Utah Geological Association Officers 1980-81

Utah Geological Association Officers 1980-81

1980-81 Field Trip Committee

Banquet Speakers

Introduction

This year’s field trip focuses attention upon a number of applied geoscience fields that are in the forefront in Utah and the nation.

Dams are among the most critical of facilities. They are becoming increasingly more important do to the growing need to control and conserve water for the State’s growing megalopolis; yet sites without problems are becoming almost impossible to find. With evolvement of the state-of-the-art in earthquake engineering comes a greater dependence upon the geologist for regional and site specific data. An example is the creation in recent years of the U.S. Bureau of Reclamation’s Seismotectonic Branch. Studies are currently underway in back valleys of the Wasatch Range examining neotectonic structures. Work of this regional a scope is relevant to both existing and proposed impoundments. Our visit to the proposed Jordanelle Dam site will afford us an opportunity to examine other geologic concerns as well, particularly some arising from the mining sector.

Metal values in the ground may have been placed there by man, in an earlier mining era, in the form of mine tailings. We’ll look at environments associated with the Park City Mining District in which two operations to reprocess tailings are proposed for the very near future. In both of these operations the reduction of surface and groundwater contamination is promised as one important benefit.

Low temperature geothermal prospects offer solutions for low cost energy, particularly when in proximity to urban centers. Application of this resource is current at the south end of Salt Lake County and speculation as to potential prevails at Wasatch County’s Midway area. Both are to be visited with updates on recent exploration results.

The Central Wasatch Mountains offer spectacular scenery, diversified geology, fascinating orogenesis, and complex mineralization – and man is still far from taming this environment to suite his purposes. In this field trip lets have a good time looking at his attempts, transiting the field by road, rail and aerial tramway to acquire our perspective.

Illustrated Road Logs with Abstracts

Field Trip Route Map

Miles	Cumulative	Road Log
0.0	0.0	Utah Geological and Mineral Survey, University of Utah, Research Park, 606 Black Hawk Way. (Figure 1) SPEAKER: Howard R. Ritzma3.
		SEVIER-UINTA-WASATCH JUNCTION
		The imprints of three successive episodes of tectonism are evident in the central and northern Wasatch Mountains. The Sevier Orogeny (throughout Cretaceous) is evident in the prominent, multiple traces of thrust faults that strike north-south and dip at low angles to the west (Figure 2). The thrust sheets of the Sevier Orogenic Belt are older to the west and involve successively older rocks westward. The easternmost (leading edge) of the thrust belt, the Hogsback Thrust, causes formations of Jurasssic and Cretaceous age to override formations of late Cretaceous age. To the east of the thrust belt are two foreland folds, the Church Buttes-Moxa Arch and the Douglas Creek Arch-Southern Rock Springs Uplift structural element.
		In late Paleocene through middle Eocene time the Uinta Arch popped up at right angles to the Sevier orogenic trends. The arch is flat-crested with over-steepened flanks that are prominently thrust out-ward to north and south. The low-dipping thrust sheets of the Sevier Orogenic Belt wrap around the west plunge of the Uinta Arch like low-dipping beds. The leading edge of the Sevier belt, the Hogsback Thrust, has apparently been overridden by the “overhang” (hanging wall) of the North Flank Fault of the Uinta Uplift, and the two foreland folds are sharply truncated by the uplift.
		The most recent tectonic episode is the block faulting of the Basin and Range which began in late Oligocene (?) or early Miocene time and continues to the present. The Wasatch Fault which bounds the range on the west is usually considered the eastern boundary of the Basin and Range, but Basin and Range-style structural imprints are evident within the range in the Cache Valley graben, several half grabens such as Bear Lake Valley, and the Wasatch Plateau graben-horst complex that extends north into the Strawberry Reservoir area. Protruding through the whole complex are the late Cenozoic igneous intrusions of the Park City and Little Cottonwood areas, notable for their mineralization.
		– H. Ritzma
0.4	0.4	Turn right onto Sunnyside Ave. (840 S.)
0.2	0.6	Turn left onto Foothill Drive (Utah 186)
2.9	3.5	Take freeway entrance, right ramp, I-80 east.
3.3	6.2	Utah Portland Cement Co. cement rock quarry.
1.3	7.5	1-80 road cut rock slide.
		Bedding, jointing and irregular shear planes and faults can be seen to be controlling structures in the creation of these “wedge” failures, in the Twin Creek Limestone highway cuts. Note high angle of dips and changes in atitude over short distances. The talus slopes comprised of smaller rock fragments act as ramps for the rolling of large boulders to the road shoulders and pavement.
		– B. N. Kaliser
1.9	9.4	Another rock cut failure.
0.3	9.7	Mountain Dell Dam (Figure 3).
		MOUNTAIN DELL DAM
		Owned by Salt Lake City, this structure is an early example of a reinforced concrete dam in the innovative multiple-arch design (Figure 3) developed by John S. Eastwood, who built nineteen of these in various parts of the world. The buttresses are set on centers 35 feet apart and originally enclosed 11 bays. In 1924, ten years after completion, the dam was increased in height from 105 to 145 feet with the addition of 5 bays at the top.
		Geotechnical concerns over the years have included blasting of cuts in the immediate vicinity for the Interstate highway, potential for oil or gas occurrences beneath the structure and seismic safety.
		– B.N. Kaliser
0.1	9.8	Exit right to Recreation Area.
0.2	10.0	Turn left taking underpass to East Canyon.
1.2	11.2	STOP NO. 1: PROPOSED LITTLE DELL DAM SITE.
		(Figure 4)
		SPEAKERS: George Toland4
		Lee McQuivey5
		LITTLE DELL WATER SUPPLY PROJECT STUDIES
		The Little Dell water supply project located on Dell Creek approximately one mile northeast of Mountain Dell Reservoir (see Figure 5) has been under consideration since 1951. This was the date Dr. R. Marsell made the first geological evaluation of the site for the Salt Lake City Corporation. The Corps of Engineers made their first study in 1954. In 1962 Berger and Associates, Inc. were employed by the Metropoliton Water District to perform a preliminary design evaluation. Dames & Moore performed the soils and geological investigation for Berger. The project included:
		1. A preliminary design for a 315 foot high earth and rock filled dam.
		2. Two and one-half miles of concrete pipe conduit.
		3. Two and three-fourths miles of diversion tunnels.
		Studies to date indicate the project is technically feasible, The availability of funds appears to have been the reason for delaying the project. This talk summarizes the preliminary soils, geology and seismic conditions defined by our study.
		— G. Toland
		SITE GEOLOGY
		A rolled earthfill dam with a height of 253 feet, width of 30 feet and crest of 2250 feet is proposed for this site, 1 1/2 miles upstream from the Mountain Dell Dam and 0.3 miles north of Stop No. 1. The gross pool area would take in 318 acres, impounding 30,000 acre feet, almost 1 1/2 miles in length. Intended use is for flood control, municipal water and recreation.
		Foundation is to be in the Kelvin Formation; poorly to moderately indurated red siltstone, claystone, sandstone and conglomerate (Figure 6). Terrace remnants on the west side (max. thickness of 83 feet) will serve as the primary borrow sources for the embankment fill. Approximately 25 feet of recent alluvium exists on site. Situation is on the northwest limb of the Parleys Canyon syncline; bedding striking northeast and dipping 60° - 80° southeast.
		The Little Mountain Fault, with several thousand feet of displacement, comes within 3/4 mile of the right abutment. The fault is not seen to displace Eocene Knight Conglomerate northwest of the damsite.
		Rock at the damsite is moderately to highly permiable but the Kelvin and Frontier under the reservoir are judged by the U.S. Army Corp of Engineers to be sufficiently tight to hold water.
		– B. N. Kaliser
1.2	12.4	Left turn onto I-80 ramp.
1.1	13.5	Next 0.5 mile, colluvial soil failures in road cuts.
1.3	14.8	Lambs Canyon
0.1	14.9	Next 0.7 miles, additional soil failures.
2.9	17.8	Parleys Summit.
0.4	18.2	Soter Summit Subdivision on right.
2.0	20.2	New Jeremy Ranch Subdivision, Recreation Area, etc. on left.
1.0	21.2	Pinebrook Subdivision, on right.
1.4	22.6	Turn right at Park City exit.
0.6	23.2	Turn right on Utah 224.
1.8	25.0	Silver Springs development; impoundment under construction.
0.9	25.9	Park West Ski Resort on right. Note old building stone quarries in vicinity.
2.3	28.2	Park City Condominium Development.
0.6	28.8	Jet. Utah 224/248. Turn left.
0.8	29.6	Prospector Square Subdivision on old tailings, on right. New school construction on left.
1.6	31.2	Turn right onto old highway.
0.6	31.8	Municipal waste disposal operation on left.
0.5	32.3	STOP NO. 2: ABANDONED TAILINGS DEPOSIT
		(Figure 7A)
		SPEAKERS: Wade Barnes6
		B.N. Kaliser
		G.C.Toland
		RICHARDSON AND ATKINSON FLATS TAILINGS AREAS
		Distributed over an area some 4 1/2 miles in length, north of this stop, are some 2 1/2 million tons of Park City Mining District tailings.
		M. Barnes & Associates has a management contract to extract approximately 1 million tons from Atkinson Flat, at the north end of the deposits, east of Silver Creek Junction. During World War II some tailings were reprocessed from Richardson Flat but the Atkinson Flat area is undisturbed to date. Deposition in the latter area occurred from about 1870 to the 1920’s. Thicknesses vary from 3 to 7 feet, averaging 5 feet. Tailings reprocessing is to commence in 1982 over a 100 acre area and over a six to eight month operating season. Values appear to be over 2 oz. silver/ton, 1.5% lead, 2% zinc and a trace of gold. A modification of the cyanide heaps leaching process is employed to yield silver, gold and zinc.
		Environmental ramifications are interesting in that the operation should reduce the leaching of metals (primarily lead and zinc) by surface and ground waters in the vicinity.
		– B. N. Kaliser
		KEETLEY JUNCTION TAILINGS POND EXPANSION
		The original tailings pond at Keetley Junction was constructed more than 80 years ago. The original dam embankments were constructed without control on material type or density. Trash and city dump materials were included in the embankment increases. In 1974 Dames & Moore was commissioned by Park City Ventures Corporation to upgrade the tailings disposal area for reuse in conjunction with their new mill.
		Our geotechnical investigation and design engineering to meet MSHA design regulations produced recommendations and plans and specifications that resulted in the present disposal system. This system includes:
		1. Diversion ditches to collect runoff from the hillsides and direct the flow around the pond.
		2. An earthen embankment immediately downstream of the existing embankment with a cutoff trench extending to the volcanic breccia bedrock and an embankment section of compacted clay and sand-and-gravel.
		3. Confining dikes in excess of one mile in length to control the pond area.
		4. A perimeter tailings discharge line to deposit a beach area adjacent to the pond dikes and embankments.
		The field discussion will describe the geotechnical parameters and technical design aspects of the project.
		– G. Toland
0.9	33.2	STOP NO. 3: RAILROAD CUT IN IGNEOUS ROCK
		(Figure 7B)
		SPEAKERS: Calvin Bromfield7
		Leon Hansen8
		Dennis Williams9
		Object of this stop is to see some of the volcanic breccias that make up much of the Keetley Volcanics. The breccias are well exposed in the railroad cut south of the road. Radiometric ages on volcanic rocks in the Keetley Volcanics range from about 33-36 m.y. and confirm an early Oligocene age for much of the field.
		– C. Bromfield
1.3	34.5	Turn right onto U.S. 40.
1.6	36.1	New Deer Valley Ski Resort at distance on right (Figure 8A).
0.9	37.0	STOP NO. 4: KEETLEY
		SPEAKER: Calvin Bromfield.
		Deer Valley: the object of this stop is to obtain a distant view of some aspects of the stratigraphy, structure and ore deposits along the east flank of the Park City anticline. The east side of the valley is chiefly Park City Formation, with some overlying Woodside Shale. The north-trending Frog Valley thrust fault is concealed by alluvium at the foot of this valley wall. The thrust brings Weber Quartzite on the west over Park City and Wood Side Formation on the east. The dump on the east side of the valley is from the Park City Consolidated mines, which produced silver from two north-east-trending fissure veins on the east side of the Frog Valley Fault.
		– C. Bromfield
		Deer Valley Ski development is a very large, new complex of residential facilities being presently constructed largely on Weber Quartzite terrain. Engineering and environmental geologic aspects of interest include: (1) housing and buried utilitiy installation on resistant bedrock terrain with little or no soil cover; (2) urbanization of a potentially significant recharge zone; (3) slope stability, particulalry of road cuts and fills in and on colluvium on north facing slopes; (4) presence of shallow depth underground openings, to some extent, at least, un-documented; (5) local occurences of vegetated dumps; (6) siting of run-off detention basins on valley bottom alluvium; (7) siting of single family dwellings in potential rock fall and flood zones.
		– B. N. Kaliser
1.7	38.7	Prospected area, Elk Horn District on left.
0.3	39.0	Turn right at Hailstone Jet. onto old paved road.
0.5	39.5	Turn right through metal gate.
0.4	39.9	STOP NO. 5: OVERVIEW, PROPOSED JORDANELLE DAM SITE
		(Figures 8B, 8C, 9A, 9B, and 16A).
		SPEAKERS: Howard Ritzma
		Calvin Bromfield (Figure 10, Tim Sullivan10 11,12)
		Dennis Williams
		Leon Hansen
		Greg Cox11
		George Toland (Figure 17)
		JORDANELLE SEISMOTECTONIC STUDY
		Seismotectonic investigations for the proposed Jordanelle damsite involve the evaluation of the activity of faults in the dam and reservoir areas as well as a determination of maximum credible earthquakes for both local and regional structures.
		Regional geologic investigations are focused on the back valleys of the Wasatch Mountain: Heber, Kamas, Morgan, and Ogden valleys. Previous geological and geophysical work in these back valleys indicates that they are grabens or fault bounded synclines filled with Oligocene and younger deposits. The displacement history of the bounding faults is thought to extend into the Pliocene or Early Pleistocene. The emphasis of geologic studies in the back valleys is on the evaluation of evidence for Late Pleistocene movement on these faults. Methods include aerial reconnaissance, field mapping, and test pit and trench excavation.
		A scarp in alluvial fan deposits on the south side of Heber Valley has been identified in the published literature as a suspected Quaternary fault. A backhoe trench was excavated across this scarp during June 1981. No evidence of deformational structures was found during logging of this excavation. We have concluded that this scarp has an erosional origin related to a Late Pleistocene adjustment of the base level of erosion in Heber Valley.
		The basin north of the proposed Jordanelle damsite, which will be a part of the reservoir, exhibits physiographic similarities to other back valleys. Drill holes in this portion of the reservoir show that the base of Quaternary(?) basin fill is at lower elevation than the bedrock outlet at the damsite, as is the case in Heber and Ogden Valleys. This is considered to result from displacement on north trending graben bounding faults within the basin which do not appear on published geologic maps. The faults have been identified based on drill hole, outcrop, and geophysical data. Trenches excavated across one of the bounding faults show that the upper 20 feet of the basin fill has not been displaced. Work is in progress to assess the age of the deposit.
		The proposed dam and reservoir are located within 15 km of the Wasatch Fault which is considered capable of eathquakes up to magnitude 7.5. A band of moderate magnitude historical earthquake activity, east of the Wasatch Fault, extends from Cache Valley to Heber City, adjacent to the damsite area. The Bureau of Reclamation has contracted the services of the University of Utah to monitor small magnitude earthquake activity in the Jordanelle area.
		– J. T. Sullivan
		JORDANELLE DAMSITE GEOLOGIC INVESTIGATIONS
		Geologic investigations for the proposed Jordanelle Dam, a 298 ft. high earthfill embankment impounding 320,000 acre ft. of water, is a comprehensive study to evaluate rock quality at the embankment foundation, reservoir basin water holding characteristics, and seismic considerations to be used in the design of the dam.
		Core drilling, trenching, detailed geologic mapping, and geophysical surveys conducted at the damsite and in the proposed reservoir area over the last twelve months indicate the presence of an intrusive Tertiary age diorite stock positioned between the Park Premier stock to the west and the Mayflower stock to the east. This previously unmapped stock is probably related in time and origin to other intrusive stocks in the Park City-Jordanelle area. At the damsite, the diorite stock is found in discordant contact with older Triassic age shale and Oligocene age pyroclastic units. A portion of this diorite intrusive stock will form the foundation of the dam embankment and most of the appurtenant structures.
		Several faults, possibly related to the emplacement of the diorite stock, can be traced through the right abutment. However, the more significant geologic structures related to the damsite are previously unmapped, north trending faults bounding a graben block that forms the physiographic characteristics of the proposed reservoir basin valley, a valley similar to other back valleys behind the Wasatch Front. The graben valley has filled with Quaternary(?) age alluvial, colluvial, and lacustrine deposits to depths of 350 feet. The valley fill deposits drilled and tested to date reveal extremely low permiability rates.
		Geologic investigations at the Jordanelle dam and reservoir sites will continue through 1982, with a final geologic report scheduled for completion in 1983.
		– D. R. Williams
		EAST PARK CITY GEOLOGY AND THE PROPOSED JORDANELLE DAM
		The Park City Mining District is located at the junction of one of North America’s major structural crossroads – where the Uintah Mountains intersect the Wasatch Mountains. A series of intrusives extend east-northeasterly for over 14 miles from the Alta-Brighton area through Park City and east of Keetley. A similarly oriented intrusive series may be followed westerly through Bingham and extends for several hundred miles through Nevada – obviously oriented with structures persistant both regionally and in time (Figure 13).
		Several stages of east-northeasterly trending fault-veining cut the intrusives and have been followed for over 6 miles to the west side of Tunnel Creek. Similar structures have been followed in mapping, drilling and excavations for another mile or better east of Tunnel Creek. These structures have been exposed by approximately 1000 miles of workings (Figure 14) spanning a period of over 100 years of nearly continuous mining. This faulting and veining along with complementary but generally subordinate north-northeasterly trending structures cut a complex series of volcanics including tuffaceous pyroclastics, agglomerates and lahars which overlie an east dipping shattered limb of the Park City Anticline. Several varieties of high grade silver, lead, zinc, gold and copper ores, valued in the billions, have been produced from fissure veins within both sedimentary and intrusive rocks and from related bedding hosts. Ore reserves remain in several mines within the district.
		Underground water flows have always been and are still a serious problem for the mines. The proposed Jordanelle Reservoir would cover most of the faults and fissure-veins where they cross easterly through the Tunnel Creek area. These structures cut through extensive water-bearing aquifers (including tuffaceous agglomerates, lahars, the shattered Weber Quartzite, etc.) and provide inter-connecting channel-ways as part of a very complex “greater aquifer” system. One of the larger fault zones (the Cottonwood) is believed to project through the proposed west dam abutment.
		– L. A. Hansen
		Noranda Mining Inc. acquired an operating interest in the United Park City Mines properties in the Park City district through Park City Ventures in August 1979. The United Park properties are a district-wide consolidation of several mines, some dating back to the 1870’s, These include the Ontario, Daly West, Judge, Park Utah, and Silver King (Figure 15). Noranda under a separate agreement has obtained a lease on the adjacent Park City Consolidated Mine.
		The mines in the Park City district have produced over 15 million tons of silver, lead, and zinc ore. The Mayflower Mine in the southeast part of the district has been a primary gold producer. The orebodies occur as (1) replacement manto deposits in favorable limestone strata of late Paleozoic and early Mesozoic age and (2) as vein deposits in generally east-west trending normal faults.
		Noranda’s operating base has been from the Ontario Mine where both vein and manto ores have been mined. Inadequate metal prices and development delays, due to excessive water and poor ground conditions, have led to a deferment of production. Exploration and several aspects of development are continuing at the Ontario and exploration is taking place in the Silver King and Park City Consolidated Mines.
		High Water flows in operating areas have hampered mining in the district since its inception. Throughout the history of the district drainage has been provided by the construction of the Hanauer, Alliance, Anchor, Ontario No. 1, Ontario No. 2, Spiro, and Mayflower tunnels. The present and future working levels are over 800 feet below the level for practical drainage. The water developed in the lower working levels is pumped to the Ontario No. 2 tunnel and flows out of the mine at Keetley. This drain tunnel is at its average annual capacity of 7000 gpm. Any increase in the water flows in the lower levels that may be caused by a reservoir nearby will have a significant adverse effect on the viability of any future operations in the Park City District.
		– G. Cox
–	–	Reverse direction and return to old highway beyond metal gate.
0.4	40.3	Turn right onto old highway.
0.7	41.0	STOP NO. 6: RIGHT ABUTMENT OF PROPOSED JORDANELLE DAM
		(Figure 16B)
		SPEAKERS: Leon Hansen (Figure 18)
		Dennis Williams
–	–	Proceed on old highway to gate.
0.1	41.1	Turn right onto U.S. 40.
0.2	41.3	Upper Provo River bridge.
1.9	43.2	Old (1909) Utah Power & Light Hydro Plant.
0.8	44.0	Turn right on county road to Midway and Homestead Resort.
3.1	47.1	Turn right onto Burgi Lane (1050 N)
0.3	47.4	Interlaken Estates on right hillside.
0.7	48.1	Keep right at intersection on Pine Canyon Road (400 W).
0.1	48.2	Turn left onto Carix Lane (1100 N).
0.3	48.5	Turn Left to Homestead at “T” inter-section.
0.5	49.0	Turn left into Homestead.
0.2	49.2	STOP NO. 7: HOMESTEAD TUFA CONE
		(Figures 19A and 19B)
		SPEAKERS: Calvin Bromfield
		Peter T. Kolesar12
		Richard Fox13
		LOW-TEMPERATURE GEOTHERMAL SYSTEM, MIDWAY, UTAH
		Much of the Midway area is underlain by Quaternary tufa deposits produced through the activities of warm springs. These tufa deposits have been quarried for many years, and have been used locally as building stones.
		Two types of warm springs are found in the area today: (1) those issuing from fractures in the bedrock and flowing over the surface; and (2) those found in large, conical mounds, known locally as “hot pots”. The largest of these hot pots is found at the Homestead Resort. Activity of the springs today is minimal, but the widespread tufa deposits suggest that the springs were much more active in the past.
		During winter months, certain regions of Midway tend to be snow-free, suggesting relatively high rates of heat transfer to the earth’s surface (Figure 20). This observation, together with the presence of both the large tufa deposits and the warm springs, suggest that the Midway area might be a potential geothermal resource.
		Four thermal gradient wells were drilled in the area (Figure 20) to further study this possibility. Lithologic logs of the wells are shown in Figure 21 and the thermal profiles in Figure 22. The profiles in wells 1 and 3 were isothermal, and consequently no gradient could be calculated. Well 2, near the northern edge of the tufa, has gradient of 70° C/km. The heat flow is about 7 HFU (321 mW/m2). At the southern, thickest part of the tufa, well 4 has a gradient of 30° C/km, and a heat flow of about 1 HFU (44 mW/m2), just about what is considered a “normal” heat flow.
		Chemical analyses of warm spring waters provided data for calculating potential reservoir temperatures using the silica geothermometer (Fournier and Rowe, 1966) and the Na-K-Ca geothermometer (Fournier and Truesdell, 1973). Calculated reservoir temperatures ranged from 47 to 78° C. Mixing calculations (Fournier and Truesdell, 1974), applied to two of the warm springs, showed that 70 to 90% of the water could be of cold water origin, and that the reservoir temperature might be as high as 125° C.
		One model developed to account for the geothermal system envisions a series of relatively young, small intrusions north of Midway (Figure 23). Meteoric water seeps into the ground near the intrusions, is heated, and moves toward Midway through highly fractured Weber Quartzite and underlying carbonates. The water moves to the surface through minor faults and fractures along the crest of an anticline beneath Midway. This model is supported by several pieces of evidence: (1) the difference in thermal gradient and heat flow between the northern and southern portions of the region; (2) measured temperatures of 65° C in the workings of the Mayflower mine, north of Midway; and (3) artesian flow of hot water in gradient well 3, drilled mostly in Weber Quartzite.
		Calculated reservoir temperatures (47 to 125° C) are too low for the system to have any electrical generating potential. However, the temperatures are in the range for direct use applications, such as space heating or drying.
		– P. T. Kolesar
–	–	Return to county road.
0.1	49.3	Turn left onto county road.
1.2	50.5	Turn right onto 200 W., Midway.
0.2	50.7	Turn left onto Main Street.
0.3	51.0	Turn right onto Center Street (Utah 113).
2.5	53.5	Upper Provo River Inlet crossing, Deer Creek Reservoir.
1.4	54.9	Turn left at U.S. 189.
–	–	Next 1.8 miles, suspected fault traces on right slope.
1.8	56.7	Turn right onto 3000 S.
1.3	58.0	Turn right onto Big Hollow Rd. (570 W)
0.5	58.5	STOP NO. 8: WASATCH COUNTY PIT, DANIELS: FAULTING
		(Figures 24, 25A, and 25B)
		SPEAKERS: J. Keith Rigby14
		Bruce N. Kaliser
		Tim Sullivan
		Truncated alluvial fan of Big Hollow (Figure 24); approximately 1/2 mile southwest of Daniels, at the south end of the Heber Valley.
		This feature, along with others extending westward to Charleston, have been suspected by B. N. Kaliser (1976) to be evidence of neotectonic movement. Recent faulting is suspected because of physiographic position, well defined geomorphic expression, vegetation anomalies, alignment of bedrock (truncated spurs) and alluvial soil lineaments, condition of bedrock in juxtaposition and change in elevation of bases of scarps in alluvium.
		– B. N. Kaliser
–	–	Return on Big Hollow Road.
1.1	59.6	Turn right onto 3000 S.
0.5	60.1	Turn left onto Daniel Rd. (050 W).
1.4	61.5	Turn right onto U.S. 189, to stop sign.
0.1	61.6	Turn left onto U.S. 40.
1.0	62.6	Turn left onto 100 S., Heber City (old stone house on northwest corner) to Heber Creeper Railroad Depot.
0.5	63.1	TRANSFER POINT: REST STOP AND TRAIN LOADING STATION.
		(Figures 26A, 26B, and 27A)
		Trip participants proceed by train to Bridal Veil Falls.
		DISRUPTION OF RAILROAD TRACKS BY MASS MOVEMENTS
		In route to Deer Creek Dam the train skirts the shoreline of Deer Creek Reservoir. Near mileposts 9 and 10 two small landslides have been a continual concern since the spring of 1978.
		The milepost 9 landslide appears to have its failure plane in Tertiary Tibbie Formation bedrock underlying the 15 to 20 feet of roadbed fill. Lake beach sand and gravel covers much of the slide area so that relationships are not perfectly clear. Toe of the slide is under water and scarps of 3 to 6 feet have appeared at the head of the slide, in the vicinity of the tracks. Dimensions of the fracture are a width of 175 feet and a length of greater than 160 feet.
		The second slide, approximately one mile farther (milepost 10), is in a cut section and appears to involve sandy and silty clay colluvium and fill placed earlier to restore embankment elevation. The slide is situated on Pennsylvanian Oquirrh Formation terrain of considerable slope. A width of 110 feet and a length greater than 100 feet (toe under water) was measured by UGMS in 1979.
		– B.N. Kaliser
		Automobile log estimated at Deer Creek Dam, northwest abutment, after traveling Utah 113 via Midway and Charleston and U.S. 189 around Deer Creek Reservoir.
14.4	77.5	STOP NO. 9: DEER CREEK DAM
		(Figure 27B)
		SPEAKERS: Neil Murdock15
		Keith Rigby. (Figure 29)
		DEER CREEK DAM
		Deer Creek dam is located on the Provo River 17 miles northeast of Provo, Utah. Highway 189 crosses the dam at the lower end of Heber Valley. The dam is an earth embankment 150 feet high (Figure 28) and containing 2,810,000 cubic yards of impervious and semi-pervious fill. It was completed in 1941 to furnish irrigation and culinary water to residents of Utah and Salt Lake valleys.
		Bedrock at the damsite is all part of the Oquirrh Formation of Pennsylvanian age. This is a thick series of limestone, shaly limestone and quartzitic sandstone. This rock is jointed and fractured but has proved to be a satisfactory foundation. Deep overburden of stream gravels overlie the bedrock in the channel. This permiable material required an 86 foot deep cutoff trench to prevent seepage under the dam. No problems have developed with either the bedrock or the overburden. Satisfactory embankment materials were secured near the site, and quartzite riprap shows no signs of deterioration or erosion.
		The spill way is founded on overburden of clay, silt, sand, and angular boulders. This material has proved to be satisfactory and competent to support the structure with no settlement or seepage.
		The outlet tunnel is all in bedrock of limestone, shaly limestone, and sandstone. This rock dips upstream at 30° and is fractured to a moderate degree. It stood unsupported during the excavation of the tunnel, but although it was grouted, it was not completely sealed. Several small seeps issue from the construction joints and from weep holes in the section downstream from the gate chamber. Except for this minor seepage the tunnel has proved entirely satisfactory.
		Bottom of the reservoir rests on stream gravels which overlie the sedimentary series, ranging in age from Paleozoic to Tertiary. The sides of the reservoir rest against the exposed outcrop of these same formations. Two large thrust faults cross the reservoir near the town of Charleston. These faults have had major effect on geologic conditions in the area, but are of no consequence to the water-holding capabilities of the basin.
		– N. Murdock
0.9	78.4	Next 0.7 miles, U.S. 189 road damage and repair zone from mass movements.
1.0	79.4	Next 0.1 mile, severe, repeated road dislocations (repaired).
3.1	82.5	Typical Provo River Terrace deposits (Figure 30A).
1.8	84.3	STOP NO. 10: BRIDAL VEIL FALLS (Figure 30B) (Aerial Tramway)
		SPEAKER: Keith Rigby
		Bridal Veil Falls (Figure 30B) flow over the Lower Pennsylvanian West Canyon Member of the Oquirrh Formation. The stream issues from springs in the cavernous upper part of the limestone, well over 305 meters above the valley floor.
		Periodically, the ornamental retaining wall in the parking lot area is broken by avalanches and ice falls that come from the south side during heavy winter and spring snowstorms. A couple of times, in past years, cars have been buried in the parking lot area during these avalanches. Small lakes were ponded upstream from the avalanche until the Provo River excavated a channel through the avalanche debris.
		Exposures on the north side of the canyon are part of the Oquirrh Formation. The lower Qquirrh beds are of Morrowan age (Figure 29). Atokan and Desmoinesian rocks are exposed higher on the bluffs as the tan-and buff-colored slopes and cliffs. The lower part of the Oquirrh Formation is cyclic, with massive fossiliferous limestone inter-bedded with thin, shaly-bedded, crinoidal-bryozoan limestone. The formations on the north and south sides are abundantly fossiliferous.
		Upper Falls Resort area: just beyond the Upper Falls Resort area is the screening and processing plant for the Salt Lake aqueduct.
		The highway swings out around the toe of the Slide Canyon alluvial fan. Slide Canyon also has a history of repeated avalanches and snowfall debris slides. Slides in 1978 produced a debris fan 15 meters deep and more than 0.8 kilometers wide across the highway. Vegetation is sheared off by the snow and rock debris.
		West Aspen Grove fault: a view is afforded of the West Aspen Grove fault which downdrops the upper part of the Oquirrh Formation, on the east, against the lower part of the Oquirrh Formation on the west. The brownish quartzitic talus fans here are typical of the upper part of the unit. The West Aspen Grove fault is traceable for several miles to the north, along the east side of Mount Timpanogos, through the Aspen Grove development. Talus fans are spectacular here just east of the fault system. The canyon assumes a steep, V-shaped profile in areas where the lower part of the Oquirrh Formation is exposed. To the east the geologic structure rises so that we look beneath Deer Creek thrust slices to the underlying rocks through windows in the fault, at road level. In these window areas, the canyon widens out.
		– J. K. Rigby
–	–	TRANSFER POINT: Reboard bus.
2.0	86.3	Turn left onto Squaw Peak Trail Road.
0.5	86.8	STOP NO. 11: VIEWPOINT – PROVO CANYON LANDSLIDE
		(Figure 31A)
		SPEAKER: Keith Rigby
		This side road continues southward up a subsequent valley carved in Manning Canyon Shale. This is the same shale that is creeping down into the canyon, forming the hummocky topography in the valley on the north side.
		On the north side of the canyon, the aqueduct is about at the plane of a major thrust fault, the Charleston Deer Creek-Nebo Thrust, which has eastward apparent movement of the overlying block.
		A spectacular assymmetrical fold in the basal Oquirrh Formation is exposed in the high canyon wall to the east. This fold is thought to be associated with the forces that caused the thrusting in the area. A minor cave has developed in the crest of the anticline in the massive, bedded limestone.
		– J.K. Rigby
–	–	Return to U.S. 189.
0.4	87.2	Turn left onto U.S. 189.
2.0	89.2	Turn right onto access road (Utah 52) to I-15.
1.1	90.3	Turn right onto 800 E., Orem.
1.0	91.3	Turn right onto un-named access road; trespass plant gate and circle to the right.
0.8	92.1	STOP NO. 12: UTAH VALLEY WATER PURIFICATION PLANT, Central Utah Water Conservancy District.
		(Figure 31B)
		SPEAKERS: Keith Rigby
		Bill Gordon16
		Bruce Kaliser
		Mervyn Smith17
		UTAH VALLEY WATER TREATMENT PLANT, CUWCD
		This modern water filtration plant was completed in 1979, as a part of the Central Utah Project (Figure 32), providing water to all municipal systems in Utah County from Provo north to Alpine.
		With its location in the Wasatch Fault Zone it had to be critically sited with respect to faults and other geologic hazards. It has been designed to conform to earthquake standards for a 0.2 g. horizontal acceleration.
		Interestingly, during the February 20, 1981, Orem, Richter magnitude 3.6 earthquake one of its filter beds liquified. The filter building will be seen in the tour of the plant.
		From the site there is an imposing vista of the Wasatch Range and Utah Valley graben.
		– B. N. Kaliser
–	–	Return to Utah 52.
2.1	94.2	Turn right onto Utah 52 and proceed west to I-15.
2.6	96.8	Turn right onto I-15; proceed north beyond Point of the Mountain.
16.7	113.5	Turn right on Exit 291 to State Prison and Bluffdale.
1.1	114.6	STOP NO. 13: CRYSTAL HOT SPRINGS
		(Figures 33A and 33B)
		SPEAKERS: C. Kim Blair18 (Figure 34)
		L. B. Owen19 (Figure 35)
		R. Klauk20
		CRYSTAL HOT SPRINGS
		With a temperature of 86°C (max) and a content of 1500 mg/l of total dissolved solids this resource looks particularly attractive.
		The spring system is situated between two closely spaced range front faults with a third fault intersection. Host rock is Paleozoic quartzite, buried some 80 feet.
		Discussion at this stop will include results of the shallow ground temperature survey, water chemistry, ground and aerial magnetic surveys, regional gravity and drill hole data for gradient determination.
		Utilization of the resource is being made by Utah Roses, Inc., a private horti-cultural enterprise and by the State.
		– B. N. Kaliser
–	–	Return to I-15.
1.1	115.7	Turn left (north) onto I-15 to Salt Lake City. Proceed to I-80 turnoff (Laramie), east to Foothill Drive (Utah 186).
23.0	138.7	Turn right at ramp; proceed north on Foothill Drive to UGMS Bldg.

Generalized Late Cretaceous - Early Tertiary Structural Trends. Northeast Utah, Southwest Wyoming, Northwest Colorado

Mountain Dell Dam Design, Parley’s Canyon

STOP NO. 1. Little Dell dam site

Aerial Photograph of Proposed Little Dell Dam

East-West Cross Section Along Little Dell Dam Axis

Stop No. 2. Tailings reprocessing site, Richardson Flat.

Stop No. 3. Chevron phosphate loading facility.

Stop No. 4. Deer Valley, above Ontario dumps.

Stop No. 5. Upper Provo drainage and Uinta Arch (distance).

Stop No. 5. Jordanelle Dam site overview.

Stop No. 5. Fault exploration trench inspection.

Stop No. 5. Fault exploration trench and dam site.

General Geology of Central Wasatch Front and Park City

Stratigraphic Column of the Park City District, Utah

Stratigraphic Column Showing Igneous Intrusions

Principal Park City Fissures and Vein Zones in Relation to the Proposed Jordanelle Reservoir

Comparative Depths of Shafts and Tunnels with Proposed Jordanelle Reservoir Projected into East-West Section, Looking Northerly. (Vertical Scale is 5 Times Horizontal.)

Geographic Sketch Map Park City District Utah

Stop No. 5. Mayflower Mine impoundment.

Stop No. 6. Angle drilling at west dam abutment.

Cross Section Mayflower Tailings Pond Dam

Proposed Jordanelle Dam Site Photos

Stop No. 7. Tufa cone at Homestead Resort.

Stop No. 7. Thermal water use at Homestead.

Indications of Abnormal Heat Flow Near Midway, Utah

Lithologic Logs of Temperature-Gradient Wells, Midway, Utah

Temperature Profiles of Gradient Wells 1-4.

Generalized Geology of the Midway Hot Springs Area

Suspect Fault Scarp Across Big Hollow Alluvial Fan

Stop No. 8. Wasatch County Pit at Daniels.

Stop No. 8. Fault exploration trench across truncated fan.

Transfer Point Heber Creeper Station.

Railroad cuts, northwest side of Deer Creek reservoir.

Railroad cuts, northwest side of Deer Creek reservoir.

Stop No. 9. Deer Creek reservoir dam.

Deer Greek Dam, Plan and Sections

Stratigraphic Section - Provo Area, Spanish Fork Canyon

Generalized Diagrammatic Cross Section, Provo Canyon to Heber Valley

Provo river terrace.

Stop No. 10. Bridal Veil Falls Tramway.

Stop No. 11. Major landslide, lower Provo Canyon.

Stop No. 12. Orem Water Treatment Plant, CUWC District.

Central Utah Project - Bonneville Unit Showing Purification Plants

Stop No. 13. Crystal Warm Springs near State Prison.

Stop No. 13. A bargain “basement” deal.

Monitoring Locations - Crystal Hot Springs Area

Logs Of USP/Test Hole No. 1 - Crystal Hot Springs