Volume I GEOLOGIC SUMMARY REPORT OF THE 1990 EXPLORATION PROGRAM SUNNYSIDE TAR SANDS PROJECT CARBON COUNTY UTAH

Transcription

1 Volume I GEOLOGIC SUMMARY REPORT OF THE 1990 EXPLORATION PROGRAM SUNNYSIDE TAR SANDS PROJECT CARBON COUNTY UTAH for ROBERT E. LUMPKIN DIRECTOR, SOLID RESOURCES AMOCO CORPORATION NAPERVILLE, ILLINOIS by WM. S. CALKIN, D.Sc. CONSULTING GEOLOGIST GOLDEN, COLORADO February 28,

2 Volume I Table of Contents Page SUMMARY AND CONCLUSIONS RECOMMENDATIONS INTRODUCTION LOCATION AND INFRASTRUCTURE GEOLOGY Price Area Sunnyside Area Bruin Point Area Water Coal Mines in Sunnyside Area Mancos Shale Blackhawk Formation Castlegate Sandstone Price River Formation North Horn Formation Flagstaff Limestone Colton Formation Green River Formation Parachute Creek Member Garden Gulch Member Douglas Creek Member TAR SANDS 27 General 27 Controls 29 Correlation 31 Tar Zone Isopachs 34 Upper Group 35 Middle Group 37 Lower Group 38 Bottom Group 40 Interpretation 42 Synopsis 44 MEASURED SECTIONS

3 Table of Contents (continued) Page STRUCTURE 47 Book Cliffs 48 Roan Cliffs 48 ENGINEERING GEOLOGY 50 Major Factors 50 Minor Factors 52 Conveyor Routes 54 REFERENCES 57 APPENDIX Photos 1-13 Figures 1-26 Tables ii

4 Volume I Photo 1 Photo 2 Photo 3 Photo 4 Photo 5 Photo 6 Photo 7 Photo 8 Photo 9 Photo 10 Photo 11 Photo 12 Photo 13 List of Photos Aerial Mosaic of Sunnyside Tar Sands Panorama of Sunnyside Tar Sands, Part I Panorama of Sunnyside Tar Sands, Part II Panorama of Sunnyside Tar Sands, Part III Panorama of Sunnyside Tar Sands, Part IV Clark Valley and Canyons in the Book Cliffs Near Sunnyside Stratigraphy in Lower Portion of Book Cliffs Stratigraphy in Upper Portion of Book Cliffs Roan Cliffs, Central Area of Project and South Conveyor Route Stratigraphy in Lower Bear Canyon Looking Down B Canyon into Clark Valley Looking Up Left Fork of A Canyon From Clark Valley Looking Up Proposed North Conveyor Route From West Ridge iii

5 Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure 26 Volume I List of Figures 1 Location Map From Price to Sunnyside Tar Sands 1A Geology Map From Price to Sunnyside Tar Sands 2 Location Map of Sunnyside Area, Carbon County, Utah Tower Identification Near Bruin Point Underground Coal Mines in the Sunnyside Area, Utah Generalized Lithologic Section, Sunnyside Mines Generalized Lithologic Section, B-Canyon Coal Property Columnar Stratigraphic Section of Blackhawk Formation, Sunnyside, Utah Southwest to Northeast Cross Section Through Sunnyside Coal Mining District Typical Section B Canyon Coal Property Generalized Stratigraphy Chart for the Book Cliffs, Helper to Sunnyside, Utah Northeastern Utah Correlation Chart Utah Paleogeography in Lake Cretaceous Utah Paleogeography in Lake Paleocene Utah Paleogeography in Early and Middle Eocene Generalized Cross Section of Late Cretaceous Rocks in East-Central, Utah Diagramatic Cretaceous Section in Central Utah Diagramatic Section of Late Cretaceous and Tertiary Rocks Near Castle Valley, Utah Well Locations Near Clark Valley Important Stratigraphic Markers in the Green River Formation, Sunnyside Tar Sands, Carbon County, Utah Stratigraphic Markers in the Parachute Creek Member, Sunnyside Tar Sands, Carbon County, Utah Schematic Diagram Illustrating Patterns of Deposition and Erosion Within a Stratigraphic Sequence, Sunnyside Tar Sands Depositional Stacking Patterns of Progradational, Retrogradational and Aggradational Parasequences Comparison of Sandstone Distribution Based on Lithostratigraphic Versus Chronostratigraphic Correlation Location Map of MS-62, 63 and 64 Structural Trends of Surface Joint Sets and Subsurface Faults, Sunnyside Area, Carbon County, Utah Earthquakes in State of Utah and Price Area IV 01

6 Volume I List of Tables Table 1 Data From Deep Drill Holes in Clark Valley Table 2 Data From Shallow Drill Holes in Clark Valley Table 3 Data From Shallow Drill Holes in Book Cliffs Table 4 Bitumen Data by Tar Zone, Sunnyside Tar Sands Table 5 Tar Zone Data from MS-62, 63, v

7 SUMMARY AND CONCLUSIONS 1. An overview of important geographical and geological features of the Sunnyside Tar Sands is seen in Photos 1 through 5. The geology of the area and the location of the proposed north and south conveyor routes are included on the new Regional Geology Map and Cross Section. 2. The tar sands are associated with lithologic cycles that consist of an unconformity overlain by bituminous sandstones, overlain by shales, overlain by limestones that are overlain by another unconformity. These cycles of unconformitysandstone-shale-limestone-unconformity exist throughout the Sunnyside Tar Sands area and represent fourth order stratigraphic sequences that formed during suggested 100,0 00 year climatic cycles (see Figure 21). 3. Correlation of the numbered tar zones has been based on these unconformities and the overlying bituminous sandstones. In essence chronostratigraphic correlation has been extensively utilized. Significant differences in sandstone geometry exist between chronostratigraphic correlation versus lithostratigraphic correlation. Chronostratigraphic correlation is more accurate as shown in Figure Individual isopach maps of the fifteen numbered tar zones have been completed and are in Volume II. The fifteen numbered tar zones have been separated into four groups: upper group, middle group, lower group, and bottom group as shown in Table 4. The isopach maps within each group are quite similar. The upper group contains 12.8% of the bitumen resource and exists between the Blue Marker and the base of the Carbonate Interval. The middle, lower and bottom groups exist between the Carbonate Interval and the base of saturation. They contain 87.2% of the bitumen resource. The lower group contains 48.5% of the bitumen resource as well as the first, second and fourth most important tar zones which respectively are Zones 36, 37 and 53. Zone 31 is the third most important tar zone and exists in the middle group. 5. The individual isopach maps illustrate that the numbered tar zones are continuous sheet sands of irregular thickness. The tar zones are characterized by areas of thick sand intervals and adjacent areas of thin sand intervals. The highs, or thick sand intervals, are commonly feet thick and the lows are commonly feet thick. The highs are commonly feet apart and are particularly abundant near the Roan Cliff face below the North Overlook, Bruin Point and the Central Overlook. The frequency of the highs diminishes toward Range Creek and the South Area

8 6. From one isopach map to the next the highs and lows commonly have an inverse relationship and indicate lateral shifting of depositional sites from one stratigraphic sequence to the next. Portions of isopach maps in the lower group have symmetrical bimodal patterns that suggest deposition near the terminus of distributary channels. The three main ridges that extend in a southwest direction from the Roan Cliffs represent important loci for distributary channels. These loci include the ridge line from Bruin Point to the Shell Curve, the ridge line that extends out from the Central Overlook near the top of Measured Section 3, and the ridge line that extends out from the pilot mine site in the North Area. 7. The four groups of the fifteen numbered tar zones are characterized by different types of deposits. The bottom group contains stream channel and distributary channel deposits. The lower and middle groups are characterized by distributary channel and distributary mouth bar deposits. The upper group is characterized by beach deposits and minor distributary mouth bar deposits. 8. The north conveyor route represents the best route for the conveyor system with one modification. The Left Fork of A Canyon contains an alternative site for the tunnel that needs to go through the Book Cliffs as shown in Figure 2. Two important factors affect the engineering geology in both B Canyon and the Left Fork of A.Canyon. First, box canyons are associated with two different sandstones. The box canyons have a potential for flash floods and both sandstones have a potential for hazardous rockfalls. Second, the dominant northeast structural trend of joints and faults (see Figure 25) may cause tunnelling problems if the tunnel is oriented nearly parallel to this dominant direction of structural weakness. B Canyon is tight and would intensify the effects of rockfalls and flash floods; in addition the tunnel orientation almost parallels the dominant direction of structural weakness (see Photos 8 and 11). The Left Fork of B Canyon is open and would limit the effects of rockfalls and flash floods (see Photo 12); in addition, the tunnel orientation would be oblique to the dominant direction of structural weakness. 9. The south conveyor route is not recommended as it contains some formidable box canyons and cliffs that would present significant engineering problems (see Photos 6, 9 and 10). In addition, the south route passes over workings of underground coal mines (see Regional Geology Map). 10. In the proposed tailing site area of Clark Valley the Blue Gate Member of the Mancos Shale exists beneath feet of alluvium. Data from well logs indicates that the Blue Gate Member of impervious marine shale averages 1357 feet thick and

9 overlies the Ferron Sandstone Member that averages 171 feet thick (see Table 1). This information can be utilized in the design of the tailings site

10 RECOMMENDATIONS 1. The discrepancies that exist between the field data and computer data base on the tops and bottoms of numbered tar zones should be corrected. These differences mainly exist in the South Area and are largely the result of data determined from relogging of the Mono Power RCT drill holes during the summer of If the continuous core from Great National Corporation or Chevron Resources drill holes becomes available, it should be relogged. Since the siltstones and limestones were often improperly logged, the tops and bottoms of numbered tar zones are usually incorrect. The relogging of core from Great National and Chevron Resources would better define the true thickness of numbered tar zones near the Roan Cliffs and put all drill hole data within the Sunnyside 'Tar Sands area on the same basis. The thirteen drill holes of Great National total 11,816 feet. This continuous core is stored in Price at Eastern Utah Storage, which is owned and operated by Scott Wheeler. If the storage fees are unpaid for over one year, the core may become available for the minimal cost of back rent. If so, the core should be purchased by Amoco rather than discarded by Scott Wheeler. The thirteen drill holes of Chevron Resources total 11,390 feet. Much of this continuous core is stored in an old non-operating gilsonite plant which belongs to Chevron and is located at the Cowboy Vein near Bonanza, Utah. 3. If the hydrocarbon lease agreement or extension requires due diligence, additional field work can be completed at a minimal cost with infill measured sections along the Roan Cliff face. This closer spacing of measured sections would create better control on the continuity of thickness and bitumen grade in numbered tar zones. 4. Additional engineering geology work needs to be completed in the area of B Canyon and Left Fork of A Canyon to determine the best location for the tunnel through the Book Cliffs. 5. Before actual mining begins the numbered tar zones should be examined in more detail to determine why the tar zones are not more uniform in thickness as suggested in Photo 2. This approach along with more infill drilling and infill measured sections will further define the distribution, thickness and bitumen grades of the numbered tar zones. This approach will definitely benefit mine planning S

11 INTRODUCTION This 1990 report is a supplement to the extensive 1989 report. This 1990 report concentrates on results of the following four categories: (1) regional geology and engineering geology needed to investigate the feasibility of conveyor routes that will bring the tar sand ore down from the Roan Cliffs through the Book Cliffs to Clark Valley (see Regional Geology Map and Cross Section in Volume II as well as Figures 2 and 25 in Volume I); (2) completion of three short measured sections in the "hot spot" of the. South Area to further delineate the extent and grade of Zones 31, 32, 33 and 35 (see strip logs in Volume II); (3) composite photos prepared to identify the outcrops of numbered tar zones along the Roan Cliffs (see Photos 2, 3,4 and 5 in Volume I); (4) presentation and interpretation of an isopach, or thickness, map for each of the fifteen numbered tar zones (see Isopach Maps in Volume II). The first two categories were accomplished during a one month summer field program from mid-june to mid-july The last two categories were completed during the ensuing months of office work. The detail in the composite photos is the result of eleven years of exploration work

12 LOCATION AND INFRASTRUCTURE Price Area Price is the commercial center and county seat of Carbon County and has a population between 8,000-10,000 people. Price has an average annual rainfall of almost ten inches. Price is surrounded on the north and east by the Book Cliffs and on the west by the Wasatch Plateau. This mountainous rim outlines the so-called Castle Valley. This rim of cliffs contains extensive underground coal deposits that have been mined since the early 1890's. The economy of the Castle Valley has been chiefly related to coal mining for nearly a century. Figure 1 shows various aspects of the infrastructure that exist in the Price area. These include the -water treatment plant at Wellington that services the Helper-Price-Wellington region, two coal wash plants, two powerlines, a twenty inch pipeline, and the county airport with a 6000 foot runway. The twenty inch pipeline is owned and operated by Mountain Fuel Supply Co. and Utah Natural Gas Co. The new business highway south of Price and Wellington opened in early July and its alignment is shown on Figure 1. The main line of the Denver & Rio Grande Western goes through Price with a major depot at Helper and a spur line that serves the coal mine at Sunnyside. The Sunnyside Tar Sands exist in the high Roan Cliffs located about twenty-five miles east of Price (see Figure 1). Access to the tar sands project from Price is via Wellington to Sunnyside Junction, hence to Sunnyside and then to Bruin Point. The distance from Price via Wellington to Sunnyside Junction on US Route 6 is about fifteen miles. The distance from Sunnyside Junction to Sunnyside on Utah Route 123 is about ten miles. Utah Route 123 is a newly upgraded road that was improved during the summers of 1986 and 1987 for heavy trucks. The distance from Sunnyside to Bruin Point is about eight miles. A four wheel drive vehicle is needed for the last two miles from the Asphalt Mine to Bruin Point as grades of 15-20% are common. The trip from Price to Bruin Point takes about 1.5 hours. The Sunnyside Tar Sands are located along the crest of the Roan Cliffs near Bruin Point, elevation 10,131 feet. Some portions of the tar sand area including Bruin Point can be seen from numerous places around Price. Near Sunnyside and East Carbon the tar sand area is hidden behind the Book Cliffs. The right hand portion of Figure 1 contains an outline of the tar sand area. Figures 1 and 2 along with Photo 1 can be used to comprehend the local geography. oi^

13 Sunnyside Area The City of Sunnyside is located near the base of the Book Cliffs and the entrance to Whitmore Canyon. The City of Sunnyside was incorporated in The area has a semi-arid climate with an annual rainfall of inches (30-35 cm) and a temperature range of -10 to 90 F (-23 to 27 C) as stated by Lynn Huntsman (1978). Extensive climatic records for Sunnyside exist in City Hall. The Sunnyside Municipal Watershed was established by the United States Congress in 1920 or 1921 for the City of Sunnyside and is located near the upper portion of Range Creek within sections 11, 12, 13 and 14 of T14S, R14E (see Figure 1). Drinking water was obtained via a now abandoned pump station in Range Creek located in SE/4, section 36, T14S, R14E. The water was piped over Patmos Ridge and down Number Two Canyon. A proposed water tunnel between Range Creek and Number Two Canyon was never completed due to the Great Depression (personal communication, 1981, Lynn Huntsman). This watershed is no longer being used by the City of Sunnyside as the City now obtains its culinary water from Grassy Trail Reservoir located about five miles upstream from Sunnyside (see Figures 1 and 2). The Sunnyside water storage tank is painted white and located near the rodeo grounds about two miles up Whitmore Canyon from Sunnyside (see Figure 2). Some of the infrastructure in the area is illustrated in Figure 2. Sunnyside and East Carbon have a combined population of about 2,000-3,000 people. The boundaries of the City of Sunnyside and East Carbon City are outlined. East Carbon City was incorporated in and consists of the communities of Dragerton and Columbia. The East Carbon water storage tank is painted light brown and located near the new baseball field in Sunnyside. A power substation exists near Columbia. The coke ovens located between Columbia and Dragerton operated from the early 1900's to the mid-1950's, supposedly closing in The Carbon County Railroad shipped coal from the Columbia Mine and from the Geneva Mine, located in Horse Canyon some fifteen miles to the south (see Figures 4 and 25). The siding of the Carbon County Railroad at Columbia Junction was disconnected from the Denver & Rio Grande Western in the spring of One thousand tons of bituminous sandstones were shipped by rail to Chicago in The rock was trucked from the Asphalt Mine to the loading facilities and sidings at the wash plant near Wellington (see Figure 1)

14 Bruin Point Area Seven important communication complexes exist near Bruin Point. The Bruin Point area is located along the crest of the Roan Cliffs and represents a commanding position for these significant complexes. The detailed location of these seven communication complexes is shown in Figure 3 and from north to south include the following towers: microwave; BLM and FAA; US West; UP&L; Motorola; and Mountain Fuel. The following paragraph contains brief descriptions of some pertinent information of these communication complexes. Starting on the north and going south, the large microwave towers serve as an important radio-telephone-tv relay station and are managed by Western Telecommunications of Denver. The second floor of the two-story green building contains the communications system for the Bureau of Land Management, Moab district. The first floor of the two-story green building contains surface to air communications for the Federal Aviation Administration, western district. This FAA complex is a very important system for air traffic control (personal communication, 1990, Clayton Parker, Seattle, Washington). It is extensively utilized between Denver and the entire Pacific coast and helps to explain the frequency of high flying aircraft seen during summer field work. The US West Telephone towers are used for communication within the entire Uinta Basin (personal communication, 1990, Lou Arnold, retired AT&T operations, Helper, Utah). A small fenced area contains communication systems of UP&L. Utah Power and Light is a major utility company in the State of Utah and has a number of power generation plants in the Castle Valley. The facility at Bruin Point is used over a four county area. A small white trailer contains systems of Motorola. It is managed by Royce Communications of Moab, Utah. The large tower complex in the south belongs to Mountain Fuel of Price and Salt Lake City. This microwave system is used as a telemeter to monitor fuel lines (personal communication, 1990, Lou Arnold). The following paragraph contains brief descriptions of the land ownership on which these seven communication systems are located. Starting in the north and going south, the microwave towers are on a surface lease from the BLM that started in The microwave towers exist on NOL property of the United States Government. NOL stands for "not open for lease" and applies to subsurface rights. USGS Bruin is also located on this NOL property and is an important survey point in the State of Utah coordinate system. The two-story green building that contains systems of BLM and FAA is on private fee land owned by h St. Mary's Parish (a Louisiana company) and h Crosby Corporation (a Utah Corporation). The FAA and BLM jointly leased the property from St. Mary's Parish, which is now controlled by Coca Mines Inc. of Denver. The US West, UP&L, and Motorola complexes are located

15 in the NW/4, section 3, T14S, R14E that is part of Amoco's fee land purchased from Kaiser Steel Corporation in In 1980 when Ed Chelchowski of the Chicago office, Standard Oil Company of Indiana, was on the property I recall him saying "Yes, Amoco gets a check from AT&T every month". I assume Amoco also gets checks from UP&L and Motorola. The Mountain Fuel complex exists on Gibbs Heirs property of which Amoco has an undivided 1/6 surface and mineral perpetual interest from Gibbs Heirs, a state of Utah entity in Salt Lake City. The feasibility of removing or replacing these seven communication complexes would, in part, depend on the terms of the leases with the various land owners. US West has a 99 year lease on this property that began in 1965 (personal communication, 1990, Lou Arnold). The identification and general utilization of these towers was verified in December 1990 by a number of telephone calls to the appropriate operators, owners and wellinformed people. Allen Orton of the State of Utah Highway Patrol, Price office, is a radio engineer for the Superintendent of Communications, State of Utah. His comments were particularly helpful. Lou Arnold knows the telephone complex at Bruin Point very well and is an active, but retired, AT&T operations expert who lives in Helper, Utah. His comments were also particularly helpful. Water Water is scarce in the Price-Sunnyside area. Price has an average annual precipitation of 9.72 inches (data from Carbon County Chamber of Commerce, 1987). The Wellington water treatment plant may be the most viable source for large quantities of water. The Wellington water treatment plant serves the Helper- Price-Wellington area and was built in 1984 for a capacity of 8,200,000 gpd. It is currently processing 2,500,000 gpd. The effluent from the treatment plant meets all EPA standards. The effluent water could be purchased for a negotiable price from the plant before it is emptied into the Price River. After the effluent is emptied into the Price River it cannot be bought as it reverts to conditions under standard water rights. Above data summarized from personal communication in June and July 1990 with Harold Marston of the Price Planning and Zoning Commission and Phil Palmer, manager, Wellington water treatment plant. The City of Sunnyside has a semi-arid climate with an average annual rainfall of inches. Detailed precipitation records exist in the files at Sunnyside City Hall. The

16 Sunnyside coal mine makes about 1,500,000 to 2,000,000 gpd of nonculinary water that is used for community needs such as watering the grass in the municipal park, golf course, as well as football and baseball fields. The Columbia coal mine is flooded. Grassy Trail Reservoir was built in 1952 with a capacity of 940 acre-feet. Since that time there has been nearly a twenty percent loss by siltation. Grassy Trail Reservoir is the source of culinary water for both Sunnyside and East Carbon. Above data summarized from personal communication in June and July 1990 with Barbara Jaramillo, secretary, Sunnyside City Hall and Tom Anderson, councilman, City of Sunnyside. Water rights for twelve second-feet from the Green River are available for purchase. The owners are John C. Osmund, Englewood, Colorado and Mrs. Juanita J. Meyer (widow of Daniel H. Meyer, then President, Bituminous Sand Corporation of America). The application was submitted on or about April 16, 1964 as Nos and Assignment occurred on October 22, John Osmund gave me a xerox copy of the application when I met with him on October 24, 1990 to inquire about the details of these water rights. Surface water in the project area is available from four springs, all of which represent perched springs above oil shale intervals in the Parachute Creek Member. Two springs exist in upper Range Creek not far from Bruin Point. The North Spring located in the NE/4, section 3, T14S, R14S produces about 5000 gpd from above the R-2 oil shale. The South Spring located in NE/4, SW/4, section 2, T14S, R14E produces about 100,000 gpd from above the R-2 oil shale. The North Spring and South Spring are both located on Amoco fee land. Two other springs are located in distal portions of the tar sand area and exist within the West Tavaputs Plateau. Stone Cabin Spring is located about 1.2 miles northeast of Mount Bartles in NE/4, NW/4, section 8, T13S, R14E and produces about 15,000 gpd from above the R-5 oil shale. This spring is controlled by Dick Calder of Nine Mile Canyon and Bountiful, Utah. Cold Spring is located some 3.7 miles northeast of Bruin Point in NW/4, SE/4, section 24, T13S and R14E and produces some gpd from, above the R-2 oil shale. This spring is controlled by Jim Wilcox, manager of the Nutter Ranch in Nine Mile Canyon. These four springs have supplied the necessary water for drilling operations in 1980, 1981, 1982, 1984 and Coal Mines in Sunnyside Area In the Sunnyside area the underground coal production has come from a narrow band almost fifteen miles long by one to two miles wide as seen in Figure 4. The coal from this long

17 narrow band contains some of the highest quality coking coal in the western United States (Averitt, 1966). Coal mining operations in the area have been continuous since they began in the late 1890's (Huntsman, 1978). Within the entire Castle Valley all mineable coal exists with the Blackhawk Formation that contains as many as nine coal beds. The principal seven coal beds from bottom to top are: Spring Canyon, Castlegate, Kenilworth, Gilson, Rock Canyon, lower Sunnyside and upper Sunnyside (Doelling, 1972). Commonly, each mine has a minimum of only two mineable coal beds, and the mineable coal beds are often different from mine to mine. In the Sunnyside area coal production is from the Sunnyside coal zone that contains the upper Sunnyside (or Upper Seam) and the lower Sunnyside (or Lower Seam). Both of these are important coal mining seams that are often separated by a 1-40 ft thick split (see Figures 5 and 6). The floor of the lower Sunnyside coal seam is a foot thick sandstone, locally termed the Sunnyside Sandstone (see Figure 7). The coal mines at Sunnyside consist of the No. 1, No. 2 and No. 3 Mines (see Figure 2) and the Sunnyside coal zone extends about seven miles along the outcrop and one to two miles downdip toward the northeast. The No. 1 Mine heads northwest for about four miles and goes from beneath the surfaced road in Whitmore Canyon to B Canyon. The No. 1 Mine almost parallels West Ridge of the Book Cliffs. The No. 2 Mine heads southeast for about three miles to where the Columbia Mine begins (see Figure 2). The No. 3 Mine is an incline and heads downdip toward the east. The majority of the early coal mining, pre-1960, at Sunnyside was completed in the upper Sunnyside as this Upper Seam has a stronger roof and the coal has a lower sulfur content. Early on, coal was extracted by hand in erratic patterns from portions of the No. 1, No. 2 and No. 3 Mines. Later on, continuous mining machines were used with room and pillar mining methods. Gradually longwall mining methods took over. Above paragraph"" summarized from Huntsman (1978). In the No. 2 Mine the Sunnyside coal zone has two seams that come together near the Columbia Mine. Near the portal of the No. 2 Mine, located in Number Two Canyon, the Upper and Lower Seams are separated by 7-8 feet. This separation gradually diminishes to 4-5 feet halfway to the Columbia Mine. The split between the Upper and Lower Seams continues to gradually diminish until the two seams merge near the Columbia Mine. Within most of the No. 2 Mine the Upper Seam was mined first, then the waste rock in the split and finally the Lower Seam. This lead to the high amount of reject and high cost of mining. The No. 2 Mine was closed around Above data from personal communication, 1990, Lynn Huntsman

18 In the No. 3 Mine the split between the Upper and Lower Seams is up to forty feet thick. The Upper Seam is feet thick, while the Lower Seam is 5-14 feet thick. Pre-1950 all mining in the No. 3 Mine was confined to the Upper Seam. In the early 1950's Kaiser Coal Company began to mine the Lower Seam beneath the erratic patterns of the old workings in the Upper Seam. Numerous bounces, also termed bumps or rock bursts, began to form in the Lower Seam. This caused hazardous conditions and high-cost mining in the Lower Seam. And it resulted in the advent of the first longwall system at Sunnyside that finally worked in virgin portions of the Upper Seam. Since 1964 longwall mining in the No. 3 Mine has been confined to the Upper Seam. Above paragraph summarized from Huntsman (1978). In the No. 1 Mine the Upper and Lower Seams commonly come together. However, near B Canyon, in the northwest portion of the No. 1 Mine, the Sunnyside coal zone again separates into two parts. Both the Upper and Lower Seams are each 6-7 feet thick with a split that is 2-20 feet thick. In the vicinity of Water Canyon and Bear Canyon the coal mining is at a depth approaching feet. The coal mining in the No. 1 Mine is usually located 150 feet below the base of the Castlegate Sandstone. Since 1961 most of the coal production in the No. 1 Mine has been completed by longwall mining methods. Poor roof conditions prevail on top of the Upper Seam and extraordinary roof support measures are required. Above paragraph summarized from Huntsman (1978). The Sunnyside coal contains 40 percent volatiles, 53 percent carbon, less than 1 percent sulfur and 6 percent ash. The coal is classified as a high volatile B bituminous (Doelling, 1972). The mine plan of the No. 1 Mine is oriented northwestsoutheast and can be visualized by looking northwest at Figure 2. In an attempt to relate the plan of the underground coal mine to the surface topography, the No. 1 Mine has been divided in western, central and eastern segments. This overall scheme has been synthesized from mine maps supplied in 1990 by Byron Allred, mine surveyor of SRS, Inc. Central segment: The central segment nearly parallels West Ridge and contains the main entryway or motor road. This central segment extends to the right of the motor road as far as the surface trace of the creek in Whitmore Canyon. The coal in most of this central segment was extracted by room and pillar mining methods from The coal in the northernmost portion of this central segment beyond the manshaft was extracted by longwall mining methods from Western segment: The western segment extends from the left of the motor road to the surface outcrops on the west side of the Book Cliffs. The coal in this western segment was extracted by longwall mining methods from About

19 500 feet from the surface outcrops, the coal is oxidized; only 2% oxidized coal kills the flotation process that is used in the wash plant to upgrade the coal product (personal communication, 1990, Lynn Huntsman). Eastern segment: The eastern segment extends from the surface trace of the creek in Whitmore Canyon to the right toward the Roan Cliffs. The coal in the eastern segment has been extracted by longwall mining methods since The northern limits of current mining are about 5000 feet to the northwest of the manshaft that is located near the mouth of Water Canyon. A sense of the central, western and eastern segments of the No. 1 Mine adds a third dimension to the Book Cliffs and Whitmore Canyon. The two small generalized cross sections of Figures 8 and 9, as well as the large cross section that goes with the Regional Geology Map, show the location of the Sunnyside coal beds. The Columbia and Geneva Mines are southern extensions of the Sunnyside coal zone (see Figure 4). The Columbia Mine extends for almost six miles between the southern limits of the Sunnyside No. 2 Mine and the northern limits of the Geneva Mine. The northern boundary of the Columbia Mine exists at the east-west line between sections 16 and 21, T15S, R14E. The southern boundary of the Columbia Mine is a major fault that trends N80 E and has a displacement of feet. This major fault is located about 4000 feet north of the Carbon County- Emery County line (see Figure 25). The Columbia Mine operated from when it was finally closed because of numerous N20-30 W trending minor faults with displacements of 2-30 feet that caused dangerous mining conditions. The Geneva Mine exists south of the major fault. The Geneva Mine is now flooded but some geological data is available in Osterwald, Dunrud and Maberry (1969) as well as in Doelling (1972). In the Geneva, Columbia and southernmost portion of the Sunnyside No. 2 Mine, the upper and lower Sunnyside coal seams commonly merge or are separated by less than a foot. The merged coal seam is commonly feet thick (see Figure 4). Important structural data regarding joints and faults has been obtained as the result of this synopsis of the coal mines in the Sunnyside area and is discussed under Structure. In addition, knowledge of these underground coal mines helps to understand rock qualities for tunneling and surface areas of potential subsidence along conveyor routes

20 GEOLOGY The area from Sunnyside to Bruin Point contains both the Book Cliffs and the Roan Cliffs. Both cliffs are part of a regional monocline that dips 5-10 northeast. Each mass of cliffs contains different rock units. The Book Cliffs contain rocks of Upper Cretaceous and lower Tertiary age that were deposited some million years ago under marine conditions, at first, which slowly changed to coastal plain, then alluvial plain, and finally lake environments (see Figures 12 and 13). The Roan Cliffs contain rocks of lower and middle Tertiary age that were deposited some million years ago under alluvial conditions of continental environments which slowly changed to environments associated with a large lake (see Figure 14). Because of the gentle dips in the regional monocline there is some repetition of formations in the upper portion of the Book Cliffs and the lower portion of the Roan Cliffs. Within these two sets of cliffs there are eight formations that are over 7000 feet thick and were deposited during some 50 million years. These eight formations from bottom to top with the geological symbol and average thickness in parenthesis are: Mancos Shale (Km, over 2000 ft); Blackhawk Fm. (Kbh, 600 ft); Castlegate Sandstone (Kc, 150 ft); Price River Fm. (Kpr, 375 ft); North Horn Fm. (TKnh, 150 ft); Flagstaff Limestone (Tf, 75 ft); Colton Fm. (Tc, 1100 ft); and Green River Fm. (Tgr, over 2800 ft). The paleogeographic setting during the early part of this fifty million year history was mountains in central Utah with the ocean in eastern Utah and Colorado. As the sea regressed, the marine conditions were replaced by coastal plain environments. Much later, as additional mountains continued to develop a large lake, at least half the size of Lake Michigan, formed in an intermontaine basin. During the history of this major lake in Green River time, sandstones were deposited in marginal lacustrine environments. Later, these sandstones became the reservoir rocks for the bitumen of the Sunnyside Tar Sands. The distribution of these eight formations is shown on.the Regional Geology Map and the Cross Section of the Book and Roan Cliffs (see Volume II). These rock units were mapped and described on the basis of field geology completed in June and July of Ten years of work on the Sunnyside Tar Sands simplified the field mapping of the area as I was familiar with many of the rock units. Other geology maps and descriptions were integrated into this composite study that was partially based on Doelling (1972) and Osterwald, Maberry and Dunrud (1981). The rock record is contained in the generalized stratigraphic chart of Figure 10. Brief descriptions of these rock formations follow and include both geological and engineering factors

21 Mancos Shale This regionally extensive, thick marine shale is well exposed along the base of the Book Cliffs and throughout the Castle Valley area (see Figure 1A and Photo 7). Surface exposures are often feet thick. In many areas the Mancos Shale is covered with feet of alluvium (see Photo 6). Subsurface data near Clark Valley indicates the average depth to the base of the Mancos Shale is 1758 feet (see Table 1). The Mancos Shale will underlie the proposed tailings disposal area. This shale is light gray to medium gray to dark gray in color; a relatively homogeneous marine unit; and contains carbonaceous, calcareous and gypsiferous matter. The Mancos Shale is impervious to water infiltration. Erosion forms flat desert surfaces and badland topography. Precipitation dissolves the chemical matter and evaporation of the runoff leaves white alkali patches. This thick shale unit accumulated in offshore marine environments that originally extended to the west of Price toward the mountain front in western Utah shown in Figure 12. Periodic influxes of deltaic sands prograded in an easterly direction into this Cretaceous interior seaway. Thus, the Mancos Shale consists of three principal shale members and two principal sandstone members (see Figures 10 and 11). From bottom to top the shale members are Tununk, Blue Gate and Masuk and the two sandstone members are Ferron and Emery as shown in Figure 15. The Emery Sandstone tongue (Kme) and its related Garley Canyon Beds (Kmgc) do not extend east of Price (see Figure 1A). The Tununk Member (Kmt) formed during a major marine transgression in Greenhorn time, the Blue Gate Member (Kmgbg) formed during the sustained marine transgression in Niobrara time and the Masuk Member (Kmm) formed during a final transgression that occurred in Eagle time (Hale and van de Graaff, 1964). Excellent exposures of the Blue Gate (Kmbg), Ferron (Kme), and Tununk Members (Kmt) exist in the Farnham Dome/Cat Canyon area 4-6 miles east of Wellington (see Figures 1 and 1A). The exposed core of the Farnham Dome contains rocks of the Cedar Mountain Formation (Kcm). The Farnham Dome produced carbon dioxide from sandstones at depths between feet in five wells (Hansen and Bell, 1949). These sandstones are the Navajo Sandstone (Mahoney and Kunkel, 1963). Production in the 1940's and 1950's ranged from 2 million to 12 million cubic feet CO2 per day per well and was piped to a now abandoned plant in Wellington for dry ice manufacturing. In the Price-Sunnyside area the Mancos Shale averages about feet thick with the following members and their thickness from bottom to top: Tununk Shale (Kmt, 600 ft); Ferron Sandstone Member (Kmf, 100 ft); Blue Gate Shale Member (Kmbg, 2200 ft); and Masuk (Kmm, 800 ft). The Dakota Sandstone "

22 exists beneath the Tununk Shale Member (see Figures 10 and 11). Above data summarized from Doelling (1972), Hintze (1973) and Weiss, et al (1990). Well logs from five locations in the Clark Valley area were interpreted to give the data shown in Table 1. This subsurface data on three members of the Mancos Shale was compiled to benefit further studies of the tailings disposal area. The data from these five deep drill holes in Clark Valley indicates the Blue Gate Shale Member averages 1357 feet; the Ferron Sandstone Member averages 171 feet; and the Tununk Shale Member averages 230 feet. The Ferron Sandstone Member consists of an upper sandstone interval that averages 81 feet, a middle shale interval that averages 66 feet, and a lower sandstone interval that averages 24 feet (see Table 1 for thickness data and Figure 18 for the well locations). Within Clark Valley the depth to the top of the Ferron averages 1357 feet (range feet). The upper and lower Ferron sandstone intervals form prominent ledges in the Farnham Dome area. As the Cretaceous sea that deposited the Mancos Shale finally regressed it was followed by coastal environments that formed the Mesaverde Group of rocks that consists of the Blackhawk Formation, Castlegate Sandstone and Price River Formation (see Figure 10). Blackhawk Formation In the Sunnyside area this is the most economically significant unit in the Book Cliffs as it contains all the commercial coal deposits. It is divided into the Kenilworth Member on the bottom and the Sunnyside Member on the top (see Figure 7 and Photo 7). The base of the Blackhawk Formation is marked by thin sandstone intervals that gradually thicken upward. The Blackhawk Formation consists of cyclic alternations of sandstone, shale and coal that were deposited in shoreline, lagoonal and swamp conditions; the Blackhawk coal swamps were localized along the Cretaceous coastline in deltaic, interdeltaic and coastal plain settings (Balsley, 1982). Numerous plant fossils and biogenic structures or trace fossils exist and include Ophiomorpha and Thalassinoides as determined by Maberry (1971). These stated biogenic structures indicate shallow water conditions as noted by Chamberlain (1978). In the western part of Castle Valley the coal beds of the Blackhawk Formation are frequently cut by channel scours, while in the eastern part of the Castle Valley near Sunnyside the coal bed continuity is rarely interrupted by channel scours (personal communication, 1986 and 1987, Lynn Huntsman). This detailed information suggests the western part of the Castle Valley is further up the coastal plain than is the Sunnyside area; this

23 concurs with the regional geological framework with the source area to the west and the seaway to the east. The Kenilworth sandstone and the Sunnyside sandstone are two prominent units in the Blackhawk Formation, and both commonly form sandstone cliffs identified in Photo 7. A more detailed discussion of the coal seams is given in the section on Coal Mines in Sunnyside Area. The Kenilworth sandstone is commonly medium to fine grained, while the Sunnyside sandstone is commonly fine grained to very fine grained. The lower Sunnyside coal bed exists immediately above the Sunnyside sandstone. The coal bed is recognized in outcrop by the ocher colors and "red dog" nature of the burned and oxidized coal seam. "Red dog" is a coal miners 1 term applied to surface areas of coal seams that have been baked and burned to form red colors (personal communication, 1986 and 1987, Lynn Huntsman). Rock textures including plant fragments and biogenic structures are commonly preserved. The colors of the rocks have been dramatically changed by kiln-like baking and oxidation resulting from natural fires started near the surface. This burning and baking of the rocks causes ocher (red, yellow and brown) colors to vividly predominate. Locally the rocks may have melted and cooled rapidly to form slag-like textures. Characteristic colors noted in the outcrops of the lower and upper Sunnyside coal seams include moderate reddish orange (10R 6/6) to moderate orange pink (10R 7/4) to moderate reddish brown (10R 4/6) to pale yellowish orange (10YR 8/6) with some dark gray (N3) slag-like material. The color designations are from the Geol. Soc. Amer. Rock-Color Chart (Goddard, et al, 1963). Accessible areas of "red dog" outcrops exist in Sunnyside across the street from the railroad tunnel at the coal loading facility. The outcrops are located in N/2, SW/4, section 32, T14S, R14E. In addition, the baking appears to have modified rock densities as some rocks are lighter than normal while others are heavier than normal. The productive coal beds in the Sunnyside area exist about 150 feet below the Castlegate Sandstone. Castlegate Sandstone The Castlegate Sandstone forms a prominent foot cliff above the Blackhawk Formation. This sandstone forms the lower box canyon unit along the Book Cliffs northwest of Sunnyside (see Photo 6). This sandstone is commonly 150 feet thick and represents a regressive tongue of a fluvial-deltaic complex that unconformably overlies the Blackhawk Formation (see Figure 7)

24 In the Sunnyside-Horse Canyon area this thick sandstone unit represents a blanket sandstone of fluvial origin. Paleocurrent directions are toward the east. In Whitmore Canyon twenty-nine sets of readings have a mean azimuth vector of 110. In Horse Canyon twenty-nine sets of readings have a mean azimuth vector of 82. The fluvial facies of the Castlegate Sandstone are dominated by large scale cross bedding that is overlain by horizontal laminations and current ripple laminations with plant root structures at the top. Above data summarized from van de Graaff (1972). The megascopic lithology of this unit is characterized by fine grained well sorted quartz grains. These sand-sized grains are commonly fl-vfu and megascopically more than 90% quartz. The color of the outcrops is commonly grayish orange pink (5YR 7/2) to light brown (5YR 6/4). The jointing in the Castlegate Sandstone is closely spaced with about one joint per foot. This is about four times the estimated joint density of the upper box canyon unit. This pattern of closely spaced joints adversely affects rock stability. The massive rockfalls off the Castlegate Sandstone located in the northern portion of section 25, T14S, R14E (see Figure 2, and Regional Geology Map) were caused by longwall mining of the upper Sunnyside coal seam. Maps of the Sunnyside Mine indicate longwall mining occurred from in this area, and the major portion of the rockfalls occurred between (Osterwald, et al, 1981). Price River Formation The Price River Formation is about feet thick and consists of two members: an unnamed slope forming member in the lower portion; and the cliff forming Bluecastle Member in the upper portion. The unnamed slope forming member is feet thick and consists of thin interbedded mudstones, claystones, siltstones and thin, fine grained sandstones. This unnamed slope forming member conformably overlies the Castlegate Sandstone, is easily eroded and commonly consists of vegetated slopes.. The Bluecastle Member is feet thick and forms the upper box canyon unit (see Photo 8). The Bluecastle Sandstone Member contains multiple cross bedded sandstones that consist of medium to fine grained (ml-fu) quartz-rich sand grains. This unit is commonly grayish orange (10YR 7/4) in color with a moderately spaced joint system of one joint per 4 feet. The Bluecastle Sandstone Member was deposited in a upper coastal plain to lower alluvial plain environments during the Upper

25 Cretaceous (see Figures 10 and 11). From the Wasatch Plateau to the Book cliffs to the Green River both the average grain size and thickness of the Price River Formation diminish significantly eastward (Osterwald, Maberry and Dunrud, 1981) as shown in Figure 16. The unnamed slope forming member of the Price River Formation exists between the lower box canyon unit of the Castlegate Sandstone and the upper box canyon unit of the Bluecastle Sandstone Member. This relationship is best seen in the left side of Photo 12. The Bluecastle can be distinguished from the Castlegate by its higher stratigraphic position, its slightly larger grain size, its lower density of joints and its tendency to form two or more ledges. The Price River Formation is conformably overlain by the North Horn Formation. North Horn Formation This formation is feet thick and consists of sandstones and shales. The base is easily recognized by a foot massive cliff of sandstone with a distinct desert varnish coating of manganese oxides. This massive cliff is the lowest sandstone unit next to the road at the entrance to Water Canyon. Underground this massive foot thick sandstone unit is a.local aquifer. (personal communication, 1990, Byron Allred, mine surveyor, SRS Inc.). This sandstone unit is a medium grained quartzose sandstone with 5-10 percent hornblende; contains small to medium scale trough cross bedding; weathers to a medium gray (N5) to dark gray (N3) color; is weakly jointed with one joint per ten feet; and forms some very large elongated rectangular-like boulders. Three separate 2-5 foot thick sandstone units that get progressively thinner upsection have similar characteristics to the foot massive cliff and interfinger with the overlying Flagstaff Limestone. The North Horn Formation is of flood plain origin and contains fluvial channels. The Cretaceous-Tertiary boundary exists within the North Horn Formation but is poorly defined (Osterwald, et al, 1973, and Weiss, et al, 1990). The North Horn Formation is transitional to and interfingers with the overlying Flagstaff Limestone. Flagstaff Limestone The Flagstaff Limestone is about feet thick and is recognized by light colored limestones that weather to form breccia-like surface textures. Good exposures exist

26 on the north side of both Water Canyon and Bear Canyon as well as in upper portions of B Canyon. Prior to the geological mapping in June and July 1990 the specific distribution of the Flagstaff Limestone was not known to me. The limestones are light gray and grayish orange in color with interbedded shales of greenish gray color. The Flagstaff Limestone is capped by a distinct 1-3 foot thick medium gray biomicrite to packstone that contains 3-5% pelecypods and gastropods. Some of the gastropods weather out intact and can be found on open slopes slightly below the distinctive gray capping biomicrite. These fossils are of fresh water origin and formed between late Paleocene to early Eocene. The fossils consist of only one species of Pelecypoda (Pleisielliptio sp) and some ten species of Gastropoda (see Osterwald, et al, 1981, p. 23). The Flagstaff Limestone was deposited in Lake Flagstaff which once existed in the Castle Valley area (see Figure 13). The Flagstaff Limestone is conformably overlain by the Colton Formation. Colton Formation The Colton Formation contains continental deposits of predominantly red mudstones and red nonbituminous sandstones that total some feet thick. The Colton Formation is readily separated into a lower member and an upper member. This designation was utilized by Osterwald, et al (1981) and is a valid and helpful concept. The lower member is characterized by slope forming mudstones that are often landslide prone and three minor but separate small cliff forming yellowish gray sandstones. The sandstones of the lower Colton are commonly yellowish gray (5Y 7/2 and 5Y 8/1) in color and medium grained (ml) to fine grained (fu) quartz feldspar sandstones with 10% mafics. The sandstones are moderately jointed with one joint per 2-4 feet. The lower member is commonly feet thick. Good exposures exist near the road along the north portion of Grassy Trail Reservoir, on the northern slopes of Water Canyon and Bear Canyon as well as the upper western slopes of the Book Cliffs. See Photos 8 and 10 for the detail of outcrop exposures. The upper member is a massive sheer cliff forming unit of reddish brown sandstones that are feet thick. The sandstones of the upper Colton are pale red (5R 6/2) to light brown (SYR 5/4) in color and medium grained quartz feldspar sandstones with 5-10% mafics. The sandstones are moderately jointed with one joint per 1-3 feet. Thus the upper sandstone in the upper Colton are slightly coarser in grain size and more

27 closely jointed than the sandstone in the lower Colton. Good exposures for the upper member are shown in Photos 8 and 10. The Colton Formation was deposited in fluviatile to flood plain environments that existed during an interlacustrine time interval between the presence of Lake Flagstaff that formed the Flagstaff Limestone and Lake Uinta that formed the Green River Formation. When the Flagstaff Limestone is not present in the stratigraphic section the Wasatch Formation is the equivalent term for the Colton Formation as shown in Figures 10 and 11. In previous years of the project the distribution of the Flagstaff Limestone was not established and the continental deposits that formed in Colton time were referred to as the Wasatch Formation. Since the Flagstaff Limestone is distributed throughout the Sunnyside region (see Regional Geology Map), the correct geological terminology is Colton Formation, not Wasatch Formation. The transitional and conformable contact of the overlying Green River Formation is placed in different locations by different geologists with no common agreement.. The following discussion of the Green River Formation applies to my work completed on Amoco*s Sunnyside Tar Sands project. Green River Formation The Sunnyside Tar Sands are confined to the Green River Formation which has been separated into a lake, shore and delta facies. The Green River Formation formed in environments associated with Lake Uinta during middle Eocene time some million years ago. The Green River Formation consists of three formal members: Parachute Creek Member, Garden Gulch Member and Douglas Creek Member. These three members were delineated in the field on the basis of different colored shales, biota content, presence of oil shales, abundance and distribution of limestones and sandstones. The Parachute Creek Member is dominated by gray shales and oil shales; it represents the lake facies and contains limited volumes of bituminous sandstones. The Garden Gulch Member is dominated by green shales and abundant fossiliferous limestones which contain ostracods, algal structures and garpike fish scales; it represents the shore facies and contains minor volumes of bituminous sandstones. The Douglas Creek Member is dominated by red shales and bituminous sandstones as well as nonbituminous sandstones; it represents the delta facies and contains major volumes of bituminous sandstones and minor amounts of fossiliferous limestones

28 In addition, the Douglas Creek Member has been separated into three informal portions (upper, middle and lower) on the basis of oil saturation and a red shale-limestone marker interval. The tar sands are concentrated in the upper portion of the Douglas Creek Member. The middle portion is between the base of saturation and the red shale-limestone marker interval. The lower portion is below the red shale-limestone marker interval and above the Colton Formation. Nonbituminous sandstones exist in both the middle and lower portions of the Douglas Creek Member. The distribution of the lower, middle and upper portions of the Douglas Creek Member is identified in Photo 13. The distribution of the Green River Formation is shown on the Regional Geology Map (scale l"=2000ft) and agrees with the work of Doelling (1972) and disagrees with the work of the U.S. Geological Survey (Osterwald, et al, 1981, and Weiss, et al, 1990). An important ostracod interval was located this past summer on West Ridge slightly below hill 8898 located in the NW/4, section 12, T14S, R13E and confirms the presence of the Green River Formation on West Ridge. A thin zone of tar sands containing 2wt% bitumen exists in a saddle along the jeep road on West Ridge located above the top of B Canyon. The map of Doelling (1972) is helpful to delineate the distribution of the Green River Formation outside the area of the Sunnyside Tar Sands. Parachute Creek Member The Parachute Creek Member exists at the top of the Roan Cliffs and within the upper parts of the West Tavaputs Plateau. It is feet thick and lies above the areally extensive Blue Marker, which represents the base of this member. During the field work of 1986 and 1987 various oil shale intervals were initially defined in the numerous measured sections. During the drilling program of 1988 the correlation of these six oil shale intervals was finalized from well logs and continuous drill core. Six oil shale zones are recognized and represent the R-2, R-3, R-4, R-5, R-7 and R-8 zones defined by Ziemba (1974) in Tract C-a of the Piceance Creek Basin. The six oil shale zones in the Bruin Point area were numbered on the basis of well log correlations with those from Tract C-a. The R-7 oil shale zone represents the Mahogany Oil. Shale. The inch thick Wavy Bedded Tuff exists east of Range Creek and is an excellent marker to identify the look-alike oil shale doublets of R-5 and R-7. The Wavy Bedded Tuff exists 35 feet above the top of the R-7 oil shale zone as shown in Figure

29 The R-2 oil shale zone represents the Blue Marker and contains a diagnostic inch thick coal seam about 1.5 feet above the R-2 oil shale. A one inch lignite coal seam represents about ten inches of original peat as noted by Falini (1965). This suggests a reasonable quantity of peat accumulated during the transition between Garden Gulch time and Parachute Creek time. Thin (1-3 inch thick) algal zones occasionally exist in the core of oil shale zones R-2, R-3 and R-4. No ostracods have ever been noticed in over 6000 feet of logged drill core from the Parachute Creek Member. The chemistry of the lake waters during Parachute Creek time with no ostracods was different from that of Garden Gulch time when ostracods flourished. Garden Gulch Member The Garden Gulch Member represents the lake or green shale facies, is commonly feet thick and contains the important' Carbonate Interval of Tar Zones 25 and 26 with the included interburden. The foot thick Carbonate Interval contains three parts upper, middle and lower. The upper part consists of the foot thick Zone 25 that is limestone and ostracod-rich. The middle part is dominated by light greenish gray shales that are burrowed to weakly bioturbated. The lower part consists of the foot thick Zone 26 that is limestone and ostracod-rich. Within the Garden Gulch Member Zones 21 and 22 commonly represent beach deposits, while Zone 23 commonly represents a mouth bar deposit that has been locally reworked. Tar Zones 25 and 26 are usually bituminous carbonates but occasionally are represented by bituminous beach deposits. Voluminous tar sands exist below the Carbonate Interval. The limestones within both the Garden Gulch Member and the Douglas Creek Member contain significant amounts of fresh water biota in the form of algae reefs and ostracod coquinas. The algae reefs are up to three feet high and consist of multiple laminated stromatolites commonly referred to as cabbage heads. The thickest algae reefs are associated with the base of Tar Zones 31, 32 and 33. The greater part of the algae reefs of the Green River Formation consist of Chlorophyta (green algae), chlorellopsis coloniata as classified by Bradley (1929). This is a unicellular stromatolite-forming algae. Stromatolites consist of cyanophyta (blue green algae) as classified by Wray (1977). These green or blue-green algae are chlorophyll-bearing and precipitate calcium during photosynthesis. They live in the photic zone

30 associated with very shallow waters under quiet stable conditions with very limited influx of detritus material. The water depths range from 1-15 feet and categorically are from intertidal to nearshore. In detail the stromatolites are laminated, columnar to hemispherical in shape, and consist of alternating sediment-rich and algae-rich layers. Stromatolites are sediment trappers or binders. The stromatolites are nonskeletal boundstones and also represent an important producer of calcium carbonate in this Eocene shoreline area. Beds of ostracod coquinas are often 1-4 feet thick. Ostracods are microscopic benthic crustaceans that moult their calcite-rich bivalve shells about eight times during their lifetime. The calcium carbonate from these ostracod coquinas and algae reefs was available through ground water leaching to cement the sandstones in the Bruin Point area prior to the emplacement of the bitumen. The composition of the cement in the Sunnyside Tar Sands was determined by Remy (1984) after Core Labs had removed the bitumen in specific core samples. The cement is 1.2% calcite and 2.0% dolomite as identified in thin-section by the use of Alizarin Red S staining that distinguishes calcite (CaCC>3) from dolomite (CaMgCC>3). Douglas Creek Member The Douglas Creek Member represents the delta or red shale facies and is about feet thick. The vast majority of the tar sands occur in the upper 800 feet. The Douglas Creek Member contains both bituminous and nonbituminous sandstones, the base of saturation, a red shale-limestone marker interval as well as numerous ostracod/algal intervals. The Douglas Creek Member can be separated into a lower, middle and upper portion on the basis of oil saturation and the foot thick red shale-limestone marker interval. From a distance this red shale-limestone marker interval forms a distinct dark maroon colored band (see Photo 13). The upper portion of the Douglas Creek Member extends from below the Carbonate Interval to the base of saturation and contains all the bituminous sandstone intervals between Tar Zones The base of saturation exists between elevations of 8800 to 9200 feet along the Roan Cliffs as shown on the Regional Geology Map and in Photos 2, 3, 4 and 5. This upper portion contains numerous algal and ostracodal intervals especially below the base of each numbered tar zone. The middle portion of the Douglas Creek Member exists between the base of saturation and the red shale-limestone marker interval. The middle portion averages some feet

31 thick with a range of feet. It contains numerous yellowish light brown colored nonbituminous sandstones and various ostracod-algal limestone intervals such as the one at the hairpin turn below the Asphalt Mine, or in other words, the next hairpin curve just above the hairpin curve with the huge hanging rock and the partially fallen tramway cable. On the road to the Asphalt Mine the red shale-limestone marker interval is located about 1800 feet up the road from the Texaco curve and is defined by the red shale and two separate ostracodal limestone beds that outcrop along the road. This red shale area of the road is slippery and dangerous when wet. The lower portion of the Douglas Creek Member exists between the red shale-limestone marker interval and the Colton-Green River gradational contact. This lower portion averages about 300 feet thick with a range of feet. The lower portion contains nonbituminous fine grained sandstones that weather to a light brown 5YR 6/4 to 5YR 5/6 to 5YR 8/4. The reddish hue of the medium grained sandstones of the Colton Formation is not obvious in this lower portion of the Green River Formation. The nonbituminous sandstones both above and below the red shalelimestone marker interval are of similar grain size, color and geomorphic expression. They contrast with the reddish brown cliff forming sandstones of the upper Colton Formation. On the west side of the Roan Cliffs this lower portion of the Green River Formation exists down to elevations between feet. The upper, middle and lower portions of the Green River Formation have been utilized to illustrate gross relationships along the Roan Cliffs but were not fully incorporated into the Regional Geology Map. Only the good outcrop areas of the red shale-limestone marker interval are indicated on the map. Detailed field work within the confines of the major limits of the Sunnyside Tar Sands outlined in Figure 1 separated the Green River Formation into three formal members: Douglas Creek Member (delta facies); Garden Gulch Member (shore facies); and Parachute Creek Member (lake facies). The areal extent and contacts associated with these three formal members are shown on the geology maps in previous yearly reports. The location of the gradational contact between the Colton and Green River Formations is based first on the presence of ostracod beds, second on the color change of the nonbituminous sandstones, third on fine grained versus medium grain size of the sandstones, and fourth on the geomorphic expression of the sandstones. The ostracods are of fresh water origin and belong to the Green River Formation. The cliff forming medium grained sandstones with red hues

32 belong to the Colton Formation. The relatively uniform slopes that contain sandstones with yellow hues belong to the Green River Formation. The red shale-limestone marker interval could be interpreted as a tongue of the Green River Formation. But since there are at least separate ostracod beds that periodically occur within the Green River Formation, no attempt has been made to define these multiple minor transgressions and regressions

33 TAR SANDS General Photos of panoramic views along the Roan Cliffs were made to show the distribution and continuity of the fifteen numbered tar zones within the Bruin Point area. These panoramas have been reduced and presented as Photos 2, 3, 4 and 5. The panoramas contain labelled outcrops of the numbered tar zones as well as the positions of the Blue Marker, Carbonate Interval and base of saturation. With these four panoramic photos it is easy to visualize the vertical stacking of tar zones; the sheet-like nature of the tar sands; the base of saturation; and the depth of overburden in the South, Central and North Areas. The overall geometry of these tar sands is an elongated wedge that parallels the Roan Cliffs and thins downdip toward Range Creek. The tar sands are associated with stacked sequences of sandstone-shale-limestone-unconformity. The top of the limestone interval is usually eroded to depths of feet. The beds above and below the unconformity, or erosional interval, are essentially parallel. Above the unconformity which is at the base of nearly every sandstone, there is often an IFC (intraformational conglomerate) that represents a lag deposit and commonly consists of rip up clasts of shale and limestone with calcareous nodules and algal fragments. These IFC's exist above the unconformity and represent lag deposits formed during prograding of the sands across the carbonate shoreline deposits. Each limestone interval contains some ostracod-rich or algal-rich beds. Some IFC's represent transgressive lags due to storm deposits. The bitumen in the Sunnyside Tar Sands is almost entirely associated with fine grained sandstones that are completely saturated above the base of saturation. The average grain size of the sandstones is 17% medium grained, 54% fine grained, 23% very fine grained with 6% silt and clay (data averaged from Remy, 1984, and Banks, 1981). The mineralogy of the sandstones averages 33% quartz, 12% K-feldspar, 17% plagioclase feldspar, 8% rock fragments, 4% minor constituents, 6% cement and matrix and 20% porosity (data averaged from Remy, 1984, and Banks, 1981). The porosity and permeability data was completed by Core Labs, Inc. of Denver. The bituminous sandstones have an average porosity of 27% (range 24-29%) and average permeability of 812md (range md). Minor amounts of bitumen are associated with siltstones and limestones. The siltstones are partially saturated and characterized by a streaky saturation appearance caused by

34 alternating bands of dark colored saturation and light colored nonsaturation. The siltstones have an average porosity of 22% (range 18-26%) with an average permeability of 64md (range md). The limestones consist of irregular saturation associated with both micrites and biomicrites. The limestones have an average porosity of 18% (range 15-24%) with an average permeability of 0.6md (range md). The differences in average permeability of the sandstones, siltstones and limestones are dramatic and have greatly affected the distribution of the bitumen. The fifteen major tar zones have been defined and numbered by a two digit code for computer modelling. The first digit applies to the member (i.e., 10's for the Parachute Creek Member; 20's for the Garden Gulch Member; with 30's and 40's for the Douglas Creek Member). The second digit applies to the specific tar sand interval. The fifteen major tar zones now include 21, 22, 23, 25 and 26, 31, 32, 33, 35, 36, 37, 38, 41, 42, 43, 45. Obviously some second digits are not sequential as the interval was not areally extensive, was less than 10 feet thick, or had a grade of less than 10 gallons per ton. In any case, the interval did not meet economic criteria. From the fifteen numbers it is apparent there are no important tar sands in the Parachute Creek Member. Zones 25 and 26 represent the top and bottom of the Carbonate Interval and are considered undesirable for processing due to their high content of calcium carbonate. The Garden Gulch Member contains 12.8% of the bitumen resource, while the Douglas Creek Member contains 87.2%. From Table 4 and Photos 2, 3, 4 and 5 it is obvious that most of the tar sands exist below the Carbonate Interval. Some tar sands exist above the Blue Marker in the Parachute Creek Member. They are very limited, commonly less than ten feet thick and of low grade (i.e., l-3wt% bitumen). In the early years before the complete delineation and significance of the Blue Marker was established in both core and outcrop, Tar Zone 11 was sometimes above and sometimes below the Blue Marker. This is stratigraphically inconsistent and was changed in the 1989 Exploration Report. Most of the old Zone 11 has become the new Zone 21. A proposed tar zone designation within the Parachute Creek Member relates the tar zones to the stratigraphic position of oil shales. Tar Zone 10 exists between R-7 and R-5 oil shales and represents the brown cliff that separates the lookalike oil shale intervals of^r-5 and R-7. There is no R-6 oil shale in the Mount Bartles-Bruin Point area. There are no tar sands between the R-5 and R-4 oil shale intervals. Tar Zone 11 exists between the R-4 and R-3 oil shales. Tar Zone 12 exists between the R-3 and R-2 oil shales

35 Controls The Sunnyside Tar Sands accumulated near Bruin Point from both structural and stratigraphic controls. The structural controls include a regional monocline that has been interrupted by the Mount Bartles-Bruin Point flexure. This flexure is segmented and consists of an eastern, central and western segment. As seen from the Regional Geology Map and its accompanying Cross Section A-A 1 the tar sands are localized in the western segment. This western segment exists near the Roan Cliffs, has beds that dip 4-12 northeast and sandstones that contain 4-12wt% bitumen. The central segment has beds that dip 4-7 northeast and sandstones that contain 4-7wt% bitumen. The eastern segment has beds that dip 3-5 northeast and sandstones that contain 0-4wt% bitumen. The stratigraphic controls are sandstones associated with the repetitious sequences of sandstone-shale-limestoneunconformity that are stacked one on top of each other. Each sandstone-shale-limestone-unconformity cycle is a fining upward sequence. These stratigraphic sequences represent 4th order sequences with durations measured in hundreds of thousands of years as based on Van Wagoner, et al (1990) and Vail, et al (1977). These sequences formed in response to cycles of relative rise and fall of lake levels that are interpreted to be the result of Milankovitch climatic cycles with durations of 100,000 years (see Figure 21). No flooding surfaces have been recognized but unconformities are usually visible in outcrop and recognized in well logs by gamma ray kicks of API units above background. Each stratigraphic sequence is commonly almost 100 feet thick with the lower half as the bituminous sandstone. Available averages based on computer results of 1982 and 1984 indicate each stratigraphic sequence averages 83.6 feet thick with 39.7 feet of bituminous sandstone in the lower portion. The area contains excellent reservoir rocks with less obvious seals; the source rocks are downdip in the Uinta Basin. The reservoir rocks are fine grained sandstones of almost uniform grain size and mineral composition. These sandstones were distributed by a northeast flowing fluvial-deltaic complex that dispersed the sands along the northwest trending shoreline of Lake Uinta. The base of saturation map contains a five square mile area with a nearly flat gradient or terrace that interrupts the dip slope. This flat area is localized near Bruin Point and contains the vast majority of the tar sands (see Base of Saturation Map, Exploration Report). This flat terrace-like catchment area is immediately updip from that main axis of the flexure. Another small flat terracelike catchment area exists to the west of the Roan Cliffs and

36 helps to explain the isolated occurrence of tar sands located in the Whitmore Canyon area. The seals are interpreted to consist of biodegraded bitumen in updip portions of the sandstones; shales that range from grayish red to greenish gray to light olive gray; and thin oil shales. The source rocks were the thick lacustrine shales and oil shales located some miles downdip near the axial portions of the Uinta Basin. The bitumen formed from Type I kerogen (i.e., algal kerogen) and migrated laterally during diagenesis to the rim of the basin. Then it was concentrated in the sandstones of the Bruin Point area and later biodegraded to the bitumen that now has an API gravity of about 10. All the bitumen in the Sunnyside Tar Sands area is strongly biodegraded. Biodegradation occurs at the oil-water interface. Bacterial activity requires both water and oxygen. The bacteria live in the aqueous phase where dissolved oxygen is available. The bacteria preferentially consume portions of the oil phase. Above summarized from Connan (1984). Near Bruin Point at North Spring in Range Creek abundant CO2 gases exist in a one square mile area at depths of feet below the surface. These CO2 gases are located near the base of saturation and their limits are outlined on the base map of Drill Hole Locations For Isopach Maps in Volume II. These CO2 gases suggest that biodegradation is currently in progress. The Uinta Basin is an asymmetrical basin with the steeply dipping flank on the north and the gently dipping flank on the south (Wells, 1958, and Osmond, 1965). Oil fields are prevalent in the northern flank and tar sands exist in both the northern and southern flanks. The PR Spring and Sunnyside Tar Sand deposits both occur on the southern flank and have somewhat similar lake-shore-delta geology. Sulfur isotope studies by Mauger (1972) are useful to explain the accumulation of bitumen in various sandstones within the Uinta Basin. Sulfur is composed of four natural occurring isotopes: 32 S, 33s, 34s and 36s. In the northern steeply dipping flank of the Uinta Basin sulfur isotope data from bituminous sandstones indicates that values of 34s are consistent throughout the stratigraphic interval that is saturated. The uniform sulfur isotope distribution in the bituminous sandstones of the northern flank (data from Raven Ridge, Asphalt Ridge and White Rocks) may have resulted from vertical migration of oil from accumulations at depth. But at PR Spring in the gently dipping southern flank of the Uinta Basin the values of 34s are consistent only within an individual saturated sandstone and increase going upsection. This indicates that the sandstones were impregnated separately, one by one. The oil in the sands of the delta facies at PR Spring accumulated by lateral migration. The sands acted as

37 paleoaquifers that drained the fluids from the deeper portions of the basin during compaction. Above paragraph summarized from Mauger (197 2). How did all the biodegraded bitumen form in the Sunnyside Tar Sands area? Perhaps each tar zone in the Bruin Point area was impregnated separately and then biodegraded separately from the top down as the water level dropped. The unconformities at the base of each tar zone probably served as important paths for oil migration. Correlation The Sunnyside Tar Sands have been correlated on the basis of lithology and unconformities. The tar sands were initially correlated on the basis of lithology obtained from well logs, core and outcrops. The cycles of sandstone-shale-limestoneunconformity were recognized from outcrop patterns in measured sections. These outcrop patterns were then integrated into the drill hole data. It was then realized that unconformities exist at the base of nearly all tar sands. Later it was realized that these cycles of sandstone-shale-limestone-unconformity represent sequence stratigraphy with each sequence bounded by an unconformity. These relatively flat unconformities represent an important horizon for use in time-stratigraphic correlation. Since the base of a tar sand has always been used for correlation, the correlation of numbered tar zones in the Bruin Point area is based on both rock-stratigraphic (lithostratigraphic) and timestratigraphic (chronostratigraphic) criteria. A brief chronology of these correlation methods follows. In 1980 field work separated the Green River Formation into three members based largely on the color of shales but also biota. Gray shales are associated with the Parachute Creek Member or lake facies. Green shales are associated with the Garden Gulch Member or shore facies. Red shales are associated with the Douglas Creek Member or delta facies. Utilization of these shale colors is highly effective in delineating environments of deposition associated with lake, shore or delta facies. In 1981 Golden Associates used geophysical data from well logs to assign numbers to the tar sands in order to facilitate mine modeling of tar zones. Gamma ray and density logs at a scale of 1"=10 feet were utilized to determine any similarity or variations of log curves associated with sandstones, shales and limestones. Well log correlations are based mainly on curve matching of log shape, amplitude and frequency (Serra, 1986). Stratigraphic relationships gained from measure sections and lithology logs of continuous core were utilized to confirm the well log correlations. Direct comparisons of well logs

38 at a scale of 1"=10 feet and core logs at a scale of 1"=10 feet show remarkable coincidence with only minor adjustments of 1-3 feet per hole. The ability to compare well logs and continuous core throughout the property has helped immensely to establish correlations. The infrequent errors by the drillers in boxing the core were corrected in the core shack before the core was logged. 1 In 1982 correlation of sandstones in the Bruin Point subdelta and Dry Canyon subdelta was troublesome. Red and green shale horizons were utilized to resolve the problem. The correlation problem was caused by a major split of Zone 36. Based on continuity of shale intervals Zone 36 was renumbered into Zone 36 and Zone 99. In 1984 during measured section work the conglomerates and siltstones were mentally dropped from the lithology packages and patterns of sandstone-shale-limetone-unconformity became apparent. These cycles of sandstone-shale-limestone-unconformity represent patterns of upward fining sequences that are characteristic of the Green River Formation, especially in the shore and delta facies. The tar zone numbers utilized in mine modelling were incorporated into the strip logs of both measured sections and drill holes. In 1986 surface gamma ray data from a portable minispectrometer was first utilized in MS-27. Surface gamma ray anomalies are distinctive and coupled with stratigraphic intervals take the guesswork out of establishing tar zone numbers in outcrops. The surface gamma ray data is so helpful it is now a standard part of measured section methodology. Initial work began on the correlation of oil shale intervals. In 1987 the distribution and significance of the Blue Marker (oil shale R-2) was determined from outcrop data and surface gamma ray anomalies. The Wavy Bedded Tuff was first located in the West Tavaputs Plateau within MS-56. The Wavy Bedded Tuff represents an excellent time-stratigraphic unit but unfortunately is eroded from the Roan Cliffs. The Wavy Bedded Tuff has a poor well log expression. In 1988 the stratigraphic detail and vertical separation of five oil shale zones (R-2, 3, 4, 5 and 7) was firmly established with the help of drill hole data. Numerous outcrops of the Wavy Bedded Tuff were recognized in areas east of Range Creek and the main axis of the Mount Bartles- Bruin Point flexure. The Wavy Bedded Tuff exists thirty-five feet above the Mahogany Oil Shale and is most helpful to distinguish between the look-alike R-5 and R-7 oil shale zones. The significance of the Carbonate Interval began to emerge

39 In 1989 relogging of Mono Power core continued to confirm the now well-established stratigraphic intervals shown in Figures 19 and 20. In 1990 sequence stratigraphy was applied to the Sunnyside Tar Sands. The important differences between rock-stratigraphic and time-stratigraphic correlation were applied to the tar sands to make sure the correlations of the tar sands were correct. The important work of Van Wagoner, et al (1990) illustrates significant differences in sandstone geometry when chronostratigraphic correlation is utilized instead of lithostratigraphic correlation. "A rock-stratigraphic unit is a subdivision of the rocks in the earth's crust distinguished and delineated on the basis of lithologic characteristics" (AAPG, 1961, vol. 45, no. 5, p. 649). "A time-stratigraphic unit is a subdivision of rocks considered solely as the record of a specific interval of geologic time" (AAPG, 1961, vol. 45, no. 5, p. 657). Sequence stratigraphy groups rocks into a relatively conformable succession of genetically related strata that are bounded on the top and bottom by unconformities (Mitchum, 1977, and Van Wagoner, et al, 1990). The geometry of sandstones associated with progradational, retrogradational and aggradational parasequences is shown in Figure 22. Parasequences are bounded by flooding surfaces with no subaerial erosion, while sequences are bounded by unconformities formed by subaerial erosion (Van Wagoner, et al, 1990). The unconformities of sequences represent relatively flat surfaces, make good to excellent time markers and can be utilized in chronostratigraphic correlation as noted by Van Wagoner, et al (1990). Figure 23 of this report illustrates important differences in the distribution of sandstones based on chronostratigraphic versus lithostratigraphic correlations. This research on sequence stratigraphy and related distinctions between time-stratigraphic and rock-stratigraphic units has prompted additional explanations of just how the correlations of numbered tar zones were made in the Bruin Point area. Well log correlations of tar sands began in 1981 when John Rozelle was at Golder Associates and have continued through the years by John Rozelle at Pincock, Allen and Holt, Inc. Computer generated zone maps were obtained from manually prepared maps of the top and bottom of each tar zone. The bottoms of each tar zone represent a smoother plane than the tops. John Rozelle has always put more faith in the bottom position of the tar zone for correlation than the top position. In other words, the relatively flat unconformity at the base of each tar zone has been utilized for correlation. The correlation of tar sands by use of the unconformity at the start of a stratigraphic sequence is chronostratigraphically correct as long as the correlation exists within the boundaries of that particular sequence. If a tar zone correlation crosses

40 a sequence boundary the correlation is incorrect and needs to be adjusted. Over the years John Rozelle and I have continued to work together to firmly establish, adjust and fine tune tar zone correlations. Numbered tar zones in measured sections have been used in tar zone correlations and present an accurate picture of the deposit as seen in Photos 2, 3, 4 and 5. The correlation of numbered tar zones represents a combination of time-stratigraphic (chronostratigraphic) and rock-stratigraphic (lithostratigraphic) criteria. Tar Zone Isopachs Separate isopach maps of the fifteen numbered tar zones were made to illustrate the thickness and distribution of the fifteen pay zones and are included in Volume II. The isopach maps of each zone contain seven reference locations as well as the State of Utah coordinate system. The seven reference locations include Asphalt Mine, Bruin Point, North Overlook, Central Overlook, South Overlook, North Spring and Shell Curve. These seven reference locations can be used in conjunction with the panoramas of Photos 2,3, 4 and 5 to form a more complete three dimensional picture of the entire tar sand deposit. The Tar Sand Isopach Map in the 1989 Exploration Report is of the entire area and contains the total thickness of all fifteen numbered tar zones. The separate isopach maps have been keyed to a small base map (scale 1"=1500') that contains all drill hole locations as well as the seven reference locations (see Volume II). All isopach maps look northeast across the Roan Cliffs toward Range Creek. Gaps in isopach lines represent no possible data and are caused by erosion associated with numerous drainages in this mountainous terrain. Each zone map is on a frosted mylar and can be overlaid on the base map or on the next zone above or below for orientation or comparison of thickness and depositional trends. The isopach maps include the following fifteen zones: 21; 22; 23; Carbonate Interval of zones 25 and 26; 31; 32; 33; 35; 36; 37; 38; 41; 42; 43; and 45. Each tar zone is discussed separately from the top down but has been segregated within one of four groups. For convenience, these fifteen isopach maps were separated into four groups which all exist below the Blue Marker as noted in Table 4. The upper group with four isopach maps includes Zones 21, 22, 23 and the Carbonate Interval of Zones 25 and 26; these are all within the Garden Gulch Member and have relatively simple patterns. The middle, lower and bottom groups all exist within the Douglas Creek Member and have relatively complex patterns. The middle group with three isopach maps includes Zones 31, 32 and 33. Isopach patterns of this middle

41 group get more complex with increasing depth. The lower group with four isopach maps includes Zones 35, 36, 37 and 38; this group has the most complex isopach patterns. Finally, the bottom group with four isopach maps includes Zones 41, 42, 43 and 45. This bottom group also has complex isopach patterns but the areal dimensions are smaller as the base of saturation is approached and data is lacking. Bitumen and average thicknesses of these fifteen tar zones are listed in Table 4. In general the thickness of the tar zones thin upward from 71 feet near the Asphalt Mine to 10 feet near Bruin Point. In general the bitumen grades gradually decrease upward from 17-18gpt near the Asphalt Mine to 14-16gpt near Bruin Point. Drill holes were continuously cored through all the various tar zones to depths that penetrated feet of the first clean nonbituminous sands. Thus the base of saturation was firmly established. Three drill holes in the area were cored to considerable depths below the base of saturation. Amoco Drill Hole A-4 was completed to depths 194 feet below the base of saturation and defined the tops and bottoms of nonbituminous Zones 42, 43 and 45. Mono Power drill hole BP-1A was completed to depths 313 feet below the base of saturation. Relogging of this continuous core in 1987 defined the tops and bottoms of nonbituminous Zones 38, 41 and 42. Great National drill hole GN-14 was completed to depths 4 09 feet below the base of saturation and passed through three major nonbituminous zones whose numbers have not been firmly established since the core has not been relogged. The separate isopach maps are the result of a combined effort by John Rozelle and Bob Sandefur of Pincock, Allen and Holt, Inc. and myself. The maps were generated and initially contoured by computer. Later, as necessary, the isopach lines were modified by hand to include the 1989 data from relogging of thirteen RCT drill holes of Mono Power in the South Area. This 1989 data has yet to be posted in the computer model. Upper Group This group contains the four isopach maps from numbered tar zones 21, 22, 23 and Carbonate Interval. The fossiliferous limestone-rich zones of 25 and 26 as well as the shale-rich interval in between represent the Carbonate Interval. This upper group exists below the Blue Marker and above the base of the Carbonate Interval. It is confined to the Garden Gulch Member or shore facies. This upper group contains 12.8% of the total bitumen resource (see Table 4). Zones 21, 22 and 23 contain 11% of the resource, while Zones 25 and 26 contain 1.8% of the resource. Throughout this group clusters of thick sands

42 are often feet apart and trend nearly perpendicular to the Roan Cliffs. The major trend of sand influx is interpreted to be N70-90 E. This upper group exists in the South and Central Areas shown in Photos 2, 3 and 4. This upper group is eroded from the North Area as shown in Photos 4 and 5. The isopach map of Zone 21 is based on 53 drill hole intercepts and has an average thickness of 10.0 feet (range 4-49 feet) with a bitumen grade of 13.7gpt. This zone contains 0.9% of the total bitumen resource. Zone 21 (old 11) contains six principal cones that represent depositional centers of sand within an area 5000 feet x feet. The long dimension is parallel to the Roan Cliffs and depositional strike of the area. Two large cones are clustered in an area between the Central Overlook and North Spring. This main cluster has an orientation of N75 E and suggests this is the major trend of the distributary that deposited'the sand. Within Zone 21 the Central Area contains more tar sands than the South Area. The isopach map suggests a general but nonuniform thinning to the northeast beyond Range Creek. These sands do not indicate significant dispersal by shoreline processes of Lake Uinta. The isopach map of Zone 22 is based on 61 drill hole intercepts and has an average thickness of 23.1 feet (range 4-60 feet) with a bitumen grade of 15.9gpt. This zone contains 6.8% of the total bitumen resource. This isopach map is marked by distinct areas of thickening and thinning. Zone 22 (old 21) contains five principal cones or sites of deposition in a 5000 feet x feet area. The distribution of sands is similar to the patterns within Zone.21. The principal sands exist between the Central Overlook and the North Spring. Based on the distribution of highs and lows the thickness trends suggest an orientation of N70 E as the major trend of sand influx. Within Zone 22 the Central Area contains more tar sands than the South Area. The isopach map of Zone 23 is based on 53 drill hole intercepts and has an average thickness of 17.8 feet (range 2-59 feet) with a bitumen grade of 15.7gpt. This zone contains 3.3% of the total bitumen resource. Zone 23 contains four cones, two of which are aligned in a N90 E trend from the Central Overlook to North Spring. These sands thicken and thin noticeably to the left and right of this N90 E depositional trend. There is little change in the depositional trend and sites of sand accumulation from Zones 22 and 21. In general the sands near the Roan Cliffs are thicker and roughly 25 feet thick, while those sands to the east of Range Creek are thinner and roughly 15 feet thick. Thus these sands thin downdip toward the Uinta Basin

43 The isopach map of the Carbonate Interval is based on 60 drill hole intercepts that have an average combined thickness of 60.0 feet with a bitumen grade of 12.7gpt for Zone 25 and 13.0gpt for zone 26. Zone 25 contains 0.7% of the total bitumen resource, while Zone 26 contains 1.1% of the total bitumen resource. The Carbonate Interval contains some 1.8% of the total bitumen resource. The Carbonate Interval is somewhat uniform throughout the area with a slight thickening downdip toward the West Tavaputs Plateau and partial thinning updip toward the Roan Cliffs. The Carbonate Interval separates the tar sands into two distinct categories. The sands above are thinner and of lower grade with relatively simple isopach patterns. The sands below are thicker and of higher grade with relatively complex isopach patterns. Photos 2, 3 and 4 show the spatial relationship of the Carbonate Interval to the Roan Cliffs and the various numbered tar zones. Middle Group This group contains the three isopach maps from numbered tar zones 31, 32 and 33. The isopach patterns get more complex with increasing depths. Photos 2, 3, 4 and 5 contain views of zone locations and their depths. These three zones exist below the Carbonate Interval and are in the Douglas Creek Member. Zones 31, 32 and 33 contain 22.2% of the total resource (see Table 4). The isopach map of Zone 31 is based on 7 6 drill hole intercepts that have an average thickness of 31.6 feet (range 3-90 feet) with a bitumen grade of 17.8gpt. Zone 31 contains 12.6% of the bitumen resource and is one of the four most productive pay zones 1 This zone exists throughout much of ;the resource area. The isopach map contains three major cones or centers of deposition that are feet apart. One cone is near the Central Overlook, another is near Bruin Point, while the other is centered on drill hole RCT-7 near Range Creek. Commonly the sites of high deposition have laterally adjacent areas of low deposition. The major trend of sand influx is N65 E. Outcrop data indicates the average paleocurrents flowed northeast. The various ridges that extend off the Roan Cliffs are believed to represent important paleogeographic trends and mark the loci of secondary distributary channels. The isopach map of Zone 31 shows that the vast majority of the sand deposition is between the Roan Cliffs and Range Creek. This area contains sheet sands deposited by distributary channels near the lake shore. These sheet sands roughly average 30 feet thick with local highs of feet and local lows of feet. These cones or local highs imply rapid dumping from distributaries located near the edge of the lake. Within Zone 31 the Central Area contains more tar sands than the South Area

44 The isopach map of Zone 32 is based on 35 drill hole intercepts that have an average thickness of 14.8 feet (range 3-47 feet) with a bitumen grade of 16.5gpt. Zone 32 contains 2.7% of the bitumen resource and is one of the least important pay zones. The three principal cones or primary sites of deposition are centered on A-70, RCT-3A and RCT-13. Zone 32 is best developed in the South Area and poorly developed in the Central Area. It has been eroded from the North Area. The principal sites of deposition are located above 5000 feet apart. The isopach map of Zone 33 is based on 77 drill hole intercepts that have an average thickness of 26.2 feet (range 5-81 feet) with a bitumen grade of 16.5gpt. The zone contains 6.9% of the bitumen resource. The isopach map is characterized by numerous cones or sites of deposition between the Roan Cliffs and Range Creek. The principal site of deposition is located near Bruin Point and the North -Overlook. The major trend of sand influx is considered to be N50 E and parallels the ridge line from the Shell Curve to Bruin Point. This ridge line represents a major distributary system of the Sunnyside delta complex. Near Bruin Point this major distributary system contains adjacent lows. Two other sites of major deposition exist between the Central Overlook and North Spring and are separated by a low. Another site of important accumulations exists near South Knoll and is centered on drill hole GN-14. This isopach map illustrates irregular hummocky surfaces with numerous highs (45-80 feet thick) and lows (5-10 feet thick). The density of the depositional sites has increased as the cones are frequently only 3000 feet apart instead of 5000 feet apart as noted in the isopach maps of the upper group. Lower Group This group contains the four isopach maps from numbered tar zones 35, 36, 37 and 38. It is the most important group as it contains three of the four most significant pay zones and contains 48.5% of the bitumen resource. The isopach patterns are complex and show inverse relationships of sand thickness from one isopach map to the next. This is caused by lateral shifting of the sands from one depositional site to another through time and is a common feature of channel and deltaic sedimentation. The depositional sites are commonly fe apart. The major trend of sand influx is consistently N50 E. The map of Zone 3 5 is based on 7 9 drill hole intercepts that have an average thickness of 36.2 feet (range feet) with a bitumen grade of 16.9gpt. The zone contains 12.0% of the bitumen resource and is one of the four most important pay zones. The three principal depositional sites are located near the Central Overlook, Bruin Point and beyond Range Creek at drill site A-68. This suggests a first pulse of deposition

45 near the Roan Cliffs and a second pulse located about 5000 feet downdip. The largest depositional site is located near the Central Overlook and contains MS-3 and drill holes GN-11 and A-6. Measured Section 3 contains the anomalously deep 45 foot scour on the Roan Cliff face. Unfortunately, one would need a helicopter to get a good view of this mega scour which is the largest ever noted within sixty-four measured sections completed on the area. The major trend of sand influx is N50 E. The depositional system around the Central Overlook has symmetrical bimodal patterns. Lindsay, Prior and Coleman (1984) noted that sediments associated with the Mississippi delta distributaries often accumulate in symmetrical bimodal patterns that probably form as a result of river plume dynamics. The data from the RCT drill holes relogged in 1989 were not posted in the computer data base, so new isopach lines were redrawn by hand. Data from GN-5A was not used as the nearby, some 70 feet away, A-24 drill core was logged by myself and contains data with a higher degree of confidence. When this isopach map from Zone 35 is overlain on the isopach map of Zone 36, there is an inverse relationship of the distribution of highs and lows. The isopach map of Zone 3 6 is based on 77 drill hole intercepts and has an average thickness of 52.6 feet (range feet) with a bitumen grade of 17.4gpt. Zone 3 6 is the most productive pay zone in the area and accounts for 14.6% of the total bitumen resource. Zone 36A (old 36) and 36B (old 99) were combined to make one interval and a more meaningful isopach map of Zone 36. The principal site of deposition is Bruin Point. The major trend of sand influx is N50 E. This parallels the main ridge line from the Shell Curve to Bruin Point. The principal site of deposition at Bruin Point has symmetrical bimodal patterns based on two adjacent highs with maximum sand thicknesses of 125 feet. Another site of major deposition exists near the Water Tower and the proposed pilot mine site in the North Area. A minor site of deposition exists near the South Knoll on the right portion of the map. Another minor site exists near the bird's foot area in the upper left portion of the map centered on drill hole A-39B. The main portion of sand deposition exists between the Roan Cliffs and Range Creek. The computer generated isopach lines toward the West Tavaputs Plateau east of Range Creek are considered too high as based on stratigraphic thinning noted in measured sections. Drill hole A-66 is located in the West Tavaputs Plateau but the thickness of Zone 36 cannot be determined as the hole was T.D.'d after penetrating 14 feet of clean sand in Zone 36. The isopach map of Zone 37 is based on 59 drill hole intercepts that have an average thickness of 47.1 feet (range feet) with a bitumen grade of 18.5gpt. Zone 37 is the second most productive pay zone in the area and accounts for 13.2% of the total bitumen resource. The major sites of

46 deposition are in the vicinity of Bruin Point and the Central Overlook and extend downdip toward Range Creek. This area contains clusters of depositional sites that are feet apart. The highs contain feet of sands, while the lows contain feet of sands. The lows are commonly laterally adjacent to the highs. The stacking relationship of highs and lows from Zones 37 to 3 8 or 37 to 36 continue to be inverse and attest to the lateral shifting of depositional sites. This feature is very characteristic of deltaic systems. The main trend of sand influx is N50 E which parallels the main ridge line from the Shell Curve to Bruin Point. The isopach map of Zone 38 is based on 55 drill hole intercepts that have an average thickness of 49.4 feet (range feet) with bitumen grades of 18.4gpt. Zone 38 contains 8.7% of the total bitumen resource. The principal sites of deposition continue to be the Bruin Point-Central Overlook area and downdip toward Range Creek. The sites of major, deposition are about feet apart. The major trend of sand influx is about N50 E. The.area near Bruin Point and the North Overlook is marked by symmetrical bimodal patterns. The isopach map illustrates the irregular hummocky surface associated with numerous highs and lows. The relief from these highs to the lows ranges from feet per 1000 feet. In the North Area the isopach lines are only partially developed and trends are difficult to establish because of the thin ridge line that dominates the North Area. Bottom Group This group contains the four isopach maps from numbered tar zones 41, 42, 43 and 45. This bottom group contains 16.5% of the total bitumen resource. These isopach maps contain numerous important sites of sand deposition within an area that continues to decrease in size with increasing depth. The base of the tar sand deposit is shaped like a shallow bowl with the deepest portion some 1200 feet below Bruin Point. Since the deepest portion of the gently arcuate base of saturation exists in the area defined by North Overlook- Bruin Point-Asphalt Mine, these four isopach maps appear to shrink toward Bruin Point. The isopach map of Zone 41 is based on 42 drill hole intercepts that have an average thickness of 76.2 feet (range feet) with a bitumen grade of 17.6gpt. Zone 41 contains 5.8% of the total bitumen resource. The map shows seven major deposition centers located near North Overlook-Bruin Point- Central Overlook, South Knoll and the Water Tower. The major trend of sand influx is N50 E and centered near Bruin Point and the North Overlook. Symmetrical bimodal patterns of sand

47 deposition exist on either side of the main distributary that feeds the Bruin Point area. The trend of this main distributary parallels the ridge line from the Shell Curve to Bruin Point. The principal sand clusters exist between the Roan Cliffs and Range Creek. When the isopach maps of Zone 38 and 41 are superimposed, the highs and lows are reversed and illustrate inverse relationships caused by lateral shifting of the sand deposits. Some 3000 feet southeast of the Central Overlook the anomalously tight interval should be disregarded as there is an unresolved discrepancy between adjacent drill hole data of A-24 and GN-5. The isopach map of Zone 4 2 is based on 27 drill hole intercepts with an average thickness of 60.7 feet (range feet) and an average bitumen grade of 18.5gpt. This zone contains 6.2% of the total bitumen resource. The principal site of deposition is beneath Bruin Point and the North Overlook. The major trend of sand influx is N55 E. A second important site of sand deposition is located beneath the Central Overlook. A third important site of sand deposition exists to the west of the Water Tower. The sands in Zone 42 are mainly deposited between the Roan Cliffs and Range Creek and thin toward Range Creek and the West Tavaputs Plateau. The upper surface of the sand has an irregular hummocky nature with highs from 80 to 115 feet thick and lows from 5 to 35 feet thick. The distance between major depositional centers is about feet. The isopach map of Zone 43 is based on 15 drill hole intercepts that average feet in thickness (range feet) with a bitumen grade of 17.3gpt. The thick tar zones in the Asphalt Mine are associated with Zone 43 as seen in Photo 3. This zone contains 2.8% of the total bitumen resource. A major deposition center is clustered around Chevron drill holes CR-25, CR-12 and CR-23. The major trend of sand influx is N75 E. This zone contains limited data as most wells do not penetrate to this depth since it is often well below the base of saturation. The isopach map of Zone 45 is based on 26 drill hole intercepts that have an average thickness of 35.9 feet (range feet) with grades of 16.4gpt. This zone contains 1.7% of the total bitumen resource. The principal tar sands are associated with the area between the Central Overlook and the North Overlook or, in other words, on either side of the Asphalt Mine. The trend of the major influx of sand is some N50 E and nearly parallels the ridge line between the Shell Curve and Bruin Point

48 Interpretation The overall geometry of these sandstone zones is defined by the isopach maps. These geometric patterns reflect variations in sandstone thickness and are dominated by piles of thick intervals or highs and adjacent depressions of thin intervals or lows. These highs and lows represent an irregular hummocky type topography at the top of the isopach maps. These separate isopach maps clearly indicate that the sandstone thicknesses are not uniform as suggested in the panorama of Photo 2. It appears as though uniform sheet sands are the exception rather than the rule. The sandstone bodies must represent either stream channel deposits, distributary channel deposits, distributary mouth bar deposits, or beaches and dunes. Stream Channel Deposits: Within the isopach maps it is very difficult to establish S-shaped' or meandering patterns between the Roan Cliffs and Range Creek. Epsilon cross bedding, shale laminations and log fragments are commonly associated with point bar deposits from channels in the alluvial plain or upper coastal plain. In the Sunnyside Tar Sands epsilon cross bedding is rare and shale laminations or drapes are not abundant. Log fragments are abundant on a small portion of the Asphalt Mine. Bell-shaped well log curves are considered a characteristic feature of channel deposits; bell-shaped well log curves are not common but do exist in the lowest portions of the tar sand deposit. Abrupt pinchouts of sand are a feature of stream channel deposits. Abrupt pinchouts of sand exist in outcrops of tar zones in the bottom group. Stream channel deposits are common in the bottom group of tar zones. Distributary Channel Deposits: Trends of sand influx from all four groups of tar zones are oriented northeast to east. The trends in the bottom group are N50-75 E; those in the lower group are consistently N50 E; those in the middle group, are N50-65 E; and those in the upper group are N75-90 E. These slight changes in orientation suggest shifting of the paleodrainage directions. Lateral shifting of drainage directions is a characteristic feature of channel and deltaic systems. Limestones that formed in shallow water lacustrine environments exist beneath nearly every sandstone zone. The sandstones often scoured the limestones to depths between 1-5 feet. The scouring of the limestones is interpreted to be from distributary channels in a lake shoreline fringe or lower coastal plain; and not from stream channels located up in the alluvial plain or upper coastal plain. Cylindershaped well log curves are a characteristic feature of distributary channel deposits and are frequent in the well logs of the Sunnyside Tar Sands. The isopach maps are characterized by irregular thicknesses of sandstones with lows of feet and highs of feet. It appears as

49 though some smoothing of the highs and lows has occurred. The sands are definitely not uniform as the isopach maps characteristically portray a hummocky surface with both convex and concave components. These piles of sand suggest deposition associated with distributary channels. Distributary Mouth Bar Deposits; Distributary mouth bars form at the terminus of distributary channels. Lindsay, Prior and Coleman (19 84) noted that the sediments that form at the terminus of the Mississippi delta distributaries often accumulate with symmetrical bimodal patterns. Near Bruin Point piles of highs and lows frequently have symmetrical bimodal patterns. The lower and middle groups contain numerous distributary mouth bar deposits that are marked by symmetrical bimodal patterns. The maximum activity of the Sunnyside lacustrine delta occurred during the formation of the lower and middle groups. The highs of one isopach map commonly occur over the lows of the next map, either above or below, and attest to lateral shifting of deposition centers from one stratigraphic sequence to another. The depositional centers in the upper group are commonly feet apart, while the depositional centers in the lower group are commonly feet apart. Since the depositional centers of the upper group are further apart than those of the middle, lower and bottom groups, it suggests the delta activity was declining within Garden Gulch time. The delta activity and presence of sandstones is very limited above the Blue Marker within the Parachute Creek Member or lake facies. The various northeast-southwest trending ridge lines that extend off the northwest trend of the Roan Cliffs represent paleodrainage trends and help to define some details of the lacustrine delta system that dominates the Sunnyside Tar Sands. Beach and Dune Deposits; The beach deposits noted in the field are commonly less than ten feet thick and rarely qualify as a numbered tar zone. They would, therefore, be difficult to delineate on these isopach maps that are contoured at 5 foot intervals. The isopach maps lack the linear aspects of beaches; cheniers (a type of relict beach ridges); or the elongate aspects of offshore bars. The isopach maps do contain the highs and lows that are often associated with dunes. However, the sand grains are 72% angular to subangular with only 10% rounded to well rounded. No frosting of any grains has been noticed. Since the grains are not rounded, subrounded or frosted, it is difficult to make a case for dune deposits Q7

50 Synopsis A synopsis of the separate isopach maps indicates the following: 1. The tar sands are not of uniform thickness and are characterized by distinct areas of thickening and thinning within each separate isopach map. Commonly sites of high deposition have laterally adjacent areas of low deposition. 2. The isopach maps show inverse relationships of sand thickness from one isopach map to the next. This feature indicates lateral shifting of sand deposition from one zone to the next. 3. Extensive accumulations of tar sands exist along the Roan Cliff face near North Overlook, Bruin Point and the Central Overlook. 4. The fifteen numbered tar zones have been separated into four groups that contain different types of deposits. The bottom group contains stream channel and distributary channel deposits. The lower and middle groups are characterized by distributary channel and distributary mouth bar deposits. The upper group is characterized by beach deposits and minor distributary mouth bar deposits. 5. Trends of sand influx for all four groups are oriented northeast. The trends in the bottom group are N50-75 E. Those in the lower group are consistently N50 E. Those in the middle group are N50-65 E. Those in the upper group are N75-90 E. These changes in trends of sand influx suggest slight lateral shifting of paleodrainage directions. The main northeast trending ridges that extend off the Roan Cliffs contain the main feeders to the Sunnyside delta complex. 6. The depositional centers in the bottom, lower and middle groups are commonly feet apart, while those in the upper groups are commonly feet apart. This suggests the delta system is dimishing in activity as one goes up section

51 MEASURED SECTIONS Three measured sections were completed in the South Area to determine continuity of the tar zones within the "hot spot". These three sections exist in the well-exposed cliffs south of the South Overlook. The measured sections are about 1000 feet apart. They are numbered sequentially from north to south as MS-62, 63 and 64, and located in Figure 24. The tar zone data from these three measured sections is included in Table 5. MS-64 contains Zone 26 of the carbonate interval. This was helpful to establish the position of Zone 31. These three measured sections contain bituminous Zones 31, 32, 33 and 35 as noted on the strip logs in Volume II. In the southern portion of the South Area the "hot spot" is represented by Zones 31 and 32. The bituminous content decreases both vertically downward and laterally to the south. Tar Zones 31 and 32 are the richest (3-llwt% bitumen) with diminishing bitumen content in zones 33 and 35 (0.1-7wt% bitumen). The base of saturation is climbing irregularly to the south. The base of saturation exists at elevations of 9365 feet in Zone 36 of MS-62, at 9510 feet in Zone 34 of MS-63, and at 9475 feet in Zone 35 of MS-64. The highlights of each measured section are listed below: MS-62 Highlights 1. TSAT 155 DSAT 0 MSAT 129 BSAT 309 or 9365 ft. 2. Three thick MSAT's & two thin MSAT's. Zone Thickness 35ft. 30ft. 10ft. 44ft. 8ft. Grade 18.4gpt 14.4gpt 15.9gpt 13.0gpt 8.1gpt Excellent exposures of tar sands & sequence stratigraphy. Bitumen content commonly highest in fine grained sandstones with medium scale, medium angle trough crossbedding. Grain size & sedimentary structure are both important controls for bitumen content

52 MS-63 Highlights 1. TSAT 62 DSAT 0 MSAT 49 BSAT 170 or Zones 31 & 32 represent only MSAT's Zone Thickness Grade ft. 19ft. 12.8gpt 9.7gpt 33 10ft. 6.8gpt 3. Grades of other tar zones are low. 4. Ostracodal content of limestones has decreased. 5. Limestones commonly exist unconformably below tar sand zones. 6. The repetition of a cycle containing from bottom to top, SS-SH-LS-UNCONFORMITY is common and each complete cycle represents a sequence. MS-64 Highlights 1. TSAT 116 DSAT 93 MSAT 69 BSAT 345 or 9475 ft. 2. Zone 31 is the only good tar zone., Zone Thickness 49ft. 21ft. 22ft. 33ft. Grade 18.5gpt 9.7gpt 2.3gpt 0.4gpt 3. The lower portion of the Carbonate Interval is well exposed above the most significant tar zone. The limestone exposures are in Zone This is the first measured section south of the South Overlook (top of MS-6) that has good exposures of portions of the Carbonate interval. 5. Zone 36 is at least 100 ft. thick and is totally nonbituminous. The two most salient features of the 1990 measured section work are: (1) repetition of upward fining cycles is common. Each cycle from the bottom to top is dominated by sandstoneshale-limestone-unconformity. Each complete cycle represents a sequence as used by Van Wagoner, et al (1990). Repetitious sequence stratigraphy persists in the South Area and the pay zones are confined to the bituminous sandstones. (2) The bitumen content is commonly highest in fine grained sandstones with medium scale, medium angle trough crossbedding. This suggests that both grain size and sedimentary structures have an important control over porosity and permeability and thus bitumen content

53 STRUCTURE Book Cliffs The sedimentary beds in the Book Cliffs strike northwest and dip some 7-10 northeast. The impressive pile of rocks in the Book Cliffs are best seen in the late afternoon sun. Regional faults are not abundant in the area, but important local faults do exist. The Book Cliffs are part of the extreme northeastern portion of the San Rafael Swell. This major anticlinal uplift is some one hundred miles long by fifty miles wide and has a north-northeast trend. Both strike faults and diagonal faults exist in the Sunnyside area. Strike faults-parallel the regional trend of the Book Cliffs and are visible in underground coal mines. The Sunnyside fault is the largest strike fault and has displacements ranging between 1-35 feet. Underground this fault commonly consists of three separate steps or blocks with almost vertical, clean, abrupt breaks as seen in slides from the Sunnyside No. 2 Mine (personal communication, 1990, Lynn Huntsman). The main portion of the Sunnyside fault has displacements up to feet and prevails in the Sunnyside mine south of Fan Canyon; north of Fan Canyon the displacements have magnitudes of 1-4 feet (Osterwald, 1962). The strike of the Sunnyside coal seam parallels the trend of the Sunnyside fault. The coal seams dip to the northeast with an average grade of ten percent (5.7 ) but have dips of twenty-two percent (12.5 ) near the outcrop (personal communication, 1986 and 1987, Lynn Huntsman). Diagonal faults cut across the regional trend or strike of the Book Cliffs and have displacements of feet. The diagonal faults are visible in both underground coal mines and surface outcrops. These diagonal faults are almost cross faults and have larger displacements than the strike faults. At Sunnyside diagonal faults are best exposed in Slaughter Canyon as mapped by Maberry (1968). The Columbia-Geneva fault has an overall trend of N70 E with displacements of feet (Dunrud and Barnes, 1972). This important diagonal fault separates the Columbia Mine from the Geneva Mine (see Figure 25). Joint patterns within the Book Cliffs are reasonably consistent. They consist of a strong dominant N66-68 E trend and two secondary, less intense, north and northwest trends. The north trend is between N7 W-N14 E and the northwest trend is bewteen N23 W-N78 W. Along the Book Cliffs the joint data is based on joint measurements recorded by Osterwald, et al (1981). This data base contained no reference to joints that are parallel to bedding. The data was re-evaluated to determine the statistically dominant joint trends illustrated

54 in Figure 25. The strong dominant northeast trend represents the tension joint that nearly parallels the regional dip. The two secondary joint trends form the planes of conjugate shear. In Whitmore Canyon a regional structure is associated with the Book Cliffs and Roan Cliffs. The crest of the Book Cliffs with elevations up to feet is separated from the crest of the Roan Cliffs with elevations up to feet by three to five miles. In other words, Whitmore Canyon locally separates the Book Cliffs from the Roan Cliffs. The large area north of Grassy Trail Reservoir and between the Left Fork and Right Fork of Whitmore Canyon contains a block of essentially horizontal rocks. This can be noticed from the Shell curve on the road to Bruin Point. On a large scale the Book Cliffs and Roan Cliffs represent inclined blocks between the flat Whitmore Canyon block and the flat West Tavaputs block. This large scale regional structure is best seen from drill site RCT-1, located in SE/4, section 15, T14S, R14E. Roan Cliffs The structure within the Roan Cliffs is a simple monocline that contains a segmented flexure with a subtle surface expression. The monocline is visually apparent in the field and specifically defined by the Structure Contour Map of the Blue Marker which shows a relatively uniform monocline that dips 3-7 to the northeast. The segmented flexure begins where the regional dip of three degrees starts to gradually increase to seven degrees. The subtle changes in dip and related structural evidence for the segmented flexure were determined from mapping in 1986, 1987 and This segmented flexure exists within the monocline and trends northwest. It contains a western, central and eastern segment. The position of the flexure coincides with areas of increasing dips defined by the Structure Contour Map of the Blue Marker (see 1989 Exploration Report). The main axis of the flexure exists along the lineament in upper Range Creek and continues northwestward to slightly east of Mount Bartles (see Regional Geology Map). Numerous chaotic slump blocks and northwest trending linear troughs define the northwestern portion of the Mount Bartles-Bruin Point flexure (see Geology Map, 1989 Exploration Report). This N20-40 W trending flexure is divided into three segments based on differences in regional dips and bitumen content. The beds in the western segment have dips of 4-12 northeast and sandstones that contain 4-12wt% bitumen. The western segment contains the vast majority of the tar sands. The main axis of the flexure separates the western and central segments. The beds in the central segment ~ 01412

55 have dips of 4-7 northeast and sandstones that contain 4-7wt% bitumen. The beds in the eastern segment have dips of 3-5 northeast and sandstones that contain 0-4wt% bitumen. The eastern segment of the flexure exists within the West Tavaputs Plateau. Joint patterns within the Roan Cliffs contain prominent northeast and northwest trends. The joint data is based on 1232 joint measurements recorded by O'Sadnick (1982) in the area near the Asphalt Mine and Bruin Point. This data was utilized to determine the dominant joint trends illustrated in Figure 25. The northwest trends of the joint patterns parallel the N W trend of the Mount Bartles-Bruin Point flexure. The northwest joint patterns parallel the regional strike of the beds. The northeast joint patterns parallel the regional dip of the beds. Faults within the Roan Cliffs are scarce and have minimal displacements of one to five feet, Slickensides were often noted in the drill core. The trends of the joint patterns in the Book Cliffs are similar to the trends of the joint and fault patterns in the Roan Cliffs (see Figure 25)

56 ENGINEERING GEOLOGY Various categories of engineering geology were examined during the field work on the long conveyor routes needed to transport the tar sands down from the Roan Cliffs through the Book Cliffs to the proposed plant site location in Clark Valley. The proposed conveyor routes were laid out by Pincock, Allen and Holt, Inc. with maximum grades of fifteen degrees, are 6-10 miles long and include foot tunnels. The proposed north and south conveyor routes are indicated on the Regional Geology Map. Field work on these two routes was completed in June The various categories of engineering geology have been separated into major and minor factors based on applicability to construction and maintenance conditions. Major Factors The major aspects of engineering geology to consider for the conveyor routes are related to the following four items: (1) box canyons; (2) potential rockfalls; (3) steep cliffs; and (4) structural analysis for tunnel orientation and portal location. Item (1) Box Canyons: The west side of the Book Cliffs contains the Castlegate Sandstone that forms the lower box canyon unit and the Bluecastle Sandstone Member of the Price River Formation that forms the upper box canyon unit. Portions of these box canyons can be seen in Photos 6, 8 and 11. Box canyons can present formidable geographic barriers to construction and are also loci for flash floods and rockfalls. Massive blocks from the Castlegate Sandstone and the Bluecastle Sandstone Member exist in the canyon floor of the South Conveyor Route on the west side of Book Cliffs. Item (2) Potential Rockfalls: The Castlegate Sandstone is particularly susceptible to rockfalls because of its closely spaced joint pattern. Areas of massive rockfalls exist on the west side of the Book Cliffs near Fan Canyon as noted on the Regional Geology Map and Photo 6. These massive rockfalls were caused by longwall mining of the Sunnyside coal seam that is located 150 feet below the base of the Castlegate Sandstone. Major rockfall potential is associated with the Castlegate Sandstone. Moderate rockfall potential is associated with the Bluecastle Sandstone Member of the Price River Formation. Minor rockfall potential is associated with the upper member of the Colton Formation (see Photos6, 8 and 10). In general the tighter the canyon the more severe is the potential for damaging rockfalls and increased maintenance costs

57 Item (3) Steep Cliffs: The upper member of the Colton Formation consists of foot cliffs that represent formidable barriers. This is particularly noticeable in Photos 9 and 10. Conveyor routes should avoid these steep cliffs. Item (4) Structural Analysis for tunnel orientation and portal location: Figure 2 shows the location of the proposed tunnel and alternative tunnel through the Book Cliffs. Figure 25 summarizes the orientation of joint sets and faults in the area of the Book Cliffs and Roan Cliffs. It is based on 2605 joint measurements as well as surface and subsurface data on faults. Whenever possible tunnels should be oriented at oblique or near perpendicular angles to the prevailing rock fabric, and orientations that parallel major structural trends should be avoided (personal communication, 1990, Howard Earnest, mining engineer and manager of operations, Rio Blanco Oil Shale Company). Interpretation of the structural analysis shown in Figure 25 suggests that the best orientations for tunnels through the Book Cliffs would trend about N3 0 E or N40 W. Note the motor road alignment of the Sunnyside No. 1 Mine is oriented N4 0 W±5 as seen in Figure 2. Within the Book Cliffs the proposed north conveyor route is oriented N50-55 E and parallels the straight alignment of B Canyon. The proposed tunnel is oriented N55 E and nearly parallels the major joint trend of N67 E. Figures 2 and 25 illustrate this data. The orientation of the proposed tunnel is at an unfavorable oblique angle of 12 to the major joint trend. In addition, the west portal of the proposed tunnel is located in relatively incompetent rocks of the lower member of the Colton Formation and at an elevation near 7800 feet. The east portal of the proposed tunnel is at a favorable outcrop location near 8000 feet in elevation and exists in competent sandstone outcrops of the lower to upper Colton Formation. On the west side of the Book Cliffs an alternative tunnel location with a good west portal site near feet in elevation exists in the Left Fork of A Canyon. Here the west portal site is in the Bluecastle Sandstone Member or upper box canyon unit. The alternative tunnel would be oriented N15 E. This orientation has a favorable oblique angle of 52 to the major joint trend of N67 E, an oblique angle of 22 to the secondary joint trend of N7 W and a 93 angle to the tertiary joint trend of N78 W. As seen in Figure 25 all joints are essentially vertical. Near horizontal joints that parallel bedding planes do not exist in the data base. The alternative tunnel would intersect the east portal of the proposed tunnel as shown in Figure

58 Minor Factors The minor aspects of engineering geology for the conveyor routes and tailings area are related to the following seven items: (1) landslides, (2) surface deposits, (3) groundwater, (4) earthquake hazards, (5) faults, (6) coal mine subsidence, and (7) Mancos Shale. Item (1) Landslides: Four areas of active landslides exist near Whitmore Canyon and are indicated on the Regional Geology Map. Two are in the lower portion of Water Canyon, one is located near Grassy Trail Reservoir and one is in the lower portion of the Right Fork of Whitmore Canyon. These known areas of active landslides were caused by excessive amounts of rainfall in short periods of time. The two large landslide areas in the right side of the lower portion of Water Canyon started to form in and are still active. Small active landslides exist on both sides of the dam at Grassy Trail Reservoir; these slides were activated in the rainy summer of This is the same year that the massive wellpublicized Thistle Slide occurred some 25 miles west of Soldier Summit on Route 6 between Price and Provo. Beyond Grassy Trail Reservoir another large landslide area is adjacent to the Right Fork of Whitmore Canyon and located in the SE/4, section 31, T13S, R14E. This area contains an old inactive landslide in the left lobe with 2-4 feet headwall scarps and no ponded water; on the right lobe there is an active landslide area denuded of trees that formed sometime between 1982 and Even if this entire slide area of the left and right lobes became larger and more active, a natural buttress exists just before the confluence with the Right Fork of Whitmore Canyon. This massive natural buttress would protect a conveyor line built on the right or southeast side of the Right Fork of Whitmore Canyon. Item (2) Surface Deposits: The thickest alluvium deposits exist in Clark Valley where they are commonly feet thick. Other alluvium and colluvium deposits in the area are relatively thin and should present no engineering problems. Soil horizons throughout the area are relatively thin (commonly 0-2 feet) and should be stockpiled for redistribution after any construction. Item (3) Groundwater: Springs were not seen along any of the conveyor routes. The sandstone units of the North Horn Formation are underground aquifers (personal communication, 1990, Byron Allred) and these will be intersected in a tunnel through the Book Cliffs as seen in the cross section in Volume II. Rates of water flows from this sandstone aquifer are not known

59 Item (4) Earthquake Hazards: The principal earthquakes in the State of Utah occur along the active Wasatch Fault Zone that passes through Salt Lake City (see Figure 26). The Castle Valley and Price area experience relatively mild earthquakes that are commonly in the range of 2-4 on the Richter scale. On August 14, 1988 the Castle Valley area had three tremors (3.5, 4.3 and 5.6) and on August 18, 1988 there were two more tremors (5.4 and 5.6). These earthquakes were centered within a remote area of the San Rafael Swell about 34 miles south of Price, 14 miles east of Ferron and some 41 miles southwest of Sunnyside. On August 14 Rob Roy and I were in Denver. On August 18 Rob Roy and I were in the core shack at Price in the morning and on the mountain near Bruin Point in the afternoon. We did not feel or see anything unusual. In the right hand side of lower Bear Canyon two minor landslides with 3-6 foot headwall scarps were formed during this earthquake (personal communication, 1990,' Byron Allred, surveyor, Sunnyside coal mine). There is an important seismic station at the University of Utah, Salt Lake City and a minor seismic station at the College of Eastern Utah, Price. Item (5) Faults: area are inactive. The faults in the Sunnyside-Bruin Point Item (6) Coal Mine Subsidence: Surface subsidence from coal mining is very minimal over the mined out area of the Sunnyside coal mines. An outline of the area with extensive underground coal mining from is shown on the Regional Geology Map. In 1986 the coal mine at Sunnyside established a surface subsidence network on 500 feet centers. Only two areas of surface subsidence have been determined from the survey. These two locations are both within the lower portion of Bear Canyon as partially indicated in Photo 9. These two locations have experienced up to 0.5 feet of subsidence and both are located over the center of longwall panels that exist some 1400 feet below the surface (personal communication, 1990, Byron Allred). Coal mining in the Sunnyside area was done by room and pillar mining methods until about 1965 and is currently being done by longwall mining methods. The room and pillar method and the longwall method produce two different types of subsidence. The longwall method produces instantaneous maximum subsidence as roof control is lost rapidly. The room and pillar method produces long term slow subsidence as roof control is maintained. These contrasting differences in subsidence are caused by entirely different rock conditions in the roof. In longwall mining the wallrocks are fractured ahead of the mining face, and the area is surrounded by destressed ground in which the rocks have lost their elasticity; this results in instantaneous deformation and initial maximum

60 subsidence. The longwall mining equipment contains hydraulically supported shields that protect the men and equipment during the coal extraction process. In room and pillar mining the wallrocks fracture after mining, and the area is surrounded by stressed ground in which the rocks retain much of their elasticity; this results in delayed deformation and initial minimum subsidence. Partial and ultimate failure of the stressed ground may produce rapid rock bursts and violent shockwaves as well as caving to the surface over long periods of time measured in tens to hundreds of years. Above summarized from Labasse (1965). Item (7) Mancos Shale: After the surface alluvium is stripped from the tailings disposal area, the Mancos Shale will be exposed. The tailings disposal area may or may not be lined depending on the permeability properties of the Mancos Shale and environmental requirements. Even before the stripping operations begin the permeability and other pertinent properties of the Mancos Shale can be tested from hillside exposures in Clark Valley and additional exposures in the Farnham Dome area (see Figure 1A). Conveyor Routes The proposed north and south conveyor routes have been investigated, and the north route is by far the most feasible. Both routes can be separated into a Book Cliffs part and a Roan Cliffs part. The north route can be improved with an alternative tunnel through the Book Cliffs part. The Roan Cliffs part of the north conveyor route that goes from the east portal of the tunnel through the Book Cliffs past Grassy Trail Reservoir and straight up the Right Fork of Whitmore Canyon is free of engineering problems (see Photo 13). The south route is not recommended as there are significant engineering problems associated with both the Book Cliffs part (see Photo 6) and the Roan Cliffs part (see Photo 9). The positive and negative factors of each route and the alternative route are discussed separately. The location of the north and south conveyor routes are shown on the Regional Geology Map. The alternative tunnel route for the Book Cliffs part of the north conveyor route is shown in Figure 2. On July 10, 1990 portions of the north and south conveyor routes and the alternative tunnel route were examined with Howard Earnest, mining engineer and manager of operations, Rio Blanco Oil Shale Corporation. The north conveyor route goes up B Canyon, tunnels through an upper portion of the Book Cliffs, comes out of the Book Cliffs near Grassy Trail Reservoir, then goes across the northern portion of Grassy Trail Reservoir, and finally straight up the

61 Right Fork of Whitmore Canyon with a transfer station at 9300 feet near the crest of the Roan Cliffs. This route is shown on the Regional Geology Map. Positive factors: Negative factors: a) short and direct with a 4000 foot tunnel b) good east portal rock in sandstones of lower Colton Formation c) open valley of Right Fork of Whitmore Canyon with limited landslide potential and good potential for winter sun d) avoids mined out areas of Sunnyside coal seam. a) B Canyon is tight without much winter sun b) must negotiate upper box canyon unit c) poor location of west portal in shale slopes of lower Colton Formation near an elevation of 7800 feet, and some 400 vertical feet above upper box canyon unit d) potential rockfalls from both the Castlegate Sandstone (lower box canyon unit) and the Bluecastle Sandstone Member (upper box canyon unit) e) tunnel orientation of N55 E subparallels major joint direction of N67 E with secondary joint directions of N78 W and N7 W. The south conveyor route goes up the unnamed canyon northwest of Fan Canyon, goes into the Book Cliffs in the lower box canyon unit, comes out of the Book Cliffs near Bear Canyon and goes up the ridge line between Bear Canyon and Water Canyon to the transfer station at 9300 feet near the crest of the Roan Cliffs. This route is shown on the Regional Geology Map. Positive factors: None other than it is the most feasible way to bring tar sands down from the south area of the deposit. Negative factors: a) b) c) two box canyon units in tight drainage of Book Cliffs severe rockfall potential severe flash flood potential noted by levees in lower portion of drainage in Book Cliffs

62 d) east portal of tunnel through Book Cliffs is in surface debris and relatively incompetent rocks of the North Horn Formation and Flagstaff Limestone e) prominent cliffs along route between Bear Canyon and Water Canyon f) route passes over workings of underground coal mine for some 11,000 feet g) tunnel orientation of N45 E subparallels major joint direction of N67 E with secondary joint trends of N78 W and N7 W. The alternative route for the Book Cliffs part of the north conveyor route goes southeast from the proposed plant site, then up the Left Fork of A Canyon to the Bluecastle Sandstone Member (upper box canyon unit) located at the joint pattern shown on the Regional Geology Map in the NW/4, SE/4, section 13, T14W, R13E. Hence, via a 6400 foot tunnel oriented N15 E to the east portal site of the proposed tunnel. The locations of the alternative tunnel and the proposed tunnel are shown in Figure 2. Positive factors: Negative factors: a) open canyon that avoids the lower box canyon unit and uses the upper box canyon unit as a portal b) minimizes potential rockfall hazard c) an open canyon that would provide good winter sun d) west portal at elevation near 7600 feet e) tunnel orientation of N15 E forms maximum obtuse angle with the major joint direction of N67 E and secondary joint directions of N78 W and N7 W f) minimizes potential of flash floods g) unmined Sunnyside Coal Seam is well oxidized and of very limited economic interest; SRS Inc. is looking at the Right Fork of A Canyon for belt entries (personal communication, 1990, Byron Allred). a) alternative tunnel through Book Cliffs is about 2400 feet longer than proposed tunnel b) conveyor line is about 2000 feet longer

63 REFERENCES American Association of Petroleum Geologists, 1961, American Commission on Stratigraphic Nomenclature: Amer. Assoc. Petrol. Geol., v. 45, no. 5, p Arabasy, W.J., Smith. R.B., and Richins, W.D., 1979, Earthquake studies in Utah 1850 to 1978: University of Utah Seismograph Studies Special Publ., 552 p. Armstrong, R.L., 1968, Sevier orogenic belt in Nevada and Utah: Geol. Soc. America Bull., v. 79, no. 4, p Averitt, P., 1966, Coking-coal deposits of the Western United States: U.S. Geol. Survey, Bull G, 48 p. Balsley, J.K., 1982, Cretaceous' wave-dominated delta systems: Book Cliffs, East Central Utah: Guidebook (private publication) for Amer. Assoc. Petroleum field trip, 219 p. Banks, E3T., 1981, Petrographic characteristics and provenance of fluvial sandstone, Sunnyside oil-impregnated sandstone deposit, Carbon County, Utah: unpubl. M.S. thesis, Univ. of Utah, 111 p. Bradley, W.H., 1929, Algae reefs and oolites of the Green River Formation: U.S. Geol. Survey, Prof. Paper 154-G, p Brodsky, H., 1960, The Mesaverde Group at Sunnyside, Utah: U.S. Geol. Survey open-file report No. 5 95, 7 0 p. Busch, D.A., 1974, Stratigraphic traps in sandstones-exploration techniques: Amer. Assoc. Petroleum Geologists, Memoir 21, 174 p. Calkin, W.S., 1981, Geologic Summary Report of the Sunnyside Tar Sands Project, Carbon County, Utah: 2 Volume Report for Amoco Minerals Company, dated February 4, 1981., 1982, Geologic Summary Report of the 1981 Exploration Program, Sunnyside Tar Sands Project, Carbon County, Utah: 2 Volume Report for Amoco Minerals Company, dated February 24, 1982., 1983, Geologic Summary Report of the 1982 Exploration Program, Sunnyside Tar Sands Project, Carbon County, Utah: 3 Volume Report for Amoco Minerals Company, dated June 30, 1983., 19 85, Geologic Summary Report of the 1984 Exploration Program, Sunnyside Tar Sands Project, Carbon County, Utah: 3 Volume Report for Amoco Corporation, dated June 30,

64 Calkin, W.S., 1987, Geologic Summary Report of the 1986 Exploration Program, Sunnyside Tar Sands Project, Carbon County, Utah: 3 Volume Report for Amoco Corporation, dated May 19, 1987., 1988, Geologic Summary Report of the 1987 Exploration Program, Sunnyside Tar Sands Project, Carbon County, Utah: 3 Volume Report for Amoco Corporation, dated June 1, 1988., 1989, Geologic Summary Report of the 1988 Exploration Program, Sunnyside Tar Sands Project, Carbon County, Utah: 3 Volume Report for Amoco Corporation, dated June 1, 1989., 1990, Geologic Summary Report of the 1989 Exploration Program, Sunnyside Tar Sands Project, Carbon County, Utah: 3 Volume Report for Amoco Corporation, dated July 30, Chamberlain, C.K., 1978, Recognition of trace fossils in cores: in Trace Fossil Concepts, SEPM Short Course No. 5 (ed. P.B. Basan), p Clark, F.R., 1928, Economic geology of the Castlegate, Wellington and Sunnyside quadrangles, Carbon County, Utah: U.S. Geol. Survey Bull. 793, 165 p. Connan, J., 1984, Biodegradation in crude oils in reservoirs in Advances in Petroleum Geochemistry: (eds. J. Brooks and D. Welte), vol. 1, p Doelling, H.H., 1972, Central Utah coal fields: Sevier- Sanpete, Wasatch Plateau, Book Cliffs and Emery: Utah Geol. and Mineral. Survey Monograph Series No. 3, p Doelling, H.H., Smith, A.D., Davis, F.D., and Hayhurst, D.L., 19 79, Observations on the Sunnyside coal zone, Utah: Utah Geol. and Mineral. Survey, Special Study 49, p Dunrud, C.R., 1976, Some engineering geologic factors controlling coal mine subsidence in Utah and Colorado: U.S. Geol. Survey PP-969, 39 p. Dunrud, C.R. and Barnes, B.K., 1972, Engineering geologic map of the Geneva Mine area, Carbon and Emery Counties, Utah: U.S. Geol. Survey Map Falini, F., 1965, On the formation of coal deposits of lacustrine origin: Geol. Soc. Amer. Bull., vol. 76, p Goddard, E.N., et al, 1963, Rock Color Chart: Geol. Soc. Amer. Hale, L.A. and van de Graaff, F.R., 1964, Cretaceous stratigraphy and facies patterns - northeastern Utah and adjacent areas in Intermountain Assoc. Petroleum Geologists, 13th annual Field Conf., Guidebook to the Geology and Mineral Resource of the Uinta Basin, p

65 Hansen, G.H. and Bell, M.M., 1949, Oil and gas possibilities of Utah: Utah Geol. and Mineral. Survey, p Hintze, L.F., 1973, Geologic History of Utah: Brigham Young University Geology Studies, vol. 20, part 3. Hunt, C.B., 1956, Genozoic geology of the Colorado Plateau: U.S. Geol. Survey, Prof. Paper Huntsman, L., 1978, The Sunnyside coal mines, Carbon County, Utah, in Guidebook on Fossil Fuels and Metals, Eastern Utah and Western-Southwestern-Central Colorado (ed. D.R. Shawe): Prof. Contri. Colo. Sch. Mines No. 9, p Kelts, K., 1988, Environments of deposition of lacustrine petroleum source rocks: an introduction in Lacustrine Petroleum Source Rocks (eds. A.J. Fleet, K. Kelts and M.R. Talbot): Geol. Society Spec. Publ., No. 4, p Krumbien, W.C., 1942, Criteria for subsurface recognition of unconformities: Amer. Assoc. Petrol. Geol., vol. 26, p Labasse, H., 1965, Ground stresses in longwall and room-andpillar mining: Proc. of Rock Mechanics Symp.; Mines Branch, Dept. Mines and Technical Surveys, Ottawa, Canada, p Lindsay, J.F., Prior, D.B., and Coleman, J.M., 1984, Distributary mouth bar development in delta growth, South Pass, Mississippi Delta: Amer. Assoc. Petrol. Geol., vol. 68, p Maberry, J.O., 1968, Sedimentary features of the Blackhawk Formation (Cretaceous) at Sunnyside, Carbon County, Utah: Colorado School of Mines thesis T-1190., 1971, Sedimentary features of the Blackhawk Formation (Cretaceous) in the Sunnyside District, Carbon County, Utah: U.S. Geol. Survey Prof. Paper 68 8, 51 p. Mahoney, S.R. and Kunkel, R.P., 1963, Geology and oil and gas possibilities of east central Utah in Oil and Gas Possibilities of Utah, Re-evaluated (ed., A.L. Crawford): Utah Geol. and Mineral. Survey Bull. 54, p Mauger, R.L., 1972, A sulfur isotope study of bituminous sands from the Uinta Basin, Utah: 24th Intern. Geol. Congr. Section 5, p

66 McGookey, D.P., Haun, J.D., Hale, L.A., Goodell, H.G., McCubbin, D.G., Weimer, R.J., and Wulf, G.R., 1972, Cretaceous System in Geologic Atlas of the Rocky Mountain Region (ed. W.W. Mallory): Rocky Mt. Assoc. Geologists, 331 p. (oversize). Mitchum, R.J., Jr., 1977, Seismic stratigraphy and global changes of sea level, Part II: Glossary of terms used in seismic stratigraphy in Seismic Stratigraphy-Applications to Hydrocarbon Exploration (ed. C.E. Payton): Amer. Assoc. Petrol. Geol. Memoir 26, p O'Sadnick, D., 1982, Interim Report, Sunnyside Project, Geotechnical and Hydrological Study: Golder Associates Report for Amoco Minerals Company, dated February Osmond, J.C., 1965, Geologic history of the Uinta Basin: Amer. Assoc, of Petrol. Geol. Bull., vol. 49, p Osterwald, F.W., 1962, Preliminary lithologic and structural map of Sunnyside No. 1 Mine area, Carbon County, Utah: U.S. Geol. Survey, Map C-50. Osterwald, F.W., Dunrud, C.R., and Maberry, J.O., 1969, Preliminary geologic map of the Columbia area, Carbon and Emery Counties, Utah: U.S. Geol. Survey, Map Osterwald, F.W., Maberry, J.O., and Dunrud, C.R., 1981, Bedrock, surficial and economic geology of the Sunnyside coal-mining district, Carbon and Emery Counties, Utah: U.S. Geol. Survey, PP 1166, 68 p. i Remy, R.R., 1984, Report on the composition, texture, diagenesis I and provenance of the Sunnyside Tar Sands, Carbon County, [ Utah: report for Amoco Minerals Company, dated December 4, Rozelle, J.R., 1989, Final Report on 1989 update of the computerized geologic model to include the drill hole data, Sunnyside tar sands project, Sunnyside, Utah: report for Amoco Corporation by Rozelle Consulting Services. Sarg, J.F., 1988, Carbonate sequence stratigraphy in Sea- Level Changes: An Integrated Approach (eds. C.K. Wilgus, B.S. Hastings, et al): Soc. Econ. Paleo. Mineral. Spec. Publ. 42, p Serra, 0., 1986, Fundamentals of well log interpretation, 2. The interpretation of logging data: Amer. Elsevier, 684 p. Smith, R.B. and Richins, W.D., 1984, Seismicity and earthquake hazards of Utah and the Wasatch Front; paradiem and paradox in Proceedings of Conference XXVI (eds. W.W. Hays and P.L. Gori): U.S. Geol. Survey Open File Report, OF , p

67 Stokes, W.L. and Madsen, J.H., Jr., 1961, Geologic Map of Utah, Northeast Quarter: University of Utah (scale 1:250,000). Subsidence Engineers' Handbook, 1975, National Coal Board, Great Britain, lllp. Tidwell, W.D., 1975, Common fossil plants of western North America: Brigham Young University, 197 p. United States Steel, Engineering Dept., 1976, Mining Application United States Government "B" Canyon Property: Report of Western District - Coal, dated November 5, Vail, P.R., Mitchum, R.M., Jr., and Thompson, S., Ill, 1977, Seismic stratigraphy and global changes of sea level, Part IV, Global cycles of relative changes of sea level in Seismic Stratigraphy - applications to hydrocarbon exploration (ed. C.E. Payton): p van de Graaff, F.R., 1972, Fluvial-deltaic facies of the Castlegate Sandstone (Cretaceous) east-central Utah: Jour. Sed. Petrol. vol., 42, p Van Wagoner, J.C., et al, 1985, An overview of the fundamentals of sequence stratigraphy and key definitions in Sea-Level Changes - An Integrated Approach (eds. C.K. Wilgus, C.A. Ross, H. Posamentier, and C.G. Kendel): Soc. Econ. Paleo. and Mineral., Special Pubic, No. 42, p Van Wagoner, J.C., Mitchum, R.M., Campion, K.M., and Rahmanian, V.D., 1990, Siliciclastic sequence stratigraphy in well logs, cores, and outcrops: Amer. Assoc. Petrol. Geol., Methods in Exploration Series, No. 7, 55 p. Weiss, M.P., Witkind, I.J., and Cashion, W.B., 1990, Geologic map of the Price 30'x60' quadrangle, Carbon, Duchesne, Uintah, Utah and Wasatch Counties, Utah: U.S. Geol. Survey Map (scale 1:100,000). Wells, L.F., 1958, Petroleum occurrence in the Uinta Basin in Habitat of Oil (ed. L.G. Weeks): p Winters, C, Hughes, R., Wiley, R., Balaz, W., and Hunt, W., 1986, Sunnyside Mines Life-of-Mine Plan 4 Slope Alternative. Vol. I:> Perma Mining Corp., August Wray, J.L., 1977, Calcareous algae: Elsevier, 185 p. Ziemba, E.A., 1974, Oil shale geology, Federal Tract C-a, Rio Blanco County, Colorado in Energy Resources of the Piceance Creek Basin, Colorado (ed. D.K. Murray): Rocky Mtn. Assoc. Geol., p

68 APPENDIX 1426

69 Photo 1. Aerial Mosaic of Sunnyside Tar Sands Area Looking Southeast. The mosaic presents an excellent overall view of the project area. Bruin Point and the Asphalt Mine are the center of attraction. The three principal physiographic features are the Book Cliffs (lower right), Roan Cliffs (left central) and West Tavaputs Plateau (upper left). Noted geographic features in a nearly clockwise direction include the town of Sunnyside (upper right), Fan Canyon, Right Fork A Canyon, Left Fork A Canyon (far right central), B Canyon (lower right), Grassy Trail Reservoir (right central), Mount Bartles (far left), Dry Canyon Ridge (upper left), and Range Creek (upper right). The bituminous sandstones extend along the Roan Cliffs for about seven miles from Mount Bartles to beyond the South Overlook. The tar sands are concentrated along the Roan Cliffs and have been separated into three mineable areas North, Central and South. The Central Area encompasses Bruin Point. The South Area encompasses the South Overlook. The North Area is centered near the red dot at the Pilot Mine Site. The location for the proposed processing plant is at the mouth of B Canyon (lower right). Photo locations for the four panoramas that show the individual numbered tar zones exposed along the Roan Cliffs are indicated by the green dots. The two parts of the 18 0 panorama encompass the South Area and Central Area. The two parts of the North Area panorama were taken from slightly different locations to permit near perpendicular views of the numbered tar zones and to avoid shielding by the numerous topographic ridges that extend to the southwest off the Roan Cliffs. The Asphalt Mine exists at an elevation of 8900 feet. Bruin Point is at an elevation of 10,131 feet. Grassy Trail Reservoir is at an elevation of 7580 feet. The distance from Grassy Trail Reservoir along Whitmore Canyon to the mouth of Bear Canyon is 2% miles. The distance from the top of the Book Cliffs near Grassy Trail Reservoir to Bruin Point is 3% miles. The distance from Bruin Point to the South Overlook is 2h miles. The distance from Bruin Point to Mount Bartles is 4*5 miles. This aerial view also shows the drainage of Range Creek from its headwaters near Bruin Point to its mouth at the Green River. The West Tavaputs Plateau in the upper left is dissected and extends from the Green River to beyond Mount Bartles.

70 H W < lil o m z o < UJ DC < m DC & LU 9 CO : 3 SI' m m ''III < 01428

71 Photo 2. Panorama of Sunnyside Tar Sands, Part I. This photo is the right half of the 180 Panorama taken from Hill The left half of the 180 Panorama is Photo 3. Hill 9429 is located in the NW/4, section 10, T14S, R14E. The South Overlook exists on the far right at the top of MS-6 and is 1.1 miles away. The Central Overlook exists on the far left at the top of MS-3 and 54 and is about 3000 feet away. The topographic saddle to the right of MS-49 separates the South Area on the right from a portion of the Central Area on the left. The South Area contains three to five tar zones whose cumulative thickness ranges between feet. The portion of the Central Area in this photo contains six to eight tar zones whose cumulative thickness ranges between feet. The location of numbered tar zones determined along measured sections are labelled. The measured sections were completed along ridge lines. In some cases the dots have been moved laterally to permit clarity of zone continuity. Unlabelled areas contain no measured sections. Zones 31, 35, 36 and 37 are the four most important tar zones in the area. Bitumen grades and thicknesses of numbered tar zones are listed in Table 4. The Carbonate Interval is defined by the blue dots and represents the sixty foot thick fossiliferous limestone-rich Zones of 25 and 26 with the included shale interburden. The 1-2 foot thick Blue Marker is defined by red dots and exists at the base of the Parachute Creek Member or lake facies with gray shales. Insignificant volumes of tar sands exist above the Blue Marker. The 250 foot thick vertical interval between the red dot and the blue dot contains the Garden Gulch Member or shore facies with green shales. The stratigraphic position of the Blue Marker and Carbonate Interval are also indicated in Figure 19. Tar Zones 31 through 42 exist within the Douglas Creek Member or delta facies with red shales. The sheet sand nature of the numbered tar zones is readily apparent. The isopach maps of the numbered tar zones add another dimension to this view. The beds dip some 6-7 back into the Roan Cliffs. The dashed yellow line is the base of saturation with bituminous sandstones above and nonbituminous sandstones below. In MS-50 an anomalous vertical contact exists in the twenty foot thick Zone 37 and separates 4wt% bituminous sandstones on the left from nonbituminous sandstones on the right. This vertical contact is along a joint (see Photo 9, 1987 Exploration Report).

72 llfc>»p~~ r~'~«<^"? * " n C^h

73 /**,? /?* ** ^ ^ i

74 -Photo 3. Panorama of Sunnyside Tar Sands, Part II. This photo is the left half of the 180 Panorama taken from Hill 9429 and is a composite of three separate photographs. The Asphalt Mine exists at an elevation of 8900 feet, while Bruin Point is at an elevation of feet. The road from the Asphalt Mine to the Shell Curve continues on up the ridge line to Bruin Point. Grades of 15-20% are common on the road. Other roads in the photo lead to drill sites or down Water Canyon. The location of the various Great National and Chevron drill holes in the photo are indicated on the base map of Drill Hole Locations for Isopach Maps (see Volume II). The beds strike N40 W and dip 6-7 NE. The location of number tar zones determined along measured sections are labelled. The measured sections were completed along ridge lines or in drainages as within MS-45. In some cases the labelled dots were moved laterally to permit clarity of zone continuity. Unlabelled areas contain no measured sections. The area beneath Bruin Point contains the highest concentrations of thick tar sands where cumulative thickness ranges between feet. The area beneath Bruin Point and the Central Overlook, which is located just off the photo and diagonally below the NE in the upper right corner, contains tar sands whose cumulative thickness ranges between feet. Zones 31, 35, 36 and 37 are the four most important tar zones in the area. Bitumen grades of numbered tar zones and their thickness are listed in Table 4. The isopach maps of individual numbered tar zones add another dimension to this view. The dashed yellow line depicts the base of saturation with bituminous sand zones above and nonbituminous sandstone zones below. The Asphalt Mine with the north quarry visible exists in Zone 43 near the base of saturation. The area beneath the ridge line from the Shell Curve to Bruin Point is considered to be the principal distributary channel that feeds the Sunnyside delta complex. Near Bruin Point Zone 23 contains excellent exposures of a distributary mouth bar that overlies an unconformity on top of a limestone. The red dot near Bruin Point locates excellent exposures of the Blue Marker. Good exposures of portions of the Carbonate Interval exist at the blue dot on the road to Bruin Point. The next photo is a panorama view of the area behind Bruin Point.

75

76 Photo 4. Panorama of Sunnyside Tar Sands, Part III. The right portion Of this photo contains the Central Area that extends from the left slope at the Lunch Spot Overlook to beyond MS-3. The left portion of this photo contains some of the North Area. Spot elevations are labelled in white. The location of numbered tar zones determined along measured sections are labelled with the exception of those near CR-25 where there is no measured section. In some cases the dots have been moved laterally to permit clarity of zone continuity. Unlabelled areas contain no measured sections. The viewpoint for this two photo composite is from a hill shown in Photo 1 and located in the SE/4, of the NW/4, section 6, T14S, R14E (see Regional Geology Map). The Lunch Spot Overlook in this photo and the North Overlook of the isopach maps are the same spotj The Central Area contains up to fifteen numbered tar zones with cumulative thicknesses that commonly range between feet. The North Area contains seven to eight tar zones with cumulative thicknesses that range between feet. Tar Zones 31, 35, 36 and 37 are the four most important tar zones in the entire deposit. Bitumen grades and thicknesses of numbered tar zones are listed in Table 4. The base of saturation is indicated by the dashed yellow line with bituminous sandstones above and nonbituminous sandstones below. To the lower left of Bruin Point drill hole CR-25 has a T.D. of 874 feet with a base of saturation at a depth of 832 feet; continuous drill core from feet contains 710 feet of bituminous sandstones; or 85% of this hole contains bituminous sandstones; and this does not include Zones 36, 35 and 33 that exist above the drill collar and are visible in this photo. Enormous concentrations of thick tar sands exist beneath the area of Bruin Point to the North Overlook. The area beneath Bruin Point and the Lunch Spot Overlook contains the highest concentrations of bituminous sandstones in the entire Sunnyside delta complex. This area represents the main portion of the Bruin Point subdelta and was fed by a northeast trending distributary channel system that exists beneath the ridge line extending from the Shell Curve to Bruin Point. Total accumulations of tar sands in MS-22 are 547 feet, while total accumulations of tar sands in MS-9 are 470 feet. The ridge line that extends off the Pilot Mine Site along MS-9 represents the main feeder to the Dry Canyon subdelta of the Sunnyside delta complex. In the Dry Canyon subdelta Zone 36 splits into two intervals, and Zone 99 is the lower interval. The North Area differs markedly from the Central Area as Zone 31 exists near the top of the Roan Cliffs. In the Central Area the Blue Marker (red dot) and the Carbonate Interval (blue dot) have not been eroded off. The North Area has been eroded to an economically beneficial level.

77 "Photo 5. Panorama of Sunnyside Tar Sands, Part IV. This panorama of the North Area extends for 1.6 miles from the Pilot Mine Site on the right to the principal northern limits of the tar sands near MS-23 on the left. The "bird's foot" area near drill hole Shell No. 1 exists about 2500 feet behind MS-21 as seen from the base map of Drill Hole Locations for Isopach Maps (see Volume II). Small volumes of tar sands with marginal grades of bitumen extend to the left of the photo for another two miles to Mt. Bartles whose location is labelled on Photo 1. The location of numbered tar zones along measured sections are indicated. In some cases the dots have been moved laterally to permit clarity of zone continuity. Unlabelled areas contain no measured sections. Spot elevations are indicated in white. The viewpoint for this two photo composite is from a hill shown in Photo 1 and located in the SW/4 of the SE/4, section 31, T14S, R14E. This portion of the North Area contains bituminous sandstones that commonly total feet between the Pilot Mine Site and MS-13. Between MS-13 and MS-23 the bituminous sandstones commonly total feet. Tar Zones 31, 35, 36 and 37 are the four most important tar zones in the entire deposit. Bitumen grades and thicknesses of numbered tar zones are listed in Table 4. Zone 31 has been eroded from this portion of the North Area with the exception of the Pilot Mine Site where trees mask the location of Zone 31. But Zone 31 is labelled at the Pilot Mine Site in the previous photo. In the Dry Canyon subdelta Zone 36 remains split into two intervals, and Zone 99 is the lower interval. The dashed yellow line indicates the base of saturation with bituminous sandstones above and nonbituminous sandstones below. In this photo the base of saturation remains nearly horizontal at 9100 feet in elevation. This contrasts with the base of saturation that climbs through different zones in the South Area as seen in Photo 2.

78 /^»>^/>/^d>^fe^ &S<5*^^ / &?<^*^~ (Z'^r^r / ^ ^ ya

79 fz i ^ las^l /

80 '"* Photo 6. Clark Valley and Canyons in the Book Cliffs Near Sunnyside, View looks northeast across Clark Valley to the Book Cliffs that are 4-5 miles away. Sunnyside exists almost two miles to the right of the photo. Left dark blue dot is 1.5 miles away. Distance from left green dot to right red dot is 2.5 miles. light blue dots: left green dot: right green dot: right red dot: left red dot: dark blue dots: yellow dots: orange dots: right light blue dot: West Ridge along crest of Book Cliffs B Canyon Left Fork of A Canyon "H" Canyon (i.e., next canyon northwest of Fan Canyon, see Figure 2) and along alignment of proposed south conveyor route (see Regional Geology Map). location of massive rockfalls in the early 1960's caused by longwall mining of the Sunnyside coal seam that is located 150 feet below base of this cliff forming Castlegate Sandstone. Mancos Shale outcrops of Castlegate Sandstone that form the lower box canyon unit. Beds strike northwest and dip northeast to form a V shape in the drainages. The apex of the V shape points in the direction of dip. The alignment of the yellow dots visually appear imperfect but geometrically they are a sloping plane. There are no faults in the area. outcrops of the Bluecastle Member of the Price River Formation that forms the upper box canyon unit. shear cliffs of Upper Member of Colton Formation exist below Photo 11 looks down B Canyon from the crest ot the Book Cliffs. Photo 12 taken from near right green dot and looks up Left Fork of A Canyon. SI

81

82 Photo 7. Stratigraphy in Lower Portion of Book Cliffs. Photo taken in full sunlight of early evening near Pace Creek located in SE/4, section 36, T13S, R12E about 5.5 miles northwest of B Canyon. yellow dot: Castlegate Sandstone of fluvial origin that forms foot cliffs and the lower box canyon unit in drainages. Closely spaced jointing (i.e., one per foot) creates rock fall hazards from cliffs. red dot: Blackhawk Formation, Sunnyside Member of mixed shore to lower coastal plain origin. Dot on Sunnyside sandstone. "Red dog" color formed by oxidized and burnt coal which also defines shales and sandstones of Sunnyside Member. Unexposed Sunnyside coal bed slightly above red dot. Compare with Figures 7 and 10. green dot: Blackhawk Formation, Kenilworth Member of mixed nearshore to lower coastal plain origin. Dot on nilworth sandstone with thin unexposed Rock Canyon coal bed above the sandstone. Compare with Figures " and 10. dark blue dot: Mancos Shale of offshore marine origin. This pile of rocks illustrates the major late Cretaceous regression (i.e., withdrawal of the sea and encroachment of nonmarine deposits) with marine shales at the bottom, covered by mixed shore to coastal deposits of the Blackhawk Formation, followed by fluvial deposits of the Castlegate Sandstone.

83 ftlk. :S'>' '«*' '.;'V».^'' < x "pjf ' > '--ft.*'i< s \ ^tfn^v " "*,* ' *, "," -»"^i- -,*.*'"" " fls'* "' - ""*V "^:'lp i V " "--: - 1' i"i '^l-^^ """-... A - -iv'^...^ ", ' l K! ~T ii^l?, ' ^;- cx,^.,**!&." W _ %*" - i**& Y. ^^%P^^ < ' '**% ""' r~-\ *?k\c

84 Photo 8. Stratigraphy in Upper Portion of Book Cliffs. View from south side of upper B Canyon looking north to northwest from NW/4, section 13, T14S, R13E toward West Ridge above green dot. View looks across steep slopes of upper box canyon unit in foreground at excellent rock exposures on north side of upper B Canyon. Relief in this photo is about 1500 feet. Proposed west portal for conveyor route up B Canyon is located to right of yellow dot and off the photo. See Regional Geology Map for location of proposed west portal as well as Figure 2. green dot: red dot: yellow dot: light blue dot: dark blue dot: two orange dots: Green River Formation near Hill 8893 (NW/4, section 12) that contains outcrops of ostracodal limestones. well defined reddish brown cliffs of upper member of Colton Formation. poorly defined sandstone cliffs of lower member of Colton Formation. Flagstaff Limestone that interfingers with North Horn Formation. 20 foot cliff interval of North Horn Formation distinguished by MnOx staining and poorly jointed massive blocks. mark top and bottom of Bluecastle Member of Price River Formation that forms upper box canyon unit. Sandstone is moderately jointed (i.e., 1 per 4 feet). Elevation of upper box canyon about 7400 feet. Upper orange dot in this photo is at same location as lower orange dot in Photo 11. The rock exposures in this photo on the west side of the Book Cliffs correspond to similar exposures in Whitmore Canyon and the lower portion of the Roan Cliffs as seen in Photos 9 and

85 Kr-f. V. <** *«*»...* * >V*v- ^*«*&»«>-y-., ^ r*s] -^i»ah a"" 1 ***^-*!-

86 Photo 9. Roan Cliffs, Central Area of Project, and South Conveyor Route. Looking northeast at the Sunnyside Tar Sands from about four miles away. The Central Area of the tar sands deposit exists within the 8000 feet between the two upper yellow dots and the 1200 feet between the two upper green dots. Photos 2 and 3 are closer views of the numbered tar zones exposed along the Roan Cliffs. Relief in this photo is almost 3000 feet. Photo taken from hairpin turn above Bull Flat and located in SW/4, SE/4, section 19, T14S, R14E. CO upper green dot: middle green dot: left yellow dot: right yellow dot: lower green dot: red dot: central yellow dot: two light blue dots: two dark blue dots: left orange dot: right orange dot: Bruin Point, elevation 10,131 feet Asphalt Mine, elevation 8900 feet, north quarry to left, south quarry to right. This dot also marks base of bitumen saturation. Shell curve on road to Bruin Point, also near base of saturation base of saturation slightly north of measured section No. 2 area of transitional contact between Green River Formation above and Colton Formation below reddish brown cliffs of Colton Formation, upper member poorly developed cliffs of lower member of Colton Formation fossiliferous outcrops of Flagstaff Limestone 20 foot cliff interval of North Horn Formation distinguished by MnOx staining and poorly jointed massive blocks road junction at elevation of 7270 feet between coal colored dirt road in Whitmore Canyon and the light tan colored dirt road going up Water Canyon. Heavy equipment can be trucked to the junction and unloaded at a ramp. Almost four miles up dirt road in Water Canyon to Asphalt Mine, hence to the Shell curve and then Bruin Point. From the Asphalt Mine to the top of the Roan Cliffs the two mile stretch commonly contains grades of percent. Bear Canyon. Dot located about 1300 feet above mined out longwall panel. Two localities of 0.5 foot subsidence are located near this dot; data from surveyed subsidence net start in Two small landslide scarps exist in the slopes to the right and were induced by the minor earthquake of 1988 and/or coal mine subsidence. Near vertical trend of five different colored dots in central portion of photo (dark blue, licjht blue, yellow, red and orange) indicate proposed alignment for south conveyor route. Photo 10 is a closer view of the cliffs on the left side of lower Bear Canyon.

87 v'*w I2rj*^ ; '^'^m "UP?«< v &*+ " aj^ -

88 Photo 10. Stratigraphy in Lower Bear Canyon. Looking north to northeast up steep slopes located on northwest side of lower Bear Canyon. These rocks were deposited in continental environments during the Paleocene and Eocene. See Figures 10 and 11 for additional correlation of these Tertiary rocks. Relief in this photo is about feet. Small rock slide goes diagonally down from upper central portion of photo to lower right portion. Slide starts below cliffs at lower red dot and upper yellow dot. This slope would be crossed by the proposed south conveyor route. See Regional Geology Map. red dots: yellow dots: light blue dot: dark blue dot: reddish brown massive cliffs of upper member of Colton Formation. These massive cliffs are usually feet thick and are the most characteristic feature of the upper member. buff colored sandstone cliffs of lower member of Colton Formation. These three small cliffs are characteristic of the lower member and are usually relatively thin, feet thick and somewhat discontinuous. fossiliferous outcrops of Flagstaff Limestone. Top of this unit has 1-2 foot thick gray biomicrite with gastropod and pelecypod fragments. Flagstaff Limestone interbedded with three or four thin sandstone intervals that have some lithology and color as the massive 20 foot cliff interval of North Horn Formation. 20 foot cliff interval of North Horn Formation readily distinguished by MnOx staining and poorly jointed massive blocks. Other similar sandstone intervals get progressively thinner up section and are interbedded with Flagstaff Limestone

89 '^**!T :».r-l &' «. \ i*s-3 k " " >'#5i», # " # -? It?**,.-A*.- iftiil 1 «'-r^"-; -*»rtf **-S«, *%»& 5i* t-v,-**s»#s^ ^v *' "dl^-"*' tar ' ^ing***,"

90 Photo 11. Looking Down B Canyon into Clark Valley. View looks southwest down B Canyon from top of West Ridge that exists along crest of Book Cliffs. Photo taken from elevation of almost 8800 feet looking down into Clark Valley with average elevation near 6000 feet. Elevation of mesas near red dots about 6500 feet. Looking miles across Castle Valley at Wasatch Plateau along horizon. dark blue dot: two red dots: light blue dot: two yellow dots: four orange dots: located about 13 miles away, defines Farnham Dome and Cat Canyon near Wellington (see Figures 1 and 1A). Small vertical gray structure just above this dot is part of coal wash plant complex located some two miles southeast of Wellington. roughly defines location of proposed dam between these two mesa abutments of Mancos Shale capped by alluvial gravels. The dam would form a two square mile tailings disposal area that backsup to the base of the Book Cliffs (see Figure 2). location of proposed plant site at an elevation of almost 6800 feet. outlines outcrop trend of Castlegate Sandstone that has significant rock fall potential and forms lower box canyon unit. outlines outcrop trend of Bluecastle Member of Price River Formation. This sandstone member forms upper box canyon unit. Lower orange dot in this photo is at same location as upper orange dot in Photo

91 M48 ' Sy*Z&4$&Z('* ' /Wo- ^>r::^:w r -tljsm '*«&. 1 * 3? \V*

92 Photo 12. Looking Up Left ork A Canyon From Clark Valley. This view looking northeast illustrates the open nature of the Left Fork of A Canyon. The left side of this canyon should receive good sunlight in winter months that will benefit maintenance of a conveyor route. This is the most open canyon in this portion of the Book Cliffs and represents the canyon that should have the least number of rock falls from either of the two box canyon sandstone units. For additional location see Figure 2. green dot: West Ridge of Book Cliffs and outcrops of the Green River Formation. two red dots: reddish-brown outcrops of upper member of the Colton Formation. central orange dot: approximate location of upper box canyon unit near creek bed. Location of alternate west portal of tunnel through the Book Cliffs to east portal near Grassy Trail Reservoir. Elevation of the alternate portal site near 7600 feet and located at cluster of joint patterns on Regional Geology Map in NW/4, SE/4, section 13, T14S, R13E. The massive 100 foot high cliffs at the level of the canyon floor should make an excellent portal rock. left and right orange dots: left and right yellow dots: left blue dot: sandstone outcrops of Bluecastle Member of Price River Formation which form the upper box canyon unit in drainages. outcrops of Castlegate Sandstone that forms the lower box canyon unit exposed on both sides of creek near the central yellow dot. near where jeep road splits to Right Fork and Left Fork of A Canyon. Jeep road continues up Left Fork where it becomes impassable below Castlegate Sandstone near central yellow dot.

93 t?v ^.» ^ ^^^^ ^, >>-1HL-. ** %%!' ^ *,> Vyl -*....4S. K* *<.«" *^!is.-, - If o /.f/^0

94 Photo 13. Looking Up Proposed North Conveyor Route From West Ridge. Looking northeast up the Right Fork of Whitmore Canyon along the proposed north conveyor route which is shown by the alignment of four light blue dots. Bruin Point exists off the upper right side of this photo. All rock exposures belong to either the Colton Formation or the Green River Formation. Photos 4 and 5 show a closer view of the numbered tar zones exposed along the Roan Cliffs at the horizon. Grassy Trail Reservoir cannot be seen but exists some 1300 feet below in Whitmore Canyon and is located between the lower light blue dot and the foreground. The location of Grassy Trail Reservoir is shown in Photo 1, Figure 2 and on the Regional Geology Map. For location of viewpoint refer to Figure 2 near crest of West Ridge above alignment of proposed tunnel and near letter p in the word jeep located in the NW/4, SE/4, section 12, T14S, R13E. Distance from viewpoint on West Ridge to Roan Cliffs above upper light blue dot about 3.5 miles. Distance from viewpoint to left horizon about 4.3 miles. Distance from viewpoint to right horizon about 3.5 miles. Distance along visible horizon about 3.5 miles. green dot: two yellow dots: three red dots: central red dot: two orange dots: location of proposed north area pilot mine. alignment between these two dots represents base of tar sands. exposures of reddish brown sandstone cliffs of the upper member of Colton Formation. bedrock bench above red dot represents transitional interval between Colton Formation and Green River Formation. location of red shale-fossiliferous limestone interval that has been used along with the base of saturation to separate the Douglas Creek Member of the Green River Formation into three different portions. Lower portion located between central red dot and right orange dot. Middle portion located between right orange dot and right yellow dot. Upper portion located between right yellow dot and midway to green dot. This upper portion of the Douglas Creek Member contains the vast majority of the tar sands. The Garden Gulch Member of the Green River Formation also contains bituminous sandstones and exists above the upper portion of the Douglas Creek Member to the horizon.

95 "',.&. J' J''''' &0" t /.- ^ I' B' m H E Kr G /ys^

96 ;.^^-^ 7? ~.-- / 7)...faiE&KMJ.v. ^«ip (w T TB0K,-""wVv 1 *^fs3^'*'t ; /''i^/.' J )7\/'>V\ V,,-..? IISP^^'ivaKi- / V^~^/wMfc^,>jfe- : ;..ita.ti.,1. / L? 7 '»* i i (i (77 s> 7-7'7777/ /7 '^ :-- ^ H --r^ ' ^ up*, _ A J " 'I *u; 1 W:lB ' 1^- *-* 1 CONTOUR UrtpWll JOPT j'\ i "-.. " IS 7 gn FiquflE 2 LOCATION MAP OF SUNI^YOIDE AflEA CARBON, COUNTYj, UTAH' VI "f / /74, ^\77 y!:--.'--.-71/( V f7t tv74'r.i ^777^M M7

97 O/VS-/ FIGURE 3 TOWER IDENTIFICATION NEAR BRUIN POINT SCALE: 1"=1000'

98 EXPLANATION coal outcrop mined out area 10 Sunnyside Zona isopachs 12 Sunnyside Coal Zone Area. Doelling, et al, 1976 Figure 4. Underground Coal Mines in the Sunnyside Area, Utah

99 U P P E R C R E T A C E O u s BLACKHAWK ro ui O Ul 1" 1 TO "".I -g P. f FORMATION o 1 *" MESA i- <D VERDE - CASTLEGATE SANDSTONE PRICE RIVER FORMATION ; i (+ (D H (+ H H <^> 00 <7i 1 l lal. BfBta 1 o or :;:;:;>: : : : : : X'Xv ;X,'*X' ;Xx"x*x*X II II 1111,111 II II X*X*X*X*X II II i i! i! i J i i i J i J iji i I ijili i i i i i i II ii i I&ssi i i i i II i i i II i i i i iii i i i i i i i i i x^iii? II i iji i i II I'I I'lji i I'I'I i i i i i i i i i \?:&x'sx&s: '[ i *IJMIi' i X*KvX;X'X*XvX lr.li 3) ^KX&P** X'X-x-X'X-X'X-x- _ T o ^v^ii/ o, -> '- * F 55 * m r n x > z 73 o ^ ' D CREEK ION ( NILWO x S'P. t\j Or M - o w - ro_ ~ Z o. o ^L x' 1 $$: vx'i* ;Xv[x SIS C.11 i. I.I 1 '.1-1 C 9 * -o S 3 (/> </> UNNYSIDE JNNYSIDE ^L T- 6. m z. O r o 1 * isilis xw&ws jljl&xli: X'J'XvXvIv il^iw ix&jx&yi'ft i*i"ivi : i"s"x"i : { ' ' ' 'vx'x** i i i i i i i i i i i i JX:*X;X:X- ' i'! i' i i i' i vb8$$3i i 'ivxv : ; : : *x"x*s*x!! ; X* *X'X*x*xx*x"x*i"x*x***x" x*x*x*>x*x"x*x*x*x :jx.xivix'i-ixoxxi'i'sxv:-: ivx*xvsivx'x"x*:vx*x *i*x"*x*lv***""" : **'x"*x'vi : x* : v:*x't""'*i*x*vx*'i"ivi'x*v : : ) >.* ui» X;X;XvX*XvX;»vXvXv *X;Xi.vXvI»X:X, X;*;X**v ^ISSg^iii^**^ -.. < rn a) H o > r~ o > r - m II O o. ^llpp^ r en H GENE HOLO UNNY en O 33 ALIZED C SECT DE MINI 8?.o 2 t i l l 1 J* *^ H- (D

100 Figure 6. tafeneralized VtttHQLOGIC SECTION ^CANYON COXji PROPERTY ~ "=I- k' V Vertical Scale 1"=100 ==m\upper SUNNYSIDE SEAM 3'T06' ^..is^ Z. W V? SUNNYSIDE SEAM 5-5'TOIO'-0' GILSON SEAM o' TO 4' US Steel, 1976

101 Young,1955 Castlegote lember, Biogenic Structures labyrinth castings(lc) mollusc shells large horizontal burrows (Ihb) Sunnyside coal bed OphiomorghaCO). Cyl indrichnus (C) chevron trails (ch),r,uhespuren(r), Arenicolites(A). Gyrochorte(G). Aulichnites(Au). plurcl curving tubes(pct) R.O.ArthroDhvcL's(Ar). Teichichnus(T). Thalassinoides(Th) Ic Ic Ihb C\C,ch -Rock Canyon coal bed R,G,A,0,Au,Ar, ch.,pct T,R,0,Ar,Th O.C T,Au,Th,A,ch Rp.ArJ.Th.lc G,ch,R,0,pct R.O^r,T,Th ' '.-.' '.:Ir.': medium-grained sandstone -gs#~gs carbonaceous siltstone,claystone,shale ^csdlstjc coal "V iii*2?? thickbedded, fine-grained sandstone '.. ';'..,;; -,;,^ thinbedded very fine-grained sandstone jt^-l-sg interbedded sandstone and siltstone -rj-~-0- mudstone Figure 7. Maberry, 1963 Columnar Stratigraphic Section of Blackhawk Formation, Sunnyside, Utah.

102 Southwest Northeast Flogiloft Formation Wll Ridf Southwest To Northeast Cross Section Through The Sunnyside Coal Mining District Figure 8. Sella In Fail Ml.f OatirwoK, al al (1(71) to Winters, et al, 1986

103 VS7/;. ".'I'//: '/// i"ii'i'ii I O LU CO -J < o o z < o I m cc LU a O DC a < O o a) a) D Cn fa Z DC O I I cc O z z o H < 5 cr O Li. cr LU > cc HI o cc Q. LU z o H CO D Z < CO LU 1- < a HI _l 1- co < o z o h- < 5 cr O Li. * 5 < X o < _l m LU < I CO CO O O z < 5, a. 1: * 01460

104 System Series Stratigraphic unit Thickness (feet) Description Eocene Green River Formation Greenish gray and white claystone and shale, also contains finegrained and thin-bedded sandstone. Shales often dark brown containing carbonaceous matter. Full thickness not exposed. Colton Formation 300-2,000 Colton consists of brown to dark red lenticular sandstone, shale and siltstone, thins westwardly and considered a tongue of the Wasatch. < a: Wasatch Formation 3,000 Wasatch predominantly sandstone with interbedded red and green shales with basal conglomerate. Found in east part of field and equivalent to Colton and Flagstaff in west. Paleocene Flagstaff Limestone Flagstaff mainly light gray and cream colored limestones, variegated shale, and fine-grained, reddish brown, calcareous sandstone. Danian Maestrichthian North Horn Formation MINOR COAL Tuscher Formation 350-2, Gray to gray green calcareous and ssty shale, tan to yellow-gray fine-grained sandstone and minor conglomerate. Unit thickens to west. Light gray to cream-white friable massive sandstone and subordinate buff to gray shale that exhibits light greenish cast. Contains minor conglomerate and probably represents lower part of North Hom, only present in east part of field. Price River Formation MINOR COAL 500-1,500 Yellow-gray to white, medium-grained sandstone and shaley sandstone with gray to olive green shale. Contains carbonaceous shale with minor coal and thickens along east edge of field. Campanian D. a o Castlegate Sandstone MINOR COAL Blackhawk Formation MAJOR COAL SEAMS White to gray, fine- to medium-grained, argillaceous massive resistant sandstone thinning eastwardly with subordinate shale. Carbonaceous east of Horse Canyon but coal is thin and bgnitic ,100 Cyclical littoral and lagoonal deposits with six major cycles. Littoral deposits mainly thick-bedded to massive cliff-forming yellow-gray fine- to medium-grained sandstone, individual beds separated by gray shale. Lagoonal fades consist of thin- to thick-bedded yellow-gray sandstones, shaley sandstones, shale and coal. Coal beds form basis of Book Cliffs coal field. Unit thins eastward grading into the Mancos Shale. O u o < g Masuk Tongue Star Point Sandstone Yellow-gray massive medium- to fine-grained littoral sandstone tongues projecting easterly separated by gray marine shale tongues projecting westerly. Mancos Shale 4,300-5,050 Gray marine shale, locally heavily charged with carbonaceous material, slightly calcareous and gypsiferous, nonresistant forming flat desert surfaces and rounded hills and badlands. Separated mainly to the west into tongues by westward projecting littoral sandstone which eventually grade into shale. Sandstones'are fine- to medium-grained, yellow-gray to tan and medium-bedded to massive and cliff forming. Blue Gate Shale Turonian Ferron Sandstone MINOR COAL Cenomanian Tununk Shale Dakota Sandstone Heterogeneous sandstone, conglomerate and shale, thin resistant cuesta former. Doelling, 1972 Figure 10. Generalized Stratigraphic Chart for the Book Cliffs, Helper to Sunnyside, Utah

105 en t>2 Chart Illustrating stratlgraphlc nomenclature and correlation of major Alblan to middle Eocene rock units from the Sanpete Valley of central Utah to the Book Cliffs of eastern Utah (modified from Fouch and others, In press). Vertical line through strata Indicates a change In stratlgraphlc nomenclature. Fouch, et al, 1983 Figure 11. Northeastern Utah Correlation Chart.

106 LATE CRETACEOUS LATE CRETACEOUS The Colorado I'latean area in Late Cretaceous time. The area was part of a coastal plain that extended eastward from the foot of mountains in central Arizona and central Utah. The edge of the Late Cretaceous Sea was to the east In Colorado. Hunt, 1956 Figure 12. Utah Paleogeography in Late Cretaceous, O /i(zj

107 r LATE PALEOCENE EXPLANATION C D K M SJ SR Ua Un Z Circle Clifls upwarp Defiance upwarp Kaibab upwarp Monument upwarp San Juan Mountains San Rafa«l Swell Uinta Mountains Uncompahgrc upwarp Zuni upwarp The Colorado Pin tea u area in late Paleocene time. The l*l:il*staff lake \va* f»irm»m.l iili»ns tin- western etljro of the Plateau an-a. Hunt, 1956 Figure 13. Utah Paleogeography in Late Paleocene

108 EARLY AND MIDDLE EOCENE y-. : <-'Un' ^ -» \, V -.:,.- _ ~ :r. '?*+*.- "^I"^ _ >. ' > ' 3? c D K M SJ SR Ua Un Z EXPLANATION Circle Cliffs upwarp Defiance upwarp Katbab upwarp Monuir.ent upwarp San Juan Mountains San Rafael Swell Uinta Mountains Uncompahgre upwarp Zuni upwarp The Colorado Plateau ar*»a in early and middle Koroiw tini**. D<i\vnwarpin^ of the T'inia J'.asin produced tho Green River lake, which covered most of the north part of the Plateau ap-a. Most of the uplifts, like the Sao Itafael Swell, probablv stood higher than the lake and shed sediments into It. Hunt, 1956 Figure 14. Utah Paleogeography in Early and Middle Eocene

109 WEST WASATCH PLATEAU 4 UTAH-COLORADO STATE LINE EAST Sondtton* orin* Shot* Mudtton* van de Graaff, 1972 Figure 15. Generalized Cross Section of Late Cretaceous Rocks in East Central. Utah.

110 SEVIER OROGENIC ABELT \ l = MONTANA ^tts^j "COLORADO LOWER CRETACEOUS Figure 3: RESTORED DIAGRAMMATIC SECTION ACROSS THE ROCKY MOUNTAIN GEOSYNCLINE IN CENTRAL UTAI. R. L. Armstrong, 1908; l>y penn. Ceol. Soc. Amcr. McGookey, et al, 1972 Figure 16. Diagramatic Cretaceous Section in Central Utah.

111 AGE. m^mm AGE Horizontal scale 10 0 I i i i i I i Emery sandstone memherof Mancos 20 Miles _J Vertical scale Feet I i i i I i i i i I After Spieker, 1946 Hunt, 1956 Figure 17. Diagramatic Section of Late Cretaceous and Tertiary Rocks Near Castle Valley, Utah.

112 FIGURE 18 WELL LOCATIONS NEAR CLARK VALLEY, PROPOSED PLANT SITE & CITY OF SUNNYSIDE, CARBON COUNTY, UTAH BASE: K-15, APC DENVER SCALE: I^BOOO 1 R14E

113 APPROXIMATE FOOTAGE INTERVALS DESCRIPTION MARKER NAME 350 i /20 FT. OIL SHALE, OUTCROPS AS DOUBLETS, IGAMMA RAY LOG = 3 PRONGS POSITIVE SLOPE BROWN CLIFF WITH MUD CRACK MOLDS IN BROWN SILTSTONES 2 FT. BIOTITE TUFF WITH ASH FRAGMENTS 20 FT. OIL SHALE, OUTCROPS AS DOUBLETS, GAMMA RAY LOG = 3 PRONGS NEGATIVE SLOPE ONE INCH TO 3 FT. BIOTITE TUFF WAVY BEDDED TUFF MAHOGANY OIL SHALE R-5 OIL SHALE LOWER TUFF tr. u m S HI S u iii tr. u iii Z> X u < tr < Q. 1-2 FT. DINNER PLATE OIL SHALE & 0.5 INCH COAL SEAM BLUE MARKER cc CO 70 1 TOP HAS GAMMA RAY KICK OF 600 API UNITS MULTIPLE OSTRACOD-RICH INTERVALS (ZONE 25) MULTIPLE OSTRACOD-RICH INTERVALS, NO SPECIFIC GAMMA RAY KICK (ZONE 26) T CARBONATE INTERVAL IXI x u -J z> u z LLI Q tr < SCALE: 1" = 100' DATE BASE: OUTCROPS & DRILL CORE COMPILATION: W. CALKIN DATE: FIGURE 19 IMPORTANT STRATIGRAPHIC MARKERS IN THE GREEN RIVER FORMATION, SUNNYSIDE TAR SANDS, CARBON COUNTY, UTAH

114 APPROXIMATE FOOTAGE INTERVALS BRIEF DESCRIPTION STRATIGRAPHIC MARKERS U.S.G.S. OIL SHALE ZONATION T 19-23" BIOTITE-RICH TUFF WITH ERODED V'ASH FRAGMENTS WAVY BEDDED TUFF 47.0± 1.8 m.y II 18-27'OIL SHALE, OUTCROPS AS SEPARATE DISTINCT DOUBLETS 10-^40' BROWN CLIFF, ABUNDANT MOLDS OF MUDCRACKS IN LT BROWN SILTSTONES MAHOGANY OIL SHALE R m I o m z < cc 20 " ~ "A" II 50 I v 18-22'OIL SHALE, OUTCROPS AS SEPARATE DISTINCT DOUBLETS 2-5' OIL SHALE 1-14" BIOTITE-RICH TUFF, CORE & RARE OUTCROP R-5 OIL SHALE R-5 LOWER TUFF m.y. R ' OIL SHALE R-3 70 _L ' OIL SHALE, OUTCROPS AS 1-2' DINNER PLATE OIL SHALE WITH 0.5" COAL SEAM 1-1.5' BELOW BLUE MARKER BASE OF PARACHUTE R-2 SCALE: 1" = 50' DATA BASE: DRILL CORE OUTCROPS COMPILATION: W. CALKIN DATE: FIGURE 20 STRATIGRAPHIC MARKERS IN THE PARACHUTE CREEK MEMBER, SUNNYSIDE TAR SANDS, CARBON COUNTY, UTAH

115 DATA INTERPRETATION SEQUENCE OR CYCLE LAND SHORE LAKE & high stand of lake level -< retrogradatlon & still stand of lake level aggradation I & low stand of lake level progradation SS LS - UNCONFORMITY low sediment Influx M DRY CLIMATE SH SS high sediment Influx erosion & Inclsement during low stand < UJ >- o o T- UJ _J o *> O h- < 2 -j o v 1-4 miles *l WET CLIMATE DRY CLIMATE WSC FIGURE 21 SCHEMATIC DIAGRAM ILLUSTRATING PATTERNS OF DEPOSITION AND EROSION WITHIN A STRATIGRAPHIC SEQUENCE, SUNNYSIDE TAR SANDS

116 RATE OF DEPOSITION RAT EOF ACCOMMODATION LOCATION Or SCHEMATIC. WELL-LOG RESPONSE A_ PROGRADATIONAL PARASEQUENCE SET SCHEMATIC WELL-LOG RESPONSE SP - r f RES J < RETROGRADATIONAL PARASEQUENCE SET I ^JJ/VTG OF^EPOSJJjON RATE Or'ACCOMMODATION < 1 -,'tritn, «*..'.» >jii t, jl-t.!, >,tv!&i>' '.i a* ^-*-». ^ ^r^-^ff: ^^^K^-^.^ AGGRADATIONAL PARASEQUENCE SET SP RES KATE OF DEPOSITION RATE OF ACCOMMODATION ^ -_Jl -L O [~~ " SHALLOW-MARINE SANDSTONES SHELL MUOSIONfcS CO CO l N0IVIDU AL PARASEQUENCES VAN WAGONER ET AL, 1990 FIGURE 22 DEPOSITIONAL STACKING PATTERNS OF PROGRADATIONAL, RETROGRADATIONAL AND AGGRADATIONAL PARASEQUENCES

117 i : Ob (i) (c).... m^^m] ^S^^^feM^j" W^VSgl-Jg m w -> ^*tote^.-+«m*mk..-2r>: TZ»H*I*y^ah^y. I ^ LOCATIONS VAN WAGONER ET AL 1990 FIGURE 23 COMPARISON OF SANDSTONE DISTRBUTION BASED ON LITHOSTRATIGRAPHfC VERSUS CWtONOSTRAOGRAPHIC CORRELATION 01473

118 RGURE 24 LOCATION OF MS 62, 63, & 64 SCALE: 1"=1000' portion of *89 Geology Map

119 FIGURE 25 STRUCTURAL TRENDS OF SURFACE JOINT SETS AND SUBSURFACE FAULTS -o SUNNYSIDE AREA, CARBON COUNTY, UTAH Vi

120 /Hansel Volley M 3 R T «S \.! "-"fia7 \ WJ. ** *** UVV*.. r', 1 - I. V I! ; «"" L Ew- '"SALT LAKE CITY ir 1HM ' 41 * v. M2_;\»\ Wasatch Fault Zone i I ft-40 > "39 i i roflfl \ r:iwi[f.tl: J 'Sevier* Fault ' UTAH EARTHQUAKES. JULY JUNE 1978 r- so IOO i i i. j «n 1 10 n."-n{ runt sc«* MI :: 6 «? 1.5 ^37 09 Arabasy, et al, 1979 Figure 26. Earthquakes in State of Utah and Price Area

121 r > r ' r r i r A Table 1. Data From Deep Drill Holes in Clark Valley MANCOS SHALE Drill Hole Location Comp TD Elev Elev Depth from Thickness Thickness Thickness Total Depth from KB GL KB to Blue Gate Ferron Mbr Tununk Thickness KB to top Ferron Mbrl Mbr Mancos Shale top Dakota SS Mbr Fm Pan Am Cullen No S-13E ( ) Arco Chambers No S-13E ( ) Mtn. Fuel Sunnyside # S-13E ( ) Oil Securities Marakis # S-12E ( ) Oil Securities Marakis # S-12E ( ) avgl357 avgl71( ) avg230 avgl758 avgl758 1 not adjusted for thickness of alluvium or distance from KB to GL 2 three separate numbers in parentheses represent upper sandstone interval-middle shale intervallower sandstone interval 3 core between feet is available at USGS Core Library, Denver Federal Center well log data and interpretation WSC, November '90 -J

122 Table 2. Data From Shallow Drill Holes in Clark Valley Drill Hole Location (sec-t-r) TD Depth of Alluvium GT-1 GT-2 GT-3 GT-4 GT-5 GT-6 T-l 22-14S-13E 21-14S-13E 21-14S-13E 15-14S-13E 16-14S-13E 21-14S-13E 16-14S-13E Pincock, Allen and Holt data of 1988

123 Table 3. Data From Shallow Drill Holes in Book Cliffs Drill Hole Location (sec-t-r) TD Upper Sv innyside Coal Seam Split ft Lower Sunnyside Coal Seam Depth to top Th. ickness Depth to top Th ickness B-l 13-14S-13E B S-13E B S-13E B S-13E US Steel data of 1952 from SRS Inc, 1990 CO

124 TABLE 4 BITUMEN DATA BY TAR ZONE, SUNNYSIDE TAR SANDS ZONE NO. DRILL HOLES AVG. THK. IN FT. AVG. GRADE BBLSIN % DISTR gpt MILLIONS OF BBLS PARTS BLUE MARKER-* 21 (OLD 11) (OLD 21] INTERBURDEN 26 RBONATEINTERVAL a. Z> * a-* CC Q. Q. Z> a. Z> O or CO, I o _l z> o ' Q UJ 5 _l < << O o J (N ^ Q Q A (OLD 36) 36B (OLD 99) 36 COMBINED c Z> o w cd <=!3f oi CO UJ LU QC U to < I o D O Q in Q. z> o CC _ 43 ASPHALT MINE O m LOWEST BASE OF SATURATION MODIFIED AFTER DATA OF ROZELLE (1989)

125 TAR ZONE DATA EXPLANATION FOR TABLE 5 collar elevation of drill hole total depth of drill hole designated tar zone, top and bottom top picked by geophysics no core not drilled not a designated tar zone used in mine model less than 5 feet thick not present no analyses nonbituminous bituminous weak bitumen content moderate bitumen content weighted average bitumen by analysis in wt%/gals per ton 5wt% bit visual estimate continuous tar sands 114 feet thick multiple tar sands, cumulative thickness noted 24 feet of nonbituminous sandstone drilled; drill hole stopped before full thickness of zone was penetrated top elevation of measured section bottom elevation of measured section not measured environment of deposition delta front distal bar beach beach-bar offshore nearshore interdistributary bay levee distributary mouth bar distributary channel 01451

126 r i r i r ' r ' r 1 Table 5. Tar Zone Data, MS-62 thru MS-64 Bruin Point Subdelta Tar Zone Data Sunnyside Tar Sands Measured Section Data Measured Section Zone-* Data! T 25 B T 26 B T 31 B T 32 B T 33 B T 35 B T 36 B T 37 B BSAT MS-62 r~ in ai ai W W MS-63 O CH co in ai a> EH m MS-64 (N O co *r CA ai EH ffl Elevation Depth Thickness X Bit EOD Elevation Depth Thickness X Bit EOD Elevation Depth Thickness X Bit EOD Eroded Eroded Eroded est NS /18.4 DMBtoBB /12.8 DMBtoBB /18.5 DMB /14.4 DMB /9.7 B /9.7 B /15.9 B /6.8 B NP /13.0 DMB /0.6 BB /2.3 B /8.1 B NM /0.4 DMB ,2/0.4 B NM NM

127 25200 VILLAGE CIRCLE WILLIAM S. CALKIN, D.Sc. CONSULTING GEOLOGIST GOLDEN^OLORADO %g&s^&il S^ i&!ij2&~~ *& *., February 28, 1991 Mr. Robert E. Lumpkin Director, Solid Resources Amoco Corporation Suite East Shuman Boulevard Naperville, Illinois Dear Mr. Lumpkin: This two volume report represents a summary of the work completed during the 1990 exploration program. The field work was completed with the helpful assistance of George Barnett. The summary and conclusions, as well as the recommendations, occur at the beginning of the report in Volume I. All photographs, figures and tables are in numerical order in the Appendix at the end of Volume I. Volume II includes the new Regional Geology Map, one cross section, fifteen isopach maps of the numbered tar zones and three strip logs of new measured sections. The support and cooperation of Amoco during both the field and research phases of this project-is gratefully acknowledged. The excellent drafting on maps, figures and panorama photographs was completed by Shari Foos of Amoco Production in Denver. This drafting greatly enhances the value of this report. Ten copies of this report have been made. Eight copies will be sent to your office for distribution. Two copies have been retained here in Denver - one copy for John Rozelle and one copy for myself. If there are ever any questions regarding this report, or the geological aspects of the Sunnyside Tar Sands project, please contact me. Sincerely, uc^'s Wm. S. Calkin Consulting Geologist 01358

128 r L r L r L Amoco Production Company