points on the graph in figure 29 multiplied by 0.15 (the specific yield for the valley as a whole). Net depletions, excluding net loss to the ground-water reservoir, were computed by subtracting (a) surface-water outflow from the valley plus net losses of surface water to the ground-water reservoir from (b) surface- water inflow to the valley plus precipitation on the valley plus net gains in surface-water flow derived from the ground-water reservoir. As pointed out on page 132, depletions other than losses to the ground-water reservoir consist largely of evapotranspira- tion, increase in soil moisture, and storage as snow. The magni tude of evapotranspiration, the largest of these depletions, is affected by such factors as volume of water available, tempera ture, wind velocity, relative humidity, hours of sunshine, and length of the growing season. Although an attempt was made to establish a constant relationship between the magnitude of evapotranspiration and the factors affecting it, none was found.
TABL
E 2
4.
Est
imat
ed a
nnua
l ch
ange
s in
sur
face
-wat
er s
uppl
y of
the
Gal
lati
n V
alle
y, w
ater
yea
rs
1935
th
roug
h 19
51,
in
thou
sa
nds
of a
cre-
feet
Water year
19
35
.. ...
....
.1936..........
1937..........
1938..........
1939
..........
1940..........
1941
..........
1942..........
1943
..........
1944..........
1945..........
1946..........
1947..........
1948..........
1949..........
1950..........
1951
..........
Surface-water
inflow
to Gallati
n Valle
y
570
568
560
716
642
644
546
816
930
730
713
757
948
1,04
4 69
6 76
2 73
0
Surface-water
outflow from
Gallati
n Valle
y (Gallatin
River at Loga
n)
396
469
448
610
559
596
481
820
900
711
667
709
928
1,07
7 71
2 71
0 71
5
Net
gain (
+) or loss ( )
in
surface-water flow
-174
-99
-112
-106
-83
4
8^
-65
+
4
-30
-19
-46
-48
-2
0
+ 3
3 +
16
-52
-15
Acc
retio
ns o
ccur
ring
wit
hin
Gal
lati
n V
alle
y
d o 1 o, '8 £ O
l
330
300
410
380
380
390
460
430
560
470
370
410
520
570
420
420
370
Sfe
1sl
f~
- £
t.
i »
S-i
'Sl?
%al
l II
4»
P
OB
H <
£o>
K 4>
Wte
$5 «"
- « 54 23 0 20 32 27 23
3 o H 330
354
410
380
403
390
460
430
560
470
390
410
520
602
447
420
393
Dep
letio
ns o
ccur
ring
wit
hin
Gal
lati
n V
alle
y
-m-S
ill
|||.§
&"§
o >
Sl&l
£B
*E 447
453
469
436
486
438
520
415
585
471
436
423
530
569
431
432
408
^ £
S>
£
0«
1 S
ftsl's mil
Jg
^
1-c
57 53
50 0 5 11 5 18 35
10 40
"3
1 504
453
522
486
486
438
525
426
590
489
436
458
540
569
431
472
408
Net
gain
(
+) or loss ( )
occurring
within Gallati
n Valle
y
-17
4
-99
-112
-106
-83
-48
-65
+4
-30
-19
-46
-48
-20
+
33
+ 1
6 -5
2
-15
Total
accretions to surface-wat
er supp
ly of
Gallatin
Valley (tot
al surface-water inflow
plu
s total
accre tions
withi
n valley)
900
922
970
1,09
6 1,
045
1,03
4 1,
006
1,24
6 1,
490
1,20
0 1,
103
1,16
7 1,
468
1,64
6 1,
143
1,18
2 1,
123
Total
depletions
of surface-wat
er supp
ly of
Gallatin
Valley
(total depletio
ns within
valley
plus
surface- water
outflow
)
900
922
970
1,09
6 1,
045
1,03
4 1,
006
1,24
6 1,
490
1,20
0 1,
103
1,16
7 1,
468
1,64
6 1,
143
1,18
2 1,
123
a 90 90 a TO o (3
90
O CO on
136 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
It is probable, therefore, that the relationship is complex and not easily resolved.
HYDROLOGIC UNITS WITHIN THE GALLATIN VALLEY
VAXLEY FLOOB
The floor of the Gallatin Valley is underlain by alluvium de posited by the Gallatin and East Gallatin Rivers. In this report, the valley floor has been subdivided arbitrarily into five sub- areas the Gateway, Belgrade, Central Park, Manhattan, and Up per East Gallatin (fig-. 2).
GATEWAY SUBAREA
The Gateway subarea extends northward from the inlet at the south end of the valley to the vicinity of Bozeman Hot Springs, a distance of about 10 miles, and comprises an area of about 16 square miles. Most wells in this subarea are 10 to 40 feet deep, though near the margins some of the wells are considerably deeper.
The alluvium of the Gallatin River in this subarea ranges in width from about li/2 miles to 2 miles and is bordered along its east margin by a narrow terracelike belt of stream deposits and colluvium derived from Goochs Ridge. The alluvium was de posited in a trench cut by the Gallatin River into relatively im permeable Tertiary strata. The subsurface configuration of the trench is not known, but in cross section probably appears as represented by one of the sketches in figure 32. A well (D3-4- 3ca) near Gallatin Gateway was drilled through 80 feet of allu vium before entering Tertiary strata, and test hole D2-4-lldc, 1 mile north of the downstream boundary of the subarea, pene trated 68 feet of alluvium before entering Tertiary strata. The average thickness of the alluvium in the subarea, however, is estimated to be about 55 feet. No evidence indicates that the alluvium is other than uniformly coarse and permeable. The coefficient of transmissibility, as determined by aquifer tests, was 380,000 gpd per foot at well D2-4-26dc and 170,000 gpd per foot at well D3-4-llbdb. A similar test made at well D2-4-lldc, just north of the subarea but in the same aquifer, gave a coef ficient of transmissibility of 270,000 gpd per foot.
The main sources of recharge are the irrigation canals that cross the subarea and the streams that enter it from the high lands on either side. During years of heavy snowfall, if the soil is not frozen, spring snowmelt also is an important source of recharge. The ground water moves downvalley and toward the
HYDROLOGIC UNITS WITHIN THE GALLATIN VALLEY 137
Goochs Ridge
CALL AT IN RIVER
'V'"- '.' ;' " ' : '^'AI luviu
Tertiory strato
Colluvium ond olluvium
FIGURE 32. Diagrammatic sections of the Gateway subarea showing two possible interpretations of subsurface geologic relationships.
Gallatin River. Most of it either discharges into the Gallatin River or leaves the subarea as underflow to the adjoining Bel grade subarea; a small amount discharges into a few small streams, principally Fish Creek, on the alluvial plain southwest of Axtell Bridge; and the remainder is discharged by evapotrans- piration, especially along the Gallatin River.
At present the water table is between 10 and 15 feet below the land surface throughout much of the Gateway subarea. During a period of dry years, however, the ground-water level undoubt edly would decline. For example, if annual recharge over a period of years were only half the present rate, decline of the water table east of the Gallatin River probably would average about 10 feet, and at the extreme east margin of the subarea it would be as much as 20 feet. West of the river the decline probably would not be as great. However, as the flow of the Gallatin River where it enters this subarea is dependably large and as several major irrigation canals either cross or skirt the area, it is unlikely that recharge would be deficient for a succession of years.
508919 O-60 10
138 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
A graph showing- the cumulative departure from the volume of saturated material as of the end of June 1952 in the Gateway sub- area (fig. 33) indicates that ground-water discharge exceeded ground-water recharge during all the months of water year 1953 except May and June, when recharge exceeded discharge. From the spring of 1952 to the spring of 1953, ground-water discharge from the Gateway subarea as surface water is estimated to have
GATEWAY SUBAREA
BELGRADE SUBAREA
\
CENTRAL PARK SUBAREA
MANHATTAN SUBAREA
SONDJANFMAMJ JA SONDJANFMAMJ J A S OCT
FIGURE 33. Graphs showing the cumulative departure from the volume of saturated material as of the end of June 1952 in the Gateway, Belgrade, Central Park, and Manhattan subareas and in the Bozeman fan.
HYDROLOGIC UNITS WITHIN THE GALLATIN VALLEY 139
been at least 25,000 acre-feet. This estimate is based on the gain in flow of the Gallatin River between the Gallatin Gateway and Axtell Bridge gaging stations during November and Decem ber 1952 and January and February 1953 (table 9), which were months of negligible gain from surface runoff and months in which no diversions were made. However, because ground-water discharge from the Gallatin Valley as a whole during that year was somewhat above average for the preceding 18-year period (table 18), it is assumed that the volume of ground water dis charged as surface water from the Gateway subarea that year was above average in about the same ratio as was that from the valley as a whole. Therefore, the average annual dicharge of ground water from the Gateway subarea as surface water is estimated to be about 20,000 acre-feet. Because, in general, aver age annual recharge equals average annual discharge, the average annual recharge to the Gateway subarea is at least 20,000 acre- feet plus the volume of ground water discharged by evapotrans- piration within the subarea and by underflow downvalley to the Belgrade subarea.
Thus, the average annual volume of ground water theoretically available for additional consumptive use in the Gateway subarea is at least 20,000 acre-feet. If this or a lesser amount were con sumptively used, the annual flow of surface water across the north boundary of the subarea would be reduced by an equivalent amount but would not be less than the annual flow of surface water into the subarea. If much more than 20,000 acre-feet were pumped each year and no part of the pumped water re turned to the zone of saturation, the water table eventually would be lowered to a level below that of the river. Recharge from the river would result, and surface-water outflow from the subarea would be less than inflow.
Pumping of ground water on a large scale in the Gateway sub- area would lower the water table, of course, and thereby tend to relieve waterlogging in poorly drained places. The hypothetical effect on the water-table position that would result from increased consumptive use of ground water is illustrated in figure 34. In an aquifer that discharges principally by seepage into a stream, such as the alluvium in the Gateway subarea, the lowering of the water level in wells tapping the aquifer would be in propor tion to the initial height of the water level in the well above the level of the surface of the stream. In reality, however, the posi tion of the water table would be affected by factors other than the volume of withdrawals. Some recharge may now be rejected,
140 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
EXPLANATION
Present position of water table
Position of water table if annual consumptive use of ground water equals one-fourth annual recharge
Position of water table if annual consumptive use of ground water equals one-half annual recharge
DISTANCE FROM RIVER, IN MILES
FIGURE 34. Diagrammatic section of the Gateway subarea showing the theoretical changes in position of the water table that would result from increased consumptive use of ground water.
and additional pumping might salvage some of it, so that the de cline would not be so great as might otherwise be expected.
BELGRADE SUBAREA
Northward from Bozeman Hot Springs, the surface of the alluvium of the Gallatin River broadens into an extensive plain that merges on the southeast with the alluvium of Middle (Hya lite) Creek and on the east with the alluvium of the East Gallatin River. (See pi. 2.) The Belgrade subarea comprises about 67 square miles. Its northern boundary is the east-west county road half a mile south of Central Park.
The alluvium underlying the Belgrade subarea is the principal ground-water reservoir in the Gallatin Valley. Most of this al luvium was deposited by the Gallatin River and consists of cobbles and coarse gravel, intermixed with varying amounts of sand, silt, and clay.
The alluvium thickens to the north. In test hole D2-4-lldc, near the south boundary of the subarea, it was 68 feet thick, and in test hole Dl-4-25aa2, about 4 miles north, it was 137 feet thick. Test hole Al-4-25dc, about 5 miles farther north, was drilled in alluvium to a depth of 400 feet without penetrating strata of Tertiary age. Although, locally, layers of clay and silt reduce its permeability, the alluvium generally is rather perme able and fairly homogeneous. The coefficient of transmissibility of the alluvium in this subarea was determined by aquifer tests
HYDROLOGIC UNITS WITHIN THE GALLATIN VALLEY 141
at 13 sites. The values obtained at 9 of the sites were between 94,000 and 290,000 gpd per foot and averaged 200,000 gpd per foot. At 3 of the sites it was less than 70,000 gpd per foot and at 1 it was 670,000 gpd per foot.
One of the smaller values, 58,000 gpd per foot, was obtained at test hole Al-5-28db2, which was drilled into the alluvium of the East Gallatin River. This value confirms the inference, based on examination of test-hole samples, that the alluvium of the East Galfatin River is less permeable than that of the Gallatin River. Another of the smaller values was obtained from test hole Dl-5-9cd, which was drilled into alluvium deposited by either or both the East Gallatin River and Middle (Hyalite) Creek. The coefficient of transmissibility obtained at this site was 50,000 gpd per foot, but it represented only 11 feet of satu rated material. The coefficient of permeability, therefore, was about 4,500 gpd per square foot, which is the same as the co efficient of permeability computed for the 58-foot thickness of saturated material in test hole D2-4-lldc. Underlying the 11- foot water-bearing zone in test hole Dl-5-9cd was an imperme able layer, possibly lime-cemented silt. The alluvium beneath the impermeable layer also yielded water, but no satisfactory test of its hydrologic properties was made; thus, although the co efficient of transmissibility of the entire saturated section is not known, it probably is considerably more than that for the 11- foot zone. A value of 70,000 gpd per foot for the coefficient of transmissibility was obtained from well D2-4-14bb, which was only 11.1 feet deep. This coefficient of transmissibility probably is representative of only part of the alluvium, especially in view of the much larger value, 270,000 gpd per foot, obtained from nearby test hole D2-4-lldc.
The largest coefficient of transmissibility, 670,000 gpd per foot, was obtained at well Dl-4-lcb and was more than double that obtained from any other test in this subarea. The flatness of the water table in the vicinity of the well (pi. 5) also indicates a high transmissibility. As no description of the water-bearing material was available for study, the reason for the high trans missibility could not be determined. The gravel penetrated in the drilling of the somewhat deeper well Dl-4-2dd, only half a mile south of well Dl-4-lcb, was very silty and when tested was found to have a coefficient of transmissibility of 130,000 gpd per foot. As no geologic evidence indicates that the saturated thickness of the alluvium changes substantially between these wells, it seems likely that the higher coefficient of transmissibility at well Dl-
142 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
4-lcb is due to greater permeability of the water-bearing ma terial. In general, it is probable that the coefficient of trans- missibility is greatest in the north-central part of this subarea where the alluvium is thickest. However, as no well in the Bel grade subarea north of well Dl-4-25aa2 is known to have been drilled through the entire thickness of the alluvium, transmis- sibility values from tests in that part of the subarea would not necessarily represent the transmissibility of the full thickness of the alluvium.
The coefficient of transmissibility of the part of the Tertiary section tested at test hole Dl-4-25aa2 was 17,000 gpd per foot, which is much lower than any of the values for the alluvium.
Seepage from irrigation canals and applied irrigation water, influent seepage from the Gallatin River, and ground-water un derflow from upgradient areas are the principal sources of re charge to the alluvium of the Belgrade subarea, though influent seepage from the East Gallatin River also is significant. Re charge by precipitation is of minor importance. Water in the zone of saturation moves in a generally northward direction and is discharged by underflow to the adjoining Central Park subarea. Some, however, is discharged into the Gallatin and East Gallatin Rivers and into Middle (Hyalite) Creek, and some is discharged by evapotranspiration where the water table is close to the surface.
Recharge to the Belgrade subarea during water year 1953 be gan to exceed discharge in April and continued to do so through July; discharge exceeded recharge in all the other months of the year. (See fig. 33.) From the spring of 1952 to the spring of 1953 about 135,000 acre-feet of ground water was discharged from the Belgrade subarea as surface-water flow and as ground- water underflow to downgradient subareas. This estimate is based on the average monthly rate of decrease in ground-water storage in the Belgrade subarea during the period November 1952 through February 1953 (fig. 33), when recharge to the subarea consisted only of underflow from the adjacent upgradient subareas and when discharge of ground water by evapotrans piration was negligible. Because ground-water discharge as surface-water flow was above normal that year, the average an nual discharge by this means plus that by underflow is estimated to be at least 100,000 acre-feet. Therefore, average annual re charge within the subarea is at least 100,000 acre-feet plus an amount equal to the volume of ground water discharged by evapotranspiration.
HYDROLOGIC UNITS WITHIN THE GALLATIN VALLEY 143
The Gallatin River is influent in the reach from Cameron Bridge (sec. 22, T. 1 S., R. 4 E.) northward to a mile beyond Irving Bridge (sec. 4, T. 1 S., R. 4 E.). Streamflow loss in this reach during the period November 1952 through April 1953, when the only significant diversion was into Baker Creek, was about 12,700 acre-feet. (See table 25.) If the ratio (0.10) be tween total streamflow losses (12,700 acre-feet) and the flow at Cameron Bridge for the same period (122,400 acre-feet) was ap plied to the flow at Cameron Bridge for 1952 (628,000 acre-feet) and for 1953 (369,000 acre-feet), recharge to the ground water by influent seepage from the Gallatin River was about 63,000 acre-feet in 1952 and about 37,000 acre-feet in 1953.
TABLE 25. Monthly losses in flow of the Gallatin River between Cameron Bridge and Central Park, in acre-feet
Month
1962
196S
Total. .......
Cameron Bridge (Gallatin River
near Belgrade)
1
17,20023,700
22,50018,600IQ con20,600
Baker Creek
2
1 QQft
1,110
790670650770
5,380
so
3
15,700on 7nn
in nnn15,80016 , 500OA infl
Central Park
(Gallatin River near Manhattan)
4
14 400on cnn
on onn15,70017 SJAO
18,300107,000
Gain (+) or loss ( ) between Cameron and Irving Bridges
l-(2+3)
-100-1,900
-2,700-2,100-2,600
+300
Gain ( +) or loss ( ) between Irving Bridge and Central Park
3-4
-1,300-100
+1,200-100
+ 1,300-1,800
_o
1,4002,000
2,7002,2002,6001,800
12,700
1 Preliminary data from U.S. Bureau of Reclamation.
The East Gallatin River between Lux Siding (sec. 23, T. 1 S., R. 5 E.) and Penwell Bridge (sec. 29, T. 1 N., R. 5 E.) also is influent during part of the year. (See table 26.) Middle (Hya lite) Creek (measured in sec. 32, T. 1 N., R. 5 E.) and Churn Creek drain (measured in sec. 23, T. 1 S., R. 5 E.) are tributaries of the East Gallatin. During the period December 1952 through June 1953, the East Gallatin River in that reach lost about 9,500 acre-feet by influent seepage and during the remainder of 1953 it gained in flow.
In this subarea the water table generally is highest near the end of July or in early August (fig. 33), at which time the water table is less than 20 feet below the land surface in most of the
144 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
TABLE 28. Monthly gains and losses in flow of the East Gallatin River be tween Lux Siding and Penwell Bridge, in acre-feet
[Preliminary data from U.S. Bureau of Reclamation]
Month
1962
December ...........
1958
February ............March ..............April ................May ................June. ...............July ................
September. ..........October .............November ...........
East Gallatin River near Lux Siding
1
3,8004,120
4,1302,5804,1007,170
21,30036,2007,1504,2203,8403,6803,700
Churn Creek drain
2
11169
12816023625232572b2440394554
Middle (Hyalite)
Creek
3
48528
103378928
1,4604,1207,4002,0302,2302,4602,3201,570
East Gallatin River at
Penwell Bridge
4
4,8903,650
3,9002,6604,9107,560
22,600131,000
9,380,olO
7,1806,5305,680
Gain (+) or
loss ( -)
4- (1+2+3)
+490-570
-460 460 o50
,oUU-3,100
i -3,300+ 180+320+840+480+obO
1 Estimated.
area. The depth to the water table is somewhat greater in the vicinity of Belgrade than elsewhere; even at its highest position during the year, it may be as much as 40 feet below the land surface. The difference between the highest and lowest positions of the water table ranges from about 10 feet or less along the margins of the area to more than 40 feet in the vicinity of Bel grade. (See pi. 7.) Water-level fluctuations in selected wells are illustrated on plate 9. Near the margins of the Belgrade sub- area most of the wells are 20 to 60 feet deep, whereas in the vi cinity of Belgrade wells are 60 to 200 feet deep.
In this subarea some of the ground water occurs under water- table conditions and the remainder under artesian conditions. It is thought, however, that confinement of water is only local in extent. Water-level data suggest the presence, in part of the area, of a relatively impermeable layer that retards infiltrating re charge and creates, thereby, a temporarily perched zone of satu ration. Test drilling, together with additional information on water-level fluctuations, is needed to determine the exact nature and extent of the indicated condition.
In drilling test hole Dl-4-25aa2, artesian water was encoun tered in the Tertiary strata at a depth of 149 to 223 feet. The water was under about 13 feet of head at the land surface. Avail-
HYDROLOGIC UNITS WITHIN THE GALLATIN VALLEY 145
able evidence, however, indicates that the Tertiary strata would not yield sufficient water for irrigation.
Consumptive use of part or all of the 100,000 acre-feet per year of ground water estimated to be theoretically available for use in the Belgrade subarea would cause a lowering of the water table and a corresponding decrease in the volume of natural ground-water discharge from the subarea. If it is assumed that 100,000 acre-feet of the ground water added to storage within the subarea is discharged annually along the northern boundary of the subarea, consumptive use of 25,000 acre-feet of ground water within the subarea theoretically would cause a 9-foot low ering of the water level in a well 2 miles south of the northern boundary and an 18-foot lowering in a well 3.5 miles south of the northern boundary. (See fig. 35.) Correspondingly larger declines of the water level would occur if annual consumptive use of ground water were greater. If net withdrawals became great enough, the point at which the Gallatin River becomes in fluent would migrate southward, and the East Gallatin River, in stead of gaining in flow, would become a losing stream. Dis charge of ground water by evapotranspiration and by springs
EXPLANATION
Present position of woter table
Position of woter toble if onnuol consumptive use of ground woter equols one-fourth onnuol rechorge
Position of woter toble if onnuol consumptive use of ground woter equols one-holf onnuol rechorge
DISTANCE FROM NORTHERN BOUNDARY OF BELGRADE SUBAREA, IN MILES
FIGUBK 35. Diagrammatic section of the northern part of the Belgrade subarea showing changes in position of the water table that would result from increased consumptive use of ground water.
146 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
and effluent streams in the Central Park subarea also would be reduced if withdrawals of ground water in the Belgrade subarea resulted in a reduction of underflow into the Central Park subarea.
A succession of dry years would lessen recharge and have simi lar effects on the position of the water table and the amount of ground-water discharge from the subarea, However, as a result of reduction in recharge alone, the summertime position of the water table probably would not drop lower than the wintertime low reached in the early months of 1952 and 1953.
CENTRAL PARK STJBAREA
The Central Park subarea is that part of the valley floor ex tending northward from the Belgrade subarea. It has an area of about 40 square miles. It is characterized by a high water table, and much of it is swampy throughout the year.
Compared with the alluvium of the Belgrade subarea, that of the Central Park subarea is finer grained and better sorted. Test drilling indicates that the alluvium north of the postulated east trending Central Park fault, near the south margin of the subarea, is much thinner than that south of the fault. Test hole Al-4-19cb, about a fourth of a mile south of the fault, was drilled to a depth of 301 feet without completely penetrating the alluvium, and test hole Al-4-15da2, almost on the fault, entered Tertiary strata at a depth of 215 feet. In contrast, test hole Al-4-5da, about 2 miles north of the fault, penetrated only 31 feet of alluvium before entering material thought to be of Tertiary age.
The coefficient of transmissibility of the alluvium was deter mined at five sites. At test hole Al-4-22dc the coefficient was 480,000 gpd per foot, and at test hole Al-4-19cb it was 480,000 gpd per foot for the material between depths of 5 and 94 feet and 180,000 gpd per foot for the material between depths of 117 and 180 feet; these coefficients assume that the 2 zones are effec tively separated at least so far as the duration of the tests is concerned. The coefficient of permeability of the 2 water-bearing zones in test hole Al-4-19cb was 5,500 and 2,900 gpd per square foot, respectively. Three values for the coefficient of transmis sibility of the alluvium north of the Central Park fault were 38,000, 100,000, and 110,000 gpd per foot, and computed coef ficients of permeability were 1,500, 4,000, and 4,000 gpd per square foot, respectively. The thinning of the alluvium north ward from the Central Park fault is reflected by the lower trans missibility. The coefficient of transmissibility of Tertiary strata penetrated by test hole Al-4-15da2 was 3,700 gpd per foot.
HYDROLOGIC UNITS WITHIN THE GALLATIN VALLEY 147The Central Park subarea contains the largest tract of poorly
drained land in the Gallatin Valley. Throughout nearly all the subarea the water table is less than 5 feet below the land surface, and most wells are less than 25 feet deep. Typical hydrographs of the water-level fluctuations in wells are shown in figure 36.
r i< WELLAI-4-5da
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JAN. FEB. MAR. APR. MAY JUNE JULY AUG. SEPT. OCT. NOV. DEC. JAN. FES. MAR. 1953 1954
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JAN. FEB. MAR. APR. MAY JUNE JULY AUG. SEPT. OCT. NOV. DEC. JAN. FEB. MAR. 1953 1954
FIGURE 36. Hydrographs of the water level in wells Al-4-5da and Al-4-22dcl.
The ground-water reservoir in the part of the subarea between the Gallatin and East Gallatin Rivers is recharged principally by underflow from the Belgrade plain. The bottom land west of the Gallatin River is recharged mainly by underflow from that part of the Belgrade subarea west of the Gallatin River, the Camp Creek Hills, and the Manhattan terrace; the bottom land east of the East Gallatin River is recharged by underflow from the Dry Creek subarea and the Spring Hill fan.
In the Central Park subarea, more ground water is discharged at the surface than in any other part of the Gallatin Valley. Be cause the alluvium north of the Central Park fault cannot transmit all the water entering- the subarea by underflow (estimated to be 300,000 acre-feet per year), some of the ground water is
148 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
forced to the surface, where it is discharged by spring flow and effluent seepage into streams and by evapotranspiration. It is estimated that 70,000 acre-feet of water is discharged annually to the principal spring-fed streams that rise in this subarea. (See fig. 37; table 7, p. 69.) Because Thompson Creek is least affected by extraneous influences, the hydrograph of its flow il lustrates best the seasonal streamflow pattern of the spring-fed
o: 1000 <
FIGURE 37. Hydrographs of the flow of the principal streams rising in the Central Park subarea.
HYDROLOGIC UNITS WITHIN THE GALLATIN VALLEY 149
streams. Except for the comparatively minute amount of ground water that leaves by underflow through the outlet of the Gallatin Valley at Logan, all the ground water that is transmitted by the jalluvium in this subarea is discharged eventually by seepage into the Gallatin or East Gallatin Rivers.
The graph showing cumulative departure from the volume of saturated material as of the end of June 1952 (fig. 33) indicates that net recharge characterized the period March through June and that net discharge characterized the other months of the year. The magnitude of the changes in volume of saturated ma terial is far less than in the Belgrade subarea.
Although increased consumptive use of ground water in up- gradient parts of the Gallatin Valley would result in some reduc tion of ground-water underflow into the Central Park subarea, it is unlikely that the water table would be lowered significantly in more than the extreme southern part of the subarea.
Even though underflow into the subarea were considerably less, the alluvium north of the Central Park fault probably still would be incapable of transmitting all of it. Therefore, lowering of the water table north of the fault can be effected only by artificially increasing discharge. Pumping of ground water for the express purpose of lowering the water table is not considered feasible because so many wells would be needed. Surface drains probably would be much more effective and would cost less than wells. Two types of drainage measures may be practicable one, the construction of interception drains, as recommended by the U.S. Soil Conservation Service (Long, 1950, p. 11), and the other, the deepening and straightening of existing streams and construction of new drains parallel to the present streams. Some drains of the interception type have been constructed. Under the existing pattern of water use, deepening of present streambeds would lower the water table about as much as the amount of deepening.
No foreseeable increase in consumptive use of ground water in the Central Park subarea would lower the water table appreciably, nor would a succession of dry years.
MANHATTAN SUBAREA
The Manhattan terrace is separated from the alluvial plain of the Gallatin River by a low north- and east-facing escarpment along its outer edge and from the higher Camp Creek Hills by a colluvial slope along- its southwestern border. It comprises about 8 square miles.
150 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Only a few feet of gravel overlies Precambrian bedrock in the face of the escarpment at the northwest corner of the subarea, but the gravel apparently thickens eastward to a point north of Manhattan. Test hole A2-3-33da penetrated 55 feet of alluvium before entering fanglomerate of Tertiary (?) age, and well Al- 3-4da, about two-thirds of a mile northwest of Manhattan, was drilled through 38 feet of alluvium before entering material of Tertiary (?) age. Southeast of Manhattan, near the terrace es carpment, a 30-foot thickness of alluvium was penetrated in the drilling of well Al-3-14dd. This range in thickness indicates probable channeling of the Tertiary strata before the alluvium was deposited. The average thickness of the alluvium is esti mated to be between 30 and 45 feet. The coefficient of transmis- sibility of the alluvium was determined at 4 sites and ranged from 120,000 to 140,000 gpd per foot. As the saturated alluvium is known to be thin, these values indicate that the alluvium is highly permeable.
The fanglomerate penetrated by test hole A2-3-33da crops out in draws along the north-facing part of the terrace escarpment. Fractures in this material yield water to spring A2-3-32ac and supply water to nearby wells.
Artesian water was found between the depths of 215 and 300 feet in test hole A2-3-33da. The water, which rose to within 12 feet of the land surface, was derived from Tertiary strata that immediately overlie rocks of the Belt series. Unfortunately the water contained too much hydrogen sulfide and sodium salts to be fit even for irrigation.
The graph showing cumulative departure from the volume of saturated material as of the end of June 1952 in the Manhattan subarea (fig. 33) indicates that in both 1952 and 1953 net re charge to the alluvium began in May and continued through July and that discharge exceeded recharge the remainder of the year.
The ground-water reservoir in the subarea is recharged almost wholly by seepage from irrigation canals that skirt the inner edge of the terrace, and from applied irrigation water. The wa ter used for irrigation, though diverted from surface streams, is largely return flow from irrigation in the Belgrade subarea and in the Camp Creek Hills, and, therefore, is a dependable source of supply. Discharge is mainly by underflow to the bottom land adjacent to the terrace escarpment, where it is picked up by the Gallatin River and tributary drains. Water is discharged also by evapotranspiration, mostly from a small waterlogged area south of Manhattan, and through a series of springs in the draws
HYDROLOGIC UNITS WITHIN THE GALLATIN VALLEY 151
along the north-facing part of the terrace escarpment. Dis charge of ground water from the Manhattan subarea, exclusive of that discharged by evapotranspiration, is estimated to have been 14,000 acre-feet between the spring of 1952 and the spring of 1953; the average annual discharge probably is about 10,000 acre-feet. The average annual recharge exceeds this average an nual discharge by the amount discharged by evapotranspiration.
Fluctuations in the discharge of springs A2-3-32ac, -32ad, and -33ba reflect the changes in volume of saturated material, and, thus, the dependence of the flow on recharge from irrigation water. Discharge from springs A2-3-32ad and -32ac, the 2 larg est springs, fluctuated from 22.6 and 14.5 cfs, respectively, in August 1952, to 8.3 and 3.9 cfs, respectively, in April 1953.
During the summer the water table in much of the area is within 10 to 20 feet of the land surface. Wells range from 10 to 105 feet in depth. The water-level fluctuations in well A2-3- 33da (fig. 38) are somewhat greater than in most other wells in this subarea because of the proximity of the well to the terrace escarpment.
Waterlogging in the area south of Manhattan is caused by excessive recharge. Lining the Moreland Canal in the reach adja cent to the area would reduce recharge, and a ditch in the water logged area would help drain ground water. Additional investi gation would be necessary to determine the feasibility and relative effectiveness of these measures, singly or in combination.
The alluvium underlying the Manhattan subarea is sufficiently permeable to yield water freely, but in most of the subarea is too thin to supply sufficient water for irrigation. At the peak of the irrigation season, when water shortages are sometimes acute in other parts of the valley, return flow from irrigation in the Bel grade subarea supplies much of the irrigation water used in the Manhattan subarea. This supply could be supplemented by pump ing ground water into the existing canals where they traverse the Belgrade subarea.
UPPER EAST GALJLATIN SUBAREA
The Upper East Gallatin subarea consists of the flood plain of the East Gallatin River from the river's point of entry into the valley northwestward for about 11 miles. The subarea is about a quarter of a mile wide at its upper end and broadens to about 21/2 miles at its lower end where it adjoins the Belgrade subarea. It comprises abut 10 square miles.
Well D2-6-10dc, near the upper end of the subarea, is reported to have been drilled through 29 feet of alluvium before entering
DEPTH TO WATER BELOW LAND SURFACE. IN FEET
j^roOCD<J)-^roo oo o> -& ro
XNOH 'NIXVYIVO 'saoanosaa aaxvM-QNnoao 'Aooioao
HYDROLOGIC UNITS WITHIN THE GALLATIN VALLEY 153
red clay of probable Tertiary age. Test hole Dl-5-9cd, near the lower end, was drilled to a depth of 162 feet in the alluvium without reaching the underlying- Tertiary strata. In this test hole the alluvium is poorly sorted and contains more silt and clay than the alluvium of the Gallatin River. Because Bear and Bridger Creeks, tributaries to the East Gallatin River in its upper reach, drain areas partly underlain by relatively fine grained easily eroded formations of Cretaceous age, they probably trans ported to the East Gallatin River much of the fine-grained ma terial in the alluvium.
Although several aquifer tests were made in this subarea, the coefficient of transmissibility could not be determined from the data obtained.
The alluvium is recharged by infiltrating precipitation, by un derflow from adjacent areas, and, in the upper reach of the sub- area, by seepage from the East Gallatin River and its tributaries. Ground water is discharged by evapotranspiration, seepage into the East Gallatin River in the lower reach of the subarea, and underflow to the Belgrade subarea.
The water table is within 10 feet of the land surface during most of the year. Most wells are less than 30 feet deep, and the range of water-level fluctuations is small.
Although existing data indicate that the alluvium will not yield large quantities of water to wells, additional data should be gathered in order to evaluate accurately the ground-water re sources of this subarea.
BOZEMAN FAN
An alluvial fan composed of material derived from the Gallatin Range slopes northward from the mouth of Hyalite Canyon where Middle (Hyalite) Creek enters the Gallatin Valley (sec. 14, T. 3 S., R. 5 E). The fan is bounded on the southwest by Goochs Ridge and on the east by Sourdough (Bozeman) Creek; along its northwest margin it merges with the floor of the valley and on its northeast margin with the flood plain of the East Gallatin River. The area of the fan is about 56 square miles.
The alluvium composing the fan is the principal aquifer in this area. The logs of test holes Dl-5-34cc2, D2-4-14ac, and -22cd indicate that the alluvial-fan deposits thin from nearly 200 feet near the head of the fan to a hundred feet or less near the toe of the fan where it grades into, or interfingers with, the allu vium of the Gallatin and East Gallatin Rivers. The coefficient of transmissibility of the alluvial-fan deposits, determined at 6 sites, ranged from 26,000 to 65,000 gpd per foot and averaged
508919 O-60 11
154 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
about 48,000 gpd per foot. The range in values reflects variations in permeability and thickness of the saturated material.
Even where they are drilled into the more permeable, thicker sections of water-bearing alluvial-fan deposits, wells yielding more than 500 gpm should not be expected. Alluvial deposits filling the channels of former distributaries that built the fan are the most likely sources of ground-water supplies. These deposits cross the fan from head to toe and can be located by careful test drilling. Most of the wells on the Bozeman fan are less than 35 feet deep (many are dug wells) and few are more than 75 feet deep. However, when wells D2-6-19cbl and -19cb2 were drilled about 1 mile south of Bozeman, sufficient water for domestic use reportedly was not obtained until the wells reached depths of 80 and 155 feet, respectively. It is probable that the upper part of the alluvial-fan deposits is not water bearing in the vicinity of these wells because of the draining effect of nearby Sourdough (Bozeman) Creek.
Test hole D2-5-22ccd was drilled through 165 feet of alluvial- fan deposits and 835 feet into the underlying Tertiary strata, and test hole Dl-5-34cc2 was drilled through 127 feet of alluvial-fan deposits and 123 feet into Tertiary strata. The Tertiary strata penetrated by both test holes were relatively impermeable. Well D2-6-7ac, drilled in 1936 for the city of Bozeman to augment its water supply, penetrated clay, sand, and gravel to a depth of 304 feet. Although this material, probably mostly of Tertiary age, initially yielded 450 to 500 gpm, the sustained yield, which was much less, was insufficient and the well was abandoned. All available evidence, therefore, indicates that the Tertiary strata underlying the Bozeman fan would not yield sufficient water for irrigation.
Streamflow, irrigation water, and precipitation are the prin cipal sources of recharge on the Bozeman fan. Sourdough (Boze man) and Middle (Hyalite) Creeks, near where they enter the valley, are sources of recharge, particularly during the months of high streamflow and low ground-water level in the spring. Seep age from the numerous irrigation flitches crossing the surface of the fan, and infiltrating irrigation water applied to the fields, are generally the main sources of recharge during most of the summer. In some years when irrigation water is in short supply, however, the recharge from these sources is correspondingly less.
In this part of the Gallatin Valley precipitation is somewhat greater than elsewhere. Generally much of the winter precipita tion is stored as snow; snowmelt and relatively high rainfall in
HYDROLOGIC UNITS WITHIN THE GALLATIN VALLEY 155
the spring produce appreciable recharge. This was especially true in the 1952 water year. In October 1951 heavy snowfall mantled the Bozeman fan before the soil was frozen. During the succeed ing months the average temperature was lower than usual and the abnormally heavy precipitation, nearly twice the average, accumulated as snow on the unfrozen ground. Higher tempera tures in March and April caused the snow to melt, but there was little runoff because most of the water infiltrated to the water table. The resultant rise in the water level is shown in figure 33 by the graph for the Bozeman fan. By May, before any signifi cant recharge from streamflow and irrigation water occurred, the increase in saturated material already was 65 percent of the total for the year. During the same period, the volume of satu rated material beneath the floor of the Gallatin Valley increased only 32 percent of the total increase for the year.
Precipitation was a much less important source of recharge in the 1953 water year. During the period October 1952 through February 1953, precipitation was only 72 percent of average. There was no snow cover on the Bozeman fan and the soil was frozen. In consequence, recharge by snowmelt was insignificant and net recharge did not begin until May, when streamflow and irrigation water became effective recharge factors. Recharge fol lowed a somewhat similar pattern throughout the remainder of the valley. The great difference in the amount of recharge from precipitation and snowmelt in the 2 water years indicates that this type of recharge cannot be depended upon to occur in any particular year.
Discharge of ground water from the Bozeman fan is by effluent seepage to streams, by underflow to adjacent areas down valley, and by evapotranspiration. Middle (Hyalite) and Sourdough (Bozeman) Creeks, the only streams that completely cross the Bozeman fan, are effluent in the lov/er parts of their courses across the fan. Several small streams rise about 3 miles north of the head of the fan and drain northward into either Middle (Hyalite) Creek or the East Gallatin River. During the irriga tion season most of the water in the streams draining the Boze man fan is diverted for irrigation. Evapotranspiration is great est along the streams and drains. Underflow from the Bozeman fan enters the alluvium underlying the Belgrade plain and the flood plain of the East Gallatin River.
At the head of the fan, where the land is steeply sloping, and at the toe of the fan, where the surface is dissected and drainage is adequate, the water table is more than 30 feet below the land
156 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
surface. Elsewhere on the fan, the water table is less than 10 feet below the land surface and in many places is less than 5 feet. Near the head of the fan, the water level in wells fluctu ates as much as 25 feet, but throughout the remainder of the fan the fluctuations are less than 10 feet. (See fig. 39.)
WellD -5-22ccd
J
1
^\
\/
A
l\
.
1 "
3*Wv
Ji
\Hw\r*~*r v~/ ^ ^. ^^-,r
FIGURE 39. Hydrographs of the water level in wells Dl-5-34cc2, D2-5-14ac, -16aal, and -22ccd.
At best, the aquifer underlying the Bozeman fan would yield only sufficient water for irrigating gardens or for supplemental irrigation of larger fields. If the ground-water resources of the Bozeman fan were to be developed to the extent that the flow of streams draining the fan was reduced significantly, less water would be available for irrigation by diversion from these streams. Such an eventuality should be given careful thought if large withdrawals of ground water on the Bozeman fan are planned. Underflow from the Bozeman fan to the Belgrade sub- area also would be reduced if consumptive use were increased considerably.
HYDROLOGIC UNITS WITHIN THE GALLATIN VALLEY 157
CAMP CREEK HILLS
The area of the Camp Creek Hills is about 160 square miles. Tertiary strata are exposed throughout the area except at the south end, where Precambrian gneissic rocks crop out; near Logan, where Paleozoic and Precambrian rocks crop out; and in the places where the Tertiary strata are overlain by a thin mantle of terrace gravel, alluvium, colluvium, or loess. The thickness of the Tertiary strata, where penetrated by test holes Dl-3-36bc and D2^-4-9bc, is 836 and 515 feet, respectively. The alluvium, which overlies the Tertiary strata along the east-central margins of the Camp Creek Hills, probably is no more than about 20 feet thick. Most wells on the higher surfaces in the Camp Creek Hills are between 200 and 600 feet deep, whereas those on the lower surfaces and along the draws are correspondingly shallow.
Although the Tertiary strata as a whole are relatively imper meable, they form the principal aquifer in the area, and wells drilled into the more pervious layers yield sufficient water for stock and domestic use. The coefficient of transmissibility as determined by tests at test holes Dl-3-36bc and D2-4-9bc, was 6,000 and 1,200 gpd per foot, respectively. Another aquifer test, at well Al-3-33dd, gave a coefficient of transmissibility of 26,000 gpd per foot, but it is probable that the water-yielding beds con sisted in part of alluvium.
In the Camp Creek Hills, ground water occurs under both wa ter-table and artesian conditions. Because insufficient water-level data were available, maps showing the contour of the water table or piezometric surfaces in this area were not prepared. It is probable, however, that ground water in the Camp Creek Hills moves eastward and northeastward toward the valley floor that is, in the direction of the dip of the Tertiary strata.
As precipitation on the Camp Creek Hills generally is less than that required to satisfy the evapotranspiration requirements, only a small amount infiltrates to the zone of saturation. In the lower, irrigated part of the area, seepage from irrigation canals and irrigated fields is a significant source of recharge, but, be cause the many draws and shallow canyons effect good drainage, the water table has not risen appreciably. If much additional water were used for irrigation in this part of the Camp Creek Hills, however, the low-lying land along the east margin of the irrigated area might become waterlogged.
Available evidence indicates that the Tertiary strata in the Camp Creek Hills are incapable of yielding more than enough water for domestic and stock supply.
158 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
VALLEY FRINGE
Bordering the valley floor on the northeast and east are the Dry Creek, Spring Hill, and South Bridger subareas, and border ing the Bozeman fan on the east is the Fort Ellis subarea and on the southwest the South Gallatin subarea. These five sub- areas are referred to collectively as the valley fringe.
DRY CREEK SUBAREA
Most of the Dry Creek subarea, an area of about 89 square miles, is underlain by Tertiary strata. Along the stream courses the Tertiary strata are mantled by alluvium; along the east margin of the area they are mantled by alluvial fans from the Bridger Range. The entire area has been dissected by Dry Creek, its tributaries, and other tributaries of the East Gallatin River.
Insofar as can be determined from a reconnaissance of this subarea, the hydrologic properties of the Tertiary strata seem to be similar to those of Tertiary strata in other parts of the valley. The stream alluvium and alluvial fans seem to consist of coarse and moderately permeable material, but because the latter are dissected by draws and small canyons, they probably are well drained and contain little ground water.
Although a few wells tap the Tertiary strata, most wells in the Dry Creek subarea tap either alluvium along the stream courses or alluvial-fan deposits. Springs along the mountain front are a source of water on several ranches. Ground water moves toward Dry Creek except at the south end of the subarea, where the direction of movement is southwestward toward the valley floor.
Streamflow from the Bridger Range and precipitation along the east margin of the subarea are the chief sources of recharge. Ground water discharges principally as streamflow, but along several of the streams, such as Bear and Reese Creeks, extensive bottom-land areas are waterlogged.
Because the Tertiary strata are relatively impermeable and the alluvial fans contain little water, it is probable that large yields of ground water cannot be obtained in the Dry Creek subarea.
SPRING HILL, SUBAREA
The Spring Hill subarea is an alluvial fan having an area of about 11 square miles. This fan is of later origin than the other fans in the valley fringe, and its surface is smooth and undis-
HYDROLOGIC UNITS WITHIN THE GALLATIN VALLEY 159
sected. The lower end of the fan merges with the flood plain of the East Gallatin River. As no test holes were drilled into the alluvial fan, little is known of its thickness and subsurface char acteristics. The coefficient of transmissibility, as determined at wells Al-5-21bc4 and -26cd, was 7,000 and 30,000 gpd per foot, respectively. These values, however, may not be representative of the full thickness of alluvial-fan deposits because the wells used in making the tests were very shallow.
Runoff from the Bridger Range and precipitation near the mountain front are the principal sources of recharge. The ground water moves toward the valley floor, and that not lost by evapo- transpiration either discharges into Smith Creek or percolates into the alluvium of the East Gallatin River.
Additional information is needed before the ground-water sup ply in the Spring Hill subarea can be evaluated accurately.
SOUTH BRIDGER SUBAREA
The South Bridger subarea consists of remnants of a rather high dissected surface that fringes the Bridger Range between the Spring Hill fan and the valley of the East Gallatin River. North of Bridger Creek alluvial-fan deposits are the surficial material, whereas, south of Bridger Creek, Tertiary strata are at the sur face. Both parts of the subarea are well drained and it is likely that supplies of water sufficient for irrigation cannot be de veloped. The subarea comprises about 33 square miles.
FORT ELLIS SUBAREA
In general, the geologic and hydrologic characteristics of the Fort Ellis subarea are similar to those of the Dry Creek sub- area. It is probable, on the basis of available evidence, that the ground-water reservoir would not yield more than enough water for stock and domestic supply. The Fort Ellis subarea is about 18 square miles in extent.
SOUTH GALLATIN SUBAREA
The South Gallatin subarea comprises about 29 square miles and consists of remnants of high-lying alluvial fans that rest on Tertiary strata. A prominent fingerlike ridge, Goochs Ridge, extends northward into the valley. The alluvial-fan deposits are so well drained that they contain little or no water, and the Tertiary strata, as in other parts of the valley, yield water suf ficient only for stock and domestic use.
160 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
CHEMICAL QUALITY OF THE WATER
By R. A. KRIEGER
The chemical quality of the water in the Gallatin Valley was determined from the analyses of 58 samples of ground water and 45 of surface water. The ground-water samples were collected between July 1951 and September 1953 from wells, test holes, and springs. Surface-water samples were collected from May 1949 to September 1952 from the Gallatin River and most of its important tributaries.
The locations of the sampling points for both ground and sur face waters are shown on plates 10 and 11. In addition, the chemical characteristics of the water are shown by means of patterns as devised by Stiff (1951). The chemical analyses the ground- and surface-water samples are given in tables 27 and 28, respectively.
GEOLOGIC SOURCE AND SIGNIFICANCE OF THE IONS
The water samples were analyzed chemically to determine the concentration of the mineral constituents that affect the usability of the water. Characteristics of the water, such as pH and specific conductance, also were determined. The importance of the principal ions and some of the characteristics is discussed below.
Calcium is dissolved principally from limestone, dolomite, gypsum, and gypsiferous shales; magnesium is dissolved mainly from dolomite. Water that has leached these rocks may contain as much as several hundred parts per million of calcium and magnesium, whereas water that has leached granitic or other highly siliceous rocks may contain less than 10 ppm of calcium and magnesium. Calcium and magnesium cause hardness in wa ter and scale in hot-water pipes and boilers. However, if present in suitable proportion, they are desirable in irrigation water be cause they counteract the harmful effects of sodium on the soil.
Sodium and potassium are dissolved from nearly all rocks. If ground water is connate or from rocks of marine origin, it may contain several thousand parts per million of sodium and can be classed as a brine. Sodium often is the predominant cation of surface waters in arid regions. Although sodium in water gen erally is of little importance to domestic users, it is of major im portance to irrigationists because, if sodium constitutes a major part of the cations in an irrigation water, the soil may be dam aged and become impervious to water. The relation between
CHEMICAL QUALITY OF THE WATER 161
sodium and other cations is expressed as the percent sodium, which is computed by dividing the concentration of sodium in equivalents per million by the sum of the equivalents of the four principal cations sodium, potassium, calcium, and magnesium and multiplying the quotient by 100. Because potassium usually is present in low concentrations in natural water, it is of little significance.
Carbonate and bicarbonate are dissolved from limestone, dolo mite, and other carbonate rocks. Carbon dioxide in water aids in the solution of calcium and magnesium carbonates from rocks and soils. Carbonate, if present at all, is generally low in con centration. Water from hard, insoluble rocks, such as granite, may contain only a small amount of bicarbonate, but water from limestone may contain several hundred parts per million. Car bonate and bicarbonate are important in irrigation water be cause of the possible effect of residual sodium carbonate on the soil.
Sulfate is dissolved mainly from gypsum and gypsiferous deposits. Also, it is derived from deposits of sodium sulfate and from the oxidation of sulfides. In combination with calcium, sulfate forms a hard scale in hot-water pipes and boilers.
Chloride is dissolved from nearly all rocks and soils; however, except when present in large amounts, it generally does not affect the use of the water. A high chloride concentration in water indicates the presence of brines, marine-deposited miner als, or pollution of the water from animal or industrial wastes. Drainage from irrigated land in arid regions often contains a high concentration of chloride.
Although fluoride is present in many rocks, the concentration in natural water usually is much less than that of chloride. Fluoride in drinking water may affect the teeth of children. There is evidence that children's teeth decay less when the fluoride concentration in the water supply is about 1.0 ppm; how ever, mottling of the tooth enamel may result if, during the period of formation of the permanent teeth, the drinking water has a fluoride concentration exceeding about 1.5 ppm (Am. Wa ter Works Assoc., 1950, p. 381).
Nitrate in natural water usually is not dissolved from rock ma terials as are most of the other constituents. Rather, nitrate is the end product of the aerobic stabilization of nitrogenous or ganic matter, and high concentrations of nitrate may indicate contamination of the water from sewage or from plant and ani mal wastes. If fed to babies, water containing more than about
TABL
E 27.
Che
mic
al a
naly
ses
of g
roun
d w
ater
in t
he G
alla
tin V
alle
y[G
eolo
gic
sou
rce:
P,
Pre
cam
bri
an r
ock
s; T
, st
rata
of
Ter
tiar
y a
ge;
an
d Q
, de
posi
ts o
f Q
uat
ernar
y a
ge.
Res
ult
s in
par
ts p
er m
illi
on]
05
K)
Location
Geologic sourc
M ^3 Depth
at samp time
(fee
t)
g 0 "o 3 v 0
^ !? Temperature
(2 02
'cu fe 2 h
- 1
I
S 3
be Magnesium
(IVSodium
(Na
)Potassiu
m (K
)
^ O O Bicarbonate
(t
cc Carbonate
(CC6 to 3 02
o to 'C 3
o
Fluoride
(F)
Nitrate
(NOs)
g o o
Dis
solv
edso
lids
Calculated
Residue on
evaporation at
180°C
6 o Hardness as C
6 o
Noncarbonate hardne
ss as CPercen
t sodiu
n
u o
3<
N--
Specific
conduc (mio
romhos a
ft
Val
ley
floor
Al-4-5da...
.
5dd
. . .
15da2..
19cb...
25dc...
Al-5-2
8db2
.
A2-3
-33d
a...
Dl-4
-lcb
. .
.Idc. .
.6ddcl. .
13bb
. .
25aa
2 .
Dl-5-9cd.
. .
D2-4
-lld
c...
14dac2
D3-4
-3ab
l. .
T........
Q........
T..... .
. .
Q.. ..
....
Q........
Q T. .......
T.. ..
....
TandP..
Q........
Q Q...
....
.
Q........
{9....
....
Q........
207 ....
18.0
..
315. .
. .87.
...
123.
...
301 ..
..
102. .
. .
400. .
. .
170.
..
.55...
.190
250. .
..45
0...
. 11
0. .
..10
7. .
..22.4..
65....
158. .
. .
f 32
. ..
. U56. .
..
156.
...
68.
...
145.
. . .
Spri
ng .
11.
...
Dec. 29,
195
2 (S
ept.
21, 1
951
{Sep
t.
9, 195
2 [Aug.
28, 19
53
Apr.
18, 19
53
Aug. 31, 19
53
July 23, 19
53
Aug. 25, 19
53
Nov.
30, 1
951
Nov.
26, 1
951
Aug.
31, 1
953
Aug.
28,
195
1 Se
pt.
5, 1
951
Sept
. 8, 1
951
Sept.
20, 1951
Sept
. 9, 1
952
Sept.
10, 19
52
Sept
. 22, 19
51
Sept.
23,
1951
Jan.
28, 19
53
Sept
. 9, 1
953
Sept.
15, 19
53
Sept
. 16
, 19
53
Sept.
8, 1
953
Sept.
4, 1
953
Sept
. 22, 19
51
Sept
. 9, 1
952
[Aug.
28, 19
53
Sept
. 23, 19
52
48
56
56
61
59"46
46
52
49
46
57
55
56
53
51
51
51
57
49
47' '
52
51
49
140 50
25
29
23
30
30
21
19
17
24 12
38
31
11
14
22
25
21
22
24
19
24 5.8
22
23
60
18
17 16
39
0.38
.29
.58
2.1 .91
2.6 .18
'.02
.03
.23
.08
.84
1.0 '.38
.45
.02
.06
.03
4.2
64
82
61
69
35
62
65
65
42 52
60
22 5.2
14
56
53
47
57
35
77
71
65
57
58 3.5
46 48
32
17
26
19
21 6.0
14
19
18
13 14
19
13 8.4
3.6
12
12
20
16 6.4
20
18
19
13
14 .4
12 13 8.0
13
13 9.4
11 6.7
5.2
5.3
5.8
5.7
5.6
5.2
20
187
400
421 5.
9 5.6
15 5.6
3.6
19
18
16 6.5
7.4
135 4.
9 4.
74.9
9.3
4.6
6.1
5.0
5.9
3.6
2.8
3.2
2.3
2.9
1.6
8.1
9.6
13 8.0
2.8
3.3
3.7
3.1
2.4
3.7
4.2
4.2
3.3
3.1
3.3
3.0
2.6
7.8
277
332
264
304
151
219
243
239
178
227
264
340
416
456
212
204
242
241
148
331
311
291
235
246
107
170
175
135
0 0 0 0 0 0 0 0 0 0 0 0 39
33 0 0 0 0 0 0 0 0 0 0 8 0 0 0
31
64
34
39 1.0
36
40
39
25 13
48
33
13
16
24
24
28
21 .0
26
23
24
18
17
115 33 37
26
3.0
6.0
2.0
2.5
2.0
6.5
8.0
9.0
2.5
3.5
8.5
178
330
336 2.
0 2.
5 4.5
2.0
1.0
5.5
6.0
3.5
1.0
2.5
51 2.0
2.5
2.5
0.5 .2
.2
.3
.1
.1
.1
.1
.3 .1
.5
4.0
16
18 .1
.1
.2
.1
.0
.1
.1
.1
.1
.0
10 .2 .2
.0
1.5
1.7
3.8 .3
.5
2.9
3.6
3.1
4.4
5.4
3.5
4.4
8.0
10 2.2
3.9
3.4
2.9 .7
16 8.0
11 .8
1.2 .2
1.6
1.6 .4
0.03
.03
.03
.03
.13
.03
.03
.02
.08
.01
.15
5.7
12
12 .0
1 .0
1 .03
.01
.01
.03
.01
.01
.00
.06
.21
.01
.01
.06
330
286
219
336
655
1,06
0 1,
110
350
248
313
398
288
162
278
287
210
238
234
264
262
154
323
308
245
464
212
216
198
229
312
229
260
112
212
239
235
159
17?
189
229
159 48
49
187
182
200
209
114
273
253
241
196
202 10
165
17?
172
113
2 40
13
11 0 32
40
39
13 3 13 0 0 0 13
15 2 11 0 2 0 2 3 0 0 26 28 2
11 8 8 8 11 5 5 5 7 7 6 15
70
94
94 6 6 14 5 6 13
13
12 7 7 95 6 5 6 14
503
620
464
523
242
415
460
467
332
354
380
503
1,100
1,820
1,900
378
371
434
414
227
570
532
505
389
407
679
337
345
349
272
7.9
7.5
7.7
7.5
8.1
7.9
7.5
7.3
8.2
7'.7
7.9
7.9
8.5
8.5
7.8
7.5
7.8
7.6
8.1
7.7
7.3
7.6
7.5
7.6
8.7
7.6
8^2
CHEMICAL QUALITY OF THE WATER 163CO * O i-H iC O O CD -CD
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TABL
E 28.
Che
mic
al a
naly
ses
of
surf
ace
wat
er in
the
Gal
lati
n V
alle
y[R
esul
ts i
n par
ts p
er m
illi
on]
Oi
"a
c o 1 1 2 3 4 5 6 7 8 9 10
11 12
13
14
15
16
Loc
atio
n
Gal
lati
n R
iver
at
Yel
low
ston
e P
ark
bou
ndar
y D
o. ...............................
Do.
...............................
Gal
lati
n R
iver
, R
ed C
liff
Cam
p ............
Do.
...............................
Gal
lati
n R
iver
bel
ow S
pani
sh C
reek
........
Do.
.........
......................
Gal
lati
n R
iver
in
sec.
8,
T.
4 S.
, R
. 4
E.
. . .
. G
oose
Cre
ek i
n N
EJ^
NW
J^ s
ec.
16,
T.
3 S.
,
R.
4 E
.. ...
....
.......................
Low
line
Can
al 2
% m
iles
wes
t of
Bue
ll i
n S
WJ^
SW
^ se
c. 3
3, T
. 1
N.,
R.
3 E
. .
. . .
.G
alla
tin
Riv
er a
t S
heds
Bri
dge
in S
E)^
S
EJ^
sec
. 10
, T
. 2
S.,
R.
4 E
. . ..........
Do ..
....
..........................
Gal
lati
n R
iver
at
Cam
eron
Bri
dge
in N
WJ^
N
W J
i se
c. 2
2, T
. 1
S.,
R.
4 E
............
Gal
lati
n R
iver
at
Cen
tral
Par
k R
R.
Bri
dge
in S
WJ^
NE
J^ s
ec.
19,
T.
1 N
., R
. 4
E.
. . .
Do ................................
Do.
.........
......................
Do ................................
Gal
lati
n R
iver
eas
t of
Man
hat
tan i
n S
EM
N
EJi
sec
12,
T.
1 N
., R
. 3
E ...
....
....
.C
amp
Cre
ek a
t V
ince
nt S
choo
l in
SW
J^
NE
J4 s
ec.
4, T
. 2
S.,
R.
3 E
. ..
....
....
..C
amp
Cre
ek a
t B
uell
in
SE
J^S
WJ^
sec
. 35
, T
. 1
N.,
R. 3E
.....................
Roc
ky C
reek
(E
ast
Gal
lati
n R
iver
) at
Fort
E
llis
in
SW
^SE
J^ s
ec.
24,
T.
2 S.
, R
. 6
E.
Sou
rdou
gh (
Boz
eman
) C
reek
nea
r B
ozem
an
in N
WM
SE
M s
ec.
30,
T.
2 S.
, R
. 6
E .
. . .
.
<o .1
Q 328
298
182
.5
16.3
14.0
Date
of
collection
6-24
-49
8-18
-49
10-3
0-49
8-
18-4
9 6-
24-4
9 8-
20-4
9 9-
20-5
1 6-
24-4
9 10
-30-
49
5-27
-49
9-
8-52
9-20
-51
6-25
-49
8-19
-49
9-23
-51
5-27
-49
6-25
-49
8-19
-49
10-3
0-49
9-20
-51
...d
o..
.
...d
o...
9-21
-51
9-22
-51
Temperature (°F)
36 56 ei 45 59
51 64
47 60
39 51
49
51 45
O
S S co 17
19
22
15
14
15
14
13 9.1
14 17
16 14
18 15 14
15
20
16 17
21
21
10
20
c o
0.0
5
.07
.06
.06
.05
.04
.04
.05
.04
.10
.04
.04
.05
.05
.04
.05
.05
.07
.04
.04
.04
.02
.04 0?
Calcium (Ca)
27
36
38
39
21
38
34
19
31
20 49
42 23 42 41 20
27
50
37 42
46
48
53 9:7
Magnesium (Mg)
7.8
9
.8
8.6
11
7.1
11
7.1
7.1
8
.6
5.5
20 9.2
6.5
11 8
.6
6.5
7
.9
16
12 10
10
13 18 7 9
'a g. a 3
0 6 1 3 5 3.4 13
7.4
4.5 5 4
4.2 9 7 7 12
4.6
9.4
12 7.4
3 1
Potassium
(K)
7 7 2 8 9 3 1.2
.5 .7 2.6
2.3
.3 .4 .0
.8
.6 1.6
4.1
4.0
2.0
1.7
Bicarbonate (HCOa)
110
127
140
123 84
11
5 11
0 74
118 74 234
145 92
147
142 90
112
212
130
142
170
189
199
121
Carbonate
(COa) 0 0 0 8 0 5 0 0 0 0 7 0 0 0 0 0 0 0 10 6 0 0 't 0
I -S S CO 8.0
26
24
31
19
46
32
15
39
12 8
.0
35 18
35 34 18
20
30
39 34
33
39
46 8 0
Chloride
(Cl)
1.0
.0
1
.8
.0
.0
.5
1.0
.0
1.2
.0
7.0
1.5 .0
1.5 1.0
1.0
2
.0
1.0
2
.0 1.5
10 7.5
1.5 .5
Fluoride
(F)
0.1
.1
.1
.2
.1
.2
.2
.1
.2
.1 .2
.3 .1
.2 .2 .2
.1
.2
.2 .2
.3
.3
.3
.1
O S 2 0.5
.4
1
.6
.2
.5
.5
.4
1.1
1.9 .8
2.2
.8 .8
.7 .2
1.5
.6
.9
2
.6 .7
1.1
3.0
.6
1 0
a £ o
0.0
9
".05 ".64
.07
".08
.02
.06
.04
.03
.12
.08
.10
.06
.14
.04 04
Dissolved
solids (resid
ue on evapo ration
at
180°C
)
124
159
172
171
108
181
160 96
18
6 92 236
186
116
188
188
114
132
227
192
200
228
262
250
132
Hardness as CaCOa 100
131
131
143 82
141
114 77
113 73 204
143 84
151
138 77
100
191
142
148
158
173
204
100
O
0 S
fs IJ 10
27
16
29
13
38
24
16
16
12 1
24 9 30 22 3 8 17
19 22
19
18
29 1
Percent
sodium 1 1 9 3 9 8 6 1
20 2 7 6 12 6 6 20
15 8 16 6 11
13 7 6
Specific
conductance (microm
hos at
25°C
)
196
240
275
272
172
281
239
150
265
148
407
298
183
294
284
175
214
373
302
300
351
384
401
208
a a
6.9
8
.0
7.3
8.2
7.0
8
.2
8.2
6
.6
7.3
6.6 8.4
7.7
7.3 8.1
7.8
6.6
7.2
7.9
8
.4
8.5
8.1
8.2
8.5
7.5
CHEMICAL QUALITY OF THE WATER 165
w 10 * w LO co N- oo *ioinoooN-oocoincocoh- h- 00 00 h- h- h- 0000 00 00 t~ 00 t~ 00 t~ t~ t~ t~ 00 00t- as co o oo co o -*t>. co co 1-1 * t-co o os ffl> 1-1 co oot- t- o * 1-1 >o oo t-i-i m oo oo t- oo as as <N <-i o as asCO CO CO 1-1 (N (N (N CO-* CO CO CO CO CO CO CO (N (N CO CO CO
~~5e5 ^i S co o 5< m OS ooo<N<Ni-io<NOicai-iTfin
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~^< o co co 5 co ^*-*oococoooo-*oo<NOm<Ncooo00 00 CO CO O CO -* CiO t^ 00 00 t- 00 00 00 i-i O -* 00 00
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p p p p p oo m oo IN co m 1-1 co-* i-i o * m co m * co m IN as o(N ,-1 ,-1___________________(N (N CO CO CO CO CO CO I-H 1-1 (N (N COo o co o o o o oo ^ooooooooocom
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H ^i S ^ :^ -i-i(N(N(N(N(N(N(N(N(Nn in in in -in in in in in in in in in in in TH o N o co 1-1 o oo oocoooooco<Nt-co-*inoo
^(NN<N(NT)T)(NT)T)(Ni-i 1-1
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coco cat- *-iffl>OOOOOOOOcO(N'O'^oo co m co co m i-i coo
cot-oot-cocooxNOcomt-
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1« 2^: »w >,goH^^^ B SH S^ rt s ago^^S^^^S^S^'S^os^ OOOOOOOOOO
166 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
45 ppm of nitrate may cause cyanosis (Comly, 1945, p. 112- 116).
Boron is important in determining the suitability of water for irrigation. It is one of the essential elements for plant growth, but its beneficial concentration is very low. Toxic effects may be noticed on some plants if the irrigation water has more than about 0.3 ppm of boron.
Specific conductance is a measure of the ability of a solution to conduct an electrical current. As the concentration of dis solved material increases, the electrical resistance of the water decreases and the specific conductance of the water increases. Thus, specific conductance is an approximate measure of the total amount of dissolved mineral matter in a water.
CONCENTRATION AND NATURE OF DISSOLVED CONSTITUENTS
The shallow wells and test holes in the Gallatin Valley pro duce water from stream alluvium and alluvial-fan deposits of Quaternary age or from strata of Tertiary age. Most of the deeper wells and test holes derive water from the Tertiary strata, but a few springs and test holes may derive some water from Precambrian rocks. Because the chemical compositions of the wa ter from Bozeman Hot Spring (D2-4-14dac2) and the test holes that tap Precambrian rocks are different, a wide field is provided for speculation as to the source of the ions in solution in those waters. (See table 27.)
Wells drilled in the valley floor derive water from either the Quaternary deposits or Tertiary strata, or both. The chemical characteristics of most samples are shown on plate 10A. Water from the Quaternary deposits was relatively low in dissolved solids and was of the calcium bicarbonate type. The concentra tion of dissolved solids ranged from 154 to 398 ppm. The mag nesium and sulf ate percentages of the anhydrous residue of water from wells near Manhattan are slightly higher than those of water from wells in the upstream part of the area. Analyses of water from test holes Dl-5-9cd, Al-4-19cb, and -25dc, which penetrate thick alluvial deposits, show that the mineralization of the water is uniform with depth. Wells Al-4-5da, -15da2, D2-4-lldc, and D3-4-3ca, tapping strata of Tertiary age, pro duce water that is very similar in quality to water from wells in Quaternary deposits. However, the water from Tertiary strata in test hole A2-3-33da increases in mineralization with depth and is of the sodium chloride bicarbonate type.
CHEMICAL QUALITY OF THE WATER 167
In the Bozeman fan, most of the samples were from wells tap ping Quaternary deposits. (See pi. 105.) Dissolved solids ranged from 157 to 343 ppm, and calcium and bicarbonate were the ma jor constituents. The concentration of dissolved minerals is in dependent of well depth but increases downslope. (See table 29.) The increase in mineralization may be attributed to recharge to the aquifer by infiltrating irrigation water and to longer contact of the ground water with the aquifer in the downslope areas.
TABLE 29. Changes in water quality in a downslope direction in the Bozemanfan
Location ofwell or
test hole
D3-5-3da........ .....
D2-5-22ccd ............
Dl-5-22cd.............
Sampling date
/ Sept. 22, 1951\ Aug. 28, 1953
Jan. 9, 1952Nov. 6, 1952Sept. 22, 1951
/ Sept. 23, 1951\ Sept. 9, 1952
Depth(feet)
32.132.1
145265
16.430.130.1
Dissolvedsolids
(ppm)
172157214202290343257
Percentsodium
798
117
1313
In the Camp Creek Hills ground water in the Tertiary strata varies in quality not only from place to place but also vertically in the same well. (See pi. 10(7.) Correlation of chemical quality with geology would require detailed information on the mineral composition and stratigraphy of the Tertiary strata. However, the variation in quality is relatively unimportant because the water from most of the wells was relatively low in dissolved solids and was suitable for many uses.
Ground water in the valley-fringe area was very similar in chemical type and in concentration of dissolved solids to water from the Quaternary deposits in other parts of the Gallatin Val ley. (Seepl.lOD.)
CHEMICAL QUALITY IN RELATION TO HYDROLOGY
The quality of surface water is closely related to that of the ground water because infiltration of surface water is a principal source of ground-water recharge in the upper part of the valley, and because seepage into streams is a major source of surface water in the lower part of the valley. (See pis. 10, 11.) Sur face water in the valley is of the calcium bicarbonate type. In the lower part of the valley, where streams are effluent, the total mineralization of the surface water is but slightly greater than in the upstream part of the valley, where the streams are influent.
168 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
The quality of surface water in September 1951, during a period of low flow, is shown by patterns on plate 11.
Four shallow wells in the alluvium were sampled annually in the period 1951-53 to ascertain changes in water quality. Total mineralization of water from three of the wells changed only slightly. (See table 30.) Specific conductance of the water from well Al-4-5dd ranged from 464 to 620 micromhos. In the spring when runoff is high the surface water contains a little less dis solved material than in late summer and fall when streamflow is low. Although there is no analytical proof, the mineralization of the ground water in places where water levels are directly af fected by streamflow probably varies somewhat in response to the salinity of the surface water.
TABLE 30. Annual changes in total mineralization of ground water fromshallow wells
Well
D3-4-3abl..................
Al-4-5dd. .................
D3-5-3da .................
Dl-5-22cd .................
Depth (feet)
11
18.0
32.1
30.1
Date
( Sept. 22, 1951 \ Sept. 9. 1952{ Aus 28. 1953
f Sept. 21, 1951 \ Sept. 9 1952( Aug 28 1953
f Sept 22, 1951 \ Sept. 9, 1952{ Aug 28 1953
f Sept. 23, 1951 \ Sept 9, 1952I Sept. 11, 1953
Specific conductance (micromhos at 25°C)
337 345349
620 464.523
266 263251
552548546
SUITABILITY OF THE WATER FOB IRRIGATION
The suitability of any water for irrigation depends on the amount and kind of dissolved minerals or "salts" in the water in relation to certain other factors. (See tables 31, 32.) The dis solved salts affect the ability of the plant to take in water and nutrients. The normal osmotic gradient between the soil solution and the root cells is reversed if the soil solution is highly saline; thus, a plant may wilt from lack of moisture even though soil moisture seems to be adequate. A plant may be more easily in jured by saline water during germination and early seedling stage than when older. Irrigation water of high salinity adds to the soluble salts in the soil and should be avoided; however, such water can be used if the texture of the soil is coarse, internal drainage is good, and salt-tolerant crops are planted. If the only
CHEMICAL QUALITY OF THE WATER 169
water available is saline, more water than is necessary for plant use should be applied to flush the salts from the soil and to pre vent their accumulation. Generally, water having- a specific con ductance of less than 750 micromhos can be used safely on all soils. As salinity increases, the water becomes less suitable for irrigation; and when the specific conductance is greater than about 5,000 micromhos, the water generally is unsuitable for irrigation (Thorne and Thorne, 1951, p. 11).
Sodium has a detrimental effect on the soil because it defloccu- lates soil colloids. The deflocculating effect of sodium is con trolled by the ratio of the concentrations of calcium and mag nesium to sodium. Therefore, the percent sodium is important for determining the suitability of water for irrigation.
Wilcox (1948, p. 5-6) proposed a diagram for rating the suit ability of irrigation water on the basis of specific conductance and percent sodium. This diagram, as revised by Thorne and Thorne (1951, p. 9-12), was used in rating the water of the Gallatin Valley. (See fig. 40.) The following interpretation of the revised diagram is adapted from Thorne and Thorne:
Class Rating
1 Water can be used safely on all soils.2 Water can be expected to cause salt problems where drainage is
poor and leaching of residual salts from previous irrigation is not consistently practiced.
3 Water can be used on crops of medium to high salt tolerance, on soils of good permeability, and with irrigation practices that provide some leaching.
4 Water can be used successfully only if applied to crops of high salt tolerance, on permeable and well-drained soils, and with carefully devised and conducted irrigation and soil-management practices.
5 Water is generally unsuitable and should be used for irrigation only in special situations.
Group Rating
A There should be no difficulty from sodium accumulation in soils.B Where soils are of fine texture and do not contain gypsum or lime,
where drainage is poor, and where small quantities of water are applied with each irrigation, there may be some evidence of sodium accumulation but usually not enough to injure soils or crops seriously. Serious sodium accumulation may occur in waters high in carbonate or bicarbonate.
C Serious alkali formation should not occur in permeable soils (sands to silt loams), unless poor drainage, residual carbonate in water, or limited water use are problems. Fine-textured soils must be managed with care.
D Some alkali formation should be expected in all soils irrigated with group D water. Sandy or permeable soils high in gypsum might be irrigated with such water without highly injurious sodium accumulations. Loams or finer textured soils irrigated for some time with 3D or 4D water and then irrigated with water of low salt content would probably puddle and require gypsum for reclamation.
E Generally unsatisfactory for irrigation.NOTE. 1C, ID, and IE waters often can be improved in quality by treating with gypsum to
reduce the percent sodium.
508919 O-60 12
TABL
E 31.
Che
mic
al p
rope
rtie
s re
latin
g to
sui
tabi
lity
of g
roun
d w
ater
for
irr
igat
ion
in t
he G
alla
tin V
alle
y[G
eolo
gic
sour
ce:
P, P
reca
mbr
ian
rock
s; T
, str
ata
of T
erti
ary
age;
and
Q, d
epos
its
of Q
uate
rnar
y ag
e]
Loc
atio
nGeolo
gic source
Depth at sampli
ng time
(feet)
Date
of collectio
n
a 3'a
30
C3 o
a .S'M *S8
s11 o CO
§2M
I'8
PW
o> m
ilo
aoff
l o^j
Ci
3
a>^
l<3
4-SS
o tM CQ
3
^
03
0> T3 I§
o
Equ
ival
ents
per
mil
lion
S" il n
Percent
sodiumResidu
al sodium
carbonate (epm
)
Specific con
ductance (microm
hos at
25°C)
I c! 8 3 OT §
Val
ley
floor
Al-4
-5da
. ............
5dd. ...
....
....
.
15da2...........
19cb.............
25dc.............
Al-5-2
8db2...........
A2-3
-33da............
Dl-4
-leb
....
....
....
.Idc.............
Gddc
l...
....
....
13bb............
Dl-5
-9cd
....
....
....
.
D2-4
-lld
c...
....
....
.
14da
c2..
....
....
D3-4
-3abl............
3ca.... ..
....
...
T...
....
....
.
Q..... .......
T.... ........
Q............
Q............
Q fo T T:::::
::::::
:IT and P.....
.
O O o Q Q...
.. .......
/Q............
IT............
Q............
T(7). ........
207..........
18.0........
315..........
87..........
123.
....
....
.301..........
102.
....
....
.40
0...
....
...
170.
....
....
.55
....
....
..19
0...
....
...
250.
....
....
.45
0. .........
110..........
107.
....
....
.22.4........
65..........
158.
....
....
.f 32..........
4156
....
....
..15
6...
....
...
68..
....
....
145.
....
....
.
11..........
435.
....
....
.
Dec. 29
, 19
52(S
ept.
21,
1951
Sept.
9, 1952
Aug. 2
8, 195
3 Apr. 18, 1953
Aug.
31,
1953
July
23
, 19
53A
nn-
9^ IQAQ
Nov.
30,
195
1No
v. 26,
1951
Aug. 3
1, 195
3Aug. 2
8, 195
1Sept.
5, 195
1Sept.
8, 195
1Sept. 20
, 19
51
Sept.
9, 1952
Sept.
10, 19
52Sept. 22
, 19
51Sept.
23, 19
51Ja
n. 28
, 19
53Sept.
9, 1953
Sept.
15, 19
53Sept.
16, 19
53Sept.
8, 195
3Sept.
4, 195
3Sept. 22
, 1951
f.. d
o.. .......
4 Sept.
9, 1952
Aug. 2
8, 1953
Sept. 23
, 1952
3.19
4.09
3.04
3.44
1.75
3.09
3.24
394
.
2.10
2.59
2.99
2.07 9f
i
.68
2.79
2.64
2.35
2.84
1.75
3.84
3.54
3.24
2.84
2.89 .17
2.30
2.40
1.60
1.39
2.15
1.
54
1.76
.49
1.15
1.54
1.46
1.08
1.19
1.59
1.11 .69
.30
.95
1.00
1.65
1.34 .53
1.62
1.52
1.58
1.08
1.15 .03
1.00
1.04
.66
0.57 .57
.41
.48
.29
.23
.23
.25
.25
.23
.87
8.13
17.3
918
.31
.26
.24
.65
.24
.16
.83
.78
.70
.28
.32
5.87 .21
9n
.21
.40
0.12 .16
.13
.15
.09
.07
.08
.06
.07 rut
.21
.25
.33
.20
.07
.08
.09
.08
.06
.09
.11
.11
.08
.08
.08
.08
.07
.20
4.54
5.44
4.33
4.98
2.47
3 en
3.98
3 no
2.92
3.72
4.33
5.57
6.82
7.47
3.47
3.34
3.97
3.95
2.43
5.42
5.10
4.77
3.85
4.03
1.75
2.79
2.87
2.21
0.00 .00
.00
.00
.00 nn nn .00
.00 nn .00
.00
1 3O
1.10
.00
.00
.00
.00
.00
.00
.00
.00
.00
.00
.27
.00
.00
.00
0.65
1.33
.71
.81
.02
.75
.83
.81
.52
.27
1.00 .69
.27
.33
.50
.50
.58
.44
.00
.54
.48
.50
.37
.35
2.39 .69
.77
.54
0.08 .17
.06
.07
.06
.18
.23
OK
.07
.10
.24
5.02
9.31
9.48
.06
.07
.13
.06
.03
.16
.17
.10
.03
.07
1.44 .06
.07
.07
0.03 .03
.03
.03
.13 r\i
r\i
.02
.08
.01
.15
5.7
12 12 .0
1.01
.03
.01
.01
.03
.01
.01
.00
.06
.21
.01
.01
.06
11 8 8 8 11 5 5 5 7 7 6 15 70 94 94 6 6 14 5 6 13 13 12 7 7 956 5 6 14
0.00 .00
.00
.00
.23 nn nn .00
.00 nn .00
2.39
7.17
7.59
.0
0.0
0.0
0.0
0.1
5.0
0.04
.00
.00
.00
1.82 .00
.00
.00
503
620
464
523
242
<n
467
332
380
503
1,100
1,820
1,900
378
371
434
414
227
570
532
505
389
407
679
337
345
349
272
CHEMICAL QUALITY OF THE WATER 171
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Al-5-23cc....... Al-6-18cbl...... 18cb2.....
A3-5-28dd ...... Dl-5-12ad..... D2-6-22cb ......
TABL
E 3
2.
Che
mic
al p
rop
erti
es r
elati
ng t
o su
itabil
ity
of s
urf
ace
wate
r fo
r ir
rig
ati
on
in
the
Gal
lati
n V
alle
y
"a a o 6 1 2 3 4 5 6 7 8 9 10
11 12
13
14
15
16
17
18
19
Lo
cati
on
Gal
lati
n R
iver
at
Yel
low
ston
e P
ark b
oundar
y. ..
..
Do.. ...
....
....
....
....
....
....
....
....
Do
. ....................................
Do ..
....
....
....
....
....
....
....
....
...
Do.. ...
....
....
....
....
....
....
....
....
Gal
lati
n R
iver
in
sec.
8,
T.
4 S
., R
. 4
E. ..
....
....
Goo
se C
reek
in
NE
^N
WM
sec
. 16
, T
. 3
S.,
R.
4 E
. .
Low
line
Can
al 2
J^ m
iles
wes
t of
Bue
ll i
n S
WJ£
S
WM
sec
. 33
, T
. 1
N.,
R.
3 E
. ................
Gal
lati
n R
iver
at
She
ds B
ridge
in S
EJ^
SE
J^
sec.
10
, T
. 2
S.,
R.
4 E
. .....................
Do.. ...
....
....
....
....
....
....
....
....
Gal
lati
n R
iver
at
Cam
ero
n B
ridge
in N
WM
N
WM
sec
. 22
, T
. 1
S.,
R.
4 E
. ................
Gal
lati
n R
iver
at
Cen
tral
Par
k R
R.
Bri
dge
in
SW
MN
EM
sec
. 19
, T
. 1
N.,
R.
4 E
. ..
....
....
.D
o ..
....
....
....
....
....
....
....
....
...
Do ..
....
....
....
....
....
....
....
....
...
Do. ....................................
Gal
lati
n R
iver
eas
t of
Man
hat
tan
in
SE
J^N
EJ^
se
c. 1
2, T
. 1
N.,
R.
3 E
. ..
....
....
....
....
....
Cam
p C
reek
at
Vin
cen
t S
choo
l in
SW
J^N
EJ^
se
c. 4
, T
. 28., R
. 3
E.. ...
....
....
....
....
....
Cam
p C
reek
at
Bue
ll i
n S
E^S
W^ s
ec-
35t
T.
1 N
., R
. 3 E
....
....
. .....................
Rock
y C
reek
(E
ast
Gal
lati
n R
iver
) at
Fo
rt E
llis
in
SW
MS
EM
sec
. 24
, T
. 2
S.,
R.
6 E
...........
Sou
rdou
gh (
Boz
eman
) C
reek
nea
r B
oze
man
in
Eas
t G
alla
tin
Riv
er a
t B
oze
man
in S
WJ^
SE
}^
sec.
31,
T.
1 S
., R
. 6
E .......................
Bri
dger
Cre
ek a
t m
ou
th o
f B
ridger
Can
yon i
n S
EM
NW
M s
ec.
34,
T.
1 S
., R
. 6
E. ..
....
....
..
Lym
an C
reek
nea
r B
oze
man
in
NW
J4 s
ec.
28,
T.
IS.. R
. 6
E. ..
....
....
....
....
....
....
...
Dat
e of
co
llec
tion
Jun
e 24
, 19
49
Aug
. 18
, 19
49
Oct
. 30
, 19
49
Aug
. 18
, 19
49
Jun
e 24
, 19
49
Aug
. 20
, 19
49
Sep
t. 2
0, 1
951
Jun
e 24
, 19
49
Oct
. 30
, 19
49
May
27,
194
9 S
ept.
8,
195
2
Sep
t. 2
0, 1
951
Jun
e 25
, 19
49
Aug
. 19
, 19
49
Sep
t. 2
3, 1
951
May
27,
194
9 Ju
ne
25,
1949
A
ug.
19,
1949
O
ct.
30,
1949
Sep
t. 2
0, 1
951
. ..d
o..
. ..
....
...d
o.........
Sep
t. 2
1, 1
951
Sep
t. 2
2, 1
951
Sep
t. 2
1, 1
951
...d
o..
.......
Sep
t. 2
2. 1
951
Calcium(Ca
)Mag
nesium(Mg
)
II _oJjg
(5Bicar
bonate (HCO
s)
6ll
3 cc
Chloride (C
l)
Eq
uiv
alen
ts p
er m
illi
on
1.3
5
1.8
0
1.9
0
1.9
5
1.0
5
1.9
0
1.7
0
.95
1.5
5
1.0
0
2.4
5
2.1
0
1.1
5
2.1
0
2.0
5
1.0
0
1.3
5
2.5
0
1.8
5
2.1
0
2.3
0
2.4
0
2.6
4
1.3
5
2.5
4
2.8
4
2.0
0
0.6
4
.81
.71
.91
.58
.91
.58
.58
.71
.45
1.6
3
.76
.53
.91
.71
.53
.65
1.3
2
.99
.86
.86
1.0
6
1.4
4
.65
1.1
4
.76
1.3
2
0
0.1
5
.32
.20
.18
.20
.41
.52
.32
.14
.39
.48
.02
03
03
27
08
17
23 0.0
3
02
55
03 .0
7
.06
23
19
.05
39
34
33
54
.04
.10
.10
.05
.04
.06
.02
.01
1.8
0
2.0
8
2.2
9
2.0
2
1.3
8
1.8
9
1.8
0
1.2
1
1.9
3
1.21
3.8
3
2.3
8
1.5
1
2.4
1
2.3
3
1.4
8
1.8
4
3.4
7
2.1
3
2.3
3
2.7
9
3.1
0
3.2
6
1.9
8
3.5
1
3.7
9
2.7
9
0.0
0
.00
.00
.26
.00
.16
.00
.00
.00
.00
.23
.00
.00
.00
.CO
.00
.00
.00
.33
.20
.00
.00
.23
.00
.00
.00
.20
0.1
7
.54
.50
.65
.40
.96
.67
.31
.81
.25
.17
.73
.38
.73
.71
.38
.42
.63
.81
.71
.69
.81
.96
.17
.58
.31
.38
0.0
3
.00
.05
.00
.00
.01
.03
.00
.03
.00
.2C
.04
.00
.04
.03
.03
.06
.03
.06
.04
.28
.21
.04
.01
.08
.06
.03
§1
ffl 0.0
9
.05
.04
.07
" .
08
.02
.06
.04
.03
.12
.08
.10
.06
.14
.04
.04
.02
.03
.05
Percent
sodium
1 1 9 3 9 8 6 1 20
2 7 6 12 6 6 20
15 8 16 6 11
13 7 6 9 12 1
Residual
sodium carbona
te (epm)
0.0
0
.00
.00
.00
.00
.00
.00
.00
.00
.00
.00
.00
.00
.0
0
.00
.00
.00
.00
.00
.00
.00
.00
.00
.00
.17
Specific con
ductance (micromh
os at
25°C)
196
240
275
272
172
281
239
150
265
148
407
298
183
294
284
175
214
373
302
300
351
384
401
208
377
379
306
i
CHEMICAL QUALITY OF THE WATER 173
IN IN CO'* COCOCO COCOCOCO W IN CO CO CO
00 O O IN OO OOOOOOOOOOOO O O O O OO OOOOOOOOOOOO
1C T-I O * ;~t- OOWOSCOiO^CDOINOWi^o o q q qq qwqoqqoqoqoq
q q q q qq >-H T-I T-I ,-1 T-I T-I ,-1 q o T-I T-I ,-c
* IN o IN wo -<f<<NT-HcooscOT-HCOT-icoo!N
O O O O OO COOOOOOOOOOOt- O O O O OO T-HCOOOOOOOOOT-H T-H
TH CO t^ O O CO T-H CD T-I »O OS T-I TH O »O t~ TH OS CO ^ iO OS OOO (N T-I <N rH <N CO IN O OS iC * *
io m T-H T-I cooo tot- q q q q qq qq
o t^ i-i T-I T-IO <NCO
CD 00 t-- 00 ^(N OCDOCDOSt^-OStOOT^tNt" CO 1C OS iO (NCO T-H T-I T-I O O T-H T-I tD CD 00 IN T-I
O O iO O Tt<-^< OOOOOSOSIO1COOOO5 OS CD t^ CO CDOO COiOiOiOiOiO^iOiOOiO'O
T-H T-H <N WIN IN IN IN IN (N IN IN T-H T-H <N W IN
OSOSOSOSOSOSOSOSOSOS
d T3O. O-cSe^Sfc'^'c_&M'!
W *
^oi§ |H| *' Ui -
. -^ £ ^«S -^ 2^-to n^.
..- !S"sH°1l? -*af xs^
-^3 oc
« tf « Q
(N IN IN <N(N IN
174 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
EXPLANATION
Water from Tertiary strata and Precambrian rocks,undifferentiated Water from Tertiary strataWater from Tertiary strata and Quaternary deposits,undifferentiated Area in which water from Quaternary deposits plots Spring waterArea in which surface water plots
100
90
80
70
60
50
UJu rrUJ 40
30
20
10
IA
2 A
3B
3A
-4 A
5B
5A
0 1000 2000 3000 4000 5000 6000
SPECIFIC CONDUCTANCE, IN Ml C ROM H OS AT 25°C
FIGUKE 40. Graph showing classification of ground and surface waters of the Gallatin Valley for irrigation. After Thorne and Thorne, 1951.
As irrigation water high in bicarbonate and carbonate is concentrated by evapotranspiration, calcium and magnesium may precipitate as carbonates, and an increase in percent sodium may result. The carbonate and bicarbonate content of the water in
CHEMICAL QUALITY OF THE WATER 175
excess of the calcium and magnesium content, expressed in equiv alents per million, is "residual sodium carbonate" (Eaton, 1950, p. 123-133). Water containing residual sodium carbonate raises the pH of the soil and dissolves organic matter, perhaps to the extent that the soil condition known as "black alkali" may de velop. Wilcox, Blair, and Bower (1954, p. 259-266) found that waters containing less than 1.25 epm (equivalents per million) of residual sodium carbonate are probably safe for irrigation, those containing from 1.25 to 2.50 epm are marginal, and those containing more than 2.50 epm are not suitable. These limits are tentative and may be modified by the degree of leaching of the soil and by other factors. Ground water from Quaternary deposits and surface water had little or no residual sodium carbonate; however, water from Tertiary strata had significant amounts. (See tables 31, 32.)
Boron is an essential minor element for plant growth; how ever, its beneficial effects are limited to a narrow range in con centration (Scofield, 1936, p. 275-287).
Permissible limits for concentration of boron in several classes of water forirrigation
Class of water
Excellent .......................Good ..........................Permissible .....................Doubtful .......................Unsuitable ......................
Limits for concentration of boron (ppm)
Sensitive plants
<0.33 0.33- .67
.67-1.00 1.00-1.25
>1.25
Semitolerant plants
<0.67 . 67-1 . 33
1.33-2.00 2.00-2.50
>2.50
Tolerant plants
<1.00 1.00-2.00 2.00-3.00 3.00-3.75
>3.75
The most sensitive plants include nut, citrus, and deciduous trees; semitolerant plants include most truck crops, cereals, and cotton; tolerant plants include lettuce, alfalfa, beets, asparagus, and date palms.
Water from all sources in the valley had less than 0.34 ppm of boron except water from test hole A2-3-33da, which contained 5.7, 12, and 12 ppm at depths of 190, 250, and 450 feet, respectively.
SUITABILITY OF THE WATER FOR DOMESTIC USE
Concentration limits of important chemical constituents in drinking water-for use on carriers subject to Federal quarantine regulations have been established by the U. S. Public Health Serv ice (1946). The American Water Works Association by resolu-
176 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
tion adopted the standards for public water supplies. Some of the chemical constituents, the concentration of which preferably should not exceed those shown below, are as follows:
Concentration Constituent (ppm)
Fluoride -___-_____-_,____-__________________ ._____._- _______________-_______ 1.5Iron and manganese together ___________________________________ .3Magnesium _________ _______ _____ __________________________ 125Chloride _______________________ ___________________ . ._.______ 250Sulfate --___._____________._________________________________ ..______ 250Dissolved solids _____________________ _______^ _________________________ J 500
1 1,000 ppm permitted if water of better quality is not available.
The concentration of 1.5 ppm for fluoride was exceeded in wa ter from only 3 ground-water sources. (See table 27.) Although manganese was not determined, concentrations of iron exceeded 0.3 ppm in most of the ground-water samples. Excessive con centrations of iron will stain fixtures, utensils, and laundry. Magnesium and sulfate concentration limits were not exceeded in any of the ground-water samples, but water from well A2- 3-33da contained more than 250 ppm of chloride. Dissolved solids exceeded 1,000 ppm in water from only the deeper part of test hole A2^3-33da. Concentrations of none of the constituents in surface-water samples exceeded those shown above. (See table 28.)
A sample from the shallow part of test hole Dl-3-36bc con tained 110 ppm of nitrate; this test hole was near a barn and the water may have been contaminated by animal wastes.
Hardness of water can be detected in the domestic use of water by the scum or curd formed by soap. Hard water wastes soap and detergent and forms deposits on textiles, utensils, and heating equipment. Generally, water having a hardness of less than 120 ppm (as CaC03 ) need not be softened, that between 120 and 200 ppm may require softening, and that exceeding 200 ppm re quires softening for most uses. Hardness of ground water in the Gallatin Valley ranged from 10 to 312 ppm; most of the water would need to be softened to be entirely satisfactory. Hardness of surface waters ranged from 63 to 208 ppm.
CONCLUSION
Throughout the Gallatin Valley, water for domestic and live stock use is obtained from ground-water sources. Although ground water is pumped in a few places for municipal and small- scale industrial use, large withdrawals are not made anywhere in the valley. If integrated with full use of the surface-water re sources of the valley, full development of the ground-water re-
CONCLUSION 177
sources would not only overcome, in large measure, the existing shortages of surface water but also would make possible the ex tension of irrigation to some lands now dry farmed. In parts of the valley, the supply of ground water is sufficient to fill the demands of large-scale industries.
Theoretically, the amount of ground water that could be pumped annually in the Gallatin Valley and used consumptively is equal to the average annual recharge to the ground-water reser voir. If less than this amount is pumped and used consumptively, natural discharge from the ground-water reservoir would be re duced by an amount equal to the net use, but, if the full amount is pumped and used consumptively, natural discharge eventually would cease. Under present conditions some of the surface water available for recharge to the ground-water reservoir in Gallatin Valley at times of high runoff is rejected. Thus, a large volume of water leaves the valley each spring without any use having been made of it. Development of the ground-water resources of the valley would increase the amount of space available for stor age of additional water within the reservoir and thereby would increase the capacity of the reservoir to store a greater part of the available recharge. Within limits, therefore, the greater the withdrawal from the reservoir, the greater the recharge to it.
In the Gallatin Valley under natural conditions there was an approximate balance between recharge to, and discharge from, the ground-water reservoir. Development of agriculture was ac companied by an increased and, eventually, full use of the avail able supply of surface water during the growing season. The artificial recharge to the ground-water reservoir resulting from the use of surface water so altered the water regimen that a new state of equilibrium was reached. If, in the future, the ground- water resources of the valley are developed, the regimen again will be affected.
The average annual discharge of ground water from the Gal latin Valley, exclusive of that discharged by evapotranspiration, is about 240,000 acre-feet.
Increase in the consumptive use of ground water within the valley would reduce natural discharge from the valley by an amount equal to the volume used. Because the principal areas of ground-water discharge by evapotranspiration would be the last to be affected by withdrawals of ground water, nearly all the ground-water use would be reflected by a corresponding reduc tion in surface-water outflow from the valley. The reduction would be caused in part by a diminution of ground-water dis-
178 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
charge into streams and in part by loss of surplus surface water to ground-water storage, and would occur principally during the latter part of the irrigation season.
If, in making plans for further development of the ground-wa ter resources of the Gallatin Valley, plans were made also for augmenting the recharge to the ground-water reservoir, the vol ume of ground water that could be used consumptively each year without exhausting the supply would be increased. A sound basis for "managing" the ground-water reservoir by water spreading would be afforded by the annual forecasts of runoff in the drain age basin of the Gallatin River and periodic measurements of water levels in selected wells. The many borrow pits, gravel pits, and irrigation installations are means by which the ground- water reservoir could be filled when surface water is available for artificial recharge.
If, instead of developing the ground-water resources of the val ley, surface-water reservoirs are constructed as a means of stor ing additional water for irrigation, the added recharge to the ground-water reservoir from the increased spreading of surface water would cause an increase in the amount of waterlogged land in the valley. Much of the land now waterlogged could be drained by open ditches if they were cut into the gravel that underlies the waterlogged soil. Other measures that would help to relieve waterlogging would be consolidation of irrigation canals and the lining of reaches of canals where leakage occurs.
Maximum use of the water resources of the Gallatin Valley would involve, in general terms, use of surface water for irrigation from the beginning of the irrigation season until the supply be comes short. Then, in those parts of the valley where the ground- water supply is adequate, use of ground water would supplant that of surface water, and the remaining available supply of surface water would be sufficient for continued irrigation in other parts of the valley. During the part of the year when the surface- water supply exceeded the demand, the ground-water reservoir should be recharged artificially by surface water that otherwise would be lost from the valley.
A factor, not mentioned previously, in determining the feasi bility of developing ground water for irrigation is the initial cost of the wells and the subsequent maintenance and pumping costs. The factors involved in computing pumping costs, together with other factors of interest to the individual water user, are dis cussed by Wood (1950). Furthermore, the generally close inter relationship of ground water and surface water emphasizes the
SELECTED REFERENCES 179
need for clarification of the legal status of each in relation to the other, in order that existing rights can be protected and that full development of the water resources will not be impeded.
SELECTED REFERENCES
Alden, W. C., 1932, Physiography and glacial geology of eastern Montana and adjacent areas: U.S. Geol. Survey Prof. Paper 174.
1953, Physiography and glacial geology of western Montana and ad jacent areas: U.S. Geol. Survey Prof. Paper 231.
American Society of Civil Engineers, 1949, Hydrology handbook: Am. Soc. Civil Engineers, Manual Eng. Practice 28.
American Water Works Association, 1950, Water quality and treatment: Am. Water Works Assoc. Manual, 2d ed., 451 p.
Atwood, W. W., 1916, The physiographic conditions at Butte, Mont, and Bing- ham Canyon, Utah, when copper ores in these districts were enriched: Econ. Geology, v. 11, p. 697-740.
Bennison, E. W., 1947, Ground water, its development, uses and conservation: St. Paul, Minn., Edward E. Johnson, Inc., 509 p.
Berry, G. W., 1943, Stratigraphy and structure at Three Forks, Mont.: Geol. Soc. America Bull., v. 54, p. 1-29.
Blaney, H. F., 1951, Consumptive use of water: Am. Soc. Civil Engineers Proc., Irrigation Div., v. 77, Separate 91.
Clabaugh, S. E., 1952, Corundum deposits of Montana: U.S. Geol. Survey Bull. 983, p. 58-77.
Comly, H. H., 1945, Cyanosis in infants caused by nitrates in well water: Am. Med. Assoc. Jour., v. 129, p. 112-116.
Debler, E. B., and Robertson, R. R., 1937, Report on Gallatin Valley investiga tions, Montana: U.S. Bur. Reclamation open-file report, 129 p.
Deiss, Charles, 1936, Revision of type Cambrian formations and sections of Montana and Yellowstone National Park: Geol. Soc. America Bull., v. 47, p. 1257-1342.
DeYoung, William, and Smith, L. H., 1936, Soil survey of the Gallatin Valley area, Montana: U.S. Dept. Agriculture, Bur. Chemistry and Soils Bull. 16, ser. 1931.
Dorf, Erling, and Lochman, Christina, 1940, Upper Cambrian formations in southern Montana: Geol. Soc. America Bull., v. 51, p. 541-556.
Dorr, J. A., Jr., 1956, Anceney local mammal fauna, latest Miocene, Madison Valley formation: Jour. Paleontology, v. 3, p. 62-74.
Douglass, Earl, 1903, New vertebrates from the Montana Tertiary: Pitts burgh, Pa., Carnegie Mus. Annals 2, p. 145-199.
1909, Description of a new species of Procamelus from the upperMiocene of Montana, with notes upon Procamelus madisonius Douglass:Pittsburgh, Pa., Carnegie Mus. Annals 5, p. 159-165.
Eaton, F. M., 1950, Significance of carbonates in irrigation waters: Soil Sci.,v. 69, p. 123-133.
Emmons, W. H., and Calkins, F. C., 1913, Geology and ore deposits of thePhilipsburg quadrangle, Montana: U.S. Geol. Survey Prof. Paper 78.
Fenneman, N. M., 1931, Physiography of Western United States: New York,McGraw-Hill, p. 183-224.
Ferris, J. G., 1949, Ground water, in Wisler, C. O., and Brater, E. F.,Hydrology: New York, John Wiley & Sons, p. 198-272.
180 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Gardner, L. S., Hendricks, T. A., Hadley, H. D., and Rogers, C. P., Jr., 1945, Stratigraphic sections of Paleozoic and Mesozoic rocks in south-central Montana: U.S. Geol. Survey Oil and Gas Inv. Prelim. Chart 18.
Hanson, A. M., 1952, Cambrian stratigraphy in southwestern Montana: Mon tana Bur. Mines and Geology Mem. 33.
Haynes, W. P., 1916, The Lombard overthrust and related geological features: Jour. Geology, v. 24, p. 269-290.
Horberg, Leland, 1940, Geomorphic problems and glacial geology of the Yel- lowstone Valley, Park County, Mont.: Jour. Geology, v. 48, p. 275-303.
Iddings, J. P., and Weed, W. H., 1894, Description of the Livingston quad rangle, Montana: U.S. Geol. Survey Geol. Atlas, Folio 1.
Imlay, R. W., Gardner, L. S., Rogers, C. P., Jr., and Hadley, H. D., 1948, Marine Jurassic formations of Montana: U.S. Geol. Survey Oil and Gas Inv. Prelim. Chart 32.
Lochman, Christina, 1950, Status of Dry Creek shale of central Montana: Am. Assoc. Petroleum Geologists Bull., v. 34, p. 2200-2222.
Long, W. F., 1950, Survey report on Central Park drainage project, Three Rivers Soil Conservation District in Gallatin County, Mont.: U.S. Dept. Agriculture, Soil Conserv. Service, Great Plains Region, Lincoln, Nebr., open-file report, 18 p.
McMannis, W. J., 1955, Geology of the Bridger Range, Montana: Geol. Soc. America Bull., v. 66, p. 1385-1430.
Meinzer, O. E., 1923a, The occurrence of ground water in the United States, with a discussion of principles: U.S. Geol. Survey Water-Supply Paper 489.
1923b, Outline of ground-water hydrology, with definitions: U.S. Geol. Survey Water-Supply Paper 494.
1942, Occurrence, origin, and discharge of ground water, in Hydrology(Physics of the earth, pt. 9) : New York, McGraw-Hill, or Dover Publi cations, p. 385-443.
Montana Institute of the Arts, 1951, Historical map of Gallatin County, Mont.: Bozeman, Mont., Br. History Group, Montana Inst. Arts.
Montana State Engineer, 1953a, History of land and water use on irrigated acres, Gallatin County, Mont., part 1: Helena, Mont., State Engineer's Office.
1953b, Maps showing irrigated areas in colors designating the source of supply, Gallatin County, Mont., part 2: Helena, Mont., State Engi neer's Office.
Moritz, C. A., 1951, Triassic and Jurassic stratigraphy of southwestern Mon tana : Am. Assoc. Petroleum Geologists Bull., v. 35, p. 1781-1814.
Murdock, H. E., 1926, Irrigation and drainage problems in the Gallatin Valley: Montana Univ. Agr. Eng. Sta. Bull. 195.
Pardee, J. T., 1913, Coal in the Tertiary lake beds of southwestern Montana: U.S. Geol. Survey Bull. 531-G, p. 229-244.
1925, Geology and ground-water resources of Townsend Valley, Montana: U.S. Geol. Survey Water-Supply Paper 539.
1926, The Montana earthquake of June 27, 1925: U.S. Geol. Survey Prof. Paper 147-B, p. 7-23.
1950, Late Cenozoic block faulting in western Montana: Geol. Soc.America Bull., v. 61, p. 359-406.
Peale, A. C., 1893, The Paleozoic section in the vicinity of Three Forks, Mont.: U.S. Geol. Survey Bull. 110.
SELECTED REFERENCES 181
Peale, A. C., 1896, Description of the Three Forks quadrangle, Montana:U.S. Geol. Survey Geol. Atlas, Folio 24.
Reed, G. C., 1951, Mines and mineral deposits (except fuels), Gallatin County,Mont.; U.S. Bur. Mines Inf. Circ. 7607.
Schultz, C. B., and Falkenbach, C. H., 1940, Merycochoerinae, a new subfamilyof oreodonts: Am. Mus. Nat. History Bull., v. 77, p. 213-306.
1941, Ticholeptinae, a new subfamily of oreodonts: Am. Mus. Nat. History Bull., v. 79, p. 1-105.
1949, Promerycochoerinae, a new subfamily of oreodonts: Am. Mus.Nat. History Bull., v. 93, p. 69-198.
Scofield, C. S., 1936, The salinity of irrigation water: Smithsonian Inst. Ann. Kept., 1935, p. 275-287.
Skeels, D. C., 1939, Structural geology of the Trail Creek-Canyon Mountain area, Montana: Jour. Geology, v. 47, p. 816-840.
Sloss, L. L., and Laird, W. M., 1946, Devonian stratigraphy of central and northwestern Montana: U.S. Geol. Survey Oil and Gas. Inv. Prelim. Chart 25.
Sloss, L. L., and Moritz, C. A., 1951, Paleozoic stratigraphy of southwestern Montana: Am. Assoc. Petroleum Geologists Bull., v. 35, p. 2135-2169.
Stearns, N. D., 1927, Laboratory tests on physical properties of water-bearing materials: U.S. Geol. Survey Water-Supply Paper 596-F, p. 121-176.
Stiff, H. A., Jr., 1951, The interpretation of chemical water analysis by means of patterns: Jour. Petroleum Technology, Tech. Note 84.
Tansley, Wilfred, and Schafer, P. A., 1933, in Tansley, Wilfred, Schafer, P. A., and Hart, L. H., A geological reconnaissance of the Tobacco Root Mountains, Madison County, Mont.: Montana Bur. Mines and Geology Mem. 9.
Theis, C. V., 1935, The relation between the lowering of the piezometric sur face and the rate and duration of discharge of a well using ground-water storage: Am. Geophys. Union Trans., 16th Ann. Mtg., pt. 2, p. 519-524.
Theissen, A. H., 1911, Precipitation averages for large areas: Monthly Weather Rev., v. 39, p. 1082-1084.
Thomas, H. E., and Wilson, M. T., 1952, Determination of total evaportrans- piration by the inflow-outflow method: U.S. Geol. Survey open-file report.
Thorne, J. P., and Thorne, D. W., 1951, Irrigation waters of Utah: Utah Agr. Expt. Sta. Bull. 346.
U.S. Public Health Service, 1946, Drinking-water standards: [U.S.] Public Health Repts., v. 61, no. 11, p. 371-384.
U.S. Soil Conservation Service, 1948, Preliminary examination report on water supply and distribution investigation, Gallatin Valley area, Galla tin County, Mont.: U.S. Dept. Agriculture, Soil Conserv. Service, Region 5, Lincoln, Nebr., open-file report, 17 p.
Wantland, Dart, 1951a, Seismic investigations in connection with United States Geological Survey ground-water studies in the Gallatin River valley, Montana: U.S. Bur. Reclamation Geology Rept. G-115.
1951b, Second phase of geophysical investigations in connection with United States Geological Survey ground-water studies in the Gallatin River valley, Montana: U.S. Bur. Reclamation Geology Rept. G-121.
Wenzel, L. K., 1942, Methods for determining permeability of water-bearing materials, with special reference to discharging-well methods, with a section on direct laboratory methods and bibliography on permeability
182 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
and laminar flow, by V. C. Fishel: U.S. Geol. Survey Water-SupplyPaper 887.
White, W. N., 1932, A method of estimating ground-water supplies based ondischarge by plants and evaporation from soil results of investigationin Escalante Valley, Utah: U.S. Geol. Survey Water-Supply Paper659-A.
Wilcox, L. V., 1948, The quality of water for irrigation use: U.S. Dept.Agriculture Tech. Bull. 962.
Wilcox, L. V., Blair, G. Y., and Bower, C. A., 1954, Effect of bicarbonate onsuitability of water for irrigation: Soil Sci., v. 77, p. 259-266.
Wood, H. E., II, 1933, A fossil rhinoceros (Diceratherium armatum) fromGallatin County, Mont.: U.S. Natl. Mus. Proc., v. 82, p. 1-4.
1938, Continental Cenozoic at Three Forks, Mont, [abs.] : Geol. Soc.America Proc. 1937, p. 291-292.
Wood, H. E., II, and others, 1941, Nomenclature and correlation of the NorthAmerican continental Tertiary: Geol. Soc. America Bull. v. 52, p. 1-48.
Wood, I. D., 1950, Pumping for irrigation: U.S. Dept. Agriculture, Soil Con-serv. Service Tech. Paper 89.
BASIC DATA
184 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Table 33. Logs of wells and test holes
[Interpretative information supplied by authors is enclosed in brackets]
Thickness (feet)
Depth (feet)
Al-2-29adc [Drilled by Montana Power Co. (Rice No. 1). Logged by U. S. Geological Survey]
No record..........................................................................Tertiary:
Sand, very fine to medium, angular to subangular; composed of quartz, feldspar, garnet, gneiss, obsidian, dark volcanics, and pale-green clayey siltstone...........................................
Sand, very fine to medium; contains some coarser grains and a few siltstone fragments.....................................................
Sand, poorly sorted; contains pebbles and some light-greenclaystone and siltstone fragments........................................
Siltstone, light-green; contains some claystone.........................Sand, very fine to very coarse, subangular to subrounded;
contains few fragments of light-green claystone and siltstone. .Sand, poorly sorted, subangular; composed of quartz, feldspar,
obsidian, and red and black volcanic rocks...... ......................Sand, poorly sorted, greenish due to green quartz grains;
contains pebbles and green siltstone fragments 1 .....................Sand, poorly sorted, interbedded with green siltstone.................Siltstone interbedded with green claystone................................Sand and gravel, poorly sorted, greenish................... .............Bentonite(?), light-green; swells and slakes rapidly in water.......Claystone interbedded with green siltstone................................Sand and gravel, poorly sorted...............................................Siltstone, sandy, green.............................. ...........................Bentonite(?).................... ....................................................Sand and gravel, poorly sorted...............................................Siltstone, sandy, green; interbedded with thin layers of sand.... ..Sand, poorly sorted; contains pebbles......................................Claystone, green.................................................................Sand, fine to medium, angular, greenish.................................Claystone, green............................. ...................... ............ ..Sand, poorly sorted.... ......... ................................................Siltstone interbedded with sand...............................................Sand, angular, poorly sorted................................. ................Siltstone, clayey, green.................................. ... .... ..............Sand; contains some gravel.......... ... .....................................Siltstone, green... ................................................. ............Sand; contains some gravel....................................................Siltstone, pale-green streaked with light-brown.. ........ ....... ......Sand, poorly sorted, angular; contains pebbles.........................Claystone, cream with pale-green tinge, tuffaceous(?)..... .........Sand, angular, poorly sorted, light-green................................Claystone, tuffaceous, cream-colored.....................................Sand, fine to medium, poorly sorted, gray; contains some well-
developed quartz crystals...................................................Claystone interbedded with siltstone........................................Sand, fine to medium, poorly sorted, gray...............................Claystone, green..................................................................Sand, fine to medium, poorly sorted, gray...............................Siltstone, green................. ............................................... ,.Sand, fine to medium, poorly sorted, gray...............................Siltstone, sandy, pale-green.................................... ... ..........Sand, fine, gray..................................................................Claystone interbedded with siltstone........................................
95
5
25
255
10
15
20308
1525
12433
1466217
16162232786245
29548445
128
13
95
100
125
150155
165
180
200230238253255260272276279282296302308310311318334350372375377384392398400404409
438443447455459463468480488501
The remainder of the log has been adjusted to an electric log, which begins at this point.
BASIC DATA
Table 33. Logs of wells and test holes Continued
185
Thickness (feet)
Depth (feet)
Al-2-29adc Continued
Tertiary ContinuedSand, poorly sorted, angular, gray; composed of quartz,
feldspar, gneiss, and some dark volcanic grains ..................Silts tone, light-green.........................................................Sand, poorly sorted, angular, gray.......................................Siltstone, sandy; interbedded with gray-green claystone............Sand, poorly sorted, angular, gray.......................................Siltstone, gray-green........... ..............................................Sand, poorly sorted, angular, gray.......................................Sand, silty, interbedded with Siltstone ...................................Claystone interbedded with bentonite(?) and siltstone................Sand, poorly sorted, angular, gray.......................................Claystone interbedded with gray-green siltstone......................Sand, medium-grained, angular, poorly sorted.......................Siltstone, claystone, and pale-green sandy siltstone.................Sand, fine to medium, subangular, light-gray; composed of
quartz, feldspar, gneiss, and muscovite; this is the deepest sand containing dark volcanic rocks....................................
Claystone interbedded with silty fine sand, pale-green..............Sand, fine to medium, subangular, light-gray.........................Claystone interbedded with siltstone, pale-green......................Sand, fine to medium, subangular, light-gray.........................Siltstone interbedded with claystone and thin layers of sand,
pale -green,....................................................................Sand, fine to medium, subangular, light-gray.........................Siltstone, clayey, light-green...............................................Claystone, silty, micaceous, gray-green; grades downward
to gray, medium, friable sandstone composed of quartz, feldspar, and biotite ........................................................
Claystone, greenish-gray....................................................Sandstone, coarse-grained, porous, gray...............................Claystone, greenish-gray; grades downward to green, clayey
and sandy siltstone ..........................................................Sandstone, porous, poorly sorted, angular, gray; contains
pebbles..........................................................................Claystone, green; grades downward to fine-grained sandstone....Sandstone, coarse-grained, calcareous, hard, gray; contains
pebbles..........................................................................Sandstone, coarse-grained, porous, friable, gray...................Silts tone, green.................................................................C lay s tone, gray - green ........................................................Sandstone, poorly sorted, silty, clayey, gray.........................Sandstone, fine-grained, gray; grades downward to medium-
grained sandstone............................................................Sandstone, medium-grained, gray; grades downward to fine
grained sandstone............................................................Sandstone, fine -grained, gray ..............................................Claystone, green; grades downward to fine-grained sandstone....Sandstone, fine-grained, gray............................................ ..Sandstone, coarse-grained, porous, gray...............................Sandstone, coarse-grained, porous, gray, interbedded with thin
layers of claystone..........................................................Conglomerate; composed of well-rounded pebbles of quartz and
muscovite -quartz gneiss; green.........................................Siltstone, sandy, micaceous...... ..........................................Sandstone, medium-grained, calcareous, micaceous (the
mica flakes are arranged in layers)....................................Sandstone, coarse-grained, porous, gray...............................Claystone, green..................... ............ ..............................Siltstone, sandy; grades downward to coarse-grained sandstone.
508919 O-60 13
4538464
1712275
22
7132
4735
6 1 .5
13.5
510
2144
.39.7
31027
505510513521525531535552564566573578600
604613620633635
682685690
696697697. 5
711
716726
728742746754760
766
768772776779782
788
788. 3798
801811813820
186 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Table 33. Logs of wells and test holes Continued
Thickness (feet)
Al-2-29adc Continued
Tertiary ContinuedSiltstone, green................................................................Mudstone, carbonaceous, dark-gray; contains thin coal seams . Sandstone, coarse-grained, porous, gray .............................Sandstone, medium-grained, hard, calcareous, gray..............Clays tone, green..............................................................Sandstone, silty, poorly sorted, gray..................................Siltstone interbedded with claystone, gray; contains coal seam
at 850 ft.......................................................................Sands tone, gray................................................................Claystone, silty, green......................................................Sandstone, poorly sorted, gray...........................................Siltstone, clayey and sandy, gray-green. ..............................Sandstone alternating with sandy siltstone and claystone. Each
bed averages about 2 5 ft in thickness................................Siltstone, green, maroon-streaked.......................................Sandstone, coarse-grained, porous, gray; composed of quartz,
feldspar, muscovite and biotite.........................................Claystone, green, maroon-streaked. ....................................Sandstone, coarse-grained, porous, friable, gray..................Siltstone, green................................................................Sandstone, coarse-grained, gray.........................................Clays tone, green..............................................................Sandstone, silty, poorly sorted ...........................................Siltstone, micaceous, green; contains sand............................Sands tone, gray.................................................................Siltstone, sandy, green, maroon-streaked.............................Sandstone, coarse-grained, gray..........................................Claystone interbedded with siltstone, green ............................Siltstone interbedded with fine-grained sandstone; contains an
8-in. coal seam at 1, 126 ft...............................................Sandstone, coarse-grained, micaceous, gray.........................Claystone, gray.................................................................Sandstone, coarse- to medium-grained, porous, friable, gray;
composed of quartz, feldspar, and mica.............................Claystone, gray; grades downward to sandy siltstone...............Sandstone, predominantly coarse-grained, porous, friable,
gray; composed of quartz, feldspar, and mica.....................Siltstone, clayey, gray.......................................................Sandstone, medium-grained, gray; grades downward to a gray
c lays tone.......................................................................Siltstone interbedded with claystone, gray-green.....................
Al-3-4da [Drilled by commercial driller]
Soil [alluvium]...................................................................Gravel.............................................................................C lay (no wa t e r)..................................................................Gravel... ..........................................................................Hardpan and clay [Tertiary?]...............................................
Al-3-14dd
[Drilled by commercial driller]
Gravel.............................................................................Hardpan [calcareous, siltstone; Tertiary]..............................Siltstone, harder than above................................................Siltstone...........................................................................Hardpan...........................................................................Sands tone, fine - grained ......................................................
534465
93
129
15
1576
4275445
116649
522
34
131842
3030
7215
BASIC DATA 187
Table 33. Logs of wells and test holes Continued
Thickness Depth (feet) (feet)
Al-3-29aa
[Drilled by commerical driller]
Dirt.................................................................................... 15 15Gravel................................................................................ 78 93Sandrock, soft...................................................................... 6 99Sandrock, hard..................................................................... 1 100Clay, soft, yellow................................................................. 150 250Quicksand............................................................................ 18 268Clay, soft............................................................................ 12 280Sand, fine; pumped dry in 2^ hr............................................... 7 287Clay.............................. ..................................................... 12 299Sand.............. ..................................................................... 7 306C lay.............. .......... ........................................................... ______4 310
Al-4-5da
[Drilled by contractor for the U. S. Geological Survey. Principal water-bearing zone, 5-31 ft. Depth to water December 1952, 4 ft]
Quaternary (alluvium):Loam, silty..................................................................... 5 5Gravel, calcareous (comprised largely of dark-colored
volcanic and metamorphic rocks; also contains a fewfragments of dolomite and quartzite)................................. 10 15
Gravel, silty, calcareous.................................................. 3 18Sand and gravel, silty, calcareous, tuffaceous(?); contains
limestone fragments...................................................... 13 31Tertiary(?):
Silt and clay, sandy, calcareous, tuffaceous(?), light-tan;contains pebbles............................................................ 4 35
Sand, medium, silty, calcareous, light-tan; contains pebbles.. 10 45 Silt, sandy, calcareous, light-tan; contains pebbles and a few
marly fragments. Pebbles and sand are comprised ofvolcanic rock fragments, quartz, limestone, and magnetite.. 32 77
Sand, silty, calcareous, light-tan; contains pebbles............... 30 107Silt, sandy, calcareous, light-tan; contains scattered pebbles
and siltstone fragments.................................................. 16 123Sand, silty, fine, calcareous, light-tan; contains pebbles... .... 12 135
Tertiary:Siltstone, sandy, calcareous, tuffaceous, buff; contains a
small amount of sand and gravel...................................... 22 157Sandstone, medium-grained, silty, calcareous, gray; contains
pebbles. Sand grains are subrounded............................... 11 168Sandstone interbedded with calcareous conglomerate, grayish-
brown. Sand grains and pebbles are subangular tosubrounded...................... ............................................. 39 207
Al-4-15da2[Drilled by contractor for the U. S. Geological Survey. Principal water-bearing
zones, 4-80 ft and 249-260 ft. Depth to water for upper zone, 4 ft; for lower zone only, 3 ft]
Quaternary (alluvium):Soil, silty......................................................................Gravel, fine, and coarse to very coarse sand; some dark-
brown s ilt...................................................................Gravel, poorly sorted.....................................................Sand, very fine to fine, silty, light-brown; some coarse sand
and gravel..................................................................Gravel and coarse sand....................................................Sand, very fine to fine, silty, light-brown; little fine gravel
and some cobbles .........................................................
2328
3540
45
188 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Table 33. Logs of wells and test holes Continued
Thickness (feet)
Depth (feet)
Al -4-1 5da2 Continued
Quaternary (alluvium) Continued Gravel, fine, and coarse sand; some very fine sand and brown
silt...............................................................................
Gravel and sand, poorly sorted; large amount of very fine sand
Sand, fine, silty, light-brown; some coarse sand and gravel....
Sand, poorly sorted; small amount of dark-brown silt and clay.. Sand, coarse, clean, dark-colored; some Tertiary rock
Tertiary:
Claystone, buff; some white marl; very small amount of
Claystone, buff; interbedded with calcareous tuffaceous
Sand, poorly sorted, coarser grains predominant; some silt.... Siltstone, slightly sandy, tuffaceous, calcareous, buff; inter-
Claystone, silty, calcareous, buff.......................................
4 6
20 5
14 9 9
12 6 6 7
10 30 22
10
15
5
9 2 3
11
45 10
49 55 75 80 94
103 112
124 130 136 143 153 183 205
215
230
235
244 246 249 260
305 315
Al-4-19cb
[Drilled by contractor for the U. S. Geological Survey. Principal water-bearing zones, 5-94 ft and 117-180 ft. Depth to water for upper zone, 5 ft. Water level for lower zone, 3 ft above land surface]
Quaternary (alluvium): Soil................................................................................
Clay, calcareous, light-brown to cream; fragments of very slightly tuffaceous calcareous siltstone; some marl
Sand and gravel, poorly sorted, clean; contains a few large
Sand, silty; contains pebbles.............................................
1 14 15
5 20
5 10 24
13 16
2 5 5 5
45 10
1 15 30 35 55 60 70 94
107 123 125 130 135 140
185 195
BASIC DATA
Table 33. Logs of wells and test holes Continued
189
Thickness (feet)
Depth (feet)
Al-4-19cb Continued
Quaternary (alluvium) ContinuedSand, medium to coarse; fragments of light-brown calcareous
bentonitic(?) claystone..................................................... 5 200Silt and clay, sandy, greenish-gray; contains fragments of
kaolinite(?) and some small glass shards............................ 10 210Sand and gravel, poorly sorted............................................. 10 220Sand, very fine to very coarse; some silt.............................. 5 225Sand and gravel, poorly sorted; some silt.............................. 45 270Silt, sandy, clayey, brown................................................... 10 280Sand and gravel, silty, brown............................................... 5 285Sand, poorly sorted; very little brown silt.............................. 7 292Sand, poorly sorted; contains a few pebbles, some silt, and
a little clay................................................................... 9 301
Al-4-22dc4
[Drilled by contractor for the U. S. Geological Survey. Depth to water, 3 ft]
Quaternary (alluvium):Soil, silty......................................................................... 4 4Gravel and coarse sand; some brown calcareous silt............... 11 15Gravel, coarse, sandy; very little brown .calcareous silt........... 5 20Sand, coarse; contains pebbles, brown silt, and fine sand.......... 15 35Sand, medium to coarse; some silt....................................... ______8 ___43
Al-4-25dc
[Drilled by contractor for the U. S. Geological Survey. Principal water-bearing zone, 10-55 ft; saturated from 60-400 ft. Depth to water, 10 ft]
Gravel, sandy, silty, calcareous; contains cobbles; composedof volcanic and metamorphic rocks.................................... 50 50
Gravel; contains sand lenses ............................................... 40 90Gravel, sandy.................................................................... 120 210Sand, medium to coarse; contains pebbles.............................. 30 240Gravel, sandy.................................................................... 35 275Gravel, sandy, silty........................................................... 25 300Gravel, sandy................................................................... 78 378Sand, medium, silty........................................................... 6 384Gravel, sandy ................................................................... _____16 400
Al-5-9bb
[Drilled by commercial driller]
Topsoil............................................................................ 2 2Gravel [alluvium]. Water at 25 ft......................................... 23 25Clay, sandy, yellow [Tertiary(?)]. A little water at 85 ft.......... 60 85Clay, sandy, yellow. More water......................................... 22__ 107
Al-5-28db2 [Drilled by contractor for the U. S. Geological Survey. Depth to water, 3 ft]
Quaternary (alluvium):Soil................................................................................. 6 6Silt and clay, calcareous, brown-gray; fine gravel and coarse
sand. Gravel and sand composed of fragments of gneiss and Paleozoic limestone. Numerous terrestrial gastropod shells (Recent?) in a calcareous matrix.............................. 4 10
190 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Table 33. Logs of wells and test holes Continued
Thickness (feet)
Depth (feet)
Al -5 - 28db2 Continued
Quaternary (alluvium) ContinuedSilt and clay, calcareous, gray; coarse gravel....................... 5Silt and clay, calcareous, yellow-buff; coarse sand and fine
gravel. Sand and gravel composed of fragments of Tertiary beds, Paleozoic limestone and gneiss................................ 10
Gravel and yellow-buff calcareous silt and clay...................... 10Silt, yellow-buff, and poorly sorted sand.............................. 10Sand, gravel, and buff calcareous silt............. ..................... 5Silt, calcareous, buff; some sand and gravel......................... 9Sand, gravel, and buff calcareous silt....... ........................... 26Sand, medium, well-sorted; some buff calcareous silt............ 5Sand and silt, calcareous, buff; some fine gravel; small
amount of clay............................................................... 25Gravel and sand; buff silt................................................... 35Silt and clay, calcareous, buff; some gravel and sand............. 5Sand, coarse, and fine gravel; silt....................................... 5Silt and clay, calcareous, buff; sand and gravel..................... 10Sand and fine gravel; calcareous silt.................................... 25Gravel, coarse; sand and silt.............................................. 6Sand, very fine to coarse; silt............................................. 3Gravel, coarse: sand; brown calcareous silt.......................... ______§_
Al-6-18cbl [Drilled by commercial driller]
Soil................................................................................ 5Gravel, tight................................................................... 15Water sand...................................................................... 5C lay, sandy..................................................................... 45Sand and boulders............................................................. ______3_
A2-2-35abl [Drilled by contractor for the U. S. Geological Survey]
Quaternary (alluvium):Soil................................................................................. 2Gravel and cobbles ................,....................... -. 20
Mississippian. (Madison group): Limestone, brown..................
A2-2-35ab2
_____________[Drilled by contractor for the U. S. Geological Survey]____Quaternary (alluvium):
Soil................................................................................ 2Gravel and cobbles ........................................................... 19Gravel, clayey, and cobbles............................................... 2
Mississippian (Madison group): Limestone, brown.................... ______4
A2-2-35adl
[Drilled by commercial driller]
[Quaternary (colluvium)]: Gravel............................................ 30[Tertiary(?)]: Soapstone, ivory-colored [probably claystone]....... 30[Mississippian (Madison group?)]:. Solid rock ............................ 50
BASIC DATA
Table 33. Logs of wells and test holes Continued
191
Thickness (feet)
Depth (feet)
A2-2-35ad2
[Drilled by commercial driller]
Unconsolidated deposits......................................................Solid rock, dark-colored .....................................................
A2-2-36bb
[Drilled by commercial driller]
[Quate rnary (alluvium) ]: Gravel..............................................[Devonian (Jefferson limestone?)]: Solid rock, very dark colored; ___hard to drill................................ ..................................
A2-2-36bc
[Drilled by commercial driller]
[Quate rnary (alluvium) ]: G ravel..............................................[Mississippian and Devonian (Threeforks shale or Jefferson
___limestone?)]: Red hardpan. fairly soft rock........................
A2-3-23cb
[Drilled by commercial driller]
Topsoil............................................................................[Cambrian (Wolsey shale)]:
Shale; very little water at 24 ft............................................Red rock..........................................................................Shale, blue - gray ...............................................................Sandstone, gray................................................................Soapstone, light-gray.........................................................Sandstone, light-colored (almost white); water rose to 80 ft......
[Cambrian (Flathead quartzite?)]:;Hard rock.......... .............................................................
2864
2892
15
122
15
137
17
62
17
79
31254532
9
4065
110142150152
152.6
A2-3-33da
[Drilled by contractor for the U. S. Geological Survey. Principal water-bearing zones, 32-73 ft and 215-300 ft. Depth to water for upper zone, 32 ft; for lower zone only, 12 ft]
Quaternary (alluvium): Silt........................Gravel, sandy and silty; contains cobbles. Composed predom
inantly of volcanic rock fragments; also contains some metamorphic rock fragments...........................................
Sand, medium to coarse, and fine gravel. Composed predom inantly of volcanic rock fragments; contains some gneiss and a few limestone pebbles ..................................................
Gravel, sandy, fine ......... .................................................Gravel, sandy and silty, fine ..............................................
Tertiary (fanglomerate?):Gravel, sandy, calcareous; contains cobbles of limestone and
quartzite ......................................................................Tertiary:
Volcanic ash, pure, cream-gray..........................................Siltstone, calcareous, tuffaceous, buff..................................Volcanic ash, pure, cream-gray..........................................Marl, tuffaceous; interbedded with tuffaceous claystone and
volcanic ash..................................................................Tertiary (fanglomerate):
Gravel and cobbles, angular, in a matrix of greenish silt and clay; contains several clay lenses. Gravel composed pre dominantly of dark-colored (black, gray, and brown) lime stone and chert; also contains some quartzite......................
14
2510
5
18
232
60
75
15
405055
73
757880
140
215
192 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Table 33. Logs of wells and test holes Continued
Thickness (feet)
A2-3-33da Continued
Tertiary (fanglomerate): ContinuedSand, medium, angular to subangular, dark-brown. Composed
predominantly of limestone; also contains some chert, a few crystal-quartz grains, and pyrite cubes and ortahedra...........
Gravel and cobbles (similar to that between 140 and 215 ft.. .......Sand, medium to coarse, dark-brown. Composed of limestone,
chert, and quartz containing a little pyrite...........................Sand and gravel, intermixed.................................................
Precambrian (Belt series, undifferentiated):Siltstone, in shades of buff, yellow, gray, and green; some clay
either as a matrix or in thin layers; some calcite and tarry residue on bedding planes and seams. Possibly a weathered zone..............................................................................
Siltstone interbedded with mudstone, calcareous, dolomitic, variegated (salmon, buff, gray, green, and blue); predomi nantly grayish-brown to reddish-brown. Tarry residue and calcite on seams..............................................................
Limestone, dolomitic, and dolomite, dark-gray to brownish- gray..............................................................................
Siltstone, dolomitic, calcareous, variegated; interbedded with dolomitic limestone and dolomite; dark-gray to brownish- gray.............................................................................
A2-3-34ca [Drilled by commercial driller]
Gravel...............................................................................Clay..................................................................................Gravel...............................................................................
Dl-3-13bb
[Drilled by commercial driller]
Topsoil..............................................................................Gravel..............................................................................Hardpan.............................................................................Gravel...............................................................................
Dl-3-13bc [Drilled by commercial driller]
Dirt and clay.......................................................................Gravel, tightly packed, dry..................................................Sand and gravel; small amount of water..................................Clay, sandy, dirty; little water............ .................................Sand, dirty (quicksand)........................................................Quicksand..........................................................................Sand, coarse, clean, saturated.............................................Sand, dirty............................. ....................................... ...
Dl-3-13ca2
[Drilled by commercial driller]
Topsoil.............................................................................Gravel.............................................................................Clay and gravel................................... . .............................Gravel and sand .......................... ......................................
Dl-3-'13cb2
[Drilled by commercial driller]
Topsoil and clay...................................................................Gravel and silt intermixed ....................................................
205
2040
20
87
15
28
251017
17441337
14112
5121215
560
243
67
17147
17164
BASIC DATA
Table 33. Logs of wells and test holes Continued
193
Thickness (feet)
Depth (feet)
Dl-3-24ba
[Drilled by commerical driller]
Clay.................................................................................
(?)....................................................................................
5 18 22 13 92 22
5 23 45 58
150 172
Dl-3-36bc
[Drilled by contractor for the U. S. Geological Survey. Principal water-bearing zone, 16-100 ft. Depth to water, 16 ft]
Quaternary (colluvium):
Tertiary (unit T2 ?): Gravel, sandy, silty. Gravel is composed of pebbles derived
Gravel, silty. Gravel is composed of volcanic and metamorphic
Tertiary (unit T 2 ): Silt, sandy, calcareous, tuffaceous, buff; contains fragments
Clay, calcareous, tuffaceous, light-brown; contains fragments
Tertiary (unit T!?): Siltstone, sandy, calcareous, tuffaceous, buff; interbedded with
Tertiary (unit T-^:
Clay and claystone, pyritic, dark-blue; fossiliferous(ostracodes at 715 ft)........................................................................
Sand, poorly sorted, composed chiefly of quartz, garnet, dark
Clay, silty, dark-blue; contains gypsum fragments, which
Clay and claystone, dark-blue, fossiliferous (ostracodes at
23
9 33
20 7 8
25
30 19
6 45
7 16
4 28
4 21 18
31 9
22 43 30
3 42 55 32
135
24
44
66
23
32 65
85 92
100
125
155 174 180 225 232 248 252 280 284 305 323
354 363 385 428 458
461 503 558 590
725
749
793
859
194 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Table 33. Logs of wells and test holes Continued
Thickness (feet)
Depth (feet)
Dl-3-36bc Continued
Precambrian(?):Sand, angular, bluish; contains pebbles. Sand is composed
chiefly of quartz, feldspar, and gneiss fragments. This material is probably derived from weathered Precambrian gneiss........................................................................... 23 882
Dl-4-lcd
[Drilled by commercial driller]
Soil................................................................................. 2 2Gravel, loose. Water at 28 ft............................................... 26 28Sand, water-bearing............................................................ 4 32Gravel, tight; contains some sand. Struck second water at 54 ft
and it raised to 47. 4 ft from the surface.............................. 88 120Sand, clean. More water.... ................................................ 4 124Gravel, tight; contains some sand........................................ 66 190Sand, clean. More water..................................................... 6 196Gravel, tight..................................................................... _______4 200
Dl-4-2dd
[Drilled by commercial driller. Samples examined by U. S. Geological Survey personnel]
Gravel and sand; some calcareous silt................................... 12 12Sand and gravel; little light-gray calcareous silt..................... 22 34Gravel and sand; some light-brown silt.................................. 44 78Silt, light-brown; some gravel and sand................................. 17 95Gravel and sand; varying amounts of light-brown silt.... ........... 83 178
Dl-4-6ddc2
[Drilled by contractor for the U. S. Geological Survey. Principal water-bearing zones, 14 65 ft and 150 240 ft. Depth to water for upper zone, 15 ft; for lower zone only, 28 ft]
Quaternary (alluvium):Silt, calcareous, light-gray; some clay and sand.....................Silt, calcareous, light-gray; some fine sand...........................Silt, calcareous, light-gray; some sand and gravel..................Silt, calcareous, gray; some medium sand.............................Sand, silty, slightly calcareous, gray; some fine gravel...........Gravel and sand; some gray silt................................. ..........Sand, coarse; some gray silt....................................... ........Sand, very fine to fine; some gray silt. .................................Gravel, brown sand and silt................................................Sand, coarse, and fine gravel; some light-brown silt...............Sand, fine to medium, silty, light-brown.......................... ....Gravel and sand; light-brown silt and clay..............................Sand, coarse, and gravel; light-brown silt............................ .Sand, well sorted, medium, gray-brown...............................Sand and gravel; some light-brown silt.......................... ........Silt, light-brown; very fine to fine sand; some'gravel...............Sand, medium to very coarse, and fine gravel; some light-
brown silt.....................................................................Sand, coarse, and gravel; very fine sand in silt matrix, light-
brown.. .........................................................................Sand, very fine, and light-brown silt; some gravel and clay......
51520253340455060869298
103118146151
161
186218
BASIC DATA
Table 33. Logs of wells and test holes Continued
195
Thickness (feet)
Depth (feet)
Dl-4-6ddc2 Continued
Quaternary (alluvium): Continued Sand, well-sorted, fine to medium; contains numerous grains
of magnetite. .................................................................
Gravel, fine, and medium to coarse sand; light-brown silt.......
Note: Fragments of metamorphic and volcanic rocks and quartz are the predominant constituents of the sand and gravel.
4 18
6 9
222 240 246 255
Dl-4-9bal [Drilled by contractor for the U. S. Geological Survey. Principal water-bearing
zones, 12 45 ft and 50-97 ft. Depth to water for upper zone 11 ft; for lower zone only, 23 ft]
Quaternary (alluvium):
Sand, very coarse to coarse; contains pebbles, very fine sand,
Gravel, medium to fine, sandy; some brown silt.....................Clay, sandy, light -brown, ...................................................
Sand and gravel, poorly sorted, angular to subrounded;
Note: Fragments of metamorphic rocks and some of volcanic rocks are the principal constituents of the sand and gravel.
20
15 3 7 2
14 25
11.5
20
35 38 45 47 61 86
97. 5
Dl-4-25aa2
[Drilled by contractor for the U. S. Geological Survey. Principal water-bearing zones, 5 50 ft and 149 223 ft. Depth to water for upper zone, 5 ft; water level for lower zone only, 13 ft above land surface]
Quaternary (alluvium'): Soil........................Gravel and cobbles of limestone, and metamorphic and volcanic
rocks; contains some gray-brown calcareous silt.................Gravel and sand, poorly sorted, dark-gray; some gray-brown
calcareous silt..............................................................Sand, very fine to medium, dark .........................................Gravel, fine; some sand and silt..........................................Sand, very firfe to medium, dark .........................................
Quaternary (fan alluvium?):Gravel, sandy, silty, tan to brown; contains several thin lenses
of sand and silt. Gravel composed of volcanic and metamor phic rocks. ...................................................................
Silt and very fine sand, light-brown.....................................Sand, silty, poorly sorted, very fine to very coarse, tan;
contains pebbles.............................................................Tertiary:
Silt, clayey, tan; contains fragments of claystone and tancalcareous tuffaceous siltstone; some gray ash fragments.....
Sand, poorly sorted, calcareous, tan; some fragments ofcalcareous cemented sandstone........................................
Sand, fine to very fine, and silt...........................................
13
1413
33
523
33
12
16
30434649
101104
137
149
157163
196 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Table 33. Logs of wells and test holes Continued
Thickness (feet)
Depth (feet)
Dl-4-25aa2 Continued
Tertiary: ContinuedGravel, poorly sorted, rounded, sandy; little light-brown silt.,Sand, poorly sorted, fine to coarse, gray; some tan silt in
places; fragments of calcareous tuffaceous siltstone and clays tone.....................................................................
Sand, gray, and fragments of calcareous cemented sandstone..Siltstone, tuffaceous, calcareous, tan; interbedded with buff
clay stone.....................................................................
15
432
57
178
221223
280
Dl-4-25aa3
[Drilled by contractor for the U. S. Geological Survey. Principal water-bearing zone, 5-50 ft. Depth to water, 5 ft]
Quaternary: Soil.................... ............................................................. 5. 5
9.513
616
. 5
5. 51528345050. 5
Dl-4-34bd
[Drilled by commercial driller]
[Tertiary(?)]; Clay, yellow and brown. .....................................1622
1638
Dl-5-9cd
[Drilled by contractor for the U. S. Geological Survey. Principal water-bearing zone, 14-70 ft. Depth to water, 14 ft]
Quaternary (alluvium): Gravel, poorly sorted; composed of ced and black volcanic rocks,
gneiss, and brown and gray limestone; some light-brown
Gravel, poorly sorted, sandy, dark; some brown calcareous silt...............................................................................
Gravel, sandy, and some brown slightly calcareous silt. Gravel is composed chiefly of dark volcanic rocks and gneiss;
Sand, poorly sorted, in matrix of brown silt; contains pebbles. Sand is composed of fragments of volcanic rocks and gneiss....
105
155
15
10
5 4545
7
1015
303550
60
65 110155162
Dl-5-18cc
[Drilled by commercial driller]
Gravel..............................................................................
49. 5.5
4949.550
BASIC DATA
Table 33. Logs of wells and test holes Continued
197
Thickness (feet)
Depth (feet)
Dl-5-32ca
[Drilled by commercial driller]
Clay..................Gravel...............Clay and hardpan. Hardpan. Water..
5181910
5234252
Dl-5-34cc2
[Drilled by contractor for the U. S. Geological Survey. Principal water-bearing zones, 10-39 ft, 60-83 ft, and 103-120 ft. Depth to water for top zone, 10 ft]
Quaternary (fan alluvium):Silt, buff.........................................................................Gravel, silty, sandy; composed chiefly of volcanic and
metamorphic rocks.......................................................Clay, sandy, silty, buff....................................................Sand, poorly sorted; contains pebbles. The sand is composed
chiefly of quartz with some biotite ..................................Silt, clayey, buff..............................................................Gravel, silty; contains pebbles ..........................................Sand, medium to fine, silty; contains pebbles.......................
Tertiary:Volcanic ash, gray...........................................................Siltstone, sandy, calcareous, tuffaceous, buff......................Sand, medium to coarse, silty; contains pebbles. ..................Siltstone, sandy, calcareous, tuffaceous, buff......................Gravel; composed of volcanic and metamorphic rocks............Silt, buff; contains pebbles................................................
Dl-5-36ddc
[Drilled by commercial driller]
Topsoil and dirt..............................................................Gravel, sand, boulders. Water at 30 ft...............................
D2-4-4aa
__________________[Drilled by commercial driller]_______Soil...............................................................................Gravel...........................................................................
3023
21201212
1490
33
3962
83103115127
131140154244247250
2073
2093
727
734
D2-4-9bc
[^Drilled by contractor for the U. S. Geological Survey. Principal water-bearing zones: 85-100 ft, T&5 200 ft, 433-459 ft, 497-542 ft, and 555-595 ft. Depth to water for top zone, 85 ft]
Quaternary (loess?): Silt, clayey, calcareous, buff to gray.......Quaternary (terrace deposits?):
Silt, sandy, calcareous, tan; contains pebbles.......................Gravel and sand in matrix of tuffaceous silt, tan; composed of
metamorphic and volcanic rocks......................................Tertiary (unit T2 ?):
Silt, sandy, tan....... ........................................................Gravel, sandy; contains well-rounded cobbles.......................Sand and gravel, coarse; some silicified wood fragments........
Tertiary (unit T 2 ):Sand; contains fragments of tan tuffaceous Siltstone...............Silt, sandy, tuffaceous, buff-tan.........................................Siltstone, sandy, calcareous, tuffaceous, buff; contains
silicified wood at 170 ft and bone fragments at 180 ft...........
18
12
30
101119
2515
45
18
30
60
7081
100
125140
185
198 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Table 33. Logs of wells and test holes Continued
Thickness (feet)
Depth (feet)
D2-4-9bc Continued
Tertiary (unit T 2 ) ContinuedSand, silty, calcareous, gray............................................Silt, sandy, tuffaceous, buff to gray; contains pebbles ...........Siltstone, sandy, calcareous, tuffaceous, buff......................Volcanic ash, gray..........................................................Siltstone, slightly sandy, calcareous, tuffaceous, buff ..........Volcanic ash, buff to gray.................................................Siltstone, sandy, calcareous, tuffaceous, buff; interbedded
with light-brown laminated claystone; contains some scatteredfragments of gray volcanic ash.........................................
Sandstone,moderately cemented, fine, gray...........................Tertiary (unit T!?):
Bentonite, greenish-cream; contains some fragments ofclayey silts tone..................................................... ........
Claystone, sandy, silty, calcareous, tan; interbedded withthin layers of volcanic ash...............................................
Sand, poorly sorted, dark; contains pebbles. Sand is composedof quartz, hornblende, feldspar, garnet, magnetite, mica,and a few rounded grains of volcanic rock..........................
Clay, silty, light-blue.......................................................Silt, clayey, bluish-gray...................................................Clay, silty, light-blue .....................................................Sand, medium, gray; composed of quartz, feldspar, garnet,
biotite, and hornblende...................................................Sand interbedded with clay, pyritic, blue..............................Silt, clayey, pyritic, bluish-gray........................................Sand, poorly sorted, angular, bluish-green..........................
Precambrian (Archean? type):Sand and clay, bluish-green (probably weathered gneiss). Sand
is composed of angular grains of quartz, garnet, feldspar(microcline), biotite, and hornblende................................
Precambrian (Archean type): Gneiss, coarsely crystalline,greenish......................................................................
194
762
874
10
31
26111017
19261320
20
5
191200219223299301
388392
402
433
459470480497
516542555575
595
600
D2-4-lldc
[Drilled by contractor for the U. S. Geological Survey. Principal water-bearing zone, 10-68 ft. Depth to water, 10 ft]
Quaternary (alluvium):Gravel, poorly sorted, sandy, in a matrix of gray calcareous
micaceous silt. Gravel is composed of fragments of dark volcanic rocks, gneiss, and some limestone......................
Sand and gravel; contains some gray calcareous silt. Compo sition of sand and gravel is similar to that of the gravel from 0 5 ft; contains varying amounts of limestone fragments....................................................................
Gravel, sandy, in a silt matrix..........................................Sand, poorly sorted, gray; contains gray silt........................
Tertiary (unit T2 ?):Claystone interbedded with siltstone, calcareous, light-browVi.,.Sand, poorly sorted, dark; contains pebbles .........................Claystone, light-brown, and calcareous clayey siltstone;
contains some bentonite(?)..............................................Siltstone, slightly calcareous, light-brown; contains some
marl and claystone........................................................Siltstone, light-brown; contains a few thin lenses of sand........Sand, silty, slightly calcareous, light-brown; composed
chiefly of well-sorted frosted quartz grains ......................
496
22
540
546068
7378
100
105145
150
BASIC DATA
Table 33. Logs of wells and test holes Continued
199
Thickness (feet)
Depth (feet)
D2-4-15da
[Drilled by commercial driller]
Gravel............................................................................ 19 19Clay, yellow. A little water............................................... 28 47Clay............................................................................... 63 110Sandrock........................................................................._____10_____120
D2-5-ldd2
__ [Drilled by commercial driller]
Gravel............................................................................ 14 14Clay............................................................................... 42 56Gravel. Some water......................................................... 1.5 57.5Clay and some gravel. Water at 64 ft .................................. ______6. 5 64
D2-5-2aa
[Drilled by commercial driller]
Topsoil........................................................................... 8 8Sand and gravel, dirty. Some water.................................... 47 55Clay........................................... ................................... 10 65Sand and gravel, dirty. Some water .................................... 3 68Clay, sandy.................................................................... 6 74Sand and gravel. Water .................................................... 4 78
D2-5-14ac
[Drilled by contractor for the U. S. Geological Survey. Principal water-bearing zone, 6.5-115 ft. Depth to water, 6.5 ft]
Quaternary (fan alluvium):Loam............................................................................. 4 4Gravel, sandy, calcareous; gravel is composed of subangular
to subrounded fragments of gneiss and volcanic rocks ......... 6 10Gravel, sandy and silty, calcareous ................................... 15 25Sand; contains pebbles...................................................... 2 27Gravel, medium, sandy.................................................... 28 55Sand; contains pebbles...................................................... 2 57Gravel, medium, sandy.................................................... 10 67Clay, light-brown............................................................ .5 67.5Gravel, medium, sandy.................................................... 27. 5 95Gravel, sandy and slightly silty ......................................... 20 115Gravel, sandy, silty, and clayey. The amount of clay
increases downward...................................................... 30 145Sand, fine, silty, interbedded with brown clay...................... 10 155
Tertiary(?):Sand, silty, clayey; contains pebbles .................................. 30 185Silt, clayey; interbedded with silty clay............................... 25 210Sand, silty; contains pebbles............................................. 4 214Gravel, sandy; contains cobbles......................................... 2 216Sand; contains pebbles...................................................... 8 224Silt and clay, buff; contains magnetite from 250-265ft........... _____41 265
D2-5-22ccd
[Drilled by contractor for the U. S. Geological Survey. Principal water-bearing zones, 7-25 ft and 90-165 ft. Depth to water, 7 ft]
Quaternary (fan alluvium):Loam, silty, light brownish-gray....................................... 3 3Gravel, sandy, calcareous; composed of subrounded
rnetamorphic and volcanic rocks ..................................... 22 25
200 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Table 33. Logs of wells and test holes Continued
Thickness (feet)
Depth (feet)
D2-5-22ccd Continued
Quaternary (fan alluvium) ContinuedGravel, sandy, silty...........................................................Gravel, silt, and sand; contains some cobbles........................Sand, silty, brown; contains pebbles.....................................Gravel, medium, sandy, silty..............................................Sand, silty, brown; contains pebbles......................................Gravel, sandy, silty..........................................................
Note: Fragments of volcanic rocks are more numerous thanthose of metamorphic rocks from 3 to 125 ft.
Gravel, silty, interbedded with sandy gravel; basal 5 ft arenotably micaceous; gravel is composed chiefly of fragmentsof metamorphic rocks, but contains some fragments ofvolcanic rocks................................................................
Tertiary(?):Silt, sand, and clay, buff-gray. Sand contains well-rounded
quartz grains.................................................................Gravel, sandy, silty..........................................................Sand, very fine to fine, silty ...............................................Clay and silt, buff to gray; contains rounded pebbles...............Gravel, fine, silty, sandy ..................................................Silt and sand; contains cobbles.............................................Gravel, silty; contains cobbles ............................................Sand, fine, interbedded with sandy gravel..............................Silt, sandy at top, clayey near base, light-brown....................Sand, silty, fine; contains lenses of clay. Sand is composed
of spherical quartz grains and a large amount of magnetite.... Sand, very fine to medium, calcareous, dark-brown; contains
magnetite and well-rounded quartz grains ...........................Tertiary:
Silt, sandy, calcareous; interbedded with clay light-brown;contains some fragments of light-brown calcareous tuffaceoussiltstone, also silicified wood fragments at 377 ft.................
Silt, sandy; interbedded with cream-colored marl; containssome tuffaceous siltstone..................................................
Siltstone, sandy, calcareous, tuffaceous, buff........................Clay, light-brown; contains silicified bone fragments ..............Siltstone, sandy, calcareous, tuffaceous, buff; interbedded
with light -brown clay.......................................................Silt, tuffaceous; intermixed with clay ....................................Siltstone, sandy, calcareous, tuffaceous, buff; contains
some pebbles of red and black volcanic rocks.......................Bentonite(?), tan to light-brown......................................... ...Silt, tan; interbedded with thin layers of marl.........................Silt, slightly tuffaceous, tan.................................................Silt, slightly tuffaceous, tan; interbedded with thin layers
of clay...........................................................................Silt, slightly tuffaceous, tan.................................................Siltstone, sandy, calcareous, tuffaceous, buff.........................Sandstone, poorly sorted, calcareous ....................................Volcanic ash, pure, grayish-buff..........................................Sandstone, calcareous; contains pebbles ................................Siltstone, sandy, calcareous, tuffaceous, buff........................Siltstone, sandy, calcareous, tuffaceous, buff; interbedded
with thin layers of clay.....................................................Siltstone, calcareous, tuffaceous, buff; contains pebbles...........Sand, silty, poorly sorted, subangular; contains pebbles and
much magnetite...............................................................Siltstone, sandy, calcareous, tuffaceous, buff.........................Siltstone, clayey, calcareous, tuffaceous, buff........................
2515
916
530
40
334
1315
522
83038
25
12
55
3022
5
3014
7027
30
53019
317
20
3544
47
55
5065749095
125
165
198202215230235257265295333
358
370
425
455 477 4B2
512526
596598605635
640670689692693700720
755799
803810865
BASIC DATA 201Table 33. Logs of wells and test holes Continued
Thickness Depth (feet) (feet)
D2-5-22ccd Continued
Tertiary ContinuedTuff, silicified, grayish.....................................................Volcanic ash, light-gray...................................................Sand, fine to coarse, poorly sorted, silty, calcareous, dark-
brown. ........................................................................Silts tone ........................................................................Volcanic ash, pure ..........................................................Clays tone .......................................................................Sand/ poorly sorted, silty, calcareous, dark-brown; contains
pebbles.......................................................................Silt and clay, sandy, tan; contains pebbles...........................Sand and gravel, subangular; composed chiefly of fragments
of volcanic rocks ..........................................................Silt and clay, sandy, tan, slightly tuffaceous; contains pebbles..
D2-5-35dc
[Drilled by commercial driller]
Gravel, loos e.................................................................Gravel and some sand........ ..............................................Gravel...........................................................................Gravel and sand..............................................................Sand...................... .......................................................Hardpan, clay, and sand streaks........................................Sand and silt, yellow........................................................Clay..............................................................................Sand..............................................................................
D2-6-7-ac
[Drilled by commercial driller] Soil...............................................................................Boulders........................................................................Clay, yellow...................................................................Boulders........................................................................Clay..............................................................................Gravel...........................................................................Clay...............................................................................Gravel............................................................................Clay...............................................................................Gravel....................................... .....................................Shale.............................................................................Gravel............................................................................Clay...............................................................................Gravel............................................................................Clay...............................................................................Sands tone, ha rd ...............................................................Shale..............................................................................Boulders and conglomerate ................................................Shale, tough....................................................................Conglomerate ..................................................................Shale, tough....................................................................Boulders and conglomerate ................................................Shale, tough ....................................................................C onglome rate ..................................................................Shale..............................................................................Conglomerate ..................................................................
45
1342
867869
890891892
900945
958,000
301020301040843
30406090
100140148152155
71436323471
1159
15341140198
101321143842
721243033353842495061667590
124135175194202212225246260298302304
508919 O-60 14
202 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Table 33. Logs of wells and test holes Continued
Thickness (feet)
Depth (feet)
D2-6-7da
[Drilled by commercial driller]
Clay............................................................................... 25 25Gravel............................................................................ 15 40Clay and some sand. Water ............................................... 48 88Gravel. Water................................................................. 9 97Clay............................................................................... 7 104Gravel. Little water......................................................... ?__ 104+
D2-6-10dc
[Drilled by commercial driller]
Soil, black....................................................................... 9 9Sand and gravel................................................................ 12 21Sand, gravel, and silt........................................................ 8 29Red material [clay(?)]. No water ........................................ ______3 32
D2-6-18db
[Drilled by commercial driller]
Gravel............................................................................ 13 13Clay. No water................................................................ 19 32Gravel. No water............................................................. 6 38Hardpan. Some water........................................................ _____17 '55
D2-6-19aal
[Drilled by commercial driller]
Clay, sandy..................................................................... 51 51Sand...............................................................................______7 58
D2-6-19aa2
[Drilled by commercial driller]
[Tertiary(?)]:Silt................................................................................ 19.5 19.5Gravel............................................................................ 10.5 30Silt, brown; some sand and gravel....................................... _____70 100
D2-6-19cbl
[Drilled by commercial driller]
Topsoil........................................................................... 7 7Gravel............................................................................ 5 12Sand, soft, yellow ............................................................. _____68 80
.D2-6-19cb2
[Drilled by commercial driller. Samples examined by U. S. Geological Surveypersonnel]
[Quaternary (alluvium)]:Clay............................................................................... 11 11Gravel............................................................................ 10 21Silt and fine sand, light-brown; some clay. Little water.......... 104 125
[Tertiaryf?)]:Silt, calcareous, tan; some sand and fragments of claystone.
No water...................................................................... 11 136Silt and clay, calcareous, buff; contains some sand and a few
fragments of marl and buff claystone. Little water ............. 18 154Sand, silty, buff; contains pebbles........................................ 1 155
BASIC DATA
Table 33. Logs of wells and test holes Continued
203
Thickness (feet)
Depth (feet)
D3-4-26ba2
[Drilled by commercial driller]
Gravel and boulders. No water...................................Clay, soft, pinkish. No water .....................................Clay, hard. No water................................................Silt and clay, buff ("Lake beds").................................,
D3-4-34aa
[Drilled by commercial driller]
Rock and gravel.......................................................Clay, soft [probably Tertiary]....................................,Gravel....................................................................
D3-6-6ddl
[Drilled by commercial driller]
Gravel....................................................................Quicksand, gray.......................................................Sand.......................................................................
17322
94
174951
145
414
15
414560
20145
3
20165168
204 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Table 34. Water-level measurements by tape, in feet below land-surface datum
Date Water level
Date Water II level 1
Date Water level
Al-3-2cdc2
July 31, 1951.......Aug. 28...............Sept. 26. ..............Nov. 1..... ..........Dec. 3...............
Feb. 6...............
Apr. 4...............May 5...............
3. 814. 935. 655. 566. 568. 73
11. 8013. 9813. 8615.07
Aug. 5.............
Oct. 3.............
Jan. 7, 1953....
Mar. 4.............
5. 193.024. 614. 785. 126.007. 288.66
12. 1313.43
Apr. 1, 1953.....May 8.............
July 2.............Aug. 4.............Sept. 1...... .......Oct. 2.............
Dec. 1.............Jan. 5, 1954.....
14. 3113. 864.464. 003.615. 016. 966. 207.42
10. 74
Al-3-4da
May 21, 1951.......May 31...............July 5...............Aug. 2...............Aug. 28.. .............Sept. 26...............Nov. 2...............Jan. 7, 1952.......Feb. 6...............
Apr. 4...............May 5...............
32. 8530. 9411.058.669.59
14. 3620.6128. 0129. 5932.0331. 3032.40
June 9, 1952....June 26.............July 31.............Sept. -3.............Oct. 1.............Nov. 17.............Dec. 2.............
Feb. 2.............Mar. 4.............
May 8.............
21.4614. 2113. 2711.0713. 1619.0921. 5425. 8228.6630.5931. 8230. 98
June 2, 1953.....July 2.............Aug. 3.............Sept. 2.............Oct. 1. ............Nov. 5.............Dec. 1.............Jan. 5, 1954.....Feb. 3.............Mar. 3.............Apr. 1.. ...........
18. 5612. 387.63
11.0613.9318.0721.4825. 2927. 7029. 7731.23
Al-3-9bbb
Apr. 24, 1951....... May 31.. .............July 5...... .........Aug. 2...............Aug. 28..............Sept. 26...............Nov. 2...............
Jan. 7, 1952.......Feb. 6...............
64. 71 65. 3154. 7944. 8544.4448.0953. 6156. 8257.4157. 22
Mar. 5, 1952....
June 28.............Aug. 1.............Sept. 3.............Oct. 1.............Feb. 2, 1953....
Apr. 1.............
58. 21 65. 8462. 7154.0846. 0847.2145.4260.4862. 2463.68
May 8, 1953.... June 2 ... .........July 2.............Aug. 3.............Sept. 2.............Oct. 1.. ...........Nov. 5.............
Jan. 5, 1954.....
62. 80 58. 1051.0245. 1843.4144. 5048. 8451. 7255. 72
Al-3-10bd
Sept. 24, 1952.:..... Feb. 2, 1953.......
Apr. 1...............May 1 ...............
2. 81 6. 216.987. 388.05
June 1, 1953.... July 2.............
Sept. 1.............
4.75 2.982.633.05
Oct. 1, 1953..... Nov. 5.............
Jan. 5, 1954....
2. 58 3.423. 955. 17
Al-3-12aa
Aug. 26, 1952....... Sept. 1. ..............Oct. 1.. .............Nov. 1.......... .....Nov. 25...............Jan. 1, 1953.......
3. 56 3. 243. 323. 142. 742. 62
Feb. 4, 1953....
May 8............
July 2............
2. 75 2.662. 642. 581. 961. 64
Aug. 4, 1953..... Sept. 4.............Oct. 2.............Nov. 4.............Dec. 1.............Jan. 4, 1954....
3. 27 3. 213.423. 032. 613.70
BASIC DATA 205
Table 34. Water-level measurements by tape, in feet below land-surface datum Cont.
Date Water level
Date Water level
Date Waterlevel
Al-3-23bb
Aug. 2, 1951.......Aug. 28................Sept. 26................Nov. 2...... .........Dec. 3...... .........Jan. 7, 1952.......Feb. 4...............Mar. 5...............Apr. 4...............
0.40.30. 17
.39
May 5, 1952....
June 28.............Aug. 1...... .......Sept. 3.............Oct. 1.............Feb. 2, 1953....Mar. 4.............Apr. 1.............
0.411. 281.43.63.61. 75.72.65. 62
May 1, 1953....
July 2............Aug. 3............Sept. 2............Oct. 1. ...........Nov. 5............Dec. 2............Jan. 5, 1954...
0.60. 74. 59.94.66.65. 51.46. 58
Al-3-26cdl
June 27, 1951.......July 5...............Aug. 2...... .........Aug. 28...............Sept. 26.. .............Nov. 2...............Dec. 3...... .........Jan. 7, 1952.......Feb. 4...... .........
Apr. 4...... .........
5. 765. 785. 735. 655. 545. 666. 026. 466. 546. 645.74
May 5, 1952....
June 28............Aug. 1.. ......... .Sept. 3.............Oct. 1.... .........Nov. 17.............Dec. 3.............Jan. 2, 1953....,Feb. 2.............Mar. 4.............
6.035. 967.946.046. 206. 226.486. 516. 676. 506.73
Apr. 1, 1953....May 1. ...........
July 2............Aug. 3............
Oct. 1.. ..........Nov. 5............Dec. 2............Jan. 5, 1954....
6.636.686. 155. 825.985.956. 386. 326.356.43
Al-4-3bb
Apr. 24, 1951....... May 31...... .........July 5...............Aug. 2...............Aug. 28...............Sept. 26...............Nov. 3...............Dec. 3.. .............Jan. 8, 1952.......Feb. 6...............Mar. 5...............
19.45 19. 7712.6110. 5410.6715.4917. 2618. 2618.6319. 2519. 95
Apr. 4, 1952.... May 6.............
Aug. 5.............Sept. 1....... ......Oct. 3.............Nov. 17.............Dec. 3.............Jan. 7, 1953.....Feb. 4.............
19.6017.7415. 739.688. 198. 63
12. 5416. 5116.8517.9218.91
Mar. 5, 1953.... Apr. 2............May 8............
July 2............
Sept. 1............Oct. 2............
Dec. 1.. ..........Jan. 4, 1954....
19. 10 20.0220. 9020.349.64
10. 598.698.59
13.0516.0417.94
Al-4-5ad
May 31, 1951....... July 5...............Aug. 2................Aug. 28................Sept. 26................Nov. 3................Dec. 3................Jan. 8, 1952.......Feb. 6...............Mar. 5................Apr. 7................
3.36 3. 272. 653. 082. 852. 692. 702. 813.393. 582.45
May 6, 1952....,
June 26.............Aug. 5.............
Oct. 3.............Nov. 17.............Dec. 3.............Jan. 7, 1953.....Feb. 4.............Mar. 5.............
3.23 3. 19
2.813.403.483.553. 63
3.433. 64
Apr. 2, 1953....
July 2............Aug. 1. ...........Sept. 4............Oct. 2............
Dec. 1.. ..........Jan. 4, 1954....
3. 56 3. 523. 483.092.793.053.312. 952. 973. 39
Al-4-5ba
July 5, 1951....... Aug. 2.. .............
2.99 3. 71
Aug. 28, 1951.... 3.68 Sept. 26, 1951.... 3.03
Al-4-5da
[No measurements by tape; for measurements from recorder chart, see table 35]
206 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Table 34. Water-level measurements by tape, in feet below land-surface datum Cont.
Date Water level
Date Water level
DateWater level
Al-4-6ab
May 31, 1951.......
Aug. 2...... .........
Sept. 26...............Nov. 3...............
Jan. 8, 1952.......Feb. 6. ..............Mar. 5...............Apr. 4...............
5. 904.675.074.664. 224.404. 945. 125. 175. 265.18
May 6, 1952....
June 27.............
Sept. 3.............Oct. 3.............Nov. 17.............Dec. 3.............Jan. 7, 1953....Feb. 4............Mar. 5.............
4.634.674.483. 124.073.453. 744.615.865.405.82
Apr. 3, 1953...May 8...........
July 2...........Aug. 4...........Sept. 4...........Oct. 2............Nov. 4............Dec. 1.. ..........Jan. 4, 1954...
5. 215. 165. 374.493.823. 884. 755. 385.845.90
Al-4-6bc
Aug. 9, 1951.......Aug. 28...............Sept. 26.. ........... .Nov. 2.. .............Dec. 3...... .........Jan. 8, 1952.......Feb. 6...............
Apr. 3...............May 6...............
5. 977. 739.41
10.0010. 1610. 2110.4310. 51
9. 749.88
June 9, 1952....Aug. 5.............Sept. 3.............Oct. 3.............Nov. 17.............Dec. 3.............Jan. 7, 1953....Feb. 4.............Mar. 5.............Apr. 3.............
8.834.827.829. 57
10.3710.3210.4810.3810.5510.37
May 8, 1953...
July 2............Aug. 4............Sept. 4............Oct. 2............
Jan. 4, 1954...
10.2810.07
2. 014.577.028. 819.83
10. 2410.42
Al-4-7aa
May 31, 1951....... July 5...............Aug. 2...............
Sept. 26................Nov. 2. ...............Dec. 3................Jan. 8, 1952.......Feb. 6................Mar. 5............... Apr. 7...............
2.02 3. 543.422.523. 5.13. 784.254. 29
Frozen 3. 97
May 6, 1952.....
June 26.............
Sept. 1.... .........Oct. 3.............Nov. 17.............
Jan. 7, 1953.....Feb. 4............. Mar. 5.............
4.40 4.301. 103.021. 853.232. 754.324.954. 74 4. 98
Apr. 2, 1953...
July 2.. ..........
Oct. 2............
Dec. 1. ...........Jan. 4, 1954....
4. 60 4.40
.594.411.734. 874. 314. 143.804. 80
Al-4-8ba
May 31, 1951....... July 5...... .........Aug. 2................Aug. 28................Sept. 26................
0. 64 . 18
2.72.39. 21
Nov. 2, 1951.... Dec. 3.............Jan. 8, 1952....
Mar. 5.............
Frozen FrozenFrozenFrozenFrozen
Apr. 7, 1952.... May 6............
Oct. 3............
0.46 2. 162 422.28
Al-4-10aa
July 6, 1951....... Aug. 2................Aug. 28................
Nov. 1.. .............Dec. 3................Jan. 7, 1952.......Feb. 6................Mar 5...... .........Apr. 1. ......... .....May 6...... .........
3.32 3. 303.022.963.722.703. 183.073.272. 912.31
June 6, 1952.....
Oct. 3.............Nov. 17.............Dec. 3..............Jan. 7, 1953.....Feb. 4.............
2.72 3. 243. 503.323.493. 613. 223.313.083. 27
Apr. 3, 1953....
July 2............
Oct. 5............
Jan. 4, 1954....
3.24 3. 181. 873.223. 383. 223. 363.052. 993. 12
BASIC DATA 207
Table 34. Water-level measurements by tape, in feet below land-surface datum Cont.
Date Water level
Date Water level
Date Water level
Al-4-13ad
May 31, 1951......July 6.. ............Aug. 2..............Aug. 29...............Sept. 26.......... ....Nov. 1.. .............Dec. 3...............Jan. 8, 1952......Feb. 6...............Mar. 5...............Apr. 2...............
2.503. 793. 943. 293. 323.433. 393. 683. 763. 823.32
May 6, 1952....
June 27.............Aug. 4.............Sept. 2............Oct. 3............Nov. 17............
Jan. 5, 1953....Feb. 4............Mar. 5............
1.021.322.933. 563.393.463. 493.403. 643. 533. 64
Apr. 1, 1953...
July 2............Aug. 5............Sept. 4............Oct. 2............
Dec. 2............Jan. 4, 1954...
3.563. 361. 103.043. 643.433. 513.373. 373.59
Al-4-15ba
July 6, 1951......Aug. 2...... ........Aug. 28.. .......... .Sept. 26...............Nov. 1..............Dec. 4...............Jan. 7, 1952......Feb. 6..............Mar. 5.. ............Apr. 7..............May 6.. ............
5.435. 355.344. 954. 564. 48
4.444.613. 704. 28
June 6, 1952....June 27.............Aug. 5............Sept. 3............Oct. 2............Nov. 17............
Jan. 7, 1953....Feb. 4............Mar. 5............
4.464. 915.085. 225.085. 004.694. 574.234.42
Apr. 2, 1953...May 8...........
July 2...........Aug. 4...........Sept. 4............Oct. 5............
Jan. 4, 1954...
4. 264.093. 615.075. 245. 205. 124. 894. 744. 79
Al-4-15dal
July 6, 1951...... Aug. 2..............Aug. 28...............Sept. 26...............Nov. 1. ..............Dec. 3...............Jan. 7, 1952.....Apr. 7...............May 6.. ............June 6 ...... ........
3. 81 3. 573. 122.902.742. 742. 932. 263. 303.38
June 27, 1952.... Aug. 5............Sept. 3............Oct. 2............Nov. 17............
Jan. 7, 1953....Feb. 4............Mar. 5.............Apr. 2.............
3. 15 3.493. 203. 113. 283.003. 153.043. 243. 31
May 8, 1953...
Aug. 4............Sept. 4............Oct. 5............Nov. 4............
Jan. 4, 1954...
3. 26 2.282. 583.513. 23^ 17
3.043.093. 23
Al-4-15da2
May JuneJuly
20, 1953...... 4..............2...............
4. 23
64 RO08
Aug. Sept.Oct.
4, 1953.... 4............5............
3 33
74 5142
Nov.
Jan.
4, ?4,
1953. ..I
1954...]
3. 31 3. 333. 48
Al-4-16bb
July 6, 1951...... Aug. 2...............Aug. 28...............Sept. 26...............Nov. 1.......... ....Dec. 4...............Jan. 8, 1952......Feb. 6...............Mar. 5...............Apr. 7...............
3.40 3.453. 123. 243. 113.083. 783.904.012. 11
May 6, 1952.... June 27............Aug. 5............
Oct. 2............Nov. 17............Dec. 2............Jan. 7, 1953....Feb. 4............Mar. 5............
2. 99 3.663.693.233.053.382.412.963.063. 84
Apr. 2, 1953...
July 2............Aug. 4............
Oct. 5............
Jan. 4, 1954...
3. 42 3. 382.473.453. 113.064.003.783.964.02
208 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Table 34. Water-level measurements by tape, in feet below land-surface datum Cont.
Date Water level
Date Water level
Date Water level
Al-4-21dc
July 6, 1951......Aug. 2..............Aug. 28...............
0.82. 80.64
Sept. 26, 1951....Nov. 1.... ........Aug. 5, 1952....
1. 88.51
1. 13
Oct. 2, 1952...Aug. 6, 1953...
1. 181. 62
Al-4-22dcl
[Depth to water Aug. 7, 1951, 3.98 ft. No other measurements by tape; for measurements ________ __ from recorder chart, see table 35]
Al-4-22dd
July 6, 1951.......Aug. 2...............Aug. 28...............Sept. 26 ...............Nov. 1 ...............Dec. 3 ...............Jan. 8, 1952.......Feb. 6...............
May 6 ...............
4. 534.083.633. 744. 375. 136.426. 585. 976. 76
June 6, 1952....June 27 ............Aug. 5............Sept. 3............Oct. 2.... ........Nov. 17............
Jan. 7, 1953....Feb. 4............Mar. 5 ............
5. 194.494.083.893. 994.314.675.756.267.03
Apr. 2, 1953...May 8...........
July 2...........
Sept. 4...........Oct. 5...........
Dec. 2...........Jan. 4, 1954...
7. 397. 134.474. 894. 244. 124. 254. 374. 845. 72
Al-4-24dc
July 6, 1951...... Aug. 2 ..............Aug. 29..............
3.943. 693. 19
Sept. 26, 1951....Nov. 1 ............
3. 163.34
Dec. 3, 1951... 3.745.41
Al-4-25bd
July 6, 1951.......
Aug. 29...............Sept. 26 ...............Nov. 3...............Dec. 3...............Jan. 8, 1952.......Feb. 6 ...............Mar. 5 ...............Apr. 1 ...............May 2 ...............
3. 19 2.662.342.492. 934. 135.416. 797.617.436.92
June 2, 1952.... June 27 ............Aug. 1 ............Sept. 3 ............Oct. 3............Nov. 17............Dec. 3 ............Jan. 2, 1953....Feb. 4............Mar. 5 ............
5. 68 2. 992. 292.722.993.313. 895. 166. 177. 26
Apr. 1, 1953...
July 2...........Aug. 5...........Sept. 4...........Oct. 2...........
Dec. 1. ..........Jan. 4, 1954...
7.54 7.403.683. 262.432. 632. 982. 913.465.07
Al-4-25dc
[No measurements by tape; for measurements from recorder chart, see table 35]
Al-4-29ab
July 6, 1951....... Aug. 2...............Aug.- 28 ........... ...Sept. 26 ...............Nov. 1. ..............Dec. 3...............Jan. 8, 1952....... Feb. 6...............Apr. 3 ...............May 5...............
3. 28 2. 982. 282.592. 923.313.97 4. 164. 164. 16
June 10, 1952.... June 26 ............Aug. 5............Sept. 3 ............Oct. 2............Nov. 17............Dec. 2 ............Jan. 7, 1953....Feb. 3............
4. 55 4. 744.614.644. 434. 58 4. 67 5.015. 195.40
Apr. 3, 1953... May 1 ...........
July 2...........Aug. 6...........Sept. 4...........Oct. 5........... Nov. 5...........Dec. 2...........Jan. 4, 1954...
5.41 5.414.324.434. 214.094.07 4.094. 544.63
BASIC DATA 209
Table 34. Water-level measurements by tape, in feet below land-surface datum Cont.
Date Water level
Date Water level
Date Water level
Al-4-36dc
June 27, 1952......Aug. 4.. ............
29. 6426.47
Sept. 2, 1952....Sept. 29 ............
26.4226.31
Nov. 12, 1952...Dec. 3...........
28. 1129. 65
Al-5-5da
May 28, 1951......July 6 ..............Aug. 2..............Aug. 28..............Sept. 29..............
6. 166. 647. 107. 177.84
Nov. 2, 1951....Dec. 4............Jan. 11, 1952....May 6 ............June 2 ............
8.088.368. 525. 745.76
June 29, 1952...Aug. 1.. .........Aug. 27...........Oct. 3...........
6.747. 548.008. 10
Al-5-6bd
May 14, 1951......May 31..............July 6..............Aug. 2..............Aug. 29..............Sept. 26..............
33. 7833.6733.2932. 9633. 6434. 34
Nov. 1, 1951....
Jan. 7, 1952....Feb. 6............
Apr. 7............
34.9434.4234. 7234.9135.6334. 60
May 6, 1952...
Aug. 4...........
Oct. 3...........
30.4430. 5431. 1931.7832.9033.41
Al-5-6cc
May 15, 1951......May 31 ..............July 6..............Aug. 2..............Aug. 29..............Sept. 26..............Nov. 1. .............Dec. 3...............Jan. 11, 1952......Feb. 6..............Mar. 6 ..............
22.2221. 9022. 1022. 5621. 9623.0022. 9222. 6122. 7322. 9223. 21
Apr. 7, 1952....May 6 ............
Sept. 1 ............Oct. 3............Nov. 17............Dec. 3............Jan. 5, 1953....Feb. 2............
22. 8021.5420. 9021.0920. 5920. 8021.9222. 1422. 3021.0021.07
Mar. 3, 1953...Apr. 1.. .........May 8...........
July 2...........Aug. 5...........
Oct. 5...........Nov. 5...........Dec. 2...........Jan. 4. 1954...
21. 8821. 7321.6821.0622. 1521. 1921. 6221. 9121. 7721.8321.02
Al-5-8ad
May 29, 1952....... June 29...............Aug. 1.. .............Oct. 3...............Feb. 2, 1953.......Mar. 3 ...............
9. 19 9. 75
10. 1710.4010.4110. 50
Apr. 3, 1953....
July 2............Aug. 5............
10.47 10.4510. 209.97
10.00
Sept. 4, 1953... Oct. 1.... .......Nov. 5...........Dec. 3...........Jan. 4, 1954...
10. 21 10. 9410. 1410.6410. 71
Al-5-16bcl
Aug. 2, 1951....... Aug. 28...............Apr. 1, 1952.......May 1 ...............
June 29 ...............Aug. 1.. .............Sept. 3...............
12. 89 14. 2915.6111. 189.759. 819.30
10.03
Oct. 3, 1952.... Nov. 17............Dec. 3 ............
Feb. 2............Mar. 5............Apr. 3 ............May 8............
11. 10 12. 7213. 1012.9813. 1114.0814. 2513.98
June 4, 1953... July 2...........Aug. 5...........
Oct. 1. ..........Nov. 5...........Dec. 3...........Jan. 4, 1954...
13.68 13. 2012. 7412.9312. 9313. 5613. 8114.06
210 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Table 34. Water-level measurements by tape, in feet below land-surface datum Cont.
Date Water level
Date Water level
Date Water level
Al-5-19bc
July 6, 1951.......Aug. 2...............Aug. 29 ...............
Nov. 1 ...............
Jan. 8, 1952.......Feb. 6...............Mar. 5 ...............
May 2...............
2.842.632. 141.931.922.292. 582. 772.862.632. 54
June 6, 1952....
Oct. 3............Nov. 17............
Feb. 4............Mar. 5............
2.642.632.532. 282. 182.232.172. 712.672. 76
Apr. 1, 1953...May 8...........
July 2...........
Sept. 4...........Oct. 2...........
Dec. 2...........Jan. 4, 1954...
2. 752. 702.402.582.412. 142.082.002. 202. 55
Al-5-21bc4
Dec. 4, 1951.......Apr. 1, 1952.......May 1. ..............
7.758.425. 39
June 2, 1952....
Aug. 1 ............
3. 944. 534. 98
Sept. 3, 1952...Oct. 3...........
5. 115.49
Al-5-26cd
Sept. 28, 1951.......Dec. 3 ...............Jan. 8, 1952.......Feb. 6...............
6. 526.366. 526.53
Mar. 5, 1952....Apr. 1 ............
June 2 ............
6. 616. 556. 146. 16
June 29, 1952...Aug. 1 ...........Sept. 2...........Sept. 29 ...........
6.496. 766.566.62
Al-5-30dd
July 7, 1951...... Aug. 2...............Aug. 29 ..............Sept. 26 ..............Nov. 3..............Dec. 3..............Jan. 8, 1952......Feb. 6...............Mar. 5...............Apr. 1 ...............May 6. ...............
2.68 2.652.292. 152.142.292.482. 783. 192. 812.21
June 6, 1952....
Aug. 1 ............
Oct. 3............Nov. 10 ............
Jan. 2, 1953....Feb. 4............
2.16 2.402.432. 172. 132.032. 182.632. 703.08
Apr. 2, 1953... May 8...........
July 2...........Aug. 4...........Sept. 4...........Oct. 2...........
Jan. 4, 1954...
2.94 2.861.432. 522. 562.292.352.282.412. 70
Al-5-35aa
Sept. 28, 1951....... Dec. 3 ...............Jan. 8, 1952.......
12.45 11.3311. 54
May 1, 1952....
June 29 ............
8.22 8.07
10.03
Aug. 1, 1952... Sept. 2...........Sept. 29...........
10. 82 10. 5410.05
Al-5-35ca
May 28, 1951...... Aug. 28..............Sept. 26 ..............Nov. 11..............Dec. 3..............Jan. 8, 1952......Feb. 6..............Mar. 5..............Apr. 1 ..............May 1 ..............
8.39 11.4911. 5911.3111.6811. 9112.2512. 5212.634.47
June 2, 1952....
Aug. 1 ............Sept. 2............
Nov. 11 ............
Jan. 2, 1953....Feb. 2............Mar. 3............
5.78 7.608.408. 518.238.098.208.438.388. 74
Apr. 1, 1953...
July 1. ..........Aug. 1.. .........Sept. 1.. .........Oct. 1. ..........
Dec. 1.... .......Jan. 4, 1954...
8. 19 8. 387. 287. 748.769. 239.259. 159.249.37
BASIC DATA 211
Table 34. Water-level measurements by tape, in feet below land-surface datum Cont.
Date Water level
Date Water level
Date Water level
A2-3-33da
[No measurements by tape; for measurements from recorder chart, see table 35]
A2-3-36ac
Aug. 9, 1951....... Aug. 29...............Sept. 26...............Nov. 2...............Apr. 3, 1952.......May 6 ...............June 9 ...............
7. 38 7. 518. 008. 526. 877.307.06
June 27, 1952.... Aug. 5............Sept. 3............Oct. 3............Feb. 4, 1953....
Apr. 3 ............
7.54 7.808.068. 188.068. 258.08
May 8, 1953...
July 2...........Aug. 4...........Sept. 4...........
7. 99 7. 827. 637. 707. 828.06
A2-4-2dd
May 28, 1951......July 5..............
Aug. 29..............Sept. 29..............Nov. 2..............Dec. 4 ..............
10.9611.0111.0110. 8111.0510.9811. 27
Jan. 11, 1952....Feb. 6............
Apr. 2 ............
June 28 ............
11. 1611.2211.2610. 5610.2610. 6810.64
Aug. 4, 1952...Sept. 2...........Oct. 1. ..........Nov. 10...........Dec. 1. ..........Jan. 5, 1953...
11. 1211.0811. 1111. 1711.2811.20
A2-4-12cc
May 15, 1951......May 31..............July 5..............Aug. 2..............Aug. 29..............Sept. 29..............Nov. 3..............
6.476. 827. 117. 307.277.066.79
Dec. 4, 1951....Jan. 11, 1952....Feb. 6............Mar. 6 ............Apr. 2.............May 2............June 9 ............
6.386.436. 786. 826. 155.215.68
June 28, 1952...Aug. 4...........Sept. 2...........Oct. 1.. .........Nov. 10...........Dec. 1.. ........Jan. 5, 1953...
5.976.375.876. 155.915. 586.09
A2-4-23da
May 14, 1951....... May 31...............July 5...............Aug. 2...............Aug. 29 ...............Sept. 29...............Nov. 3...............Dec. 4 ...............Jan. 11, 1952.......Feb. 6...............Mar. 6 ...............
13. 58 14.0014.4114. 8014. 7714.5414.6014. 8814. 5315.1215.33
Apr. 2, 1952.... May 2............
June 28............Aug. 4 ............Sept. 22............Oct. 1.... ........Nov. 10............
Jan. 5, 1953....Feb. 2............
14.39 13. 1013.6013. 8714.4415.0414.7914.4613.9214.6614.64
Mar. 3, 1953... Apr. 1...........May 2...........
July 2...........Aug. 1.... .......Sept. 1. ..........Oct. 1.... .......
Dec. 1.. .........Jan. 4, 1954...,
14. 85 14.5814.4913. 5513.8714.7015.0014. 8715.0615.0515.03
A2-4-24bb
May 15, 1951....... May 31...............July 5...............Aug. 2...............Aug. 29...............
36. 17 33.3732. 8629. 2231.65
Sept. 29, 1951.... Nov. 3............Dec. 4............Jan. 11, 1952....
36.85 32.0029.8830.73
Feb. 6, 1952... Mar. 6...........Apr. 2...........May 2...........
34.41 36.3136. 7635. 15
A2-4-26bal
May MayJuly
14, 1951....... 31...............5...............
20 2018
236006
Aug. Aug.Sept.
2, 1951..... 29.............29.............
18.841 18.0419.41
Nov. Dec.
3,3
11,
1951.....
1952.....
19 2019
97 4170
212 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Table 34. Water-level measurements by tape, in feet below land-surface datum Cont.
Date Water level
Date Water II level II
Date Water level
A2 -4 - 26ba 1 Continued
Feb. 6, 1952.......
Apr. 2...............
Sept. 2...............
20.2921.5121.0418.8019.2019.2018.7119.64
Oct. 1, 1952.....Nov. 10.............Dec. 1...... .......
Feb. 2.............
Apr. 1. ............May 2.............
20.0719.8019.4020.0020.8121.1521.0221.07
June 1, 1953...July 2...........Aug. 1.. .........Sept. 1...........Oct. 1...........
Dec. 1.. .........Jan. 4, 1954...
19.8618.6518.2819.3119.5819.8620.3320.71
A2-4-31cc
May 31, 1951.......
Aug. 2...............Aug. 28...............
Nov. 3...............
5.004.693.005. 146.856.81
Dec. 3, 1951....
Feb. 6............
A nr* *3
May 6 ............
DryDrv
6.446.46
June 9, 1952...June 27 ...........
Sept. 3...........Aug. 4, 1953...
6. 502. 113. 125.913.19
A2-4-36cc
May 15, 1951......May 31..............July 6..............Aug. 2..............
12. 9013. 1712.9312.71
Aug. 29, 1951....
Nov. 1.. ..........Dec. 3 ............
12. 8312.8712. 8112.84
Jan. 7, 1952...
Oct. 3...........
12. 8212; 2812.0812. 18
A2-5-6acl
May JulyAug.
Sept.
28, 1951...... 5..............2..............
29..............29..............
7. 7.7.7.7.
10 11291923
Nov.
May
2,4
11,61
1951....
1952....
7. 7.7.7.7.
13 ^1^44<?
05
June
Aug.Aug.
| Oct.
9, 1952... 28...........4..........
27...........3...........
7. 13 6. 777. 287.057. 19
A2-5-8bc
May 28, 1951...... July 5..............Aug. 2..............Aug. 28..............Sept. 29..............Nov. 3..............Dec. 4..............
24. 99 25. 9926.5-926. 3127.5527.5527.59
Jan. 11, 1952.... Feb. 6............
Apr. 7............May ] ............
June 29 ............
27.91 28.7829. 1728.8422.3423.7025.34
Aug. 4, 1952... Sept. 2...........Oct. 3...........Nov. 10...........Dec. 3...........
25. 02 24.3125.0922. 5325. 7826.80
A2-5-18ba
May 16, 1951...... May 31..............July 5.............Aug. 2..............Aug. 28..............Sept. 29 ..............
6.27 5.404.883.463.023. 32
Nov. 2, 1951.... Dec. 4 ............Jan. 11, 1952....Feb. 6............Mar. 6............Apr. 7............
3.74 5.545.735.825.915. 80
May 2, 1952...
Oct. 3...........
2.85 3.321 794. 183.024. 80
A2-5-18bc
May 16, 1951....... May 31...............July 5...............Aug. 2...............Aug. 28...............
8.12 7.738.309.078.80
Sept. 29, 1951..... Nov. 2.............
Jan. 11, 1952.....Feb. 6.............
8.45 8.819.099.188.29
Mar. 6, 1952.... Apr. 7............May 2............
June 28............
8.97 8.567.567.917.13
BASIC DATA 213
Table 34. Water-level measurements by tape, in feet below land-surface datum Cont.
Date Water level
Date Water level
Date Water level
A2-5-18bc Continued
Aug.Sept.
4, 1952....... 78
74^?n
Oct. 3, 1952..... 7 o n I
1NOV. 10, 1952... 7.65
A2-5-20ad
May 28, 1951......July 5..............Aug. 2..............Aug. 28..............Sept. 29..............Nov. 2..............
Jan. 11, 1952......
27. 8328.4128. 6628. 9128. 9329. 1029. 3329.4727.6325.33
June 29, 1952....Aug. 4 ............Sept. 2............Oct. 3............Nov. 10............Dec. 3............
Feb. 2............Mar. 3 ............Apr. 1. ...........
25.7626.3926. 9727.2127. 6227. 9328. 6228.4429.0328. 98
May 2, 1953...June 1 ...........July 2...........Aug. 1.. .........Sept. 1.. .........Oct. 1.. .........Nov. 5...........Dec. 1.. .........Jan. 4, 1954...
29. 2129.3928. 8626. 1326. 7326. 9827.4527.7228.32
A2-5-30bb
May 15, 1951......May 31 ..............July 5..............Aug. 2..............
76.0875. 9574. 8175. 80
Aug. 28, 1951....
Nov. 2 ............
75. 8475. 9876.0475. 74
Jan. 11, 1952...Apr. 7 ...........
Oct. 3.. .........
75. 8775.7575.6775.32
A2-5-33bd
May 28, 1951......July 6..............Aug. 2 ..............Aug. 28..............
12. 7116.6918.5620. 56
Sept. 29, 1951....Nov. 2............
Jan. 11, 1952....
20.0620. 9120. 8320.92
Feb. 6, 1952...Mar. 6...........
21. 5321. 7820.30
A2-5-35ba
May 14, 1951...... May 31..............July 5..............Aug. 2 ..............
13.0312.4713. 1313.48
Aug. 29, 1951....
Nov. 2............
12. 59 12. 7012.9313.09
Jan. 11, 1952... Apr. 4...........Oct. 1.. .........
13. 15 12. 7912.74
A3-5-28dd
May 15, 1951...... May 28 ..............July 5..............Aug. 2 ..............Aug. 28..............Sept. 29..............Nov. 2..............
27.67 23.0211. 7016. 8416. 9618.3819.21
Dec. 4, 1951.... Jan. 11, 1952....Feb. 6............Mar. 6 ............
23. 59 28.4630. 1430.7129. 8030.6815.31
June 28, 1952...
Oct. 1. ..........Nov. 10...........
14. 12 19 3420. 6322. 3219.3422. 1425. 33
Dl-4-lcb
July 28, 1952...... Aug. 4 ..............Aug. 18..............Sept. 2..............Sept. 10 ..............Sept. 29..............Oct. 7..............
39. 73 39. 5238.5438.0738. 1238.5939. 14
Jan. 7, 1953.... Feb. 3............
Apr. 3 ............May 8............
July 2............
50.71 54. 7358. 2661. 1460.0855. 1046. 35
Aug. 4, 1953...
Oct. 2...........Nov. 5...........Dec. 3...........
39.37Q 7 AC\
38. 1340.9843. 5849.04
214 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Table 34. Water-level measurements by tape, in feet below land-surface datum Cont.
Date Water level
Date Water || level J
Date Water level
Dl-4-2ab
May 8, 1951........
July 5................Aug. 2................
Nov. 1................rior* ^
Jan. 8, 1952........Feb. 5................TV/To R
Apr. 4................Apr. 11................Arty* 1 R
50. 7448. 1237 8433.9430. 1431. 1935.6840.7143. 1643.6345.4153.9853.0552.47
May 2, 1952....
July 9............July 18............July 28............
Aug. 18............
Sept. 2............Sept. 10............
Oct. 7............Nov. 17............
50. 9345. 3842.0536. 7534. 3033. 9033. 5432.2732. 1332.8232. 5332.6533. 3036.05
Dec. 2, 1952...Jan. 7, 1953...Feb. 3...........Mar. 4...........Apr. 3...........May 8...........June 4...........July 2...........Aug. 4...........Sept. 4...........Oct. 2...........Nov. 5...........Dec. 3...........Jan. 5, 1954...
38.4043. 8547.4550.4152.7352. 1137.8839. 8535. 7432. 8433. 7035. 8438.5143.07
Dl-4-6bb
May 9, 1951........May 31................
Sept. 26................Nov. 2................Dec. 5................Jan. 7, 1952........Feb. 6................
8.206.642. 743.434.815. 886.09
Dry
Mar. 5, 1952....
Oct. 3............Feb. 4, 1953....
DryDryDry
1.653.903. 154.075. 10
Dry
Apr. 1, 1953...May 8...........
July 2...........Aug. 6...........Sept. 4...........Oct. 5...........Nov. 5...........Dec. 2...........
8.007.605.692.844. 144.626.637.027.64
Dl-4-6ddcl
Aug. 9, 1951........Aug. 28................
Nov. 1 ................
Jan. 7, 1952........Feb. 6................
5.599. 19
10.4412. 7413.8517. 1517. 5319.2620. 5112. 59
June 9, 1952....June 28 ............
Sept. 3............Oct. 3............Nov. 17............Dec. 3............Jan. 2, 1953....Feb. 4............
3.005.495.605. 877.88
10.0013. 7214.8415.6116.92
Apr. 1, 1953...May 8...........
July 2...........Aug. 6...........Sept. 4...........Oct. 5...........Nov. 5...........Dec. 2...........Jan. 4, 1954...
18.0518. 6015. 315.207.697. 95
11.4411.9613. 2515. 18
Dl-4-6ddc2
[No measurements by tape; for measurements from recorder chart, see table 35]
Dl-4-9bal
[No measurements by tape; for measurements from recorder chart, see table 35]
Apr.May
MayJune
25, 1953........2................9................
16................23................6................
4.4.4.5.5.2.
576855230346
July&ug.A.ug.Aug.
Dl-4-9ba2
3, 1953......10..............24..............7..............
14..............21..............
2.3.3.3.4.4.
51415fi89?,f>4fi
Aug.
Oct.
28, 1953....4............
11............18............25............2............
444455
5738346905
.22
BASIC DATA 215
Table 34. Water-level measurements by tape, in feet below land-surface datum Cont.
Date Water level
DateWater level
Date Water level
Dl-4-9ba2 Continued
Oct. 8, 1953.......Oct. 15...............Oct. 29...............Nov. 12...............Nov. 20...............Nov. 25...............Dec. 2...............
Dec. 21...............
5.244.803.604.243.813.893.974.104.39
Dec. 28, 1953.....Jan. 4, 1954.....Jan. 11.............Jan. 21.............Jan. 27.............Feb. 3.............Feb. 10.............Feb. 17.............
4.414.414.674.684.184.444.764.67
Feb. 24, 1954...Mar. 3...........Mar. 10...........Mar. 24...........Mar. 31...........Apr. 7...........Apr. 13...........Apr. 22...........
4.694.844.775.045.294.884.915.16
Dl-4-12bb
Apr. 24, 1952.......June 10...............
July 18...............
Aug. 5...............Aug. 18...............Aug. 27...............
66. 7045.4840.8234.6431.7031.7031.3729.4828.64
Sept. 3, 1952....
Nov. 7............Nov. 12............Dec. 3............Jan. 6, 1953....Feb. 3............Mar. 5............
28.5028. 7131.0131.8737.3342. 5252.9556.5361. 86
Apr. 9, 1953...
July 2...........Aug. 5...........Sept. 4...........Oct. 23...........Dec. 3...........Jan. 4, 1954...
67.3565.7562.3634.5024.4823.6132.7238.5548. 10
Dl-4-13ad
July 28, 1952.......Aug. 5...............Aug. 18...............Aug. 27...............Sept. 2...............
Oct. 7...............
11.878.47
11.0010.4410.4310.4811.4413.52
Jan. 7, 1953....Feb. 3............
May 8............
July 9............Aug. 4............
36. 5943.7047. 80
+ 51. 8050.3145.7117. 9612.42
Sept. 9, 1953...Oct. 2...........Nov. 5...........Dec. 2...........Jan. 5, 1954...Feb. 3...........Mar. 3...........Mar. 31...........
13.3516.3221.2626.5934.5740.7046.3250.60
Dl-4-13bb
July 11, 1951.......Aug. 2...............
19.318.52
Aug. 28, 1951....Nov. 2............
10. 6116. 21
Dec. 4, 1951... 17.03
Dl-4-15ab
Apr. 23, 1952.......
June 28...............Aug. 6...............Sept. 8...............Oct. 3...............
22.93 13.333. 745.027.279.06
Feb. 4, 1953....
Apr. 3 ............
23. 78 24.0923.9026. 2420.905. 21
Aug. 5, 1953... Sept. 4...........Oct. 2...........
Dec. 2...........Jan. 6, 1954...
5.71 6.92
10. 1111.8614.6418.21
Dl-4-15cd
Apr. 23, 1951....... May 31...............July 6...............Aug. 1.. .............Aug. 30 ...............Oct. 1. ..............
7. 22 4. 913. 103.463.684. 12
Nov. 2, 1951.... Dec. 4............Jan. 7, 1952....Feb. 5............Mar. 6 ............Apr. 7............
4.41 5.285. 145.235.484.88
May 5, 1952...
June 28...........Aug. 6...........Sept. 8...........Oct. 10...........
8.01 5. 173.012. 765.296.50
216 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Table 34. Water-level measurements by tape, in feet below land-surface datum Cont.
Date Water level
Date Water level
Date Water level
Dl-4-17bb
July 13, 1951......
Aug. 30 ..............Oct. 1 ..............Nov. 2..............
Jan. 7, 1952......Feb. 5..............Mar. -7..............Apr. 7..............May 5..............
3.594.034.078.099. 10
11. 7814.6214. 9115.2315. 5217.90
June 9, 1952...,June 28 ............Aug. 6 ............Sept. 8............Oct. 3............Nov. 10............
Feb. 4............Mar. 4 ............
10.823.865. 914.437. 119. 249. 79
11. 3813.0415. 71
Apr. 3, 1953...May 4...........
July 2...........Aug. 6...........
Oct. 5...........Nov. 5...........Dec. 2...........Jan. 4, 1954...
15.9315.8617.0010. 124.034.767. 148.20
10.2412. 11
Dl-4-25aal
Apr. 18, 1951......May 31 ..............July 6..............Aug. 1 ..............Aug. 30..............Oct. 1.... ..........Nov. 2..............Dec. 4..............Jan. 7, 1952......Feb. 5..............Mar. 6 ..............
13.0011. 143. 854. 657.868.278.81
11.3911. 5211. 7411.91
Apr. 7, 1952....May 5............
June 27 ............Aug. 6 ............Sept. 4............Sept. 30 ............Nov. 10............Dec. 1 ............
Feb. 3............
11. 3611.05
5. 303.705. 618.049.61
11. 2912. 1013. 1113.48
Mar. 5, 1953...Apr. 3...........May 4 ...........
July 2...........
Sept. 9...........Oct. 2...........
Jan. 4, 1954...
15.4517. 1615.4610. 91
7. 635.098.539. 54
10. 1411.6713.34
*Dl-4-25aa2
[No measurements by tape; for measurements from recorder chart, see table 35]
Dl-4-25aa3 [No measurements by tape; for measurements from recorder chart, see table 35]
Dl-4-25bal
Apr. 19, 1951...... May 31..............July 6..............Aug. 1 ..............Aug. 30 ...............Oct. 1. ....... ......Nov. 2..............Dec. 4 ..............Jan. 7, 1952......Feb. 5..............
12. 85 8.291. 202.493.724. 246.308.929. 119.51
Mar. 6, 1952.... Apr. 7............May 5............June 24 ............
Aug. 6............
Feb. 3, 1953....Mar. 5 ............
9.72 18.5010.405.691. 613. 124. 186.08
13. 1214.27
Apr. 3, 1953...
July 2...........
Oct. 2...........Nov. 4...........Dec. 2...........Jan. 4. 1954...
15. 27 13.0410. 112.712.224.394. 856. 268.68
11. 14
Dl-4-26bbb
Aug. 1, 1951...... Aug. 30 ..............Oct. 1.. ............Nov. 2..............Dec. 4 ..............
3.40 4.864.985. 13Dry
Feb. 4, 1952.... Mar. 6 ............Apr. 7............
Dry Dry
June 4, 1952... June 27 ...........
Aug. 5, 1953...
5.65 3.323.803. 18
BASIC DATA 217
Table 34. Water-level measurements by tape, in feet below land-surface datum Cont.
Date Water level
Date Water level
Date Water level
Dl-4-27bb
Apr. 19, 1951......May 31..............July 6..............
Oct. 1... ...........Nov. 2..............
Jan. 7, 1952......Feb. 5..............Mar. 7 ..............
9. 528.338.228.459,36
10. 1710. 8110.4910.4410.5310. 72
Apr. 7, 1952....May 5............
June 28 ............Aug. 6............Sept. 8............Oct. 3............Nov. 10............Dec 1Jan. 2, 1953....Feb. 4............
7.259.353.938. 707.948. 259.238.939.82
10.4610.40
Mar. 4, 1953...Apr. 3...........May 4...........
July 4...........Aug. 1...........Sept. 2...........Oct. 5...........
Dec. 2...........Jan. 6, 1954...
10.5810.409.987.906.468. 158. 729.399. .48
10.2810.40
Dl-5-4dbl
Apr. 24, 1951......
July 5..............Aug. 1. .............
Sept. 26..............Nov. 1.. ............Dec. 3..............Jan. 8, 1952......Feb. 6..............Mar. 5 ..............
15.8011.8011. 969.69
10.9211.4912.6214.2514.4415.2415. 86
Apr. 4, 1952....
June 29............Aug. 1.. ..........Sept. 2............Sept. 29............Nov. 12............Dec. 3............Jan. 5, 1953....Feb. 2............
17.024. 135. 145.607. 108.078.449.61
10.1810.3612.03
Mar. 4, 1953...Apr. 2...........
July 2...........Aug. 4...........Sept. 4...........Oct. 2...........Nov. 5...........Dec. 3...........Jan. 5, 1954...
14.0415.0514. 726.447.216.817.538.569.21
11.2612.72
Dl-5-6dc
May 3, 1951...... May 31..............July 5..............Aug. 1 ..............
Sept. 26 ..............Nov. 1... ...........Dec. 3 ..............Jan. 8. 1952......Feb. 6..............
June 6 ..............
38. 15 37. 1129. 7124.8222.3421.0725.5427.2928. 8731. 2835.4429.42
June 27, 1952.... July 9............July 18............July 28............
Sept. 2............Sept. 10............Sept. 29............Nov. 7............Nov. 12............Dec. 3............Jan. 5. 1953....
24. .16 22. 7422.3021.8321.4420. 9721.0521. 2221. 2623.6925. 2230. 05
Feb. 2, 1953... Mar. 4...........Apr. 2...........May 8...........
July 2...........Aug. 4...........Sept. 4...........Oct. 2...........Nov. 5...........Dec. 3...........Jan. 5, 1954...
33.43 35.6137.4436.8835.3827. 5620.9121.2722.4123. 8426.4230.21
Dl-5-8ab
Aug. 3, 1951......
Sept. 26 ..............Nov. 1........ ......Dec. 3..............
3. 96 3. 143.924.43
Jan. 8, 1952.... Feb. 6............Mar. 5............
Dry
DryDry
June 6, 1952... June 29 ...........Aug. 1.. .........Sept. 2...........Sept. 29...........
2. 73 2. 112.632.592.79
Dl-5-9ac
July 16, 1951.......
Aug. 28...............Sept. 26...............Nov. 1. ..............Dec. 3...............
18.57 17.6913.3314.9416.0517.26
Jan. 8, 1952....
Sept. 2 ............
17.52 13.788.41
10.2711.3511.90
Sept. 29, 1952... Nov. 12...........Dec. 3...........Jan. 5, 1953...Feb. 2...........Mar. 4...........
12.48 14.4014.7816.4617.7719.72
508919 O-60 15
218 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Table 34. Water-level measurements by tape, in feet below land-surface datum Cont
Date Water level
Date Water level
Date Water level
Dl-5-9ac Continued
Apr. 2, 1953.......May 8...............
July 2...............
22.55 22.28
7.70 14.89
Aug. 4, 1953.... Sept. 4............Oct. 2............
13.14 12.70 13.61
Nov. 5, 1953... Dec. 3...........Jan. 5, 1954...
14.59 16.10 18.18
Dl-5-19cd
Feb. 3, 1953.......Mar. 5...............Apr. 3 ...............May 4 ...............
9.7911.6412.6312.60
July 2............
Sent. 9............
10.247. 125.306. 96
Oct. 2, 1953...
Feb. 24, 1954...
8.298.39
11.74
Dl-5-21ddd
Aug. 2, 1951.......Aug. 29...............Sept. 26...............Nov. 2...............Dec. 4...............
6. 876.25
DryDryDry
Jan. 8, 1952....Feb. 6............Mar. 5............Apr. 1 ............May 5............
DryDryDryDry
5.33
June 4, 1952...June 27...........Aug. 6...........Sept. 4...........Aug. 5, 1953..,
5. 195.825.806.385.61
Dl-5-23db
May 15, 1951.......May 31...............-July 5...............Aug. 1 ...............Aug. 28...............Sept. 26...............Nov. 1....... ........Dec. 3...............Jan. 8, 1952.......Feb. 5...............Mar. 5 ...............
5.306. 106.386.617.077.477.247.287.416.217. 29
Apr. 1, 1952....
June 29 ............
Sept. 2............Sept. 29 ............Nov. 10 ............Dec. 1 ............Jan. 2, 1953....Feb. 2 ............
7. 192.534.716.306. 547.347.547. 567.337.457. 15
Mar. 3, 1953...Apr. 1 ...........Mav 2
July 2...........Aug. 1 ...........Sept. 1 ...........Oct. 1 ...........Nov. 5...........Dec. 1.. .........Jan. 5. 1954...
7.196.716.574.176.315.987.437.947.877. 757.69
Dl-5-26da
July 17, 1951....... Dec. 3...............Jan. 8, 1952.......Feb. 5...............
11.57 11.7911.9112.22
Mar. 5, 1952.... Apr. 1 ............
June 2 ............
12. 39 11.2510.4110. 57
Aug. 1, 1952... Sept. 2...........Sept. 29...........Aug. 8. 1953...
11.81 11.3712.4110. 60
Dl-5-27aa
Aug. 3, 1951....... Aug. 29 ...............Sept. 26 ...............Nov. 3...............Dec. 4 ...............Jan. 8, 1952.......
9. 50 9.28
10.7811.70
Dry
Feb. 6, 1952.... Mar. 5............Apr. 1. ...........
Dry
Dry9.498.27
June 29, 1952...
Sept. 4...........Oct. 2...........Aug. 5, 1953...
7.94 9.61
10.0110.3210.44
Dl-5-30aa
Apr. 18, 1951.......May 31...............July 6...............Aug. 1.. .............Aug. 30...............Oct. 1...............
10.2910.743.883.706.477.13
Nov. 2, 1951....
Jan. 7, 1952....Feb. 5............
Apr. 7............
8.218.488.768.969.138.21
Sept. 30, 1952...Feb. 3, 1953...Mar. 5...........
June 2...........
5.829 67
U 97
12.0112.7311.78
BASIC DATA 219
Table 34. Water-level measurements by tape, in feet below land-surface datum Coat.
DateWater level
July 2, 1953.......
Sept. 9...............
5.70 3.21 4.17
Date Water level
Dl-5-30aa Continued
Oct. 2, 1953.... 6.317.34
DateWater level
Dec. 3, 1953... Jan. 4, 1954...
8.98 10.10
Dl-5-30cd
May 17, 1951.......TV/I a -,T ^ 1
July 7...............Aug. 1... ............
Oct. 1...............Nov. 2...............DGC 4Jan. 7, 1952.......
8.488. 924.704.264. 135.366.085. 725.99
Feb. 5, 1952....
Qorif 4
Feb. 3, 1953....Mar. 5............
6. 144. 404.303. 774. 184.535.007. 298.34
Apr. 3, 1953...May 4...........
July 4...........Aug. 4...........Sept. 9...........Oct. 2...........Nov. 4...........Dec. 3...........
9.7510.27
9. 544. 543.994. 324.925.246.04
Dl-5-33dd
July 6, 1951.......Aug. 1.... ...........
Oct. 1.. .............Nov. 1... ............Dec. 4...............Jan. 7, 1952.......Feb. 5...............Mar. 6 ...............
2.807.257.027.326.487.386. 817. 367.42
Apr. 7, 1952....May 2.............
June 29............Aug. 5............Sept. 4............
Jan. 6, 1953....
4. 143. 544.606.466. 567. 607. 80
DryDry
Feb. 3, 1953...Mar. 5...........Apr. 3...........May 4...........
July 4...........Aug. 4...........Sept. 9...........
7.727.667.017.077. 102.915. 76
Dry
Dl-5-34cc2
[No measurements by tape; for measurements from recorder chart, see table 35]
Dl-5-35cal
July 7, 1951.......
Oct. 1... ............Nov. 1... ............
5. 73 6.426.656. 586.07
Dec. 4, 1951..... Jan. 7, 1952....,Feb. 4.............
June 4 .............
6.23 6.425.953. 944.29
June 29, 1952... Aug. 5...........Sept. 4...........Sept. 30 ...........
4. 79 5. 116. 195.94
Dl-5-35cdl
July 6, 1951....... 5.44 5.395.46
Oct. 1, 1951.... Nov. 1.. ..........Dec. 4............
5.23 5.235.07
Jan. 7, 1952... Mar. 6...........
5. 10 5. 14
Dl-5-35cd2
May 27, 1952.......
Aug. 5...............Sept. 4...............
Nov. 10...............
3.93 4. 264.384. 734. 774.704.45
Dec. 4, 1952.... Jan. 6, 1953....Feb. 3............Mar. 5............Apr. 3 ............
4.41 4.384.284.364. 154.224.21
July 4, 1953...
Sept. 9...........Oct. 2...........Nov. 4...........Dec. 3...........Jan. 4, 1954...
4.42 4.854.484.614.374.244.36
508919 O-60 16
220 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Table 34. Water-level measurements by tape, in feet below land-surface datum Cont.
Date Water level
Date Water II level |
Date Water level
Dl-5-36ddd
July 6, 1951.......
Oct. 1.... ...........Nov. 1 ...............
Jan. 7, 1952.......Feb. 5...............
Apr. 7...............May 2 ...............
4. 604.314.274.414. 504.604. 754.895.094.984.81
June 4, 1952....,
Sept. 4.............Sept. 30.............Nov. 10.............E)6c 4Jan. 6, 1953.....Feb. 3.............
4.394.354. 214. 124. 244.905.215.415.415. 51
Apr. 3, 1953....
July 4............Aug. 4 ............Sept. 4............Oct. 2............
Jan. 4, 1954...,
5.475.425.425.354. 524. 584. 614.744.925.05
D2-3-4ac
May 16, 1951.......May 31...............
Aug. 29 ...............Oct. 1 ...............Nov. 2...............
Jan. 7, 1952.......Feb. 5...............Mar. 7 ...............
6.376.314. 944.876. 266.316.427.066.898.739.01
Apr. 2, 1952.....May 1 .............
June 30 .............
Sept. 3.............Oct. 1 .............Nov. 5.............Dec. 1 .............Jan. 2, 1953.....Feb. 2.............
6.453.223.462. 544.013.722. 854.334.984. 705. 36
Mar. 4, 1953...Apr. 1 ...........May 1 ...........
July 3...........Aug. 3...........Sept. 2...........Oct. 1 ...........Nov. 6...........
Jan. 6, 1954...
6.646. 507. 122.553. 504.696. 117.275. 876.477. 53
D2-4-lbal
June 29, 1951.......
Aug. 29...............Oct. 1 ...............Nov. 1.... ...........Dec. 4...............Jan. 7, 1952....... Feb. 5...............Mar. 6...............
3. 54 6.027.547.47
DryDry DryDry
Apr. 7, 1952..... May 2.............
June 29 .............
Sept. 4.............Sept. 30.............
Dry
9. 581.835.467. 849.79
Dry
Apr. 3, 1953...IViav 4
July 4...........
Sept. 9...........Oct. 2...........
Dry DryDry
5. 244.988.759.96
12.50
D2-4-9bc
[For measurements from recorder chart, see table 35]
June 3, 1953....... July 3...............Aug. 3 ...............Sept. 2...............
22. 79 22.2121.4221.22
Oct. 1, 1953..... Nov. 6.............Dec. 1 .............Jan. 6, 1954.. ..j
21.01 20.7220.4720.72
Feb. 4, 1954.... Mar. 3............Mar. 31............
21.12 21.4921. 78
D2-4-10dd
May 14, 1951....... May 30...............July 6...............
Aug. 29...............Oct. 1.. .............Nov. 1... ............
Jan. 7, 1952.......
8.18 6.232.532.483.624.115.767.206 79
Feb. 5, 1952....
Apr. 7............May 1.. ..........
July 28............
Oct. 1............
8.64 8.896.986.995.202.582.293.984.98
Nov. 10, 1952...
Jan. 2, 1953...Feb. 2...........
Apr. 1.. .........Mav 1
July 3...........
5.08 5.967.177.878.428.548.606.983.17
BASIC DATA 221
Table 34. Water-level measurements by tape, in feet below land-surface datum Coat.
Date Water II level 1
Date Water II level ||
Date Water level
D2-4-10dd Continued
Aug.Sept.
1, 1953....... 2.6414.67
Oct. 16
1953.... 5.6.
8? 82,44
II
Dec. j.fi
1953...1954...
6.597.96
D2-4-llcdl
May 14, 1951.......May 30 ...............July 6...............Aug. 1 ...............Aug. 29...............Oct. 1 ...............Nov. 1...............Dec. 2...............Jan. 7, 1952.......Feb. 5...............Mar. 7...............
6.345.864.314.505.615.826.316.525.486.766. 97
Apr. 7, 1952.....May 1 .............
June 28.............
Sept. 3.............Oct. 1 .............Nov. 10.............Dec. 1 .............Jan. 2, 1953.....Feb. 2.............
5. 345. 774.554.674. 214.794.837.237. 116.706. 91
Mar. 4, 1953...Apr. 1 ...........May 1 ...........
July 3...........Aug. 1 ...........Sept. 2...........Oct. 1 ...........Nov. 6...........
Jan. 6, 1954...
6.656.586.004.373.984.685. 146.365.956.336.74
D2-4-13aa
June 29, 1951.......Aug. 1.. .............Aug. 29...............Oct. 1..... ..........Nov. 1 ...............Dec. 4...............
3. 805. 815. 956.497. 13Dry
Jan. 7, 1952....,Feb. 4.............Mar. 7.............
May 1 .............June 2.............
DryDryDry
5.042. 52
June 27, 1952...Aug. 1.. .........
Aug. 1, 1953...
5.555. 385.565.406.36
D2-4-13cc
June 21, 1947....... Sept. 10...............Oct. 20...............Dec. 31...............Feb. 10, 1948.......Sept. 1. ..............Sept. 23...............Oct. 27...............Dec. 1 ...............Jan. 4, 1949.......Mar. 2...............Mar. 31...............Apr. 14 ...............May 17...............
July 27..............Oct. 18...............Nov. 26...............Jan. 4, 1950.......Feb. 14...............Mar. 8...............Apr. 12...............May 1 ...............June 5 ...............
3. 30 3.886. 107.958. 505.775.966.487.787.728. 187.587.466.654..S43.834. 837.277.758.488.077. 297.686.45
June 21, 1950..... July 27.............Sept. 28............Oct. 31.............Jan. 5, 1951....,Feb. 2.............
Mar. 28.............
May 26.............
July 6.............July 11, ............July 31.............Aug. 1 .............Aug. 29.............Sept. 3.............Oct. 1 .............Nov. 1.............Dec. 4.............Jan. 11, 1952.....Feb. 4.............
4.68 4.024. 916. 177.778.208.487.067.045.745.996.004.623.989 4.7
3. 663.773. 125.986.387.357.638.44
Mar. 7, 1952...
June 27...........Aug. 6...........
Sept. 29...........Nov. 7...........Dec. 3...........
Feb. 3...........Mar. 3...........Apr. 2...........
July 3...........Aug. 3...........Sept. 2...........Oct. 1 ...........Nov. 6...........Dec. 2...........Jan. 5, 1954...
8. 537.745.414.922.544.094.805.606.747.268. 128.257.748.207.906.683. 104. 395. 504. 816. 527.228.04
D2-4-17aa
May 15, 1951..May 30..........July 6..........
17.94N Aug. 1. 1951....18.06 I Aug. 29............14.83 II Oct. 1............
13.84 Nov. 1, 1951..12.89 Dec. 4..........13.87 II Jan. 7, 1952..
14.5414.7315.42
222 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Table 34. Water-level measurements by tape, in feet below land-surface datum Cont.
Date Water level
Date Water level
Date Water level
D2-4-17aa Continued
Feb. 5, 1952.......Mar. 7...............Apr. 7...............TVTfl v 1
Aug. 1... ............Sept. 3...............
16.7517.1816.4716.0316.3216.1214.6113.29
Oct. 1, 1952....Nov. 5............
Jan. 2, 1953....Feb. 2............IVlcLr 4Apr. 1.... ........May 1............
13.8214.9414.8615.8916.3617.0817.3017.86
June 3, 1953...July 3...........Aug. 3...........Sept. 2...........Oct. 1.. .........Nov. 6...........Dec. 1... ........Jan. 6, 1954...
16.9915.1412.2011.7613.2114.4614.5315.33
D2-4-25bd
May 22, 1951.......May 30 ...............July 6...............Aug. 1...............Aug. 29...............Sept. 28...............Dec. 4...............Apr. 4, 1952.......May 5...............
19. 5020. 1215.9417.6617. 1117. 7318.6920. 3218.72
June 4, 1952....June 27 ............
Sept. 5............Oct. 9............Feb. 3, 1953....
May 4 ............
18.9817.8318. 2217.0117.7620.6820.2620. 3220.55
June 2, 1953...July 3...........Aug. 3...........Sept. 2...........Oct. 5...........Nov. 6...........Dec. 2...........Jan. 5, 1954...
19.5717.0016.9217.8316.4518. 7219.2319.76
D2-5-2dd
May 15, 1951.......July 6...............
Aug. 29...............Oct. 1... ............Nov. 1.... ...........Dec. 3...............Jan. 7, 1952.......Feb. 5...............Mar. 6...............Apr. 7...............
12.947.708.069.769.83
11. 1711.9812. 1314.0516.2413.38
May 5, 1952....,
Aug. 5.............Sept. 30.............Nov. 10.............Dec 4Jan. 6, 1953....,Feb. 3.............Mar. 5.............
8.668.097. 167.479.57
11.3212.8414.8315.0015.95
Apr. 1, 1953...May 2...........
July 4...........Aug. 3...........Sept. 4...........Oct. 1.. .........Nov. 5...........
Jan. 4, 1954...
15.2414.7211.817.617.927.729.56
11.5312.9114.67
D2-5-5ba
July 6, 1951....... Aug. 1... ............Aug. 29 ...............Oct. 1...............Nov. 1 ...............Dec. 4 ...............Jan. 7, 1952.......Feb. 5...............Mar. 6 ...............Apr. 7...............May 2 ...............
2. 88 2.842.953. 113.273.493.884. 134.405. 245.09
June 4, 1952..... June 29 .............Aug. 5 .............Sept. 4.............Sept. 30.............Nov. 10.............Dec. 4.............Jan. 6, 1953.....Feb. 3............Mar. 5.............
4. 86 4. 854.724.614.594. 674. 724.954. 894.93
Apr. 3, 1953...IVIflv 4
July 4...........
Sept. 9...........Oct. 2...........
Dec. 3...........Jan. 4, 1954...
5.08 5. 145.345.224.984.794. 854.884.945.09
D2-5-9ccl
Apr. 19, 1951....... May 30...............July 5...............Aug. 1. ..............
4.32 4.454.044. 103.64
Sept. 27, 1951..... Nov. 1.............Dec. 3 .............Jan. 7, 1952.....Feb. 4.............
4.31 3.493.884.013.65
May 1, 1952... June 2...........Sept. 29...........Aug. 5, 1953...
3.76 4. 114.024.54
BASIC DATA 223df
Table 34* Water-level .measurements by tape, in feet below land-surface datum Cont.
Date Water level
Date Water level
Date Water level
D2-5-l3bb
June 29, 1951.......Aug. 1....... ........Aug. 28...............Sept. 27 ...............Nov. 1...............Dec. 3...............
2.804.985.074.944.895. 19
Jan. 7, 1952.....Feb. 4.............
Apr. 4.............May 1.. ...........
5.285.836.455.504.994.91
June 27, 1952....Aug. 1.. ..........Sept. 3............Sept. 29............Aug. 3, 1953....
3.093.664.034.803.93
D2-5-14ac
[No measurements by tape; for measurements from recorder chart, see table 35]
D2-5-14dd
June 29, 1951.......Aug. 2...............Aug. 28...............Sept. 27...............Nov. 1. ..............Dec. 3...............
4.414.213.025.51
Dry
Jan. 7, 1952.....Feb. 4.............Mar. 6.............
DryDryDryDry5.294.79
June 27, 1952...Aug. 1...........Sept. 3...........Sept. 29...........Aug. 3, 1953...
2.563.024.936.284.05
D2-5-15aal
Apr. 17, 1951.......May 30...............July 5...............Aug. 1.. .............Aug. 28...............Sept. 27...............
3.363.381.383. 191. 843.22
Nov. 1, 1951.....Dec. 3.............Jan. 7, 1952....,Feb. 5.............May 1.... .........
3.044.024.224.313.06
June 2, 1952...June 27...........Aug. 1...........Sept. 3...........Sept. 29...........
2.731.152.823.443.88
D2-5-16aal
[For measurements from recorder chart, see table 35]
June 2, 1953....... July 3...............Aug. 3 ...............
4.75 3.764.68
Sept. 2, 1953..... Oct. 5.............Nov. 6.............
3.95 4.925.09
Dec. 2, 1953.... Jan. 5, 1954....
5.13 5.33
D2-5-21da
May 22, 1951....... May 30...............July 5...............Aug. 1.. .............Aug. 28...............Sept. 28...............Nov. 2...............Dec. 3...............Jan. 7, 1952.......Feb. 4...............Mar. 7...............
5.99 6.212.705.405.505.675.986.078. 187. 107.25
Apr. 7, 1952...,. May 7.............
June 27.............Aug. 6.............Sept. 5.............Sept. 29.............Nov. 10.............Dec. 2 .............Jan. 6, 1953.....Feb. 3.............
5. 11 5.695.233.073.885.646. 126.346.616.896.62
Mar. 3, 1953... Apr. 2...........
July 3...........Aug. 3...........Sept. 2...........Oct. 5...........Nov. 6...........Dec. 2...........Jan. 5, 1954...
6.82 6.046. 196.303.855.585.636.096.316.446.90
D2-5-22ccd [No measurements by tape; for measurements from recorder chart, see table 35]
224 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Table 34. Water-level measurements by tape, in feet below land-surface datum Cont.
Date Water 1] level |]
Date Water level
Date Water level
D2-5-25cbl
May 10, 1951.......May 30...............July 5...............Aug. 1 ...............Aug. 28...............Sept. 28...............Nov. 2...............Dec. 3..............Jan. 11, 1952.......Feb. 4...............Apr. 7...............
5.195. 514.884.965. 545.415. 245. 165.355.645.07
May 5, 1952....
Aug. 6............Sept. 5............Sept. 29............Nov. 7............
Jan. 6, 1953....Feb. 3............Mar. 3............
5.015.024.814.495. 705. 765.665. 725.325. 826.04
Apr. 2, 1953...May 4...........
July 3...........Aug. 3...........Sept. 2...........Oct. 5...........Nov. 6...........Dec. 2...........Jan. 5, 1954...
5.865.795.795.755.286.325. 945.905.895.83
D2-5-26cc2
May 14, 1951.......Apr. 7, 1952.......May 7...............
2.001. 582.06
June 4, 1952....
Aug. 6............
1. 731.491.68
Sept. 5, 1952...Sept. 29...........Aug. 3, 1953...
1.802.341.61
D2-5-29ac
Aug. 13, 1951.......
Nov. 2...............Dec. 4 ...............Jan. 11, 1952.......Feb. 3, 1953.......
4. 705.095.225.956. 135.87
Mar. 3, 1953....
July 3............Aug. 3 ............
6.335.635.485.095.005. 19
Sept. 2, 1953...Oct. 5...........Nov. 6...........Dec. 2...........Jan. 5, 1954...
5.644.814.906.096. 10
D2-5-33dbl
May 14, 1951....... May 30 ...............Aug. 1....... ........Aug. 29 ...............
8.62 6.349.619. 19
Sept. 29, 1951..... Nov. 2.............
Jan. 11, 1952.....
9.55 8.739.91
10. 10
Mar. 7, 1952... Apr. 7...........
11.22 9.627. 34
D2-5-34ba
May 15, 1951....... May 30 ...............July 5...............Aug. 1.... ...........Aug. 28...............Sept. 28...............Nov. 2...............Dec. 3 ...............Jan. 7, 1952.......Feb. 4...............
4. 14 4. 682.003.403.623.292.894. 294. 574.715. 58
Apr. 7, 1952.....IVTa v 7
Aug. 6.............Sept. 5.............
Nov. 7.............Dec. 2.............
Feb. 3.............
4. 10 3. 713.632. 392. 834. 294. 823.893.974.404.09
Mar. 3, 1953... Apr. 2...........
July 3...........Aug. 3...........Sept. 2...........Oct. 5...........Nov. 6...........
Jan. 5, 1954...
4.82 3.473.883.913.843.054.053. 583. 583.284.41
D2-5-34cd
Apr. 23, 1951....... May 30...............July 5...............Aug. 1...............Aug. 29...............Sept. 28...............
11.37 8.922.213.465.418.09
Nov. 2, 1951..... Dec. 4.............Jan. 11, 1952.....Feb. 4.............Mar 7Apr. 7.............
10.07 10.03
May 5, 1952...
Sept. 5...........
5. 10 2.481.462.683 4R
4.35
BASIC DATA 225
Table 34. Water-level measurements by tape, in feet below land-surface datum Cont.
Date Water level
Date Water level
Date Water level
D2-5-35dc
May 14, 1951......
July 5..............Aug. 1 ..............
Nov. 2..............Dec. 3..............Jan. 11, 1952......Feb. 4..............Apr. 7..'............
35.6835. 7826.2722.9320. 1521.0824.0628.7829.6329.9227.48
May 5, 1952....
Aug. 6 ............Sept. 5............Sept. 29............Nov. 7............
Feb. 3............Mar. 3............
31.0326. 7921.5216. 1515. 3117.2922. 1125.2728. 5032.2334.99
Apr. 2, 1953...May 4...........
July 3...........Aug. 3...........Sept. 2...........Oct. 5...........Nov. 6...........
Jan. 5, 1954...
37.8039. 5639.3928.7621.5017. 1720.8422.5826.4328.90
D2-6-18cb
Aug. 3, 1951......Aug. 28..............Sept. 27..............Nov. 2..............
2.321.381.631.542.26
Jan. 7, 1952....Feb. 4............
Apr. 1.. ..........
2. 542.933.122.392.26
June 4, 1952...June 26 ...........Aug. 4...........Sept. 1.. .........Oct. 2...........
1.511.722.261.422.22
D2-6-20ab
Aug. 15, 1951......Aug. 28..............Sept. 27..............Nov. 2..............May 2, 1952......June 4 ..............June 27 ..............
Sept. 5..............
40.3540. 1740.8441.5220. 5939.5438. 5038. 1738.42
Oct. 2, 1952....Nov. 10............Dec. 3............Jan. 5, 1953....Feb. 3............
Apr. 2............May 2 ............
38.6138.7538.8538.6939.9040.6839.7439.41
June 2, 1953...July 3...........Aug. 3...........Sept. 4...........Oct. 5...........Nov. 5...........Dec. 2...........Jan. 6, 1954...
38.8838.8038.8739.0039.0838.6438.9939.10
D2-6-22cb
Aug. 15, 1951...... Aug. 28 ..............Sept. 27..............
37.00 38. 5239.24
Nov. 2, 1951.... 39. 57 43.13
Jan. 7, 1952... Feb. 4...........
44.26 44.42
D2-6-26cb
Aug. 6, 1951...... Aug. 28 ..............Sept. 27..............Nov. 2..............Dec. 3 ..............Jan. 7, 1952......Feb. 4..............Mar. 7..............
Mav 1
30.29 29.4229. 1831.7130.5631.7431.8132. 7833.4425.71
June 4, 1952....
Aug. 4............Sept. 5............Oct. 2............Nov. 10............Dec. 3............Jan. 6, 1953....Feb. 3............
24.78 27.5424.2723.2822.9223.4923.8024.049"i 1 1
26.12
Apr. 2, 1953...
July 3...........Aug. 3...........Sept. 4...........Oct. 5...........Nov. 5...........Dec 2Jan. 6, 1954...
26. 25 26. 1226. 2125.6226.3326.4926.6827. 5128.0628.77
D2-6-27aa
May 25, 1951....... May 29...............July 5...............Aug. 1...............
3.501 2.532.804.21
Aug. 28, 1951.... | Sept. 27.............Nov. 2............Dec. 3............
3.94 3.37
2.31
Jan. 7, 1952.. .| Feb. 4...........
Apr. 4...........
Frozen
2.18
226 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Table 34. Water-level measurements by tape, in feet below land-surface datum Cont.
Date Water level
Date Water 1 level II
Date Water level
D2-6-27aa Continued
May 2, 1952.......
Sept. 5...............Oct. 2...............Nov. 10...............
2.162.272.353.103.162.912.34
Dec. 3, 1952....Jan. 6, 1953....Feb. 3............
2.25
2.072.282.401.961.99
July 3, 1953...Aug. 3...........Sept. 4...........Oct. 5...........Nov. 5...........Dec. 2...........Jan. 6, 1954...
2.493.093.172.842.372.182.32
D3-4-llbdb
Aug. 22, 1952......Feb. 3, 1953......
June 2 ..............
6.1713.9414.4914.8915.5411.42
July 3, 1953....
Oct. 5............
7.748.86
10. 2011. 1211.70
Dec. 2, 1953...Jan. 5, 1954...Feb. 4...........Mar. 3...........Apr. 1 ...........
14.6514.9015.3114.8415.20
D3-4-14ba
May 18, 1951......
July 6..............Aug. 1 ..............
Sept. 28..............Nov. 1 ..............
Jan. 11, 1952......
46.5044.3932.4032.2031. 7133.9339. 9242.6643.03
May 5, 1952....
Sept. 5............Sept. 29............Feb. 3, 1953....
May 4............
43.5139.4332.0031. 8031.8433.9844.6246.0046. 38
June 2, 1953...July 3...........Aug. 3...........Sept. 2...........Oct. 5...........Nov. 6...........Dec. 2...........Jan. 5, 1954...
37.8034.5732.6632. 9634. 9336.8642.2543. 18
D3-4-27ba
May 18, 1951......
Aug. 1 ..............
Sept. 28..............Nov. 1 ..............
Jan. 11, 1952......
21.60 18. 533.485. 16
11.0311.8816. 5720.6720.84
May 5, 1952....
Aug. 6 ............Sept. 5............Sept. 29............Feb. 3, 1953....
Apr. 2............
12. 10 2. 252. 154.92
10. 19.12.9221.1022.3823. 19
May 4, 1953...
July 3...........Aug. 3...........Sept. 2 ..........Oct. 5...........Nov. 6...........Dec. 2...........Jan. 5, 1954...
23.40 22.655.705. 936.959.30
11.8219.6120.70
D3-5-lac
May 14, 1951......
July 5..............Aug. 1 ..............Aug. 28..............Sept. 28..............Nov. 2..............Dec. 3..............Jan. 11, 1952......Feb. 4..............
36. 12 37.9331.2024.9921.5521.7327.0127.6229.0133.9537.78
Apr. 7, 1952.... May 5............
Aug. 6............Sept. 5............Sept. 29............Nov. 7............Dec. 2............
Feb. 3............
32.77 30.0526.7320.2015.0815.0516.5521.09
28.0831.09
Mar. 3, 1953...
May 4...........
July 3...........Aug. 3...........Sept. 2...........Oct. 5...........Nov. 6...........
Jan. 5, 1954...
33.94 36.7339.0938.63
20.9018.5519.2821.5124.6328.40
BASIC DATA 227Table 34. Water-level measurements by tape, in feet below land-surface datum Cont.
Date Water level
Date Water level
Date Water level
D3-5-3bb
May 15, 1951......TV/fa v 9 t\
July 5..............Augv 1 ..............A 11 cf 9Q
Sept. 28..............Nov. 2..............Dec. 3..............Jan. 11, 1952......Feb. 4..............
12.2811.884.746.569.04
12.008.31
14.79
Dry
Mar. 7, 1952....
Sept. 5............Sept. 29............Feb. 3, 1953....Mar. 3............
DryDry7.606.283.013.265.846.84
15.6316.05
Apr. 2, 1953...May 4...........June 2...........July 3...........Aug. 3...........Sept. 2...........Oct. 5...........Nov. 6...........Dec. 2...........Jan. 5, 1954...
15.8711.2411.613.785.275.399.97
13.7114.5215.36
D3-5-3da
Apr. 23, 1951......Feb. 2, 1953......
May 4..............
29.2025.3626. 1029.7629.80
June 2, 1953....July 3............Aug. 3............Sept. 2............
29.435.086.018.23
Oct. 5, 1953...Nov. 6...........Dec. 2...........Jan. 5, 1954...
12.2618.2920.5622.72
D3-5-5aal
Apr. 23, 1951......
July 6..............Aug. r.... ..........
Sept. 28..............Nov. 2..............
Jan. 11, 1952......Feb. 4..............Mar. 7..............
4. 51 4.022. 923.414. 114.094.274.865.255. 576. 13
Apr. 7, 1952....
Aug. 6............Sept. 5............Sept. 29............Nov. 7............Dec. 2............Jan. 6, 1953...,Feb. 3............
5. 18 2. 522.712.542.984.664.404.765.085.185.30
Mar. 3, 1953... Apr. 2...........
July 3...........Aug. 3...........Sept. 2...........Oct. 5...........Nov. 6...........Dec. 2...........Jan. 5, 1954...
5.67 4.664.723. 743. 113. 514.504.582. 843.895.04
D3-5-9da
May 25, 1951...... July 5..............Aug. 1 ..............Aug. 28..............Sept. 28..............Nov. 2..............Dec. 3..............Jan. 11, 1952......
32.90 18.4020.4016.0118.6722.2622.6623.31
Apr. 7, 1952....
June 27............Feb. 3, 1953...,
May 4 ............
22.67 26.3224.9220.2924.2626.6928.7229.26
June 2, 1953... July 3...........Aug. 3...........Sept. 2...........Oct. 5...........Nov. 6...........Dec. 2...........Jan. 5, 1954...
31.02 23.8218.5917.6917.2318.7820.4024. 15
D3-5-18ab
Apr. 19, 1951...... May 30 ..............July 6..............Aug. 1. .............
Sept. 28..............Nov. 2..............
18.87 17.5114.6215. 6716.0016. 9617.23
Sept. 30, 1952.... Feb. 3, 1953.....Mar. 3............Apr. 2............May 4. ...........
July 3............
17.37 18.6918.7419. 1918. 7816.8213.58
Aug. 3, 1953... Sept. 2...........Oct. 5...........Nov. 6...........Dec. 2...........Jan. 5, 1954...
15.82 16.9917. 1817.4217.3717.83
228 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Date Water level
Date Water level
Date Water level
D3-6-6ac
Aug. 13, 1951.......Aug. 28 ...............Sept. 28 ...............Nov. 1... ............Dec. 3...............Jan. 11, 1952.......Feb. 4...............
Apr. 7...............
15.4016.0913.2713. 1313.7713. 9114.2015.0113.3811.46
June 27 ............Aug. 6 ............Sept. 5............Sept. 29............Nov. 7............
Feb. 3............Mar. 3 ............
10.7811. 5511. 6011. 7511.4011.9712. 8613. 2214.6415.28
Apr. 2, 1953...May 4...........
July 3...........Aug. 3...........Sept. 2...........Oct. 5...........Nov. 6...........Dec. 2...........Jan. 5, 1954...
15. 7614.6814.4113.9613.6112. 7915. 6814. 1614. 2514. 98
Tab
le 3
5.
Wat
er-l
evel
mea
sure
men
ts f
rom
rec
orde
r ch
art,
in f
eet
belo
w l
and-
surf
ace
datu
m
Day
1953
Jan.
Feb.
Mar.
Apr.
May
June
July
Aug.
Sept
.Oct.
Nov.
Dec.
1954
Jan.
Feb.
Mar.
Al-
4-5
da
1 ...
......
......
......
......
......
.....
2 .......................................
3 4 .......................................
5 .......................................
6 .......................................
7 .......................................
8 .......................................
9 .......................................
10.... ..
....
....
... .
....
....
....
....
....
...
11..
....
....
....
....
....
.................
12..
....
....
....
....
....
.................
13..
....
....
....
....
....
.................
14..
....
....
....
....
....
.................
15.......................................
16..
....
....
....
....
....
.................
17.......................................
18.......................................
19.......................................
20.......................................
21.......................................
22.......................................
23.......................................
24.......................................
25.......................................
26.......................................
27.......................................
28.......................................
29.......................................
^n 31.......................................
4.70
4.21
4.38
4.37
4.32
4.32
4.32
4.32
4.32
4.31
4.30
4.29
4.18
4.14
4.12
4.07
4.03
4.02
4.00
4.00
4.00
4.00
4.01
4.01
4.01
4.02
4.03
4.04
4.05
4.04
4.05
4.05
4.05
4.05
4.04
4.05
4.05
4.03
4.04
4.04
4.03
4.01
3,97
3.97
3.98
3.98
4.01
4.01
4.02
4.04
4.04
4.05
4.06
4.05
4.06
4.07
4.08
4.09
4.09
4.08
4.09
4.09
4.11
4.12
4.05
4.04
4.04
4.04
4.05
4.08
4.10
4.12
4.14
4.17
4.19
4.21
4.21
4.21
4.20
4.21
4.23
4.25
4.26
4.28
4.30
4.25
4.23
4.10
4.10
4.12
3.81
3.89
3.94
3.98
4.00
3.92
3.90
3.92
3.93
3.04
3.12
3.32
3.38
3.40
3.38
3.41
3.43
3.40
3.17
2.72
2.92
2.96
3.01
3.01
3.04
3.10
2.94
2.97
2.91
3.04
3.13
3.21
3.23
3.30
3.33
3.39
3.44
3.51
3.56
3.60
3.62
3.67
3.71
3.65
3.68
3.70
3.70
3.74
3.78
3.81
3.84
3.85
3.82
3.85
3.88
3.92
3.94
3.86
3.77
3.68
3.50
3.39
3.29
3.19
3.26
3.31
3.32
3.27
3.16
3.15
3.13
3.00
3.10
3.10
3.11
3.11
3.08
3.06
3.06
3.14
3.22
3.24
3.24
3.29
3.31
3.37
3.39
3.42
3.47
3.48
3.51
3.53
3.62
3.60
3.55
3.56
3.58
3.61
3.55
3.54
3.54
3.55
3.57
3.59
3.60
3.62
3.64
3.63
3.65
3.66
3.66
3.68
3.69
3.68
3.73
3.72
3.72
3.67
3.66
3.66
3.65
3.67
3.68
3.69
3.69
3.69
3.71
3.72
3.69
3.68
3.68
3.67
3.67
3.68
3.68
3.67
3.67
3.67
3.69
3.71
3.71
3.72
3.70
3.68
3.65
3.63
3.57
3.51
3.51
3.49
3.47
3.46
3.45
3.43
3.42
3.41
3.40
3.40
3.40
3.39
3.38
3.37
3.37
3.37
3.37
3.36
3.36
3.36
3.35
3.34
3.35
3.34
3.35
3.34
3.34
3.42
3.42
3.40
3.35
3.34
3.36
3.37
3.40
3.41
3.41
3.42
3.43
3.44
3.44
3.46
3.46
3.54
3.54
3.55
3.58
3.59
3.60
3.64
3.65
3.68
3.70
3.72
3.73
3.72
3.67
3.67
3.71
3.76
3.80
3.82
3.83
3.83
3.83
3.85
3.85
3.94
3.92
3.90
3.89
3.87
3.87
3.90
3.95
4.13
4.15
4.17
4.18
4.25
4.25
4.23
4.00
3.96
3.94
3.89
3.84
3.84
3.83
3.82
3.79
3.76
3.75
3.69
3.68
3.67
3.68
3.67
3.67
3.68
3.69
3.72
3.71
3.71
3.71
3.70
3.69
3.68
3.66
3.66
3.63
3.62
3.61
3.56
3.51
3.52
3.60
Tab
le 3
5.
Wat
er-l
evel
mea
sure
men
ts f
rom
rec
orde
r ch
art,
in f
eet
belo
w l
and-
surf
ace
datu
m C
onti
nued
Day
1952
Sep
t.O
ct.
Nov
.
1953
Jan
.F
eb.
Mar
.A
pr.
May
June
July
A
ug.
Sep
t.O
ct.
Nov
.D
ec.
1954
Jan
.F
eb.
1 M
ar.
Al-
4-2
2d
cl
1 .........
2 .........
<3 4
....
....
4
5 .........
6 ..
....
...
7 .........
8 ..
....
...
9 ..
....
...
10
....
....
.1
1..
....
...
12
....
....
.1
3..
....
...
14.........
15
.,..
....
,16.........
17
....
....
.18.........
19.........
9f> 21
....
....
.22........
23........
24........
9^ 26
....
....
27
....
....
28
....
....
29........
30
....
....
31
....
....
.
3.9
63.9
93.
933.9
63
.99
3.9
33.9
23.9
13
Q1
3.8
93.8
33.8
73.8
73
.92
3.9
43.9
94.0
34.0
34
.04
4.0
04
.01
4.0
14.0
03
.99
3.99
4.0
03
.98
3Q
Q
3.9
93.9
64.0
03
.98
3.9
63.9
73.9
73.9
83
.98
4.0
03.9
83.9
94.0
13
.99
3.9
84.0
14
.02
4.0
24.0
03.9
93.9
93.9
93
.99
3.9
94.0
04.0
04.0
03.9
93
.98
3Q
R
3.9
3
3.9
03.9
73.
963.9
93.9
73.9
53.9
94.
014
.04
4.0
64.0
14.0
13.9
83.9
93.9
73.9
23.
913
.95
3.9
84.0
24.0
64.1
0
4.1
4
5.3
5
6.1
0
5.78
5.8
25.8
75.9
25.9
7
6.0
76.1
06.
136.1
76.2
06.2
16
.25
6.2
76
.29
6.2
86.
266.2
9
6.3
26.3
46.3
76.3
96.4
16.3
66.2
76.2
96.3
36.3
76.4
26.4
36.4
66.4
86.4
96.5
16.5
16.4
56.4
56.4
86.5
16.5
36.4
96.4
16.4
36.4
66.4
86.4
96.3
06.2
2
6.2
46.
276.3
06.
336.
366.3
86.4
06.4
06.
366.3
56.
316.2
56.2
26.2
46.2
96.3
46.
376.
416.4
06.2
36.
115.9
45.
895.
925.7
55.7
55.
745.7
55.7
05.
615.
53
5.47
5.41
4.6
73.9
84.3
44.4
54.4
34.4
54.5
74.6
94.7
24.6
94.6
94.7
04.7
04.7
34.7
74.8
14.7
74.6
04.6
34.6
84.7
24.6
74.6
74.6
24.6
64.6
44.6
94.7
1
4.7
94.7
44.7
64.7
44.7
34.6
94.6
54.
614.6
04.5
84.5
84.5
8
4.4
14.4
34.5
04.5
84.6
04.6
04.6
0
4.4
84.4
64.4
84.4
84.4
94.4
94.4
9
4.4
34.3
74.3
04.2
64.2
94.3
34.3
54.3
54.3
44.2
64.
214.2
54.2
74.1
84.3
04.2
94.2
74.2
64.2
7
4.0
94.1
34.1
5
4.1
53.9
23.9
8
4.0
64.0
54.0
5
4.0
84.0
94.1
24.0
74.0
64.1
24.1
14.1
14.1
54.1
14.0
94.1
14.0
34.0
64.0
54.1
04.1
14.1
44.1
04.1
1
4.1
84.0
04.0
54.0
84.1
04.1
24.1
34.1
44.1
54.1
74.1
24.1
24.1
0
4.0
74.0
74.0
74.0
64.0
74.0
43.9
23.9
33.9
54.0
34.0
64.0
64.0
74.0
74.1
04.1
24.1
4
4.1
24.1
74.1
54.1
44.1
44.1
54.1
94.1
94.2
04.2
04.2
3
4.2
0
4.2
94.3
54.3
74.4
04.4
14.4
1
4.4
04.4
34.4
74.4
94.5
34.5
24.5
74.6
24.6
14.6
14.6
64.6
54.7
04.7
24.7
24.7
54.8
04.8
34.8
04.8
04.8
04.7
94.8
54.9
45.0
05.
025.0
45.
065.0
55.0
95.1
0
5.06
5.0
95.1
35.1
25.
115.0
95.0
85.0
95.1
05.1
25.2
05.2
95.3
45.
365.3
95.
415.
395.
385.
38
5.46
5.4
95.4
95.4
85.4
95.5
05.5
05.
535.5
45.5
55.
56
5.5
75.5
85.
625.
665.7
05.7
25.7
55.7
75.7
95.8
25.8
45.8
55.
765.6
75.
665.6
35.6
45.
665.
715.7
45.6
95.6
25.
665.6
45.6
85.7
35.7
85.8
0
5.8
55.
885.
915.
966.0
06.0
56.0
86.0
96.1
06.1
06.1
06.
116.1
26.1
46.1
56.1
76.1
96.2
26.2
26.2
16.1
96.2
06.1
86.1
9
6.1
0
CO
C5
Tab
le 3
5.
Wat
er-l
evel
mea
sure
men
ts f
rom
rec
orde
r ch
art,
in f
eet
belo
w l
and-
surf
ace
datu
m C
onti
nued
Day
1951
Dec
.
1952
Jan.
Feb
.M
ar.
Apr.
May
Jun
eJu
lyA
ug.
Sep
t.O
ct.
Nov
.D
ec.
Al-
4-2
5dc
1.............................................................
2 ........ .
....
....
....
....
....
....
....
....
....
....
....
....
..3
........ .
....
....
....
....
....
....
....
....
....
....
....
....
..4
............ .
....
....
....
....
....
....
....
....
....
....
....
..5
........................
...................................
6 .... .
..................
....................................
7 ................ .
......
....
....
....
....
....
....
....
....
....
8 .... .
....
....
....
....
....
....
....
....
....
....
....
....
....
..9
.... .
..................
....................................
10...........................................................
11...........................................................
1 9 13...........................................................
14
....
....
....
....
....
...
....
....
....
....
....
....
....
....
....
15
........ .
..................................................
16...........................................................
17...........................................................
18.... .
................................. ....................
19...........................................................
20
....
....
....
....
....
....
....
....
....
....
....
....
....
....
...
21...........................................................
22
....
....
....
....
....
....
....
....
....
....
....
....
....
....
...
23..........................................................
24...........................................................
25........ .
....
....
....
....
....
....
....
....
....
....
....
....
..26...........................................................
27........ .
....
....
....
....
....
....
....
....
....
....
....
....
..28
....
....
....
....
....
....
....
....
....
....
....
....
....
....
...
29
....
....
....
....
....
....
....
....
....
....
....
....
....
....
...
30...........................................................
31...........................................................
10
.57
10.5
7
10.7
0
10.7
5
10.8
3
10.7
9
10.7
3
10
.66
10.6
1
10
.54
10.4
9
10..4
3 10.4
5
10.4
9
10.5
7
10.6
3
11.6
0
11.6
6
11.6
8
11.7
6
11.8
0
11
.86
1
1.9
2
11
.97
12.0
3
12
.06
1
2.0
9
12.
17
12.2
3
12
.27
1
2.3
4
12.3
8
12
.42
12.4
8
12
.53
1
2.5
7
12
.61
12.6
8
12
.70
1
2.7
6
12
.80
1
2.8
5
12
.88
1
2.9
4
13
.00
1
3.0
3
13.0
6
13.1
1
13
.16
1
3.2
1
13
.23
13.2
8
13
.33
1
3.3
7
13.4
1
13.4
5
13.4
9
13
.52
1
3.5
5
13.6
0
13.6
2
13
.67
13.7
0
13
.73
13.7
7
13.8
1
13.8
5
14
.04
1
4.0
5
14
.08
14
. 10
14
. 14
14
. 17
14.2
0
14.2
4
14.2
8
14.3
2
14
.34
14.3
6
14
.41
14.4
2
14
.44
1
4.6
1
14
.65
1
4.6
6
14
.67
1
4.7
3
14
.73
14.7
6
14.7
9
14.8
3
14
.84
14.8
81
4.9
1
14
.93
1
4.9
6
14
.99
15.0
2
15.0
2
15.0
2
15.0
6
15
.07
1
5.1
1
15.
11
15
.10
1
5.0
7
14
.96
14.8
2
14
.79
1
4.7
0
14.6
0
14
.38
1
4.0
6
13.3
5
12.9
0
13
.03
.........
13.4
8
13
.54
13.6
2
13.6
8
13
.79
13
. 84
1
3.8
9
13.9
4
14
.02
1
4.0
6
13.8
8
13
.73
1
3.6
7
13
.63
13.6
2
13.7
1
13
.77
1
3.8
2
13.8
5
13
.86
1
3.8
4
13
.84
13.8
113.7
313.6
0
13
.45
13.3
2
13
.18
1
3.0
6
12.9
3
12
.75
1
2.4
6
12
.10
11.8
2
11.6
5
11.5
8
11
.52
11.4
5
11
.47
1
1.5
7
11
.89
11.9
5
11
.84
11.7
0
11
.61
11.2
2
10.9
3
10
.94
10.7
5
10
.51
1
0.2
7
9.9
5
9.4
0
9.4
0
9.4
7
9.3
7
9.2
5
9.2
7
9.0
9
9.0
2
8.9
0
8.7
2
8.4
1
8.0
5
7.9
0
7.8
0
7.7
0
7.5
9
7.5
7
7.6
2
7.7
2
7.9
0
7.9
7
8.0
5
8.1
0
8.0
9
7.8
7
7.6
8
7.5
8
7.8
2
8. 1
0 8.1
3
8.2
2
7.8
6
8.0
2
7.9
9
7.9
4
7.9
4
7.9
9
7.2
4
6.9
7
6.9
2
6.9
7
7.0
0
6.9
2
6.8
4
6. 7
3 6.3
6
6.4
9
6.0
9
5.9
2
6.4
3
6.7
6
6.9
7
7.0
5
7.0
0
7.2
4
7.4
4
7.5
8
7.6
2
7.7
5
7.7
8
7.8
2
7.8
7
7.8
8
7.8
8
7.8
9
7.9
1
7.8
7
7.8
9
7. 9
2 7
.99
8.0
3
7.9
2
7.8
1
7.7
7
7.7
2
7.7
1
7.7
0
7.7
2
7.7
1
7.7
3
7.7
6
7.7
9
7.8
6
7.8
7
7.8
8
7.9
3
7.9
7
7.8
0
7.8
0
7.8
0
7.7
8
7.7
6
7.7
9
7.7
9
7.7
7
7.7
8
7.8
1
7.8
5
7.8
7
7.9
0
7.9
4
7.9
3
7. 9
6
8.0
0
8.0
2
8.0
8
8. 1
4 8.2
0
8.2
3
8.2
2
8. 1
7 8
.18
8.2
2
8.2
2
8.2
4
8.3
0
8.3
3
8.3
3
8.3
7
8.4
1
8.4
4
8.4
7
8.4
9
8.5
1
8.5
3
8.5
4
8. 5
2 8
.52
8.5
5
8. 5
3 8.5
0
8. 5
1 8
.52
8.4
9
8. 5
6 8.5
5
8.6
0
8.6
7
8.8
5
8.9
7
9.0
3
9.0
9
9. 1
3 9.
18
9.2
6
9.3
0
9.3
6
9.4
0
9.4
7
9.5
6
9.6
1
9.6
7
9.7
4
9.7
7
9.8
3
9.8
5
9.9
3
10
.01
10.0
5
10.1
2
10
.18
1
0.2
4
10.2
8
10
.34
1
0.4
0
10
.45
1
0.5
0
10
.57
1
0.6
1
10
.67
10.7
3
10
.79
1
0.8
3
10
.90
10.9
5
11.0
1
11.0
6
11
.15
1
1.1
9
11
.25
Tab
le 3
5.
Wat
er-l
evel
mea
sure
men
ts f
rom
rec
orde
r ch
art,
in f
eet
belo
w l
and-
surf
ace
da
tum
Con
tinu
edto <v
i
Day
1953
Jan
. F
eb.
Mar
. A
pr.
M
ay
June
July
A
ug.
Sep
t.
Oct
. N
ov.
Dec
.
M 1 i 1
O
Jan.
Feb
. M
ar.
Apr
. H O
> i
A1
- 4 -
2 5d
c C
on
tin
ued
1 .............................
2 ........................
....
.3
.............................
4 ........................
....
.5
........................
....
.6
.............................
7 .............................
8 ........................
....
.9
........................
.....
10.............................
11.............................
12.............................
13.............................
14.............................
15.............................
16.............................
17.............................
18.............................
19
....
....
....
....
....
....
....
.2
0..
....
....
....
....
....
....
...
21
....
....
....
....
....
....
....
.2
2..
....
....
....
....
....
....
...
23.............................
24...
...
....
....
....
....
....
...
25
....
....
....
....
....
....
....
.26.............................
27
....
....
....
....
....
....
....
.2
8..
....
....
....
....
....
....
...
29
....
....
....
....
....
....
....
.30.............................
31
....
....
....
....
....
....
....
.
11.3
111
.35
11.4
111
.47
11.5
611
.61
11.6
611
.70
11.7
411
.76
11.7
811
.80
11.7
511
.76
11.8
411
.88
11.9
311
.99
12.0
312
.07
12.1
312
.18
12.2
412
.26
12.3
112
.34
12.4
012
.43
12.4
912
.53
12.5
9
12.6
312
.68
12.7
112
.75
12.8
012
.83
12.8
712
.92
13.0
013
.03
13.0
713
.14
13.1
913
.22
13.2
613
.30
13.3
513
.37
13.4
813
.51
13.5
613
.58
13.6
413
.68
13.7
313
.74
13.8
113
.83
13.8
713
.90
13.9
313
.95
14.0
214
.05
14.1
114
.14
14.0
914
.08
14.0
714
.06
14.0
514
.03
14.1
214
.16
14.1
914
.23
14.2
714
.30
14.3
414
.38
14.4
214
.47
14.5
014
.53
14.5
714
.60
14.6
414
.68
14.7
1
14.7
314
,77
14.8
014
.83
14.8
714
.90
14.9
314
.96
14.9
915
.02
15.0
515
.07
15.1
015
.12
15.1
415
.16
15.1
915
.20
15.2
215
.23
15.2
315
.24
15.2
615
.27
15.2
615
.24
15.2
315
.21
15.1
715
.10
15.0
615
.05
15.0
615
.07
15.0
815
.03
14.9
114
.74
14.5
514
.41
14.3
114
.27
14.2
714
.23
14.1
714
.12
14.1
114
.00
13.8
913
.79
13.7
013
.48
13.2
813
.13
12.9
912
.80
12.6
712
.52
12.2
61
9
f!9
11.8
3
11.6
911
,62
11.4
110
.82
10.3
210
.08
9.92
9.79
9.67
9.45
9.31
9.51
9.57
9.65
9.35
9.21
9fn
8.88
8.89
8.84
8.97
8.87
8.62
8.47
8.46
8.47
8.56
8.32
8.29
7.93
7.72
7.40
7.37
7.46
7.88
7.94
7.83
7.64
7.48
7.44
7.53
7.59
7.65
7.70
7.69
7.44
7.27
7.05
6.99
6.75
6.72
6.83
6.64
6.67
6.68
6.72
6.69
6.64
6.48
6.53
6.96
7.25
7.38
7.42
7.43
7
1^
7 Zt
1
7.61
7.67
7.65
7.45
7.57
7.61
7.59
7.60
7.68
7.69
7.71
7.73
7.77
7.82
7.83
7.88
7.93
7.96
7.96
7.98
7 99
8.00
8.06
8.06
8.06
8.09
8.12
8.09
8.10
8.13
8.13
8.19
81
Q
S.2
28.
278.
308.
328.
338.
338.
368.
398.
418.
428.
458.
478.
498.
508.
488.
508.
498.
478.
508
^4.
8.55
8.43
8.37
8.35
8.42
8.43
8.42
8.39
8.37
8.41
8.41
8.41
8.47
8.37
8.27
8.29
8.19
8.24
8.23
8.21
8.18
8.17
8.15
8.18
8.19
8.24
8.27
8.32
8.36
8.45
8^4
8.66
8.69
8.72
8.81
8.89
8.95
9.01
9.07
9.11
91 ^
9.19
9.2
29.2
79.3
59.4
49.4
89.5
59.6
49.7
19.
769.
819.8
79.9
39.9
81
0.0
410
.09
10
.15
10.2
110
.28
10
.35
10
.45
10.4
710
.52
10
.88
10.9
110
.98
10.8
3
11.0
811
.14
11.1
91
1.2
511
.30
11
.35
11.3
811
.44
11.5
011
.54
11
.60
11.6
211
.68
11
.74
11.8
011
.85
11.8
911
.94
12.1
61
2.1
912
.24
12.2
912
.35
12.3
912
.43
12.5
012
.54
12.6
0
12
.64
12.6
812
.72
12.7
712
.81
12
.88
12.9
012
.96
13.0
013
.04
13.0
913
.13
13.1
713
.21
13.2
513
.28
13.3
11
* M
13.4
313
.45
13.4
713
.52
13.5
7
13.6
013
.65
13.7
213
.77
13.8
113
.85
13.9
113
.94
13.9
814
.02
14.0
614
.11
14.1
514
.19
14.2
414
.27
14.3
114
.33
14.3
714
.40
14.4
214
.45
14.4
714
.49
14.5
2^
14.6
3
14.6
414
.67
14.6
814
.67
14.6
514.6
414
.63
14.6
214.6
214
.63
14.6
414
.66
14.6
714
.69
14.7
014
.72
14.7
314
.61
14.6
014
.59
14.5
2
Tab
le 3
5.
Wat
er-l
evel
mea
sure
men
ts f
rom
rec
orde
r ch
art,
in f
eet
belo
w l
and-
surf
ace
datu
m C
onti
nued
Day
1951
Sept.
Oct.
Nov.
Dec.
1952
Jan.
Feb.
Mar.
Apr.
May
June
July
Aug.
Sept
.Oct.
Nov.
Dec.
A2-3
-33da
1 ...
......
......
......
......
..2
.............................
3 ..
....
....
....
....
....
....
...
4 .............................
5 ..
....
....
....
....
....
....
...
6 .............................
7 .............................
8 ..
....
....
....
....
....
....
...
9 .............................
10.............................
11
....
....
....
....
....
....
....
.12.............................
13.............................
14.............................
15.............................
16.............................
17..
....
....
....
....
....
....
...
18.............................
19.............................
20
....
....
....
....
....
....
....
.21.............................
22
....
....
....
....
....
....
....
.23.............................
24.............................
25.............................
26..
....
....
....
....
......
....
.27.............................
28
........................
....
.2
9........................
....
.30.............................
31.............................
34.4
3
36.0
5
36.2
336.2
636.3
236.3
936.4
336.4
53
6.5
236.5
836.6
136.6
43
6.7
136.7
536.7
93
6.8
236.8
6
37.3
037.3
137.3
437.4
037.4
3
37.4
437.4
837.5
137.5
837.6
237.7
037.7
4
.........
39.3
9
39.3
8
39.6
83
9.6
839.6
939.7
13
9.7
2
39.7
6
39
.88
39.9
2
40
.02
40.0
240.0
340.0
440.0
440.0
640.0
640.0
940.0
940.1
4
40.1
54
0.1
540.1
540.1
54
0.1
94
0.1
940.2
540.2
540.2
5
40.2
540.2
540.2
640.2
840.3
240.3
340.3
44
0.3
440.3
54
0.3
240.3
040.3
140.3
040.3
040.3
140.3
240.3
340.1
340.1
140.0
440.0
340.0
3
40.0
340.0
340.0
340.0
540.0
540.0
540.0
540.0
540.0
5
39.9
939.9
339
.93
39
.93
39
.93
39
.93
39
.94
39.9
43
9.9
439.9
439.9
439.9
43
9.9
53
9.9
840.0
440.0
8
41.4
0
40.2
5
40.2
340.2
340.2
040.0
940.0
23
9.9
639.9
740.1
8
40.1
4
39.6
33
9.6
039.5
5
39
.49
35
.37
34.7
53
4.4
534.4
034.2
334.0
533.8
733.8
03
3.5
83
3.5
933.6
533.7
633.2
232.7
533.8
233.8
232.5
132.4
43
2.6
63
2.8
732.7
433.8
0
32.5
23
2.6
731.6
93
0.5
03
0.1
930.2
930.2
231.1
831.4
9
31.5
031.5
430.4
330.2
33
0.5
931.4
732.2
832.8
332.9
832.9
333.1
33
3.4
63
3.6
233.3
633.3
533.3
23
3.1
833.2
533.4
733.6
9
33
.47
32.9
33
2.4
732.4
532.8
632.9
732.7
332.2
3
32.0
431.3
931.1
331.0
630.4
63
0.3
230.9
430.9
03
0.4
929.0
226.8
925.5
728.5
930.5
031.5
932.2
832.7
63
2.8
53
2.7
732.7
43
2.8
03
2.7
0
32.8
432.9
33
2.9
733.0
033.0
333.0
633.1
133.1
933.2
4
33
.32
33.4
533.5
6
33.9
034.0
034.0
93
4.0
733.9
633.9
033.9
033.7
733.7
23
3.6
433.6
033.6
23
3.6
433.7
13
3.9
23
4.1
1
34.2
834
.42
34
.60
34.7
234.7
934.8
334.8
434.8
23
4.8
1
34.8
43
4.7
834.6
034.4
634.2
533.7
433.2
632.9
632.5
732.4
232.3
532.4
032.5
03
2.9
133.3
63
3.7
23
4.0
23
4.1
734.2
134.0
033.8
333.7
6
33
.78
33.8
633.9
033.9
033.9
034.4
335.0
135.3
635.5
9
35.7
33
5.8
23
5.8
835.9
636.0
13
6.0
936.1
93
6.2
736.3
63
6.4
236.4
73
6.5
836.6
636.7
536.8
336.9
03
6.9
637.0
53
7.1
23
7.2
0
37
.31
37.3
33
7.3
937.4
637.4
737.5
137.5
637.6
337.7
0
37.7
337.7
837.8
33
7.8
73
7.8
937.9
13
7.9
537.9
938.0
138.0
438.0
93
8.1
338.1
638.2
038.2
23
8.2
63
8.2
938.3
33
8.3
63
8.3
938.4
23
8.4
5
Tab
le 3
5.
Wat
er-l
evel
mea
sure
men
ts f
rom
rec
orde
r ch
art,
in f
eet
belo
w l
and-
surf
ace
datu
m C
ontin
ued
Day
1953
Jan.
Feb.
Mar.
Apr.
May
June
July
Aug.
Sept.
Oct.
Nov.
Dec.
1954 Jan.
A2-3
-33da
Conti
nued
1 ...
......
......
......
......
......
......
......
......
......
..2
....
...
....
....
....
....
....
....
....
....
....
....
....
....
...
3 ................ .
....
....
....
....
....
. ..
....
....
....
....
.4
....
...
....
....
....
....
....
....
....
....
....
....
....
....
...
5 ..
....
....
....
....
....
....
....
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....
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....
....
....
....
.6
......................
.. .
.................................
7 ..
....
....
.. .
....
....
....
....
....
....
....
....
....
....
....
.8
....
....
....
...
....
....
....
....
....
....
....
....
....
....
...
9 ..
.. .
................
....
....
....
....
....
. ................
10
....
....
....
....
....
....
....
....
....
....
....
....
....
....
..1
1........ .
................................. ...............
12......................
....
....
....
....
....
....
....
....
....
13
....
....
....
....
....
....
....
....
....
....
....
....
....
....
..1
4........ .
................................. ..
....
....
....
.15..........................................................
16..........................................................
17..........................................................
18..........................................................
19..........................................................
20..........................................................
21..........................................................
22..
.. .
.............. .
....
....
....
....
....
....
....
....
....
.23..........................................................
24................ ...
....
.. ................................
25
....
....
....
.........
. . .
.................................
26..........................................................
27..........................................................
28..........................................................
29..........................................................
30..
.. ..................
....
....
. ..
....
....
....
....
....
....
31..........................................................
38.4
838.5
238
. 56
38
.57
38.5
938
.61
38
.64
38.6
83
8.7
138.7
338
.74
38.7
63
8.7
83
8.8
038.8
338.8
538
.86
38.8
838.9
03
8.9
238
.96
38.9
73
8.9
939.0
23
9.0
33
9.0
53
9.0
739.0
939.1
239
. 15
39.1
6
39
.17
39
.19
39
.21
39
.22
39
.23
39
.25
39
.27
39
.28
39
.30
39
.31
39
.32
39
.34
39.3
53
9.3
73
9.3
83
9.4
03
9.4
139
.43
39.4
63
9.4
83
9.5
03
9.5
23
9.5
43
9.5
63
9.5
83
9.6
03
9.6
23
9.6
4
39
.65
39
.67
39
.69
39
.71
39
.72
39
.73
39
.75
39
.75
39
.75
39.7
63
9.7
739
. 79
39
.80
39
.81
39.8
13
9.8
23
9.8
339.8
43
9.8
539
.86
39
.87
39
.88
39
.90
39
.91
39.
933
9.9
53
9.9
73
9.9
840.0
040.0
14
0.0
4
40. 0
7.4
0.0
940
. 10
40.1
240
. 13
40.
1440.1
440.1
44
0.1
440
. 14
40
.15
40
.16
40
.17
40.1
940.2
14
0.2
24
0.2
44
0.2
64
0.2
74
0.2
840
. 30
(40.
3140.3
440.3
440.3
64
0.3
740.3
740.3
840.3
94
0.3
9
40.3
940.3
940.3
94
0.4
040.4
14
0.4
140.4
240.4
24
0.3
94
0.3
34
0.2
240.1
23
9.9
539
.68
39
.20
38
.55
38.
133
7.4
93
7.0
936
. 55
35
.15
35
.39
35
.88
35
.84
35
.93
35
.82
35
.82
35
.78
35.5
435
.26
35
.13
34
.90
35
.15
35.2
43
5.2
13
5.3
33
5.4
035.3
93
5.4
33
5.4
73
5.2
835.1
435.0
13
4.9
134.8
734.9
23
4.6
03
4.4
83
4.4
43
4.5
53
4.4
734
. 15
33
.17
32.
333
1.0
83
1.2
83
2.6
03
3.7
03
3.9
23
4.2
434.3
2
34.
123
3.9
63
3.8
03
3.4
33
2.8
532
.66
32.6
63
2.6
93
2.8
63
2.5
73
1.7
53
1.8
43
2.4
532.7
43
2.7
23
2.7
03
2.6
499
71
32.6
732.4
83
2.4
832.3
531.8
531
. 18
30.5
729.7
929.0
928.6
12
7.2
82
5.7
02
7.4
0
28
.32
28
.49
28
.66
28
.88
29.0
32
9.5
229.4
12
9.7
93
0.1
52
9.6
230.0
130.6
631
. 11
31
.40
31
.63
31
.82
31.
7831
. 56
31.4
63
1.4
73
1.6
83
1.7
13
1.6
931.6
03
1.6
83
1.8
23
1.8
73
1.8
43
1.8
832
. 12
32
.22
32
.32
32
.48
32.5
53
2.6
13
2.7
03
3.0
233.4
633.7
633.9
6
34.2
7
34.9
43
5.0
43
5.0
735
. 12
35.
1835.2
335.2
435.3
135.3
43
5.3
735.4
4
35.9
9
36.2
4
38
.45
Tab
le 3
5.
Wat
er-l
evel
mea
sure
men
ts f
rom
rec
orde
r ch
art,
in f
eet
belo
w l
and-
surf
ace
datu
m C
onti
nued
1953
Day
Mar
. I
Apr.
I
May
I
June
I
July
I
Aug
. I
Sep
t.
I O
ct.
I N
ov.
Dec
.
1954
Jan
. F
eb.
Mar
.
Dl-
4-6
ddc2
1 ...
......
......
......
......
......
......
......
......
......
..
3 ..
....
....
....
....
....
....
....
....
....
....
....
....
....
....
.4
....
....
....
....
....
....
....
....
....
....
....
....
....
....
...
5 ..
....
....
....
....
....
....
....
....
....
....
....
....
....
....
.6
......................
....
....
....
....
....
....
....
....
....
.7
......................
....
....
....
....
....
....
....
....
....
.8
....
....
....
....
....
....
....
....
....
....
....
....
....
....
...
9 ........ .
..............
...................................
10...........................................................
11
.... .
.................................. .
..................
12...........................................................
13..........................................................
14..........................................................
15..........................................................
16..........................................................
17..........................................................
18..........................................................
19
....
....
....
....
....
....
....
....
....
....
....
....
....
....
..20......................
.....................................
91 99 23..........................................................
94
9>i
26
....
....
....
....
....
....
....
....
....
....
....
....
....
....
...
97 28
....
...
....
....
....
....
....
....
....
....
....
....
....
....
. ..
29..........................................................
30..........................................................
31..........................................................
17.6
1
16.3
71
6.3
916.4
416.4
516.4
71
6.5
216.5
716.6
2
16.6
61
6.6
716.6
816.7
11
6.7
41
6.7
716.7
916.6
81
6.7
116.7
516.8
016.8
316.8
91
6.9
11
6.9
517.0
017
. 10
17
.12
17.
151
7.1
81
7.2
31
7.2
917.3
31
7.3
517.3
11
7.3
51
7.3
617.3
21
7.2
917.2
6
17
.25
17
.31
17
.39
17
.43
17
.49
17
.51
17.5
91
7.5
517
.51
17.5
417.5
81
7.6
41
7.7
11
7.7
71
7.8
31
7.8
8
17
.86
17
.68
17
.44
17
.23
16.9
11
6.6
5
15
.23
14
.90
14.5
314
.11
13.8
51
3.7
4
12.8
71
2.6
712.5
11
2.3
71
2.2
512.1
311.9
71
1.3
4
3.2
72.7
22.2
72
.33
2.7
02.1
13
.17
3.4
23
.70
3.8
0
4.4
54.6
14.6
64.6
54.6
74
.65
4.5
04.4
34.0
63.7
63
.98
3.7
93.4
83.9
84
.35
4. 5
54.9
15.
13
5.0
24.9
14
.64
4.6
84.9
14.6
25.0
75.2
55
.51
6.0
3
6.1
96.3
16.3
66.4
56.5
86
.62
6.6
86
.73
6.7
46.7
06.5
56.3
16
.42
6.5
26.5
46.
56
6.5
16
.40
6.3
66.3
26
.32
6.2
66.2
06.
10
5.9
74.9
95.6
95.7
65.6
75.5
65.5
4
5.5
45.4
84.2
35.4
05.7
55.8
25.9
25.8
96.
18
6.3
26
.62
5.8
96.
18
6.4
66
.72
6. 9
67
.22
7. 5
07.7
58
.00
8.2
08.4
08.7
0
9. 1
39.2
89
.44
9.6
29.7
6
9.9
11
0.0
810.2
21
0.3
41
0.4
410.6
21
0.7
21
0.8
11
0.8
91
1.0
011
. 11
11
.20
11
.28
11.3
41
1.3
61
1.3
811.4
111.4
21
1.4
51
1.4
311
.41
11.4
311.4
011.3
71
1.3
91
1.3
71
1.3
511.2
711.2
011.1
811.1
2
11
.06
11
.04
11.0
01
0.9
710.9
21
0.9
410.9
710.9
710.9
81
1.0
01
1.0
31
1.0
511.0
711.0
911
. 12
11.
1311
. 18
11
.21
11
.27
11.3
61
1.4
711
. 56
11.6
311.7
111.7
811.8
811.9
512.0
312
. 11
12
.28
12.3
21
2.3
912.4
512
. 51
12.6
212.6
81
2.7
612.8
31
2.9
11
2.9
713.0
21
3.0
81
3.1
313
. 17
13.2
11
3.2
513.3
013.3
71
3.4
213.4
613.5
113.5
713.6
2
13
.74
13.8
013.8
713.9
2
13
.97
14
.04
14.0
91
4.1
414
.21
14.2
514.3
014.3
514.4
114.4
614.5
11
4.5
51
4.5
714.6
314.7
014
.76
14.8
114.8
714.9
4
15.1
01
5.1
515.2
215.2
815
.36
15.4
215.5
015.5
515.6
315.7
015.7
6
15
.84
15.9
11
5.9
91
6.0
516
. 10
16.
171
6.2
21
6.2
71
6.3
11
6.3
416.3
816.3
91
6.3
816.2
71
6.2
51
6.2
316.2
11
6.2
01
6.2
11
6.2
11
6.2
216.2
416.2
51
6.2
51
6.2
51
6.2
516.2
71
6.2
8
16
.33
16
.37
16
.40
16.4
41
6.4
91
6.5
416.5
91
6.6
31
6.6
91
6.7
41
6.7
91
6.8
41
6.8
81
6.9
21
6.9
717.0
117.0
6
17.6
5
Tab
le 3
5.
Wat
er-l
evel
mea
sure
men
ts f
rom
rec
orde
r ch
art,
in f
eet
belo
w l
and-
surf
ace
datu
m C
onti
nued
Day
1953
Apr.
May
June
July
Aug
.S
ept.
Oct
.N
ov.
Dec
.
1954
Jan.
Feb
.M
ar.
Apr.
Dl-
4-,
9bal
1 ...
......
......
......
......
......
......
......
......
......
.2
..........................................................
3 ..
....
....
....
....
.. .
....
....
....
....
....
....
....
....
....
4 ........ ...............
..................................
5 ..........................................................
6 ..
....
....
....
....
....
....
.. .
....
....
....
....
....
....
....
7 ..
....
....
....
....
....
....
....
....
....
....
....
....
....
....
8 ........ .
....
....
....
....
....
....
....
....
....
....
....
....
9 ..
....
....
....
....
....
....
....
....
....
....
....
....
....
....
10
....
....
....
....
....
....
....
....
....
....
....
....
....
....
.1
1..
....
....
....
....
....
....
....
....
....
....
....
....
....
...
12
....
....
....
....
....
....
....
....
....
....
....
....
....
....
.1
3........ .
................................................
14..........................................................
15.........................................................
16........ .
................................................
17......................... .
...............................
18..........................................................
19..........................................................
20..........................................................
21..........................................................
22..........................................................
23
....
....
....
....
....
....
....
....
....
....
....
...........
24
....
....
....
....
....
....
....
....
....
....
....
....
....
....
..2
5..
....
....
....
....
....
....
....
....
....
....
....
....
....
...
26
....
....
....
....
....
....
....
....
....
....
....
....
....
....
..27..........................................................
28
....
....
....
....
....
....
....
....
....
....
....
....
....
....
..2
9..
....
....
....
.. .
.............................. .
.........
30....
..........................................
...........
31
....
....
....
...
....
....
....
....
. .........................
22.7
12
2.7
622.8
12
2.8
322
. 86
22.
9022
. 93
22.
9622.9
622.9
722
. 98
22
.97
22.
9522
. 90
22.
832
2.7
322
.64
22.6
122
.61
22.
5922
. 54
22.4
92
2.4
6
22.5
122.6
32
2.6
82
2.7
122.7
222.7
32
2.6
522.5
72
2.5
82
2.6
32
2.7
122.8
22
2.9
423.0
723
. 15
23
.22
23.2
52
3.2
323
. 17
22
.83
22
.27
22
.01
21
.88
21
.90
21.9
622.0
02
1.8
62
1.4
32
0.6
220.0
21
9.7
4
18.
1418
. 11
18.0
517
.98
17.9
517
.70
17.
11
14.
7314
.72
14.6
914
. 76
14.8
114
.86
14.8
614
.91
15.5
3
15
.54
15.3
515
.38
15.4
015
.40
15.4
11
5.4
4
15.3
015
.29
15.
3315
. 39
15.
3415
.32
15.3
115
.34
15.4
515
.66
15.7
615
. 75
15.4
615
.08
14.9
214
.78
14.
7114
.65
14
.84
14.7
014
.77
15.0
0
14.8
114
.72
14.6
814
.75
14.8
814
.98
15.
1115
.21
15.3
715
. 53
15.6
415
. 73
16.0
1
16.5
816
.62
16.6
616
.69
16.7
8
17.0
317
.05
17.0
417
.04
17.0
517
.05
16.9
016
.72
16.6
616
.62
16.6
016
. 57
16.5
216
. 53
16.
5716
. 59
16.6
916
.76
16.8
216
.89
17.0
117
. 13
17.2
317
.38
17.4
717
.62
17.7
01
7.8
217
.94
20.7
020.9
021
. 15
21
.30
19.
1518
. 87
18.6
3
17.
5317
.21
17.
1517
. 11
17.0
617
.03
17.0
017
.02
17.0
617
.00
16.9
11
6.8
716
.86
16
.89
16
.95
17.0
617
. 11
17
.33
17
.50
17.6
317
. 73
17.
821
7.8
917
.96
17.9
918
.02
18.
1218
. 13
18.0
117
.88
17.7
01
7.4
41
7.4
817
.55
17
.62
17.7
01
7.8
217
.91
17.9
7
18.0
618
. 13
18.2
318
.33
18.4
118
.48
18.6
518
. 72
18.8
218
.87
18.
9519
.01
19.0
419
. 13
19.
1719
.25
19.3
119
.37
19.4
119
.48
19.5
319
.59
19.6
819
.74
19.
781
9.8
219
.86
19.9
62
0.0
120.0
7
20
.13
20.1
920.2
42
0.2
72
0.3
020.3
520.4
02
0.4
620.5
120.5
620
. 62
20.6
820
. 72
20.
7720
. 83
20.8
720
. 90
20.
942
1.0
3
21
.13
21.0
820
.06
21
.08
21.
1-221
. 16
21.
182
1.2
02
1.2
52
1.2
82
1.3
0
21.3
52
1.3
82
1.4
621.4
921.5
52
1.5
92
1.6
22
1.6
52
1.6
721.7
22
1.7
321
. 76
21
.76
21
.76
21.
7721
. 78
21
.61
21
.83
21.8
82
1.9
321
. 94
21.9
421.9
521.9
621
.96
21.9
82
2.0
42
2.0
8
22
.29
22.3
52
2.4
022.4
622.5
022.4
922.4
822.4
822
.51
22
.60
22.6
72
2.7
522.7
92
2.8
32
2.8
522.8
72
2.8
92
2.9
12
2.9
42
2.9
52
2.9
92
3.0
32
3.0
62
3.0
72
3.0
623.0
723
. 14
23.
1923.2
5
23
.32
23
.33
23
.32
23.2
22
3.1
623
. 13
23.
1323.1
423
. 16
23
.21
23.2
423
.26
23
.26
23.
252
3.2
12
3.2
123.2
22
3.2
2
23.3
1
to CO
Tab
le 3
5.
Wat
er-l
evel
mea
sure
men
ts f
rom
rec
orde
r ch
art,
in f
eet
belo
w l
and-
surf
ace
datu
m C
onti
nued
Day
1953
May
June-
July
Aug
.S
ept.
Oct
.N
ov.
Dec
.D
ay19
53
May
June
July
Aug
.S
ept.
Oct
.N
ov.
Dec
.
Dl-
4-2
5aa2
1 . _
__
...
2 ............
3 ............
4 ............
5 ............
6 ............
7 ............
8 ............
9 ............
io...
. ....
....
11............
12............
13............
14
....
....
....
15............
16............
13.0
14.3
14.
914.9
15.0
15.
115
. 2
15
.215.4
15.
515.6
18.3
18.6
18
.919.3
19.7
20.
120
. 5
20.
9
22.
5
25
.0
26
.0
26
.0
25.
5
25
.0
24.8
23
.9
23
.6
22
.0
21.3
20
.6
18.
51
8.4
18.4
18.3
18.
218
. 1
18
.017.9
16.9
17
..........
18
..........
19
..........
20..........
21..........
22..........
23..........
24..........
25..........
26..........
27..........
28..........
29..........
30..........
31..........
15.6
15
.816
. 1
16.2
16
.416.4
16
.216.4
16.
516.6
16.8
17.
117.4
17
.717
. 9
23.6
24.3
26.2
26
.0
25.
5
25
.5
24.8
24.3
22.
5
20.4
20
.320
. 2
20.
1
20
.019.8
19.
718
. 8
18.
718
. 6
18.
6
16.6
15
.9
o g to 00
238 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
M'-irocpcppt-cOTpincpi-iincocpcoO'-icpi^coin ri
cococacacocococococor-r-r-r-r-r-D-r-tocDtoto ; ; ; ;
PL, in in in" in in in" in" in" in" in in in" m in in to CD' CD" CD" CD to to to to* CD to CD CD
co co co co" co* co co* co" co rt< TP rt<" * TP TP rt< rt< rt< rt< rt< in in in in in in
C3C3O'-l'-ICN>CN>COCOTt<Tt<ininCDCDCDr-r-COcaCOa5a5OO'--l'-lCN>COTt<Tt<
-I -( CM" CM" c\? CM* CM" CM* CM" CM" CM* CM" CM" CM* CM" CM co" co" co' co* CN! CNI' CNI" co' co' co' co' co co" co" co"
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co co co co co co co co co" co co O)O)O)O)OiO)O)OiO)O)O)O) 03 03 05 03 03
Jit ICOD-OC3 CNCNIOOO3ini-lt--COt--CNI CNI CO
. n - ' - iJ O*-ir- IO3OOi-iO3CNii-iCNiTt<coeoin 1 '. '. '. !rt<CDinc-ocDi-icD
cocoi> *cDCDCDCocDCDCDCDcocDinm ; ; ; ; ^-^ininininincDin
mlt co _ Q CD ; ; r-ocor-cDinin^fTpcO'-irocar-r-cDinTpcococN
i-H ; i ti »OOOOOOOOOO3O3O3O3O3O>O5O5O>O3O>
i-iocar-cDr-r-r-cacacacocOD-r-cDCDCDCDCDininTt<coocDco ; t-eo CD CD" in in in in in in in" in" in in m in in in in" in" in" in in in in in in rt<" rt<" : CM CNI
*COCNICOOt-CNICD'-linCOi-ICOOOO'-ICOTt<O3tNlint--COCOCOCOt-linO Tt<Tt<ininCDCDt~t~COCOCOO3O3OOOOO3O3COCOt--CDinTt<'-ICOtOTt<CO
O3O3 CNI CNICOCOTt<ininCDCDt~t~COCOO3OO'-l'-''-'COCO
inin CD CDCDCDtOCDCDCDCDCOtOtOCDtOt-D-C^t^C^C^C^
CN>COTt<inCDr-Caa5 '-l'-li-l'-li-ICN>CN>C\>CN>CN>CN>CN>C»]fOCN>COW
Tab
le 3
5.
Wat
er-l
evel
mea
sure
men
ts f
rom
rec
orde
r ch
art,
in f
eet
belo
w l
and-
surf
ace
datu
m C
onti
nued
Day
1953
Feb
.M
ar.
Ap
r.M
ayJu
ne
July
Aug
.S
ept.
Oct
.N
ov.
Dec
.
1954
Jan.
Feb
.M
ar.
Apr.
Dl-
5-3
4cc2
1 ......
. .
.... .
....
....
.2
......................................
3 ......................................
4 ......................................
5 ......................................
6 ......................................
7 ......................................
8 ......................................
9 ......................................
10
........................
....
....
....
..11
........................
....
....
....
..12
........................
....
....
....
..1
3........................
..............
14
........................
....
....
....
..15......................................
16......................................
17......................................
18........................
..............
1 Q
20......................................
21......................................
22......................................
23......................................
24........................
..............
25......................................
26........................
..............
27......................................
28......................................
29......................................
30......................................
31......................................
9.96
9.9
5
9.7
59.7
2
9.5
99.5
59.5
39.
519.5
09.
469.4
49.
439.4
39.
379.
379.3
59.3
4
9.33
9.3
39.
339.3
39.
339.3
29.
319.
279.2
79.
259.
239.
219
.20
9.2
09.
219.2
09
.20
9.24
9.2
49.2
49.2
49.
269.2
89.3
09.
329.
329.3
29.
339.
359.
36
9.3
89.3
99.3
99.
419.
419.4
29.
439.4
59.4
89.4
99.
519.
539.5
39.
539.5
59.
569.5
89.5
99.5
99.5
99.5
89.5
49.4
59.4
09.3
89.
329.
319.2
99.2
89.2
99.2
9
9.3
09.2
99.
268.9
58.
628.4
78.4
28.
438.
438.
468.4
88.4
98.5
18.5
08.
468.
428.
418.
107.
857.5
07.4
17.
417.0
96.7
96.5
3
6.21
6.1
66.2
26.4
4
6.6
66.5
36.5
56.6
06.6
96.8
06.8
6
5.5
05.
535.5
95.6
85.6
35.
846.1
36.3
96.6
26.8
16.
916.9
57.0
57.
227.3
07.
417.
527.6
57.7
97,
918.0
08.
12
8.2
58.3
98.
438.5
48.6
48.7
88.8
48.
928.9
99.0
89.1
39.2
09.2
69.2
99.3
29.
369.4
29.4
79.5
29.
579.6
39.6
89.7
29.7
59.8
09.
839.8
79.9
09.9
59.9
810
.01
10.0
31
0.0
610.0
910
.10
10.1
210.1
41
0.1
51
0.1
710
.18
10
.19
10.1
910
.26
10
.27
10.4
210
.43
10
.44
10.4
610
.47
10.4
810.5
010
.51
10.5
210
.53
10.5
31
0.5
410
.54
10.5
610
.56
10.5
710
.57
10
.54
10.5
210
.52
10.5
110.4
9
10.3
31
0.2
91
0.2
81
0.2
81
0.2
81
0.2
510.2
01
0.1
410.1
010
.06
10.0
41
0.0
710
.09
10
.10
10.1
01
0.1
210
.14
10
.14
10
.14
10
.15
10
.17
10.1
810.1
91
0.1
910
.19
10.1
810
.17
10.1
7W
ytS
10.1
41
0.1
410
.10
10.0
810
.05
10.0
19.9
9
9.8
09.8
09.7
89.
779.7
79.7
4
9.71
9.7
09.7
09.7
0 9
.70
9.7
09.7
19.
719.6
99.7
09.
719.
719.
739.
719.
749.7
59.
74
9.7
29.7
49.7
59.
789.
819.8
29.8
39.
839.8
49.8
59.
869.8
59.8
59.
869.8
99.9
09.9
19.
939.
96
10
.03
10.0
310
.04
10.0
61
0.0
910
.11
10
.14
10.1
510
.16
10
.19
10
.19
10
.20
10.2
010
.21
10
.22
10
.22
10.2
310
.23
10
.24
10
.24
10.2
41
0.2
410
.24
10
.24
10
.24
10.2
510
.24
10
.23
10.2
210
.22
9.9
9
9.9
09.9
09.9
09.9
09.9
09.8
99.8
79.8
69.8
59.8
59.8
69.
869.8
69.8
59.8
49.8
39.8
39.8
39.8
29.8
29.8
29.8
29.8
29.8
29.
819.
819.
819.
819.8
0
9.7
99.7
99.7
79.
619.
569.5
29.
51
9.4
99.
519.
529.5
29.5
39.5
39.
569.5
7
Tab
le 3
5.
Wat
er-l
evel
mea
sure
men
ts f
rom
rec
orde
r ch
art,
in f
eet
belo
w l
and-
surf
ace
da
tum
Con
tinu
ed
Day
1951
Au
g.
Sep
t.O
ct.
Nov
.D
ec.
1952
Jan.
Feb
.M
ar.
Ap
r.M
ayJu
ne
July
Aug
.S
ept.
Oct
.N
ov.
Dec
.
D2-4
-9bc
1 ...
......
......
....
2 ..
....
....
....
....
.Q 4
....
....
....
....
...
5 ...................
6 ...................
7 ...................
8 ..
....
....
....
....
.9
....
....
....
....
...
10...................
11..
....
....
....
....
.1
2..
....
....
....
....
.1
3..
....
....
....
....
.1
4..
....
....
....
....
.1
5..
....
....
....
....
.1
6..
....
....
....
....
.1
7..
....
....
....
....
.1
8..
....
....
....
....
.1
9...................
20
....
....
....
....
...
21
....
....
....
....
...
22..
....
....
....
....
.23...................
24..
....
....
....
....
.25...................
26...................
27...................
28..
....
....
....
....
.2
9..
....
....
....
....
.3
0..
....
....
....
....
.3
1..
....
....
....
....
.31.5
0
31.3
6
29.2
3
27.8
1
27.1
327.1
4
26.6
8
26.4
8
26.1
5
25.8
625.8
125.7
525.6
925.7
02
5.6
925.6
725.5
225.6
225.6
2
25.6
725.5
925.5
925.5
625.5
725.5
725
.52
25.4
925.4
725.5
025
.43
25.3
825
.41
25.4
125.4
825.5
525
.27
25.2
125
.17
25.1
425.0
825.1
025.0
8
25.0
7
25.2
0
25.2
325
.21
25.1
S25.2
025
.11
25.1
125.1
425.1
725.1
525.2
025.2
025.2
525.3
025.2
725.1
525.1
325
.12
25.1
5
25.2
32
5.2
925.2
925.2
92
5.2
92
5.2
72
5.2
025.2
525.3
425.2
42
5.2
325.1
725.1
42
5.1
225.1
225.0
825
.11
25.1
725.2
225.2
025.2
225.2
725.2
72
5.2
525.2
725.3
42
5.4
125.4
425.4
225.4
02
5.3
8
25.4
025
.36
25
.44
25.4
52
5.5
02
5.5
425
.52
25
.53
25
.52
25.5
525.5
42
5.5
325.5
925
.60
25
.60
25
.64
25.6
62
5.7
425.7
725.7
725.7
72
5.7
62
5.7
6
25.7
22
5.7
225
.73
25
.74
25
.77
25.8
32
5.8
82
5.8
72
5.8
725
.80
25
.82
25.8
32
5.8
825
.95
25
.99
25
.95
25.9
625
.96
25
.99
26.0
726.1
92
6.2
026
.12
26.1
22
6.1
62
6.1
92
6.2
026
.12
26.1
12
6.1
32
6.1
8
26
.30
26
.28
26.3
326
.37
26.3
626
.36
26.3
42
6.4
126
.46
26.4
226
.43
26.5
126
.52
26.5
126
.57
26.5
92
6.5
926
.51
26
.48
26.5
426
.56
26.5
426.5
426
.57
26
.58
26
.54
26
.53
26
.48
26.5
626
.56
26.5
426.5
52
6.5
326
.56
26.5
726.5
42
6.5
62
6.5
326
.61
26
.61
26
.57
26
.59
26.5
82
6.5
526.5
426
.63
26.5
126.4
426.3
72
6.3
62
6.3
62
6.3
52
6.3
12
6.3
526
.36
26.3
22
6.2
626.2
926.2
5
26
.25
26.2
72
6.2
92
6.3
326.3
226.2
826.2
926.3
326.2
826.1
226
.11
26
.11
26.1
226
.07
26.0
72
6.0
42
6.0
626.0
82
6.0
125.9
72
5.8
925
.86
25.8
225.7
72
5.7
225.6
825.5
925.5
825.5
225.5
3
25.4
725.4
52
5.4
025.3
425.2
825
.31
25.3
025.2
425
.16
25.1
825.1
725.1
425.1
225,0
424
.91
24.8
82
4.8
524
.80
24.7
52
4.7
02
4.6
12
4.6
02
4.6
32
4.4
724.4
824
.46
24
.36
24.3
024.2
52
4.1
924.1
7
24
.14
24.0
824
.06
24.0
22
4.0
123
.96
23
.92
23.9
32
3.9
023.8
723.8
223.8
023.7
82
3.7
523.7
223.7
22
3.7
223
.71
23.6
42
3.6
523.6
423
.61
23.5
823.5
523.5
323.5
223.5
42
3.5
123.4
42
3.4
623.4
5
23.4
923.4
323.4
023,3
923.3
82
3.3
523
.32
23.3
023
.26
23.2
523.2
423.2
223.2
92
3.3
023.2
42
3.2
223.2
92
3.3
02
3.3
023
.31
23.3
423
.31
23
.30
23.3
123
.31
23
.27
23
.23
23
.26
23.2
62
3.2
6
23.2
723.2
22
3.2
42
3.2
523.2
423.2
32
3.2
123.1
823.1
62
3.2
12
3.2
023.1
723.1
92
3.2
323.1
42
3.1
223.1
823.1
723.1
323
.11
23.1
02
3.1
023.0
62
3.0
62
3.0
423
.01
23.0
62
3.0
32
2.9
622
.96
22.9
1
22.9
222.9
822.9
622.9
022.9
122.9
022.8
722.9
222.8
9
22.8
622.8
022.7
822
.71
22.6
922.7
322.7
622.8
222
.81
22.7
622.8
0
22.7
822.7
7
22.7
422.7
722.6
922.6
622.5
72
2.7
022.8
0
Tab
le 3
5.
Wat
er-l
evel
mea
sure
men
ts f
rom
rec
orde
r ch
art,
in f
eet
belo
w l
and-
surf
ace
datu
m C
onti
nued
Day
1952
Nov
.D
ec.
1953
Jan
.F
eb.
Mar
.A
pr.
May
June
July
Aug
.S
ept.
Oct
.N
ov.
Dec
.
1954
Jan
.F
eb.
Mar
.A
pr.
D2-5
-14ac
1 ...
......
2 3 ..
....
...
4 ..
....
...
5 ..
....
...
6 .........
7 ..
....
...
8 .........
9 ..
....
...
10
....
....
.1
1..
....
...
12
....
....
.13.........
14
....
....
.15.........
16
....
....
.17.........
18.........
19.........
20.........
21.........
22.........
23
....
....
.24
. .......j
25
....
....
j26
. ...
....
^2
7..
....
.. j
28.. ..
....
<29........ J
30........
31........
.........
6.1
3
6.38
.........
6.6
5
6.5
8
.........
6.5
96.5
7
6.6
66.7
0
6.1
55.9
95.
91
5.9
85.9
55.9
25.
905.
915.
925.
805.
725.
685.6
45.6
25.5
45.5
2
5.5
25.5
85.6
25.6
8
5.6
55.
615.5
85.5
75.6
55.
675.6
95.6
25.5
85.6
05.6
45.6
55.6
85.
725.7
45.
785.8
25.
855.9
05.
925.9
25.9
55.
965.9
96.0
16.0
3
6.0
56.0
76.0
86.1
0
6.1
16.1
26.1
56.1
86.2
16.2
46.
266.2
86.2
96.
316.3
36.3
46.
366.3
36.2
26.1
56.1
05.7
25.
615.5
55.5
55.5
75.6
15.1
35.
485.4
95.5
4
5.5
55.5
74.9
2
3.8
63.8
94.0
34.4
04.5
34.2
44.1
94.2
04.3
94.3
34.5
5
5.6
25.6
25.0
44.4
84.3
74.3
74.6
1
5.2
7
5.51
5.53
4.8
44.5
5
4.9
04.7
25.1
75.4
45.
635.
715.
665.
764.4
15.0
25.5
55.
585.
575.
605.7
85.8
85.9
45.9
55.9
95.6
25.
725.
926.
066.1
76.2
46.2
86.2
2
6.2
7
6.1
05.
905.
735.
005.
044.9
85.
115.
365.4
95.
335.
495.
605.
665.
775.
875.7
85.9
46.0
46.1
26.1
66.2
16.2
66.
306.3
06.
266.2
76.2
9
6.3
06.2
46.2
26.2
2
6.2
36.2
46.2
96.1
86.
116.
08
5.91
5.98
6.07
6.17
6.2
06.
266.2
86.
196.2
26.2
36.3
2
6.6
56.6
86.
716.7
36.7
66.
79
6.81
6.8
46.8
56.8
6
6.8
76.8
86.9
06.9
26.9
36.9
46.
966.9
76.9
87.0
07.0
17.0
27.0
37.0
57.0
67.0
77.0
87.0
97.
107.0
97.0
97.0
67.0
57.0
57.0
57.
067.0
7
7.0
87.
107.
117.
11
7.11
7.1
47.1
57.1
57.1
57.
167.
167.1
67.1
77.
177.1
87.1
97.
207.
207.
217.2
57.2
37.1
87.1
77.
167.1
17.0
87.0
57.0
37.
01
6.9
96.9
86.9
76.9
7
6.9
87.0
07.
037.0
37.
037.
037.
037.0
47.
067.0
77.0
87.0
97.1
07.
117.1
27.1
27.1
37.1
37.1
47.1
57.1
67.
177.1
7
6.3
16.3
26.3
2
6.3
26.3
46.3
76.3
9
6.41
6.4
16.
416.
396.4
16.4
26.
436.4
36.4
56.4
76.4
86.5
16.5
56.5
76.6
0
6.7
06.7
16.7
36.7
46.7
56.7
76.7
86.7
86.7
96.8
0
6.8
06.
816.8
16.8
3
6.83
6.8
36.8
36.8
46.8
46.8
46.8
56.
866.7
46.
636.6
46.6
36.6
26.5
86.
616.6
26.6
16.4
86.4
36.3
06.2
56.2
06.
266.2
7
6.31
6.3
56.4
06.
41
6.43
6.4
56.4
76.4
86.4
96.4
66.4
96.5
36.5
76.5
96.6
26.6
36.6
46.6
66.6
76.6
76.6
56.6
56.
666.6
76.7
06.7
06.7
16.6
96.6
86.6
86.7
0
6.7
26.7
26.7
26.3
4
6.1
46.0
15.9
55.9
15.
915.
935.9
55.9
86.0
06.0
36.0
86.
116.1
36.
166.2
06.2
36.2
56.2
8
Tab
le 3
5.
Wat
er-l
evel
mea
sure
men
ts f
rom
rec
orde
r ch
art,
in f
eet
belo
w l
and-
surf
ace
datu
m C
onti
nued
Day
1951
Apr.
May
June
July
Aug.
Sept
.Oct.
Nov.
Dec.
1952
Jan.
Feb.
Mar.Ap
r.May
June
July
Aug.
Sept
.Oct.
Nov.
Dec.
1953
Jan.
Feb.
Mar.
to fe
D2-5
-16aal
1 ~~
... ........
2 ..
....
....
....
.3
....
....
....
...
4 ...............
5 ...............
6 ..
....
....
....
.7
....
....
....
...
8 ...............
9 ..
....
....
....
.10
...............
11...............
12...............
13..
....
....
....
.14
....
....
....
...
15..
....
....
....
.16..
....
....
....
.17
...............
18..
....
....
....
.19
....
....
....
...
20...............
21..
....
....
....
.22..
....
....
....
.23..
....
....
....
.24..
....
....
....
.25...............
26..
....
....
....
.27...............
28..
....
....
....
.29..
....
....
....
.30..
....
....
....
.31..
....
....
....
.
....
..
....
..
5.42
....
....
....
....
....
....
....
....
....
.......
4.86
.......
...*...
5.16
5.19
5.17
5.05
5.12
5.15
5.17
5.16
5.19
5.19
5.22
5.25
5.27
5.21
5.18
5.24
5.18
5.13
5.16
5.05
5.00
4.75
4.52
4.36
4.26
4.14
4.10
4.01
3.86
3.63
3.12
2.92
2.81
3.97
3.97
3.95
4.02
4.04
4.26
4.38
4.30
4.24
4.25
4.14
3.93
4.02
4.25
4.42
4.37
4.12
4.12
4.04
3.99
4.01
4.04
4.00
3.99
4.01
3.91
3.98
3.39
2.96
2.51
3.76
3.90
4.09
4.21
4.36
4.43
4.36
4.35
4.19
4.11
4.10
4.06
4.16
4.26
4.33
4.52
4.52
4.34
3.99
4.01
3.58
4.01
3.99
4.06
4.08
4.1d
4.02
4.07
4.15
4.20
4.23
4.23
4.29
4.30
4.24
4.35
4.50
4.27
3.93
3.86
3.94
4.07
4.22
4.35
4.43
4.51
......
.....
*
*
4.84
4.89
4.91
4.90
4.93
4.92
4.94
4.96
5.00
5.03
5.06
5.05
5.04
4.83
4.84
4.85
4.72
4.81
4.87
4.91
4.95
4.98
5.00
5.03
5¥S5
5.05
4.96
4.70
4.74
4.83
4.88
4.91
4.93
4.98
5.01
4.99
5.04
5.06
5.00
4.96
4.97
5.00
4.99
4.83
4.78
4.80
4.82
4.78
4.70
4.68
4.71
4.70
4.6E
4.68
4.6E
4.72
......
4.60
4.64
4.68
4.70
4.73
4.74
4.76
4.77
4.80
4.82
4.84
4.86
......
...*
4.96
4.98
5.00
5.01
5.01
5.01
4.97
4.94
4.93
4.94
4.98
4.97
4.99
5.01
5.03
......
5.08
5.09
5.10
5.11
5.11
5.15
5.15
5.18
......
......
..
......
5.26
5.26
5.26
......
....
...
.......
5.29
*
5.28
5.30
5.30
5.31
5.31
5.28
5.32
5.31
5.33
5.34
....
...
.......
.......
5.40
5.41
5.41
5.41
5.40
5.40
5.41
5.41
5.41
5.42
5.42
5.42
5.42
5.42
5.43
5.43
5.42
5.42
5.43
5.39
5.44
5.44
5.45
5.46
......
......
5.49
5.49
5.50
5.51
5.52
5.53
5.53
5.54
5.54
5.54
5.54
5.55
5.55
5.55
5.59
5.59
5.60
5.60
5.60
5.60
5.60
5.61
5.61
5.61
5.61
5.59
5.60
5.61
5.62
5.62
5.62
5.63
5.61
5.54
5.46
5.51
5.50
5.50
5.48
5.46
5.42
5.36
5.18
4.84
4.51
4.10
4.10
4.31
4.43
4.45
4.22
3.93
3.48
2.69
3.06
2.91
3.85
4.13
4.35
4.37
4.46
4.53
4.60
4.64
4.69
4.73
4.77
4.80
4.83
4.86
4.89
4.90
4.90
4.92
4.95
4.98
5.01
4.78
4.87
4.91
4.93
4.93
4.94
4.94
4.76
4.77
4.81
4.82
4.85
3.60
3.31
4.03
4.32
4.47
4.40
4.51
4.61
4.68
4.75
4.80
4.85
4.86
4.90
4.93
4.97
5.00
4.99
4.96
4.90
5.00
4. 97
'4.95
4.78
4.71
4.06
3.50
2.78
3.36
3.05
3.30
3.92
4.09
4.15
4.03
3.72
3.96
3.89
4.02
4.10
4.26
4.37
4.32
4.44
4.52
4.59
4.73
4.80
4.86
4.43
4.46
4.28
4.10
3.33
4.08
4.24
4.11
4.31
4.59
4.63
4.57
4.50
4.49
4.57
4.61
4.54
4.48
4.20
4.17
4.31
4.30
4.35
3.12
4.15
4.32
4.37
4.39
4.43
4.60
4.62
4,46
4.34
4.30
4.33
4.17
4.04
4.10
3.18
3.26
3.30
3.24
4.21
4.25
4.24
4.28
4.24
4.18
4.23
4.20
4.20
4.25
4.21
3.87
3.66
3.61
3.55
3.71
3.74
3.89
4.02
4.11
4.16
4.20
4.55
4.67
4.73
4.79
4.81
4.85
4.88
4.91
4.93
4.97
4.99
4.98
5.00
5.01
5.02
5.06
5.08
5.08
5.09
5.08
5.07
5.07
5.09
5.10
5.10
5.06
5.08
5.08
5.08
5.08
5.07
5.10
5.10
5.07
5.04
5.05
5.06
5.07
5.07
5.07
5.08
5.09
5.08
5.11
5.11
5.11
5.13
5.13
5.14
5.14
5.15
5.14
5.16
5.16
5.16
5.17
5.18
5.19
5.20
5.21
5.22
5.22
5.23
5.23
5.24
5.24
5.24
5.24
5.24
5.25
5.26
5.29
5.30
5.30
5.31
5.32
5.29
5.28
......
......
5.27
5.27
5.26
5.26
5.26
5.27
5.28
5.28
5.28
5.28
5.24
5.22
5.24
5.26
5.31
5.36
5.40
5.43
5.45
5.46
5.48
5.49
....
........
5.58
.......
.......
......
.......
.......
5.64
5.66
5.11
5.17
5.27
5.27
5.29
5.33
5.34
5.35
5.36
5.37
5.34
5.32
5.35
5.37
5.37
5.37
5.39
5.41
5.42
5.42
5.42
5.43
5.42
5.43
5.44
5.44
5.44
5.44
5.42
5.42
5.44
5.42
5.41
5.41
5.40
5.40
5.40
5.46
5.46
5.47
5.48
5.47
5.47
5.46
5.46
5.48
5.50
5.51
5.50
5.48
5.52
5.52
5.53
5.53
5.54
......
......
......
......
......
......
......
......
Tab
le 3
5.
Wat
er-l
evel
mea
sure
men
ts f
rom
rec
orde
r ch
art,
in f
eet
belo
w l
and-
surf
ace
datu
m C
ontin
ued
Day
1953
Mar
.A
pr.
May
Jun
eJu
lyA
ug.
Sep
t.O
ct.
Nov
.D
ec.
1954
Jan
.F
eb.
Mar
.A
pr.
D2
-5-2
2cc
d
1....
......
......
......
......
......
......
......
....
2 ..
....
....
....
....
....
....
....
....
....
....
....
..3
....
....
....
....
....
....
....
....
....
....
....
....
4 ................................................
5 ................................................
6 ................................................
7 ..
....
....
....
....
....
....
....
....
....
....
....
..8
....
....
....
....
....
....
....
....
....
....
....
....
9 ..
....
....
....
....
....
....
....
....
....
....
....
..1
0..
....
....
....
....
....
....
....
....
....
....
....
..11................................................
12
....
....
....
....
....
....
....
....
....
....
....
....
13................................................
14
....
....
....
....
....
....
....
....
....
....
....
....
15......................
....
....
....
....
....
....
..1
6..
....
....
....
....
....
....
....
....
....
....
....
..1
7..
....
....
....
....
....
....
....
....
....
....
....
..18......................
....
....
....
....
....
....
..19......................
....
....
....
....
....
....
..20................................................
21................................................
22
....
....
....
....
....
....
....
....
....
....
....
....
23
....
....
....
....
....
....
....
....
....
....
....
....
24
....
....
....
....
....
....
....
....
....
....
....
....
25................................................
26................................................
27................................................
28
....
....
....
....
....
....
....
....
....
....
....
....
29................................................
30................................................
31
....
....
....
....
....
....
....
....
....
....
....
....
10.7
810
.51
10.2
49.
999.
939.
909.
869.
849.
839.
879.
889.8
09.
769.7
79.7
99.
789.6
29.
469.
419.4
09.
369.
239.2
2
9.2
49.2
79.3
99.4
7
9.3
89.3
39.
279.2
39.1
99.
169.1
59.
119.0
89.1
7
9.76
9.8
39.
919.9
99.8
89.8
3
9.90
9.96
10.0
310
.08
10.1
310
.18
10.2
210
.28
10
.34
10.4
010
.44
10.4
710
.50
10.5
11
0.5
410
.58
10.6
210
.55
10.5
010
.36
10.2
19.
889.
769.
669.6
39.6
59.
709.
759.7
09.
729.
71
9.77
9.8
39.4
4
8.51
8.59
8.70
8.82
8.96
9.10
9.37
9.43
9.50
9.5
49.
457.
406.8
26.5
46.3
56.
666.
927.
167.
447.6
77.9
27.9
88.
078.
188.2
4
8.2
98.2
38.
328.
668.5
98.
568.
518.
508.4
98.4
88.
548.6
38.
558.
538.
468.
388.
368.
318.
468.
568.6
48.
487.
326.9
46.
466.5
2
7.1
57.
557.
78
8.11
8.3
88.5
58.6
68.8
08.8
88.8
58.9
89.
189.2
99.
269.2
79.
329.2
58.9
48.
807.5
86.8
87.0
56.6
56.8
97.
167.2
77.7
28.1
48.4
48.6
88.
919.0
89.2
49.3
8
9.4
79.5
59.5
69.
5710
.10
10
.23
10.3
21
0.4
01
0.4
41
0.4
910
.08
10.0
81
0.1
010
.10
10.1
71
0.2
11
0.2
310.1
01
0.1
810
.24
10
.23
10.2
210.2
210.1
510.2
21
0.2
710
.33
10.3
310
.28
10.2
1
10.1
710.1
11
0.0
510.0
210.0
01
0.0
01
0.0
01
0.0
09
.97
9.96
10.0
610
.14
10.1
810.2
21
0.2
410.2
610.2
61
0.2
41
0.2
310.2
510.3
21
0.3
01
0.1
810
.13
10.0
81
0.0
09.
969.
909.9
29.
929.9
8
10.0
510.1
210
.18
10
.23
10.2
710
.31
10
.35
10.3
91
0.4
21
0.4
410
.47
10
.52
10.5
510
.57
10.6
010
.63
10
.67
10.6
910
.69
10.7
010
.71
10.6
910
.61
10.5
310
.48
10.4
310
.37
10.3
510
.34
10.3
5
10.3
41
0.3
510
.39
10.4
610
.51
10.5
610
.61
10.6
710
.70
10.7
410
.77
10.8
110
.84
10.8
710
.91
10.9
210
.94
10.9
610
.98
11.0
011
.02
11
.02
11
.03
11.0
511
.06
11.0
711
.08
11.1
011
.10
11.1
111.1
2
11
.11
11.1
111
.12
11.1
211
.10
11.1
011
.11
11.0
911
.10
11.1
111.1
211
.16
11.1
71
1.1
911
.19
11.2
011.2
011.2
01
1.2
2
11
.24
11.2
311.2
311.2
311.2
21
1.2
41
1.2
51
1.2
211.1
811.1
3
11.0
911
.04
10.9
910
.93
10.8
910
.84
10.8
210
.77
10.6
810
.51
10.4
310
.51
10.0
210
.07
10.2
310
.32
10.3
910
.41
10.4
610
.51
10.5
310
.46
10.4
110
.28
10.2
31
0.2
010.2
610.2
6
10.3
010.3
310
.36
10.4
010
.46
10.5
110.5
410.5
310.5
110.4
210.4
710
.53
10.5
810
.60
10.6
210
.61
10.5
810.5
910.6
010
.60
10.6
110.6
21
0.6
210.6
310.6
510.6
610.6
71
0.6
610.6
81
0.7
110.7
5
10.8
310
.86
10.8
61
0.2
710
.13
10.0
59.
989.9
39.9
39.
919.9
29.9
49.
989.9
910
.07
10.1
510
.21
10.3
510
.41
10.4
310
.45
Q. Q.
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CO
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Cecelia E. McDonnel!Manhattan Co...........
Montana Power Co....Catherine Martin...... A. W. Overturf.........
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Type of well
Depth of well (feet)
Diameter of well (inches)
Type of casing
Type of pump
Type of power
Use of water
Description
Distance above or be low (-) land surface
Height above mean sea level (feet)
Measuring point
Distance to water level below measuring point (feet)
Date of measurement
Remarks
p"
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reported; m, meas filled in and cover
o. *^
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fnumer
03J '
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enQ.<D
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b, draw do
^33't-b<D
b S b?>co n. t-b C
3 TO
spring. Measured de
"S-3-enP
TO<'
33'
2- P3a n3^
cncr
y
td"I 03 P
rks: A, aquifer tei >, chemical analysi
Cl JJJ.cr "'
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2ac
l
2cd
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...
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4b
b..
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..9b
bb...
lObb....
lObd....
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....
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....
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....
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..22
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23
bb
....
25cb
....
26cc
....
26
cdl.
..26
cd2.
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...
29aa
....
33
dd
....
35
dd
....
36
dd
....
....
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.........................
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tie
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..................
....
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....
....
....
....
....
....
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Wm
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Cover.
.............
U.
S. G
eol.
Surv
ey........
C.
B.
Chase
.................
J. F
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hite
, E
state
.......
....
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....
....
....
....
....
....
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U.
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eol.
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ey........
J. F
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state
.......
U.S
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eol.
Surv
ey.........
Jack
Whit
e...................
J. R
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rink..................
Hel
en H
eeb.
. ................
1949
1950
1951
1952
1954
1951
1951
.......
nr nr nr nr nr nr nr nr nr nr nr nr nu nu nr nr nu nr nr nr nn nn Sp nn R nr nn nr nn DD nn
52 40 29 18.5
20 30 35 105 60 76
,680 134 30 10
.527
.633 35 6.
0
75 185 65 28
.315 9.
5
10.4
20.3
30 1531
0 99 40
25
6 6 6 12 5 5 5 6 4 6 6 6 4 1236
by
366 6 12 6 6 4 5 30
3
423
642 4 6 4 4
P P P T P P P P P P P P P T W P P P P P P P R P R P P R P P P
P
J J J Cy
Cy r, r, Cy J N J J Cy
P N r, N Cy
Cy
Cy
N N Cy
N Cy
Cy J J J
F F F, H H F, F, F, F, N F, F, H H N H F, N F, H H N N H N H W F, E
E
n n n s,o D D,S
D,S S D,S o n
n.s.
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n.s.
oN n,s
D,S o n D,S
n.s
n,s
N O P S o n D n D,S
n.s
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T,R Tp
T,s
T,,s
T,,s
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Tr
T,s
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0 0 0 .2 0 0 1.2
0 2.0
1.0
3.0
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1.0
3.8 .6 0 0 0
4,23
9
4,22
5
4,26
6
4,25
1
4,23
0
4,28
8
4,29
3
4 33
19
4,34
3
4,40
74,
357
4,35
7
15 15 4 4.01
4 6 15 15 25 34.0
540 64
.71
15 4.81
9.87
12 6 6.56
18 607 12.6
812
.60
2.10
5.49
9.56
10 10.9
526
0 48.6
012
.30
5.80
7-3
1-5
1
11
-28
-50
5-21
-51
4-2
4-5
1
9-2
4-5
22
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8-2
6-5
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Distance above or be low (-) land surface
Height above mean sea level (feet)
Measuring point
Distance to water level below measuring point (feet)
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XNOH 'A3TIVA NIXVnVO '8308110838 H3XVM-(INnOHD '
BASIC DATA 249
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C. J. Sanders............... ... .....rfn.. .-..---. .............. ...
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West Davis.................. ... Wilbur Spring............... ... U. S. Geol. Survey......... 19 Chas. Osborne, Estate... ...
Thompson Hereford Ranches, Inc. .....do......................... ...
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Edwin Seifert............... ... Roges Spring................ ... Frank Gowin................ ... Bertha Carlson............. ... Frank Gowin................ ...
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Type of well
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Distance above or be- c low (-) land surface g-
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1948
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1949
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1949
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Type of well
Depth of well (feet)
Diameter of well (inches)
Type of casing
Type of pump
Type of power
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Description
low (-) land surface
Height above meansea level (feet)
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Distance to water level below measuring point (feet)
Date of measurement
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1949
1951
1952
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1902
1943
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Type of well
Depth of well (feet)
Diameter of well (inches)
Type of casing
Type of pump
Type of power
Use of water
Description
Distance above or be low (-) land surface
Height above mean sea level (feet)
Measuring point
Distance to water level below measuring point (feet)
Date of measurement
Remarks
'INCH 'A3TIVA NIIVTIVO 'S30HriOS3H H3IVM-(INnOHO 'A001030
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INDEX
Page A
Aakjer Creek -_............._....._._.. _________..._.._ 85Acknowledgments ... _ 4-5Agriculture ..... ..._... 20, 23Alluvial fans .......... 13, 39-40, 42-43, 53, 57, 106,
153-156, 158-159; pi. 2 Alluvium .............. 43, 45, 53-55, 57, 103, 106, 131,
132, 136, 140-142, 146, 149-150,151,153, 158, 159, 168; pi. 2
American Water Works Association.... 175-176Amsden formation _.... .... ........__.......... 30Anceney, temperature . _.-................_-.-...-.... 14, 17Aquifer, artesian ............ .............._.... 100-101
water-table . _ ._ 100-101Aquifer tests ........ 9, 102-106, 136,140-142, 146,
153-154, 157, 159 Archean gneiss ........_.__._ .._..._..__.......... 27Arnold-Toohey ditch .............................. ... 84, 111Artesian water in Tertiary strata .. ... 144, 150
B
Baker Creek ................................ 62, 71, 89, 92, 143Barnes ditch ........_.._.__._..._...._.....____._._....._. 82, 111Basalt ................_ ..._... _........ 46Bear Creek ................... 63, 66, 77, 93, 95, 96, 111,
153, 158Belgrade, municipal water supply... .. 110
precipitation . 20, 119temperature _......._._......__......... 119
Belgrade plain. See Belgrade subarea. Belgrade subarea, aquifer tests ....... 104, 140-142
changes in ground-water storage... 138, 142 character and thickness of
alluvium .. . ........ 43, 44, 140chemical quality of ground water.
See Valley floor, depth to water _......._................_......._.. 143-144ground-water, discharge .... ._ 142
potential .._...._. . ....... 145-146recharge . __ .. 142
location and extent .._..............__..._..... 11, 140occurrence of ground water ._.............. 144Pleistocene sedimentation ...... __. 53water-level fluctuations ._.. 123, 145; pi. 7
Belgrade trough ....._.... .................. 53-55, 56-57Belt series ........ ......_..._... 25, 27, 48, 53Ben Hart Creek ............................ 65, 76, 95, 148Bicarbonate in water ...... ....... .___ 161Big Bear Creek ......._ ._................... 60, 70, 80, 93Big Snowy group ...._.. .._...._............. 30Bluffs. See Escarpment.Boron in water ... ___.......... 166, 175Bostwick Creek ..._.. ........................... .._.... 65, 75
Page Bozeman, municipal water supply 99
population, 1950 ......................... .. 20precipitation ........ ....._.................... 14, 18-19
Bozeman Creek. See Sourdough (Boze man) Creek.
Bozeman fan, aquifertests .............. 102-103, 105, 153-154
changes in ground-waterstorage .......................... 138, 154-155
character and thickness of alluvial- fan deposits ....... 153-154
chemical quality of ground water.... 163,166-167, 171; pi. 10
depth to water ........_.... 118, 155-156; pi. 6ground-water, discharge ......... 107-109, 155
potential ...................................... 154, 156recharge ... _.._._.__......._. 154-155
location and extent ...._.._._ 11, 13, 42, 153principal aquifer ...... 102-103, 105, 153-154
Bozeman Hot Springs ..__.......................... 50, 166Bozeman lake beds of Peale ............ 6, 25, 32, 33Bridger Creek .... 63, 73, 94, 98, 153, 165, 172Bridger frontal fault system ........ 49, 50, 52, 56Bridger Range .... 5, 9, 12, 13, 14, 25, 27, 38, 39,
40, 42, 44, 47, 48-49, 55, 56, 57,92, 94-95, 107, 159
Bright ditch ...._........_............................_..... 86Bullrun Creek ................................ 67, 78, 95, 148
Calcium in water ..._..... ........ ... . 160Cambrian rocks ........_..........._.._.... 28-29, 46, 49Camp Creek ........_.._..._....._.._........ 35, 63, 72, 83Camp Creek Hills, aquifer tests. - 105, 157
chemical quality of groundwater ......._._... 163, 167, 171; pi. 10
depth to water ..........._..........._._......_... 118drainage .................. ............ ... - 13, 14, 95geology -. . ...-. 27, 28, 32, 35, 38, 42, 44,
50, 52, 57 ground-water, discharge ....____.._ ..._.. 147
movement _....-................... 131potential ._...._...._._......_......_.... 157recharge ....._......... . 157supply ...._....__..........._ - 34, 157
location and extent .._._ .._.._.__._ 11, 12 occurrence of ground water ................ 157origin of name 5
Carbonate in water _ .. .... ........ 161Cenozoic rocks ......._.. ...__ _ 32-46Central Park fault .... .... 51, 54, 56, 146; pi. 2Central Park subarea, aquifer tests..... 104, 146
changes in ground-water storage. 138, 149 character and thickness of alluvium 43, 146
277
278 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Page Central Park subarea Continued
chemical quality of ground water.See Valley floor,
depth to water .______________..-.______.____.._______ 147ground-water, discharge ........ 110-115, 116,
147-149 recharge _....-.... ..._.. .. .... 147, 149
location and extent ............................ 11, 146waterlogging ....-...... ._ ._-.-.._.... 110, 147
Chemical quality, ground water ............ 162-163,166-167, 168, 170-171; pi. 10
sampling program ___.._......___._.__ ..._._ 9suitability of water for domestie
use ..._.....__.._._________......___..._._. 175-176suitability of water for
irrigation __...... 168-169, 174-175surface water ........ 164-165, 172-173; pi. 11
Chloride in water -____.____.____.___..____.__.__._.____ 161, 176Churn Creek .................................. 64, 74, 143, 144Climate ................................................ 14-20, 21-23Coefficient of permeability .............. 101, 104-105Coefficient of storage.. .- 101,103,104-105,106 Coefficient of transmissibiliyt. See Trans-
missibility, coefficient of. Colluvium ...............................__._............ 46, 136Colorado shale ._... ...-.... ..__._.______ 32Corundum __________.___________ 2 5 Cottonwood grove, amount of ground
water consumed ........ 110, 112-116Cowan Creek -. -.- - ............. 67, 77, 148Cretaceous rocks ...._.._..... . ...^ ........... 31-32Cumulative departures from volume of
saturated material ............ 119-128
D
Deer Creek ............................................... 64, 74, 84Depth to water ................ 118, 137, 143-144, 147,
151, 153, 155-156; pi. 6Devonian rocks ._ ._ ._. ...-.__.._.___. 29-30, 49 Dikes, clastic ........-.....-.........-.-................._.... 50Discharge from ground-water reservoir,
by evapotranspiration _ ....__. 109,110-116, 132, 133, 134, 142, 145,
148, 150, 153, 155, 177by springs .......................... 109, 116, 148, 151by streams and drains .... 109, 116-118, 137,
138-139, 142, 148, 149, 150, 153, 155, 158 by underflow .... 137, 142, 149, 150, 153, 155by wells . .. -................_.___.___._.__._ 109-110
Dissolved solids in water.. 162-165, 166-167, 176Drainage, surface, history .. _ .. ..___ 25, 56
present .........................__... 12-14, 58-99Dry Creek ...................... 27, 44, 66, 67, 77, 87, 95,
111, 158, 165, 173 Dry Creek shale member of Snowy Range
formation .................................. 29
Dry Creek subarea, aquifer tests ............. 105
depth to water ...._.....__.___.._... 118
geology ........ 27, 30, 32, 35, 38, 39-40, 47, 158
ground-water, potential ...... ........_ 158
recharge .._._. ............_....._... 158
location and extent ..._......... 11, 12, 13, 158movement of ground water ____... 158
Dry Fork Creek ............................................ 86
PageE
Earthquakes, cause of water-levelfluctuations .................... ... 128, 129
East Gallatin River, discharge measure ments ........ 63, 64, 73, 74, 83-84, 85,
87-88, 111 diversion for irrigation _... _._........ 20, 99drainage course .................. 13, 14, 38, 59, 92gains and losses in flow .___..._.......... 144relation to ground water ........ 107, 116, 142,
143, 145, 149, 153 Elk Creek ............................................... 53Ellis group -__-.--... ...-... - 31Eocene rocks ......._ ._........_. ... _..._-_- 49Escarpment, east side of Camp Creek
Hills .......................................... 12, 50east side of Goochs Ridge .................... 50east side of Madison River .... 12, 33, 36, 37,
38-39, 40, 51, 52, 53 north side of Horseshoe Hills .._...... 13northeast side of Manhattan
terrace ......................... 149, 150, 151west of Madison River ........................ 53
Evaporation, ground-water discharge by 110 measurements near cottonwood
grove .................................... 114, 116Evapotranspiration, ground-water dis
charge by .... 109, 110-116, 132, 133,134, 142, 145, 148, 150, 153, 155,
177; pi. 8
Fanglomerate ..................... 32, 38, 39, 40, 42, 150Faults ...... 33, 46, 47, 48, 49, 50-55, 56. 146; pi. 2Fish Creek ...._......-...-...........----.-- 61, 71, 137Fish hatchery ........................... ....-.- - - 23Flathead quartzite ............................. 28, 46, 47Flaxville plain of Alden .... _... ..-.... 40Fluoride in water ..._................................ 161, 169Folds, Camp Creek Hills .............................. 51-52
Horseshoe Hills ......................... ._ . 47Fort Ellis subarea .............. 11, 13, 31, 32, 40, 159Foster Creek .................................... 66, 77, 87, 111Frost dates .............................................. .. 14Fossils, vertebrate .............................. 6, 33, 38, 39
G
Gallatin Canyon ............................................ 12, 13Gallatin County Agent's Office .......... 5Gallatin County Commissioners ._.......... . 5
Gallatin Gateway ................ 13, 88-89, 92-94, 97,98, 119, 131
See also Gateway subarea. Gallatin Gateway Oil Co. ........ ................. 5
Gallatin National Forest ............................ 23
Gallatin Range .............. 12, 13, 14, 27, 28, 39, 40,43, 49-50, 55, 57, 93-94, 153
Gallatin River, alluvial deposits ...... 42-45, 103,106, 136, 140
discharge measurements __~ 58-59, 60, 61,62, 68, 69, 70-72, 78-79, 81, 82, 83,
88-92, 93, 94, 97-98, 119
diversion for irrigation ...... 20, 99, 119, 178
drainage course.. 12, 13, 14, 27, 47-48, 56-57
INDEX 279Page
Gallatin River Continuedgains and losses in flow .... __...... 89-92, 139relation to ground water ._. .... 107, 116,
136-137, 139, 142, 143, 145Gallatin Valley Water Users' Association 4, 5 Gastropods ............_ _...____._ 35Gateway subarea, aquifer tests ............ 104, 136
changes in ground-water storage.... 137-139character and thickness of alluvium 136 depth to water . 137ground-water, discharge .......... 137, 138, 139
movement ... . . .... ~ 136-137recharge ....................... _... 136, 138, 139
location and extent _...___._.___........ 11, 136potential ground-water develop
ment ...................................... 139-140water-level fluctuations __________________ 123; pi. 7
Geologic mapping .........._.......__.......... 8-9; pi. 2Geologic section, Belgrade trough ............ 53 54
Gateway subarea . _. 136, 137 monoclinal fold in Camp Creek Hills 51-52 near Logan .._................ .._..__.._......... 131-132
Geophysical methods of subsurface ex ploration ............._-...._..__...__._... 9
Gibson Creek ................................... 67, 78, 95, 148Glaciation, Bridger Range .....__._.__._.._._....... 40
Gallatin Range ............_.......................... 40, 45Madison Range . ....__....................... 45
Godfrey Creek .................._.........__..._._ 35, 61-62, 71Gold ...._..............._...._.._....._................. ... . 20Gooehs Ridge ............ 12, 32, 38, 50, 136, 153, 159Gravel cap ............_............._..._.. 40, 51, 52, 53, 56Gravel deposits, commercial use ....__.......... 25Ground water, changes in storage 119, 128; pi. 8
chemical analyses ......__...... 162-163, 170-171depth below land surface .................... 118discharge ..............__......__.._......... 109-118; pi. 8movement ........__...__...__...___...__........_..... 118potential development .........._._........ 176, 179recharge .........__....................._.._ 107-109; pi. 8
Growing season, length -_. _. .....__.._____ 14, 20
H
Hardness in water _._..__ __. ______ 160-176Hoffman ditches ._ .... _.______ 81, 111Horseshoe Hills ......_... 5, 7, 11, 12, 13, 27, 30, 34,
36, 39, 46, 47-48, 95 Hyalite Canyon __._ ._...-...._______..__._.___.._.__..._ 153Hyalite Creek. See Middle (Hyalite)
Creek. Hydrologie cycle ...... . ... ...._.. _.... 57-58Hydrologic units ..........._._ .._ 11, 120, 136-159
Igneous rocks ....__.. ._.._....________.__.__.._____ 46Industry .......__......_....___..._.. ...._._....... 23Ions in water, source and significance 160-166 Irrigation, chemical suitability of
water ......._............_............... 168-175location and extent ._...._................... 20, 24diversion of surface water .... 20, 58, 59, 89,
92, 94, 95, 99, 107, 116-117, 133, 134, 150, 151, 155, 156
Page 80
..__...._............. 48
.._......._........... 29
...._................. 13Jefferson River valley ... . . -. .. .... 25, 48Jones Creek 85Jurassic rocks .... ......... . . ._...... 30-31
Jack Creek .._...... _....Jefferson Canyon fault Jefferson limestone ........Jefferson River ....__...._...
K
Kelly Creek .___..__._._....____... ...__...................... 83Kootenai formation ............................... 31-32, 46
Laramide orogeny . .. ... ... ............. 48, 56Lead ore ....... .._..........................._........._... 25Leuciscus turneri beds of Wood ...._.......... 33, 35Lewis and Clark expedition ___. ___.__. 20 Limestone Creek ....... _.....__ 83Little Bear Creek ____ . _.... 32Livingston formation ... ... ... .._______ _ 32Lochman, Christina, quoted .................. 29Lodgepole limestone of the Madison
group ._...... - . ......_....... 30Loess ..............._........ ....-_.................. _.. 45-46Logan ............. ._._. 12, 13, 23, 28, 56, 92, 131, 149Logs, wells and test holes ............_........__. 184-203Loup Fork beds ................. ..._.............. . 33, 36Lower Creamery ditch . .... .- ._... 82Lowline Canal ..........._... ........ ......... .... 50Lyman Creek 55, 64, 74, 99
M
Madison group _____ ._.... 30, 55Madison Range ..........._.................... 13, 43, 49-50Madison River .-.............. .. -. .. ...._ 13, 56Madison Valley ...............__............... 6, 25, 33, 131Madison Valley beds .__........................_._..._.. 33, 34Magnesium in water _._ -. ..._. . 176 Mammoth ditch ................ . ................. ._.. 81, 111Manhattan, temperature _........._...._........__.. 14, 15Manhattan subarea, aquifer tests ........ 105, 150
artesian water in Tertiary strata...... 150changes in ground-water storage.... 138, 151character and thickness of
alluvium ...._................ 149-150, 151depth to ground water _......... ... ._. 151ground-water, discharge .__............... 150-151
recharge ._.__ . ... _..... 150location and extent ____....-_._........ .... 11, 149springs __...__...... . . . 151waterlogging _..________-__._...___............_.....- 151
Maurice limestone ......._ .. . . 28Maywood formation __ _.... .. _ 29Meagher limestone __ . 28, 46, 47Meinzer, O. E., quoted .._._....._........ 57, 100, 101Menard, temperature _.... _.. ......... 14, 16Mesozoic rocks ................_._..._.. 30-32, 36, 48, 49Metamorphic rocks, Precambrian ..._....... 26-27Middle Cottonwood Creek .............. 64, 74-84, 95Middle Creek Reservoir _. 99Middle (Hyalite) Creek .... 12,65,74-75,85,93,
98, 107, 111, 143, 153, 154, 155 Mineral resources .._... 25
280 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Page Miocene rocks _...... _ 25, 34Mission Canyon limestone of the Madison
group _ .-. 30 Mississippian rocks ____.. .__ ._..-.....__......... 29-30Missouri River . ....... ....... ... ... 13Montana Power Co. .... 5, 33, 34Montana State College .....__............._... 4, 5, 20, 55Montana State Engineer's Office ............ 5, 7, 20Moreland Canal ...... ... .. -. ._. 151Morrison formation __.._.............................. 31Movement of ground water ......... 118, 136-137,
139, 142, 147, 149, 150, 153, 155,157, 158, 159
Mystic Lake ... ........ ................ .... 99
N
Nichols Creek -._...... ... ... 83North Cottonwood Creek ............................ 86Northern Pacific Railway ...............__...... 20Nitrate in water ._.. ........__.... 161, 163, 176
Oligocene rocks ........_.........._.... 25, 33-34, 35, 49Ostracodes ...... .... 35, 36
Paleozoic rocks ......... ........._._ 27-30, 36, 47, 48, 49Park shale .._..................................__..._......_.._ 28Pass fault _.._ .._.. ___ .____.__.______..____....___. 48Pennsylvanian rocks __ .. _____..... 30Permeability, coefficient of, definition _... 101 Permian rocks ___.___._..__..._........._ 30Personnel .-......-. ....... _.___ .___._ 4-5Phosphoria formation .. _.___...____..__ 30Piezometric surface, definition ....__............ 100Pilgrim limestone - ......__..__._.__..,...._ 28Pitcher Creek .......... __.... ._ _.__... 83Pony series .. . .____.... __..____...._ 27Population of Gallatin County, 1950 ._....._ 20Potassium in water .. ..... .._..._...._._ 169Precambrian rocks.... 25, 26-27, 36, 47, 48, 49, 55Precipitation, annual volume during pe
riod 1935-51 ._.........._________ 134, 135at Belgrade ................ _.._.___..............._ 119, 120at Bozeman _______________ 19 collection of records _.....___........._ 8; pi. 1daily, near cottonwood grove ........ 114; pi. 4general characteristics . 14, 18, 58, 132, 133 monthly, at 18 stations ..__..._.._....._ 21-22
monthly volume during 1952 and1953 ........_............_._._ 19-20, 23; pi. 8
source of recharge .......... 107, 108, 127, 136,142, 153, 154-155, 157, 158, 159
Previous work in the area ....______._ 6-8
Pumping tests. See Aquifer tests.
Purpose of investigation .........__...._.........._... 4
Q Quadrant quartzite .___..__.......____. 30
Quaternary deposits, chemical quality ofwater ..._._... 162-163, 166-167, 168
170-171; pi. 10composition .......... ._._._.. 40-46, 140, 146, 153
Page Quaternary deposits Continued
extent and thickness .... 40, 42, 43, 57, 131,136, 140, 146, 150, 151-152, 153, 158
transmissibility ........ 102-103, 104-105, 136,140-142, 146, 150, 153-154, 159
water supply.. 40, 43, 132, 151, 154, 158, 159
R
Rainfall. See Precipitation. Randall Creek ............................................._ 63, 72Recharge of ground-water reservoir, from
irrigation water __..._.. 107, 108, 136,142, 150, 154, 157
from precipitation ......._._ 107-109, 136, 142,153, 154-155, 158, 159
from streams ............ 107-109, 137, 142, 143,153, 154, 158, 159
from underflow ............._............ 142, 147, 153Red Lion formation _.....__..__........__._... 29Reese Creek ._...._...._....... 66, 76, 86, 95, 111, 158Residual sodium carbonate in water . 161, 175 Resistivity survey . .. ...._.... ..... ... 9Reynolds Creek ._. _ .._ .......................... 67, 77Ridgley Creek .... _.. _._......................... 62, 72, 95Rierdon formation ..__........_.....-.-.-........._... 31Rocky Creek .........._..........._._..._................... 63, 72Ross Creek ._.................................. 55, 65, 76, 94-95Ross Peak . ........._......_......_._....................... 55
Sage pebble-conglomerate member ofSnowy Range formation..... 29
Salesville fault .........................__........._....... 5, 49, 53Sappington sandstone ... ... ... 29-30 Saturated material, changes in volume 119-128 Sawtooth formation _____ .._ _.. _ ___.. 31Schafer Creek ...............__.._......... ......_.. 85Sedimentary rocks ._..._.._.__.__.. ...__.. 25-46 Seepage, from canals, laterals, and ap
plied irrigation water _. 107, 132, 133, 136, 142, 150, 154, 157
from streams ........_.. 107, 142, 143, 153, 154,158, 159
Seismic survey ...._...._...... .............. ........ 9September Morn mine, lead ore __....__..._.... 25Settlement of the valley ...._....._..... ..... 20Sills ..........................._...................__..__.._._......... 46
Smith Creek _.........._......_...........__........... Ill, 159
Smith drain ............._........................... .. 82
Snow. See Precipitation.Snowmelt, recharge of ground water.. 107-109,
132, 133, 154-155; pi. 8
Snowy Range formation .......__._.......__.. 28, 29Sodium in water ......_.. _.._.................... 160, 169
Soils .. .- --- ---- 7-8
Sourdough (Bozeman) Creek ...._ 12,63,73,93,99, 154, 155
South Bridger subarea ________-....... .. .. 11, 159
South Cottonwood Creek ........ 55, 61, 70, 80, 93
South Gallatin subarea ......._...._....._.... . 11, 159
Spain-Ferris ditches ........_..._.......... 80-81, 111
Specific capacity of a well, definition.. ... 101
INDEX 281Page
Specific conductance of water ....... _._..... 166, 169Specific yield, computation of
average .................... 120, 123, 124definition ....................... .........- ....... 100-101
Spring Hill fan. See Spring Hill subarea. Spring Hill subarea, aquifer tests....... 105, 159
ground-water, discharge __...... 147, 159recharge ...._._..............-. .. . . 159
location and extent ....__...... 11, 42, 53, 158Springs, Bridger Range ............._............. 55, 99
Central Park subarea _.._.._____.__.____.________ 148Dry Creek subarea ............................ 87, 158Gallatin Range .................__.... __.__._____._. 55Manhattan subarea ........_. ....... 88, 150, 151thermal .......................... 50, 132, 162, 166, 170
Stone-Weaver ditches ................................ 82, 111Stony Creek *___....________.. _._.___...._-.._.... 67, 77, 148Storage, changes in volume of
ground-water ........ ......._... 119-128coefficient of, alluvium .... 103, 104-105, 106
definition ........._......... .._...._ .._.. 101Stratigraphic section, unit 1 ..... ._ _. ... 37
unit 2 ........................................................ 38-39Stream-channel deposits ............._... 39-41, 43-45Streamflow ............. 55, 58-99, 107, 108, 116, 117,
143, 144, 154, 155, 156, 158, 168 Stream-gaging program ..-.._._._ - 8, 58; pi. 1 Stream-gaging stations, description ........ 60-68Streams, from Bridger Range ... 94-95, 96
from Camp Creek Hills ...... ............... 95from Gallatin Range ._.._._ .............. 9b-94from Horseshoe Hills ._____._.-.......______..___ 95from valley floor .... . ......._....__...._... 14, 95monthly and annual runoff .__...._...._... 69-79occasional measurements of
discharge .. ...-_-........._.._.__..... 80-88Structure .......................................__........36, 46-55Sulfate in water ..................._...__.......___..___ 161, 176Surface water, alluvial deposits ..... 42-45, 53,
136, 140, 146. 151annual changes in supply 1935-51.. 134-136 chemical quality ...... 160, 164-165, 167-168,
172-173; pi. 11course and drainage area of princi
pal streams .... 13-14, 58-59, 92-95description of stream-gaging pro
gram __............_.........._....... 8, 58description of stream-gaging stations 60-68 discharge measurements .................... 69-88,
111, 135, 148gains and losses in flow, of East Gal
latin River ............................. 144of Gallatin River .................. 89-92, 139
general runoff pattern ..._........._.... 58, 89inflow to valley ........ 88-89, 93, 97-99, 116,
117, 128, 130, 132-136; pi. 8 monthly changes in supply
1952-53 - -...... 128, 130-132; pi .8outflow from valley ...__. 89, 92, 93, 117,
128,130, 132-136; pi. 8
Page Surface water Continued
relation to ground water .__..._..... 107, 108,117-118, 124, 136-137, 142, 143, 145-146,
147-148, 149, 153, 154, 155, 158, 159source of irrigation supply ... ... 20, 99,
116-117, 150, 156source of municipal supply .._ 99
Swift formation ........ ..._.._._.._ .____.______. 31Sypes Creek .................................................... 84
Temperature ....... .... 8, 14, 15-17, 107-108, 114,119, 155; pi. 4
Terrace gravels in Camp Creek Hills .... 42, 157Tertiary strata, aquifer tests . 102, 104-105, 142
artesian water ............ ...._...._...._..... 144, 150Belgrade subarea ..................... 142, 144-145Camp Creek Hills area .................... 131, 157description ..................... . ....._... 6, 25, 32-41Dry Creek subarea ______._._._-...____.____.____._ 158Manhattan subarea ...._......_....__........._ 150South Bridger subarea ...__...___.._....._.... 159South Gallatin subarea ._......._..._....__.... 159structure _ .. ....._... ...._.. . ...... 50-53subsurface unit ...._......._................_ 34-35test holes and wells ........... 34-35, 42, 43, 52,
136, 146, 154, 158, 166 undifferentiated ...................................... 34, 39unit 1 ....--..-...................-.. ...... 35-37; pi. 2unit 2 . -.. -. .- 38-39, 52; pi. 2vertebrate fossils ........................ 6, 33, 38, 39water derived from .... 34, 150, 159, 166, 167
Test holes, drilling program _.._ .......... 9logs ........................................................ 184-203
Thermal water .__.__.___.___.. __... ___.__________ 50, 132Thompson Creek ........................... 65, 76, 95, 148Three Forks shale ................_.................... 29-30Three Forks structural basin ...... .... 6, 25, 26,
32-33, 36, 53, 56 Topography ...._................................. 12-14; pi. 1Transmissibility, coefficient of, alluvial-
fan deposits 102-103, 106, 153-154 alluvium ...... 103, 104-105, 136, 146, 157definition _._.______.__.___..__..-.._______.________ 101Tertiary strata ........ 102, 103, 104-105,
146, 157 Transpiration of ground water by phrea-
tophytes ................ 110, 112, 113-115Transportation ........____...______.__ _.._.. ......... 2 3-24Trout Creek .................................................... IllTruman Creek ............................................... 66, 76
U
Upper East Gallatin subarea .......... 11, 151, 153U.S. Bureau of Reclamation ...... .._.... 4, 5, 7U.S. Public Health Service __..-...._.......... 175U.S. Soil Conservation Service ....... 4, 5, 7, 149U.S. Weather Bureau ................ 5, 8, 19, 20, 134
Valley floor, chemical quality of groundwater ................ 162, 166, 170; pi. 10
subareas ..........._.......................... 11, 136-153
282 GEOLOGY, GROUND-WATER RESOURCES, GALLATIN VALLEY, MONT.
Page Valley-fringe area, chemical analyses of
ground water .... 163, 167, 171: pi. 10 resume of water resources .. _........ 158-159
W
Water, suitability for domestic use .... 175-176suitability for irrigation _____________ 168-175
Water-level fluctuations, caused by earth quakes and other disturb ances --....-........._..-..._... ..... . 128
graphs ..................--. 108, 109, 112, 129, 147,152. 156; pi. 9
measurements ....... ............... ..... 8, 204-243
relation to changes in ground-waterstorage ._...-.-...-..-__. ...-.... 119-128
Waterlogging .......... ............ 7, 110, 139, 146, 147,150, 151, 158
Water-resources inventory, water years1935 through 1951 .............. 134-136
water years 1952 and 1953,analysis ............................... 132-134
evaluation ......._.... ............ 128,131-132graph .-...... ............._.............. ._. pi. 8
Water table, changes in position. 119-128, 137, 139-140, 143-144, 145-146, 149, 151,
153. 156; pi. 7
Page Water table Continued
configuration ......_.. .__......_.._______ 118; pi. 5definition .. .- .....-.._..__._.... ............. _ 100
depth to .................... 118, 137, 143-144, 147,153, 155-156; pl.6
Watts Creek ........ _. ......... _ .._..........._......_ 84-85
Weaver ditches ..._.._.............. ............ 81-82, 111
Well-numbering system ........................... 9 11
Wells, hydrographs of water level ..... 108, 109,
112, 129, 147, 152, 156; pi. 9 location ... .. ... ._......_....._... ._ 8; pi. 1
logs ....................................................... 184-203
measurements of water level .... 8, 204-243records _........-....-.... ._._._-.........--...... 244-275
West Branch of East Gallatin River .... 84, 111
West Fork of Wilson Creek ................_...__. 60, 70
White River formation ......_..._....... .. 33, 34, 36
Wilson Creek .................................... 60, 70, 80, 93
Wind velocity ............................... 118, 115; pi. 4
Wolsey shale ..........._.................................... 28, 46
Yankee Creek _............. ........................ _... 80Yellow Dog Creek ........_...___...._........_...__...... 61, 71
Yield, specific, definition ..............._..... .... 101
U. S. GOVERNMENT PRINTING OFFICE: I960 O SO89I9
The U.S. Geological Survey Library has cataloged this publication as follows :
Hackett, Orwoll Milton, 1920-Geology and ground-water resources of the Gallatin Val
ley, Gallatin County, Montana, by O. M. Hackett [and others]. With a section on Surface-water resources, by Frank Stermitz and F. C. Boner, and a section on Chemical quality of the water, by R. A. Krieger. Washington, U.S. Govt. Print. Off., 160.
viii, 282 p. illus., maps, diagrs., tables. 24 cm. (U.S. Geological Survey. Water-supply paper 1482)
Part of illustrative matter in pocket.Prepared as part of the program of the Department of the Interior
for development of the Missouri River basin.(Continued on next card)
Hackett, Orwoll Milton, 1920- Geology and ground- water resources of the Gallatin Valley, Gallatin County, Montana. 1960. (Card 2)
Bibliography: p. 179-182.1. Geology Montana Gallatin Valley. 2. Water, Underground
Montana Gallatin Valley. 3. Water-supply Montana Gallatin Val ley. 4. Water Analysis. I. Stermitz, Frank, 1907- II. Boner, Fred Charlan, 1925- III. Krieger, Robert Albert, 1918- (Series)
