Ground-Water Resources of the Bryce Canyon National Park_ Area, Utah_
With a section on THE DRILLING OF A TEST WELL
GEOLOGICAL SURVEY WATER-SUPPLY PAPER 1475-M
^ Prepared in cooperation with the \ National Park Service, \ Department of the Interior Ground-Water Resources of the Bryce Canyon National Park Area, Utah
With a section on THE DRILLING OF A TEST WELL
By I. WENDELL MARINE
HYDROLOGY OF THE PUBLIC DOMAIN
GEOLOGICAL SURVEY WATER-SUPPLY PAPER 1475-M
Prepared in cooperation with the National Park Service, Department of the Interior
UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1963 UNITED STATES DEPARTMENT OF THE INTERIOR
STEW ART L. UDALL, Secretary
GEOLOGICAL SURVEY
Thomas B. Nolan, Director
For sale by the Superintendent of Documents, U.S. Government Printing Office Washington 25, D.C. CONTENTS
Page Abstract--__-_-_-_----_--_-_---______-______-______441 Introduction.______442 Purpose and scope-_-_-----______-______-_____-____ 442 Location of the area______442 Previous investigations.______-_-______-_-___-__-______--_ 444 Personnel and acknowledgments.-----.------444 Geography ______444 Water use______445 Geology ______450 Stratigraphy. ______450 Structure. _----_-______---______----______--___-__---_ 461 Water resources-__------_--__---___--_____--__------_-_---__-_---- 461 Surface water-____-_-__--_____-______-_-_-__-_- 461 Springs____-______462 Ground water in alluvium. __-_-______..-_-____--_-_- 471 East Creek valley.--.------.-______471 Other alluvium-filled valleys..------475 Ground water in bedrock-______475 Conclusions-______477 Drilling of a test well_-_-_-_-----_-_--____------_-___---_-----_---_ 478 References cited-_-__--_-___-_-______._____-__-___-____-_-____--__- 483 Index...._-______._.__.______-___-_____.___.__.______485
ILLUSTRATIONS
[Plates 24-26 In pocket] PLATE 24. Map of Bryce Canyon National Park area, Utah, showing physio graphic features and the location of springs and wells. 25. A, Map of East Creek valley showing area underlain by alluvium. B, North-south section of East Creek valley showing inferred maximum depth to bedrock and the position of the water table in May 1957. 26. Logs of the test well at Bryce Canyon National Park. ni IV CONTENTS
Page FIGURE 51. Number of visitors to Bryce Canyon National Park from 1929 to 1956 and range of possible future attendance ______443 52. Annual precipitation and cumulative departure from normal at Bryce Canyon National Park______445 53. Water-supply developments of the Utah Parks Co. in East Creek valley showing wells, a developed spring, the spring- collector sump, and the spring pumphouse______447 54. Hydrographs of two observation wells in the alluvium of East Creek valley, April to September 1957______449 55. Geologic map of the northern part of Bryce Canyon National Park area______460 56. Generalized east-west cross section through Merrill Ranch Spring showing the movement of ground water in relation to the occurrence of all fault line springs in the area_____- 466 57. Yellow Creek Spring and the Yellow Creek Wash seen from Paria View observation point-______469 58. Selected schematic cross sections across East Creek valley showing approximate thickness of alluvium-______473 59. Schematic diagrams of saturated alluvium in parts of East Creek valley, May 1957------474 60. Graph of the water level during pumping of the test well- _ _ _ 481
TABLES
Page TABLE 1. Tropic Ditch diversions of the Tropic and East Fork Irriga tion Co_.______--______-__-__-_-_--____ 446 2. Monthly p,umpage from Utah Parks Co. well field in East Creek valley during 1957 and the net decline in water level each month in well 3______-___-______-_---___-______448 3. Summary of quantities of water available from selected sources compared to present water use and estimated future water needs in Bryce Canyon National Park ______450 4. Logs of wells and auger holes in the Bryce Canyon National Park area-____-______-_-______-----______-___-- 451 5. Generalized section of the geologic formations in the Bryce Canyon National Park area__-_--______----______-__-_- 456 6. Records of springs below the Pink Cliffs in the Bryce Canyon National Park area______-______-_-______-___-_ 464 7. Chemical analyses of water from selected springs and wells in the Bryce Canyon National Park area ______467 8. Chemical analyses of water from the test well at Bryce Canyon National Park______482 9. Measurements of springs below the rim, 1958-60-______483 HYDROLOGY OF THE PUBLIC DOMAIN
GROUND-WATER RESOURCES OF THE BRYCE CANYON NATIONAL PARK AREA, UTAH With a Section on the Drilling of a Test Well
By I. WENDELL MARINE
ABSTRACT The water need at Bryce Canyon National Park in 1957 was about 1.3 million cubic feet for a tourist season that lasted from the middle of May to the middle of October. To evaluate the adequacy of water-supply sources, a hypothetical future need of 5 million cubic feet of water per season is used. This amount of water might be obtained from the East Fork of the Sevier River, from wells in the alluvium of the East Fork, from Yellow Creek Spring and nearby springs, which are below the canyon rim, or from a well drilled about 2,000 feet to the top of the Tropic shale. Although the present source of water, consisting of wells in the alluvium of East Creek valley, may be an important supplemental source in the future, it will not yield sufficient water in dry years to meet the total demand for water at the park. The yield of Yellow Creek Spring and nearby springs is estimated at a total of 7.8 million cubic feet of water per season. The springs provide water of satis factory chemical quality, and are a reliable source even in times of drought. A serious disadvantage of using this source of water is the difficulty of con structing a pipeline over extremely rugged terrain from the source to the lodge and headquarters area. A well drilled to the top of the Tropic shale of Cretaceous age in the lodge and headquarters area might penetrate two or more aquifers, one at the base of the Wasatch formation of Eocene age and one or more in the Wahweap and Straight Cliffs sandstones of Cretaceous age. The yield of this well would depend to a large degree on the number of fractures encountered. To assure the most favorable conditions for intercepting fracture zones in the bedrock, a test-well site is proposed near the crest of a gentle anticline where tension fractures in the rocks should be common. Shallow wells in the alluvium of East Creek valley cannot be depended upon to yield sufficient water in times of drought, but they are nevertheless an important source. The water-storage capacity of the alluvium of East Creek valley in the vicinity of the wells of the Utah Parks Co. is estimated at 1.4 million cubic feet. By lowering the water table in the valley uniformly without creating excessively large cones of depression, the alluvium could supply the 1.3 million cubic feet of water per season estimated as the water need in 1957. However, in times of drought this alluvium cannot supply the hypothetical future needs of 5 million cubic feet of water per season. 441 442 HYDROLOGY OF THE PUBLIC DOMAIN
INTRODUCTION PURPOSE AND SCOPE The purpose of this investigation was to appraise the ground-water resources of Bryce Canyon National Park area and vicinity. This appraisal is intended to furnish sufficient information to enable the National Park Service to develop an adequate water supply. The water system of the National Park Service, which is the only one available for year-round use in Bryce Canyon National Park, consists of 1 well (headquarters well) that yields about 160 gpd (gal lons per day), enough to supply the needs of 1 family; one 5,000- gallon storage tank; and pipelines for the distribution of water. The Park Superintendent estimates that about 1,000 gpd was needed to supply the seven families of the National Park Service that domiciled in the park during the winter of 1956-57. During the summer the water system of the National Park Service is connected into the water system of the concessioner (the Utah Parks Co.), and the shortage of water for these families is alleviated. The water-supply system of the concessioner, however, is inadequate to supply all the water needs of the park for an entire season in times of drought. Because the Mission 66 program includes plans for the expansion of the overall facilities at Bryce Canyon National Park, a water supply much larger than that now provided by the concessioner is needed. Figure 51 shows the general increase in the number of visitors to Bryce Canyon National Park in past years and the estimated future range of attendance under the Mission 66 program. Any water supply that is planned should be able to meet not only the present water needs of the park but also future needs. The principal objectives of this investigation were to determine the quantity, quality, and dependability of all possible sources of water supply for the park. Because the water supply is needed in the lodge and headquarters vicinity, special emphasis was placed on sources that are within several miles of that area.
LOCATION OF THE AREA The area of this report is in and adjacent to Bryce Canyon National Park in the Paunsaugunt Plateau region (pi. 24). The park is in Kane and Garfield Counties, south-central Utah, between 37°42' and 37°26' north latitude and 112°05' and 112°17' west longitude. It is also on the divide between the Paria River, a tributary to the Colorado River, and the East Fork of the Sevier River, which drains into the Great Basin. NUMBER OF VISITORS, IN THOUSANDS
1930
1935
940
1945
1950
1955
\ \ 960
\\ v%^ 'vsav NOAN.VO 444 HYDROLOGY OF THE PUBLIC DOMAIN PREVIOUS INVESTIGATIONS The geology of the Paunsaugunt Plateau region was described by Herbert E. Gregory in a report (1951) that includes brief discussions of the ground-water resources of the region and of some of the most important wells and springs, and a geologic map that was used ex tensively in carrying on the present investigation. Williams (1954) gave a synopsis of the stratigraphy and structure of the Paunsaugunt Plateau region. A report by Gregory and Moore (1931) referred in part to the geology of the area. In 1939 the U.S. Geological Survey published a topographic map of Bryce Canyon National Park and adjacent area, which was extremely useful in the present investigation. A 3-day reconnaissance of the Campbell Canyon Spring and Bryce Canyon Spring areas was made in April 1954 by Ben E. Lofgren, engineer, U.S. Geological Survey. This reconnaissance included no discharge measurements, but on the basis of it Mr. Lofgren suggested to the National Park Service personnel that the Campbell Canyon Spring might be used for a park water supply. PERSONNEL AND ACKNOWLEDGMENTS This investigation was made under the direct supervision of Herbert A. Waite, district geologist of the U.S. Geological Survey in charge of ground-water investigations in Utah. Glen T. Bean, Superintendent of Bryce Canyon National Park, and employees of the National Park Service at Bryce Canyon rendered valuable assistance in all phases of the investigation. Donald Price, geologist, Ground Water Branch, assisted the writer for 2 weeks in the field investigations. Robert Burns, former Supervisory Park Ranger, and Robert Ott, of the National Park Service, were very helpful in guiding the writer to significant springs in the area. GEOGRAPHY Bryce Canyon National Park lies at the east edge of the Paun saugunt Plateau, one of the high plateaus of southern Utah, and includes part of the plateau, the rim, and the foothills bordering the plateau at a lower elevation. The altitude of the plateau top in the park ranges from about 7,600 to more than 9,000 feet. The climate of this part of the park is generally cold except in the summer months. The relief in the foothills below the rim is as great as 1,000 feet. The temperature below the rim is generally higher than that on the plateau, and the summers are longer. Figure 52 shows the annual precipitation and departure from normal at Bryce Canyon National Park from 1933 through September 1957. It also shows cumulative departure from normal precipitation. The weather station is at the headquarters, on the plateau. GROUND WATER, BRYCE CANYON NATIONAL PARK AREA, UTAH 445 30 20 10 3 s 0 10 r> o 25 rsl O ro r W - ^ ^ _o D X e o CD 20 n ; CD z f m n en V) -0 <# UJ o 2 o _- / £ 0 ? 15 _ / ', 7 / s / '/ o ; / -5 a^ o / UJ ^ '/ ^ pn £E 10 '/ / 1- t ir '/ UJ r or / -10 ui CL 7 / / Q / / ^ ^ O IO IO m CD CD FIGUBE 52. Annual precipitation and cumulative departure from normal at Bryce Canyon National Park, Utah. WATER USE The principal water users in Bryce Canyon National Park and vicinity are the public and employees using the National Park Service and concessioner water systems, the town of Tropic, and the Tropic and East Fork Irrigation Co. Other water users in the area obtain 644924 O 62- 446 HYDROLOGY OF THE PUBLIC DOMAIN small supplies from wells or springs. The town of Tropic is supplied from Bryce Spring through a pipeline about 1% miles long (pi. 24). The Tropic and East Fork Irrigation Co. obtains water from the East Fork of the Sevier River and transmits it by way of the Tropic Ditch across part of the plateau, down Water Canyon, and into the vicinity of the town of Tropic where it is used for irrigation. The diversions of the Tropic and East Fork Irrigation Co. for the last 7 years (1950- 56) are listed in table 1. Water is used in Bryce Canyon National Park for general needs at the lodge, cafeteria, and campground and for domestic needs by the personnel of the Park Service and the employees of the Utah Parks Co. TABLE 1. Tronic Ditch diversions of the Tropic and East Fork Irrigation Co. [U.S. Geological Survey gaging station 5 miles below Daves Hollow] Flow in ditch, in acre-feet Month 1950 1951 1952 1953 1954 1955 1956 April _ 138 May______1, 130 691 976 287 726 518 296 June- _ ____ 1, 110 837 1,060 549 720 392 360 July _ _ 612 427 1, 170 455 490 347 .2 650 289 999 178 104 256 3.8 September _ _ 263 84 738 107 136 437 212 October __ _ _ _ 68 42 301 1 104 62 Total . _ 3,900 2,400 4,980 1,880 2, 180 2,050 934 For many years some water has been supplied to the park facilities from Trough and Shaker Springs, but in 1956 and 1957 these springs were dry. For the past several decades some water has been obtained from springs in East Creek valley. In July 1955 the springs in that valley had so decreased in yield that it became evident that they would not supply water through the rest of the season, and in that month well 1 was drilled (fig. 53). This well was the sole source of water supply for the park from July 1955 to August 1957. It is reported that the springs dried up completely after the well pump was installed and that they did not flow in 1956. In May 1957 there was a small overflow from the spring collector sump (fig. 53), but by June of that year there was none. In February 1957 two additional wells were drilled in East Creek valley. Upon completion the wells were tested by personnel of the Utah Parks Co. to determine their yield. No FIGURE 63. Water-supply developments of the Utah Parks Co. in the East Creek valley showing wells 1, 2, and 3; a developed spring (4); the spring-collector sump (5); and the spring pumphouse (6). Note flat-floored valley bordered by bedrock side slopes. Photograph by H. A. Waite. 448 HYDROLOGY OF THE PUBLIC DOMAIN measurements of water level were made during these tests, The results of each test are summarized as follows: Pump setting Well Yield (gpm) Time(hr) below land sur face (ft) 1 180 8 18 2______90 8 24 3 25 0 1 Tested for short period and pump broke suction. The average of 4 separate measurements of the discharge of well 1 made at the Utah Parks Co. storage tanks in May 1957 was 55 gpm. Three check measurements were made in July 1957, and still the average was 55 gpm. It should be emphasized that this was the water delivered at the tanks and available for use; it was not nec essarily the same as the amount of water discharged by the well, because there may have been leaks in the 4 miles of pipeline between the pump and the tanks. In the parts of the pipeline seen by the writer, however, there were no leaks, and it is assumed in the rest of this report that 55 gpm was the discharge rate of well 1. Water-level recording gages were installed on wells 2 and 3. The records from these wells show within 15 minutes when the pump on well 1 begins to operate. These recording gages, therefore, are valuable not only to record water-level fluctuations in the basin (fig. 54) but also to indicate the duration of pumping. Table 2 shows the total number of hours that the pump was in operation during each month from April through November 1957. TABLE 2. Monthly pumpage from Utah Parks Co. well field in East Creek valley during 1957 and the net decline in water level each month in well 3 Total time Water pumped Net decline Month of pumping in water level (hours) (feet) Gallons Cubic feet Acre-feet April _ _ 0 0 0 0 0 May _ 299 986, 700 131, 500 3.04 1 1 478 1, 577, 400 213, 000 4.89 2 5 July______.___. 714 2, 356, 200 314, 000 7.22 3 0 August _ 1 496 1, 636, 800 219, 100 5. 04 8 September _ 1 338 1, 115, 400 148, 700 3. 41 4 1 200 660, 000 88, 000 2. 02 2 November _ 0 0 0 0 0 Total. _ 2,525 8, 332, 500 1, 114, 300 2,562 8.0 1 Well broke suction on Aug. 2,1957. Amount of water used from August through October was limited by decreased discharge of pump. WATER LEVEL, IN FEET BELOW LAND-SURFACE DATUM kji 1 I -?? ° £. C s-co i£' 10 B P I? Hvj;n 'vaav IVNOIJ.VN 450 HYDROLOGY OF THE PUBLIC DOMAIN On August 2, 1957, well 1 began to pump air, and from that date to the end of the season the amount of water pumped was not a true indication of the need for water in the park. The amount of water pumped in the first half of the tourist season may be used as a basis for estimating the need for water in the park. During the season, July and August are the months of maximum pumping and May and October the months of least pumping. The pump is started about May 1 and stopped about November 1. Assuming that the pumpage in August is about the same as in July, September the same as June, and October the same as May, it is estimated that the water need for one entire season (as of 1957) is about 1.3 million cubic feet. On the basis of the National Park Service's Mission 66 design of facilities for 500,000 visitors, a water need of about 5 million cubic feet per season has been selected as a basis for the comparison of various sources of water. A summary of these figures is given in table 3. TABLE 3. Summary of quantities of water available from selected sources compared to present water use and estimated water needs in Bryce Canyon National Park, Utah Total quantity per Total quantity per 4}£-month season 4V6-month season Maximum Estimated (based on estimated quantity yield after yield) measured develop in 1957 Millions Millions ment work (gpm) of gallons of cubic (gpm) Millions Millions feet of of cubic gallons feet 55 19.7 11.3 Estimated water need for planning 39 5 Water available from: Alluvium of East Creek ...... 255 38.3 31.1 55 MO <1.4 28 5.4 .7 50 9.7 1.3 24 4.7 .6 35 6.8 .9 81 16 2.1 110 21 2.9 Yellow Creek Spring and Upper Yellow Creek Wash Spring ..... 201 39 5.2 300 58 7.8 Right Fork (of Yellow Creek) 75 15 1.9 75+ 14.6+ 1.9+ Estimated yield from proposed bed rock well (based on meager infor- » 30-300 5. 8-58 0. 8-7. 8 1 Represents the estimated water requirements in 1957. 2 Well field would not sustain this yield. Well 1 broke suction on Aug. 2,1957. 3 Actual withdrawal from alluvium of East Creek. 4 Based on a sustained yield of 55 gpm. 8 Depends on the number of fractures encountered. GEOLOGY STRATIGRAPHY The oldest rock formation known to underlie the Bryce Canyon area is the Redwall limestone of Mississippian age. This formation was penetrated at a depth of 10,189 feet below the surface in an oil test in Johns Valley (table 4) about 12 miles northeast of the lodge GROUND WATER, BRYCE CANYON NATIONAL PARK AREA, UTAH 451 and headquarters area (off pi. 24). This same test hole passed through 779 feet of Pennsylvania!! strata comparable to the Molas and Her- mosa formations. Rocks of Permian age were penetrated in the Lion Oil Co. test hole, 4 miles northwest of the lodge and headquarters area (pi. 24; table 4). These rocks were the Coconino sandstone, the Toroweap formation, and the Kaibab limestone. TABLE 4. Logs of wells and auger holes in the Bryce Canyon National Park area, Utah [See pis. 24, 25^4 for location. All water levels in this table are in feet below land surface] Thickness Depth (feet) (feet) Headquarters well, National Park Service Yield, 160 gpd; diameter, 48 in. to 30 ft, 12 in. to 50 ft, 8 in. to 80 ft. Static water level, 49 ft. Alluvium: Old dug well___-_----______-___-__- 30 30 Wasatch formation: Rock_.__._..___.______.______.____._____ 10 40 Fractured rock-______-______---__ 10 50 Rock______30 80 Well 1, Utah Parks Co. Yield, 180 gpm; diameter, 12 in. Alluvium: Clay______12 12 Gravel,______3 15 Porous formation_____--_-______-___ 9 24 Tight formation______-----_-______30 Wasatch formation: Dry chalky formation______50 80 Well 2, Utah Parks Co. Yield, 90 gpm; diameter, 12 in. Static water level, 4 ft. Alluvium: Clay______.______6 Sand and gravel-______4 10 Clay__-_-____-______--__-______--.-_--- 2 12 Gravel______2 14 4 18 Gravel and sand______8 26 Clay__---______--______-____------4 30 Wasatch formation: Rock 30+ 452 HYDROLOGY OF THE PUBLIC DOMAIN TABLE 4. Logs of wells and auger holes in the Bryce Canyon National Park area, Utah Continued Thickness Depth (feet) (feet) Daves Hollow Ranger Station, Forest Service Yield, 90 gallons per hour; diameter, 6 in. Static water level, 15 ft. Alluvium: Clay, sandy, and gravel____---__-_------20 20 Kaiparowits formation: Clay, sandy, gray______15 35 Clay, sandy, gray (water).______15 50 Clay, sandy, gray______60 110 Clay, sandy, gray (very hard)______-_____-_--- 12 122 Shale, sandy, brown (caving)______3 125 Clay, sandy, gray______-__-_____---_--_ 82 207 Bryce Canyon Airport, Civil Aeronautics Administration Yield, 10 gpm; diameter, 6 in. Static water level, 33 ft. Alluvium: Conglomerate and hardpan______12 12 Clay, yellow.______4 16 Clay, light brown______7 23 Clay, blue-gray______11 34 Clay, gray-brown.______9 43 Clay, sandy, light-brown______5 48 Clay, sandy, light______-__--__-__---- 3 51 Kaiparowits formation: Sandstone, gray ______40 91 Shale, gray ______8 99 Shale, sandy, blue______--__-_------_-_ 26 125 Shale, sandy, hard, blue_-_-_-_------___-_---- 2 127 Shale, sandy, blue______9 136 Shale, sandy, hard, blue______-______--- 2 138 Shale, sandy, soft______-_-_-_-__-_---___ 12 150 Sawmill Well, E. A. Crofts Yield, 40 gpm; diameter, 6 in. Static water level, 18 ft. Alluvium: 20 20 Sand (little water)______15 35 25 60 Gravel (water) ______6 66 Kaiparowits formation: Shale, light-gray (no water) ____ 244 310 GROUND WATER, BRYCE CANYON NATIONAL PARK AREA, UTAH 453 TABLE 4. Logs of wells and auger holes in the Bryce Canyon National Park area, Utah Continued Thickness Depth (feet) (feet) Lion Oil Co. water well Yield, 10 gpm; diameter, 6 in. Alluvium : Sand rock______70 70 Rock formation, porous ______6 76 Sand rock______40 116 6 122 Sand rock______8 130 Rock, porous ______._ 6 136 Lion Oil Co. oil test Kaiparowits formation and Wahweap and Straight Cliffs sandstones.______940 940 Tropic shale______1,305 2,245 Dakota sandstone______415 2,660 Morrison formation.______1,965 4,625 Carmel formation______1. 430 6,005 Nayajo sandstone______2. 075 8, 130 Chinle formation, upper part______598 8,728 Shinarump member of Chinle formation.______129 8,857 Moenkopi formation______1, 125 9,982 Timpoweap member of Moenkopi formation____-_.___. 104 10, 086 Kaibab limestone.______479 10, 565 Toroweap formation______4J51 11,016 Coconino sandstone.____-___-__-_-__-_-____-__-_--_- 205 11, 221 The Pines Motel, Mayo Rich Diameter, 6 in. Static water level, 15 ft. Alluvium: Clay, sandy______-___ 10 10 160 170 Forest Oil Corp. oil test [about 3 miles west of Lion Oil Co. oil test, off pi. 24] 496 496 155 651 231 882 2, 398 3,280 Tropic shale______1, 130 4,410 218 4,628 Winsor formation, ______507 5, 135 470 5,605 586 6,191 Navajo sandstone. ______51 6,242 644924 O 62 454 HYDROLOGY OF THE PUBLIC DOMAIN TABLE 4 Logs of wells and auger holes in the Bryce Canyon National Park area, Utah Continued Thickness Depth (feet) (feet) California Co. oil test, Johns Valley No. 1 in sec. 22, T. 35 S. R. 2 W. Wahweap and Straight Cliffs sandstones.______910 910 Tropic shale.______898 1,808 Dakota sandstone. ______^______202 2,010 Morrison formation.______685 2,695 San Rafael group.______955 3,650 Glen Canyon group______.______2,085 5,735 Chinle formation, upper part______--______-___. 560 6,295 Shinarump member of Chinle formation ______75 6,370 Moenkopi formation ______995 7,365 Kaibab limestone______923 8,288 Coconino sandstone.______1,022 9,410 Formations comparable to Hermosa and Molas forma tions (combined) ______779 10, 189 Redwall limestone.______146 10, 335 Logs of auger holes in alluvium of East Creek valley AUGER HOLE 1 Sand, clayey, tan______14 14 Gravel and sand, tan (water) ______ AUGER HOLE 2 Sand, clayey, tan______Gravel and sand, tan (dry)______2K AUGER HOLE 3 Soil, dark clayey.______Gravel and clay, light-brown______Gravel, angular, white (water) _____ AUGER HOLE 4 Clay, sticky, gray-brown ______Sand, clayey, brown______Gravel, fine; sand and clay, tan_____ Gravel, coarse, reddish-white (water). AUGER HOLE 6 Soil, sandy, dark-gray______. Clay, sticky, gray_---______. Clay, sticky, yellow______Gravel, sand and clay, yellow (water). GROUND WATER, BRYCE CANYON NATIONAL PARK AREA, L7TAH 455 TABLE 4. Logs of wells and auger holes in the Bryce Canyon National Park area, Utah Continued Thickness Depth (feet) (feet) Logs of auger holes in alluvium of East Creek valley Continued AUGEB HOLE 6 Soil, clayey, black______2 Clay, sticky, black______-______2 Clay, sandy, (water)_.______.______1 AUGEB HOLE 7 In gully about 15 ft below general land surface. Bank of gully, red sand______-_____---_____-__-_ 15 15 Red sand______21} Gravel(dry)______2iy2 AUGER HOLE 8 Clay, sandy, dark-gray.___.______--___-______8> Gravel and clay, white______-______9 Sand, reddish-white_-_--______-_-___-__------_--- 10* _ Gravel(dry)______10*$ AUGEB HOLE 9, DAVES HOLLOW Pit.______4 4 Clay, sticky, red______8 12 Sand, fine, red-____-____-______-___-___-_-_-__---_ 1 13 Gravel, reddish-white (dry)______1 14 The thickness and the geologic and hydrologic character of the Mesozoic and Cenozoic rocks underlying Bryce Canyon National Park are given in table 5. Of these formations the oldest shown on the geologic map (fig. 55) is the Winsor formation of Late Jurassic age. The Mesozoic rocks in table 5 are predominantly sandstone and shale with only minor limestone or conglomerate beds. Except for the Navajo sandstone, most formations have gypsum as a common cementing agent. This mineral is easily soluble, and thus may be present in much of the ground water contained in these beds. Gyp sum is not so common in rocks of Cenozoic age, which are mostly limestone or sand and gravel. Oi TABLE 5. Generalized section of the geologic formations in the Bryce Canyon National Park area, Utah Based on information obtained from several sources, including Gregory (1951), Gregory and Moore (1931), and Harshbarger and Repenning (1954)] Depth to System Series Geologic unit Thickness (feet) bottom of Physical character Water supply formation 1 (feet) Gravel, sand, silt, and clay filling the valley Gravel and sand lenses in the alluvial bottoms of East Creek, Daves Hollow, and valleys on the Paunsaugunt Plateau other small streams, and the valley of the yield as much as 180 gpm to a well. East Fork of the Sevier River. Attains Gravel fill in the canyons below the rim Quaternary Recent and Alluvium 0-136 0 maximum thickness in Emery Valley. is very porous and in the washes this Pleistocene Fills valley bottoms of Water, Campbell, gravel is very permeable; yields large and Bryce Canyons, Yellow and Sheep quantities of water where saturated, but Creeks, Swamp Canyon, and other can in general the gravel contains water only yons below the rim. in the vicinity of bedrock springs, with resultant limited yields. Upper white beds present on Boat Mesa and The white beds support springs of un Whiteman Bench are white, gray, or stable yield on Whiteman Bench. light-brown sandstone, conglomerate, and A few small springs issue from sandy 500-700 at the limestone containing siliceous cement and lenses and fractures, but the beds are not rim. volcanic tuff and ash. likely to yield water to wells. 1,000 at Boat Middle pink beds, chiefly pink, gray, and Basal conglomerate beds support several Tertiary Eocene Wasatch formation Mesa. 500 white massive limestone and interbedded springs fust below the rim and in the 0-700 between sandstone and conglomerate. valley of the East Fork of the Sevier. If the East Basal conglomerate consists of pebbles lenses of conglomerate are penetrated, the Fork of the poorly cemented by calcium carbonate; basal conglomerate might yield moderate Sevier River absent in Swamp Canyon and Yellow quantities of water to wells. and the rim. Creek; 10 to 30 ft thick at Bryce Point, composed of sandstone and conglomerate; 30 ft thick at Campbell Canyon, composed of lenses of conglomerate in limestone. Absent in Dark-gray, gray-green, yellow, and tan Yields water to several springs below the Bryce and coarse- and medium-grained arkosic sand rim. Wells that penetrate this formation Kaiparowits Campbell stone poorly cemented by calcium carbon have very low yields (10 gpm or less). formation Canyons. 900 ate and in part by gypsum and iron oxide. 400 in Yellow Brown, white, and greenish limestone and Creek and blue and purple shale. Contains verte Sheep Creek brate bones, fossil wood, invertebrates, areas. and ironstone nodules and concretions. Yellow and buff fine to medium sandstone, These two formations support most of the 40 to 60 ft thick in upper part. Inter- prolific springs below the rim. Although Wahweap sand bedded sandstone and shaly sandstone in no water wells penetrate these forma stone extensive lenses in lower part. Cemented tions in the Bryce Canyon area, they mainly by calcite, but hard layers are might yield water to wells in sufficient cemented by iron oxide. Contains some quantity for a public supply. The ex gypsum and wood. tensive sandstone layers make up most 850+ 1,750 of the two formations which are saturated Tan sandstones make up 95 percent of this throughout the area; thus, most wells are Cretaceous Upper formation, and sandstone layers greater apt to penetrate water-bearing material. Cretaceous than 10 ft thick make up 60 percent. Some (Lithologic equivalent in the Navajo Straight Cliffs of the sand is fine, but most is medium to Indian Reservation yields 20 to 40 gpm.) sandstone coarse, and some conglomerates contain pebbles 1 to 3 in. across. Cemented mainly by calcite but in part by some iron oxide. Disseminated gypsum and car bonaceous beds occur. Bluish-drab clayey to sandy shale; irregu Very poor water-bearing formation. larly bedded sandstones; abundantly Forms impermeable barrier along Paun- Tropic shale 800 2,550 fossiliferous; gypsum and selenite crystals saugunt fault, causing faultline springs. are common. Contains sand lenses 2 to Sandstone lenses might produce small 15 ft thick and carbonaceous beds. quantities of water, but such water would be high in calcium and sulfate and prob ably of unsatisfactory quality. Springs issue from the base of this formation in the Paria Valley. If sufficient thick ness is penetrated, this formation would Dakota sandstone 30 2,580 Buff-gray medium- to coarse-grained sand yield some water to wells. It is saturated stone and conglomerate containing some everywhere west of the Paunsaugunt shale and carbonaceous beds. Sandstones fault. The water might be of unsatis are weakly cemented. Contains some factory quality owing to seepage from the silicifled wood. overlying Tropic shale. (Yields 5 to 10 gpm in Navajo Indian Reservation, but water is highly mineralized.) Representative of depths and thicknesses underlying the vicinity of Paris View observation point in park. Cn 00 TABLE 5. Generalized section of the geologic formations in the Bryce Canyon National Park area, Utah Continued Depth to System Series Geologic unit Thickness (feet) bottom of Physical character Water supply formation 1 (feet) Many of the creeks become perennial on or Winsor formation 600-700 3,280 Thin-bedded red- and white-banded arkosic just below the outcrop of this formation. sandstone. Sand is medium- to coarse Several springs undoubtedly issue from grained; cemented by iron oxide, calcite, this formation but only one at the base and gypsum. has been observed. Yields to wells should be moderate to small, but the water may be of poor quality. Uncon formity 110-180 3,460 Massive gypsum, dense thin-bedded lime Very poor water-bearing formation. Would Curtis stone, calcareous sandstone and shale, and yield very small amounts of highly min formation gypsiferous very sandy shale. eralized water to wells. Uncon formity Upper Thinly stratified friable fine-grained and Springs issue at various horizons from the Jurassic RafaelSangroup very fine grained red, brown, and gray Entrada, but owing to the fine texture of sandstone; some limestone, shale, and gyp the sand, yields to wells would be small Jurassic Entrada 170-240 3,630 sum beds; contains abundant gypsum, unless abundant fractures improved the sandstone which constitutes the chief cement, and permeability. Under the Paunsaugunt fills cracks. Thickest individual sand bed Plateau water would probably be highly about 30 ft. mineralized. Regularly interstratified beds of tan and Carmel 0-165 3,795 blue-gray shale, limestone, and sandstone, Very poor water-bearing formation. Water formation containing smaller amounts of gypsum probably highly mineralized. Middle and conglomerate in both thin and thick Jurassic lenticular beds. fortuity Probably would yield largest amounts of Jurassic and a o o. Navajo 1,200-1,800 5,595 Light creamy-yellow, white, and buff highly good-quality water of any formation be Jurassic(?) sandstone crossbedded sandstone. Forms the White low the Wahweap and Straight Cliffs |i!^o 60 Cliffs. sandstones. (Yields as much as 70 gpm Uncon in the Navajo Indian Reservation.) formity Upper part 600-800 6,395 Red and brown shale, sandstone, and lime Probably not water bearing. of Chinle stone. Upper Ohinle formation formation so Triassic Shinarump 0-115 6,510 Red and gray conglomerate. May yield a small quantity of water to member wells, but water would probably be some Triassic what mineralized. Uncon formity Middle(?) and Lower Moenkopi 600 7,010 Chocolate-brown shale and some sandstone. Probably not water bearing. Triassic formation i Representative of depths and thicknesses underlying the vicinity of Paria View observation point in park. EXPLANATION g Alluvium (Water bearing) Wasotch formation Koiparowits formation mm Tropic shale and Dakota sandstone, undifferentiated Winsor formation Fault Pink Cliffs escarpment FIGURE 55. Geologic map of the northern part of Bryce Canyon National Park area, Utah. Modified from Gregory (1951). GROUND WATER, BRYCE CANYON NATIONAL PARK AREA, UTAH 461 STRUCTURE The principal structural features of the Bryce Canyon National Park area are gently northeastward-dipping beds and several major normal faults. The regional dip of the beds ranges from K° to 3° north, northeast, and east. Departures from the regional dip are found only in the immediate vicinity of faults and in gentle folds. A gently north-plunging anticline in the vicinity of Willis and Reward Creeks was described by Hager (1957). The axis of this anticline is west of the Pink Cliffs escarpment in the Heward Creek area, but it crosses the escarpment in the vicinity of Sheep Creek. Faulting is restricted to a few large-scale normal faults; two of these faults the Paunsaugunt and Sevier are regional in extent. The Sevier fault is about 7 miles west of the area covered by this report. These two faults trend northward, and the east block of each fault is upthrown in relation to the west block. The Paunsaugunt fault does not coincide with the Pink Cliffs escarpment and, in fact, is not noticeable as a topographic feature of any kind. Two cross faults that trend generally eastward, connecting the Sevier and Paun saugunt faults, are evident as topographic features faultline scarps that form the borders of Emery Valley. Each of these structural features exercises some control on the occurrence and movement of ground water in the bedrock aquifers of the area. Ground water moves through the rocks in the general direction of the regional dip, which accounts for the many springs along the eastern scarp of the Paunsaugunt Plateau. Along the Paun saugunt fault, springs occur where the eastward movement of ground water is blocked by upfaulted relatively impervious beds, which force the water to rise to the surface. Tension fractures along the axis of the Bryce Canyon anticline (fig. 55) might create secondary permeability and afford an opportunity to obtain successful water supplies from wells penetrating the bedrock. WATER RESOURCES SURFACE WATER In the Bryce Canyon area there are only two perennial surface streams, the East Fork of the Sevi,er River and the Paria River, but short perennial reaches of tributary streams are fed by springs. The diversions of water by the Tropic and East Fork Irrigation Co. from the East Fork of the Sevier River into the Paria River drainage are shown in table 1. The U.S. Geological Survey gaging station (pi. 24) was installed primarily to record the amount of water in the Tropic Ditch that crosses the divide; it does not necessarily record the total amount of water released from the Tropic Reservoir. 644924 O 62 4 462 HYDROLOGY OP THE PUBLIC DOMAIN SPRINGS The springs of the Bryce Canyon National Park area may con veniently be divided into two groups: those on top of the Paunsau- gunt Plateau and those below the rim in the Paria River drainage area. Fluctuations in the flow of springs on top of the plateau are closely related to annual precipitation, whereas fluctuations of the flow of springs below the rim are not. On the Paunsaugunt Plateau are two types of springs bedrock and alluvial. The bedrock springs on the plateau may, in turn, be divided into those that issue from the white beds of the Wasatch formation and those that issue from the basal conglomerate of the Wasatch formation. On the plateau several bedrock springs (for example, Shaker, Trough, and Whiteman) occur on the north and east sides of Whiteman Bench (pi. 24). It is thought that these springs occur where per meable beds in the sandy white beds of the Wasatch formation lie in contact with the denser pink limestone beds of the same formation. Inasmuch as all the springs issue from thin alluvium, it is difficult to determine the bedrock source. These springs are recharged by rain and snow that falls on top and around the margins of Whiteman Bench; the yields are unstable and fluctuate in response to variations in the amount and distribution of precipitation. In May 1957 Shaker, Trough, and Whiteman Springs were not flowing. The upper graph in figure 52 shows that in 1956 the cumulative departure from normal precipitation was at the lowest point during the period of record, which probably accounts for the cessation of flow from the bedrock springs on the plateau. Above the Tropic Reservoir on the plateau are several springs that contribute water to short tributaries of the East Fork (pi. 24). The geologic map (fig. 55) shows that these springs issue from the Wa satch formation just above its contact with the underlying Kaiparowits formation. Gregory (1951, p. 46) states that the basal conglomerate of the Wasatch formation is present near the Tropic Reservoir, and it is thought that the springs issue from this permeable bed. How ever, these springs were not visited by the writer. Springs on the plateau whose source is alluvium are probably present in most of the larger valleys. Seven of these springs are in East Creek valley (pi. 25), and these were the only ones visited by the writer. These springs had an insignificant flow in May 1957, and by June all flow had ceased. The second region of springs is below the rim in the Paria River drainage area, where springs issue from thin patches of alluvium which obscure their bedrock source. The locations of these springs are shown on plate 24, and table 6 gives their altitudes, the geologic formations from which they issue, and their respective stratigraphic positions. The geologic formations and stratigraphic positions from GROUND WATER, BRYCE CANTON NATIONAL PARK AREA, UTAH 463 which these springs issue were determined from Gregory's geologic map (1951). Table 7 gives chemical analyses of water collected from selected springs. Springs and seeps occur at many localities in the foothills below the rim on the east side of the Paunsaugunt Plateau. These are caused by the eastward and northeastward movement of water as it follows the dip of the more permeable beds. Sheep Creek, Swamp Canyon, Yellow Creek Springs, and the springs farther south along the rim are examples of springs that owe their existence to the out crop of permeable beds. Merrill Kanch, Bryce, and Campbell Canyon Springs are faultline springs. Figure 56 illustrates the mode of occurrence of most faultline springs in this area. The upthrown block of Tropic shale forms a relatively impervious eastern barrier, which forces water from the permeable beds in the Wahweap and Straight Cliffs sandstones to rise to the surface instead of continuing its northeastward movement. Nearly all the springs below the rim issue from alluvium, which in some places is a thin layer obscuring the bedrock. The water emerg ing from these springs has a constancy of flow that indicates a bed rock source. If their source were the alluvium in the reentrants, these springs probably would not flow in dry seasons as the alluvium generally is insufficient to store enough water to support the flow, except in wet weather. The recharge area of these springs is restricted to the Paunsaugunt Plateau and immediately adjacent areas. Formations below the Wahweap and Straight Cliffs sandstones probably obtain part of their recharge from areas more distant than the plateau. Table 6 gives the measured discharge of the springs below the rim in the Bryce Canyon area. Because the conditions at each spring are different, each will be considered separately with respect to its utilization for water supply. Springs north of Campbell Canyon were not visited by the writer, and no measurements of flow or chemi cal analyses are available. Campbell Canyon Spring is within the National Park boundary and is 3 miles from the storage tanks of the Utah Parks Co. Water rises in a grassy marsh between two washes that join just below the spring. The water drops about 10 feet from the grassy area to the gravel in the stream wash proper. Within 300 feet of the point where the spring water flows onto the gravel of the wash, all surface water has disappeared. Development work might increase the yield of this spring slightly (table 3). The water is hard but otherwise of good quality (table 7), and, like that of other springs below the rim, the yield is fairly constant. The principal objection to the development of a water supply at this site is the low yield of the spring (table 6). Oi TABLE 6. Records of springs below the Pink Cliffs in the Bryce Canyon National Park area, Utah Approxi Total lift mate direct Name of spring 1 Altitude Geologic source Stratigraphic position Dis Date Method of to Utah distance to Remarks (ft) charge (1957) measurement Parks Co. Utah Parks (gpm) storage Co. storage tanks 2 (ft) tanks (miles) Above base: 7,100 inn ft 1,020 6.9 Location of spring reported utary to Cope Can by local residents; not yon). visited by writer. 6,900 _. do .. ... 100ft...... 1,220 6.5 Do. utary to Cope Can yon). 6,950 ... ..do...... 150ft...... 1,170 6.3 Do. 7,000 .....do ...... 320ft...... 1,120 4.4 Do. 7,250 .....do ...... 570ft...... 870 4.3 Do. Below top, at Paunsaugunt fault: 6,800 200ft 17 May 18 Rectangular 1,320 3.0 Straight Cliffs weir. sandstones. 28 Sept. 24 90° V- 6,900 .....do .. 350ft.. 1,220 2.3 Merrill Ranch...... 6,900 .....do .. . _ - 550ft...... 17 May 18 Rectangular 1,220 3.0 weir. 19 \ weir. 24 90° V-notch weir. Below top: Yellow Creek...... 7,220 ..do...... 100ft .. 81 May 15 Cipolletti 900 2.1 weir. 4.O do...... CO Qant Ol\ 90° V-notch weir. 7,220 .....do...... do 120 May 15 Float ...... 900 2.1 Total water available at Wash. 140 .... .do ... Upper Yellow Creek: 120 Sept. 25 do ... . May 15, 201 gpm; June 21, 183 gpm; Sept. 25, 172 gpm. Second Yellow Creek 6,900 .....do ...... 400ft...... 185 June 21 do 1,220 2.9 Wash. Eight Fork (of Yellow 7,220 do . 100ft 75 June 21 do 900 2.1 o Creek). by local residents; not visited by writer. Dis charge measured 1 mile downstream from re ported source. S onn 600ft 60 Sept. 25 Wash. mate. 7,270 200ft 11 May 20 Eectangular 870 3.4 Straight Cliffs weir. junction of Sheep Creek sandstones. and Swamp Canyon: 2 Sept. 24 90° V-notch weir. 24, 36 gpm. 7,270 i .do ...... do .... 48 May 20 Eectangular 870 do.... . weir. 34 Sept. 24 90° V-notch weir. 7,120 do. 350ft Seep; Sept. 24 Visual esti 1,000 4.0 no mate. flow. 8,200 plotted on map, but not visited by writer. 8,250 ... ..do...... do...... Do. 8 inn ... ..do...... do . Do. Above base: 8,050 250ft tion. Geological Survey topo graphic map. Neither seen nor visited by writer. 8,100 .....do ....- ._ .- 350ft. Do. 7,775 do. Do. 8 qcn .... .do...... Do. 7,500 Do. Straight Cliffs 400ft. sandstones. 7,750 ... ..do...... Do. 1 See pi. 24 for location and table 7 for chemical analysis of water. a Altitude of storage tanks (8,120) interpolated from topographic map. 01 EXPLANATION FIGURE 66. Generalized east-west cross section through Merrill Ranch Spring showing the movement of ground water in relation to the occurrence of all faultline springs in the area. Double-barbed arrows represent direction of water movement; crosshatched area represents zone of satura tion. Tw, Wasatch formation; Kk, Kaiparowits formation; Kws, Wahweap and Straight Cliffs sandstones, undifferentiated; Ktd, Tropic shale and Dakota sandstone, undifferentiated. Cj O2 O2 1-3 ffi Kj g BryceCanyon Spring. Airportwell. CanyonCampbell 02 W 2 a ^SS ^£, 2 p 1 w £ B ^0 p e S P S p g » ^3 £ »02| £ Q formation. Alluviumand 5 ip £?"&' i 5 ^ S*M Wahweapand S Kaiparowits 3. 5 P* 0> ^ 5 2. 2 S P StraightCliffs 1 IS! p 1 Ii S ? ill i * !S 1 i f || Specific conductance £* .to H- (micromhos at g s 25° C) CO r* s s -8P s oco Silica (SiOs) Cn OS ; ! o 1 O H-L 1 1 1 O 1 H-i Iron (Fe) i bO O | i I CO] OS 8 I g ~ rf*. CO CO tO 00 CO-^OtOi pi 1*-CO Calcium (Ca) g cn *J 55 o Oi cncooicc" co coos Magnesium (Mg) 00 ssS g s ^efiK e w