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Volume I
GEOLOGIC SUMMARY REPORT OF THE
19 86 EXPLORATION PROGRAM SUNNYSIDE TAR SANDS PROJECT
CARBON COUNTY UTAH
for GENE E. TAMPA
DIRECTOR TAR SANDS AND SHALE PROJECTS AMOCO CORPORATION CHICAGO, ILLINOIS
by WM. S. CALKIN, D.Sc. CONSULTING GEOLOGIST
GOLDEN, COLORADO
May 19, 1987
Volume I
TABLE OF CONTENTS
SUMMARY AND CONCLUSIONS 1
RECOMMENDATIONS 4
INTRODUCTION 5
GEOGRAPHIC SETTING 6
Location 6
Access 6
REGIONAL GEOLOGIC SETTING 8
GEOLOGY OF PROJECT AREA 10
Structure 10 Green River Formation 11
Parachute Creek Member 12 Garden Gulch Member 16 Douglas Creek Member 17
Sunnyside Delta Complex 18
Bruin Point Subdelta 20 Dry Canyon Subdelta 21 Whitmore Canyon Subdelta 2 3
PERIPHERAL HYDROCARBON LEASES 25
MEASURED SECTION SYNTHESIS 27
TAR SANDS 3 0
SURFACE GEOPHYSICS 33
REFERENCES 35
APPENDIX
Photos 1-7 Figures 1-18 Tables 1-12
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Volume I
LIST OF PHOTOS
Photo 1 Aerial Oblique of the Sunnyside Tar Sands Deposit 2 Monoclinal Flexure in Sunnyside Tar Sands Area 3 View of Measured Section 29 4 Oil Shale Intervals of the Mahogany Ledge in
Measured Section 29 5 View of Measured Section 32 6 Basal Contact of Tar Zone 35 in Measured Section 32 7 Northeast View of Clark Valley, Book Cliffs and
Proposed Plant Site
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Volume I
LIST OF FIGURES
igure 1 General Location Map 2 Area Location Map 3 Detailed Location Map 4 Cordilleran Overthrust Belt, Rocky Mountain
Foreland and Structural Divisions of Utah 5 Late Cretaceous and Early Tertiary Uplifts of
Colorado and Utah 6 Location and Time of Uplift on Laramide Ranges
in the Rocky Mountain Foreland 7 Northeast Utah Correlation Chart 8 Uinta Basin Correlation Chart 9 Late Cretaceous Paleogeography of Northeast Utah 10 Paleocene and Eocene Paleogeography of Northeast
Utah 11 Summary Diagram of Laramide Uplifts, Paleodrainage
and Source Areas for the Uinta and Piceance Creek Basins in Late Cretaceous and Early Tertiary
12 Idealized Section of Bruin Point Subdelta Showing Tar Zones and Depositional Environments
13 Oil Shale Zonation and Important Markers in the Green River Formation
• 14 Detail of Mahogany Oil Shale Terminology 15 Gamma Log Comparisons at the Base of the Parachute
Creek Member (Blue Marker), Sunnyside Tar Sands, Utah and Rio Blanco Tract C-a, Colorado
16 Gamma Ray and Bulk Density Log Comparisons of the Mahogany Zone, Sunnyside Tar Sands, Utah and Rio Blanco, Colorado
17 Location of 1986 Measured Sections and Selected Condemnation Drill Sites in the Mt. Bartles-South Ridge Area
18 Amoco Acreage, Sunnyside Tar Sands
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Volume I
LIST OF TABLES
Table 1 Measured Section Locations with Relative Position in Subdeltas
2 Elevation Data from Measured Sections 3 Member Thickness Data from Measured Sections 4 Saturation Data from Measured Sections 5 MSAT Thickness Bruin Point and Whitmore Canyon
Subdeltas 6 MSAT Thickness Dry Canyon Subdelta 7 Average Thickness of Numbered Tar Zones in Bruin Point
and Whitmore Canyon Subdeltas 8 Average Thickness of Numbered Tar Zones in Dry Canyon
Subdeltas 9 Other Company Drill Hole Data, Sunnyside Tar Sands 10 Tar Zone Data of Measured Sections, Bruin Point
Subdelta 11 Tar Zone Data of Measured Sections, Dry Canyon
Subdelta 12 Tar Zone Data of Measured Sections, Whitmore Canyon
S u b d e l t a
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SUMMARY AND CONCLUSIONS
1. Extensive field work in peripheral areas of Amoco's hydrocarbon leases provided three important results. First, eleven measured sections in lieu of thirteen condemnation drill holes have determined that no significant tar sands exist in the acreage located in the West Tavaputs Plateau. Second, a significant northwest trending flexure exists and represents a mega control for the bitumen distribution within the entire Sunnyside Tar Sands deposit. Third, surface gamma ray logs coupled with lithology from detailed measured sections have recognized three important marker horizons in the Green River Formation.
2. The distribution of tar sands in the Sunnyside deposit is related to both structure and lithology. The structural control is associated with a northwest trending flexure which segments a large monocline that slopes gently into the Uinta Basin. The lithologic control is determined by porous and permeable sandstones deposited in the Sunnyside delta complex. The tar sands have an average porosity of 27 percent and an average permeability of 812 milli-darcys.
3. The southern portion of the flexure is vividly seen in Photo 1 and extends from Range Creek to beyond Mt. Bartles. The segmented monocline consists of three segments as seen in Photos 1 and 2. The West Tavaputs Plateau segment dips 3-4 northeast and contains tar sands with 0-4wt% bitumen. The middle segments dips 7-8 northeast and contains tar sands with 3-7wt% bitumen. The Roan Cliff segment dips 7-8° northeast and contains tar sands with 4-12wt% bitumen. This northwest trending flexure is delineated on the Geologic Map and the Tar Sand Isopach Map, both at a scale 1"=1000'.
4. The Tar Sand Isopach Map illustrates four distinct factors about the Sunnyside Tar Sands deposit. First, the thickest portion of the tar sands exist near Bruin Point. Second, the tar sands are concentrated within a northwest trending belt. Third, erosion has removed portions of the tar sands. • Fourth, the Sunnyside Tar Sands deposit formed within a delta complex that can be divided into three sub-deltas. The Bruin Point, Dry Canyon and Whitmore Canyon subdeltas are delineated on the Tar Sand Isopach Map. In addition, the tar sands of Sunnyside delta complex are concentrated in an area that is six to eight miles long and one to two miles wide. The long northwest trend represents depositional strike and the short northeast trend represents depositional dip.
5. The Sunnyside delta complex was formed in river-delta-beach-nearshore environments associated with the margins of Lake Uinta during Eocene time some 50-45Ma. The Sunnyside
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delta complex consists of 15-36 stacked intervals of sandstone-shale-limestone sequences within three subdeltas. The sandstone-shale-limestone sequences represent repeated cycles formed under fluctuating wet and dry climatic conditions. The outcrops along the Roan Cliffs represent stacked deltaic and shoreline sequences. The major changes in climatic conditions are related to 100,000 year Milankovitch cycles.
6. The location of measured sections is separated into proximal, medial and distal portions of three subdeltas. The most productive portions of the tar sands are in the proximal portions along the Roan Cliff face where the MSAT's are thickest and of the highest and most consistent grades. Thinning of the saturated sandstones from proximal to medial to distal portions is pronounced.
7. The Sunnyside delta complex exists within three members of the Green River Formation. The Douglas Creek Member is at the base, represents the delta facies and consists of sandstones with intervening red shales. The Garden Gulch Member is in the middle, represents the shore facies and consists of sandstones with intervening green shales and limestones. The Parachute Creek Member is at the top, represents the lake facies and consists of predominantly gray shales with some sandstones and oil shales.
8. Surface gamma ray logs have proved to be valuable for determination and correlation of numbered tar zones and delineation of marker horizons. Gamma ray values are obtained from a portable mini-spectrometer used at continuous intervals along measured sections. When the surface gamma ray logs and lithology logs of different measured sections are compared and matched, numbered tar zones can be established with confidence. When surface gamma ray readings are taken at 1-3 foot intervals near marker horizons, the surface gamma ray log patterns are nearly identical to well log gamma ray patterns as seen in Figures 15 and 16. Detailed surface gamma ray logs coupled with detailed measured section data are a powerful field method to establish numbered tar zones and locate marker horizons.
9. The three marker horizons are the Mahogany ledge or zone, the Blue Marker and the Orange Marker. The Mahogany ledge or zone exists in the upper portion of the Parachute Creek Member in areas of the West Tavaputs Plateau. General marker horizons were first located in the field and later specifically defined by drill logs. The Blue Marker occurs at the base of the Parachute Creek Member and has been used as a prominent marker in the project drill holes since 1981. The Orange Marker is equivalent to the Carbonate Marker and is associated with carbonate-rich Zones 25 and 26.
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10. The Sunnyside Tar Sands deposit is located eighty miles east of the Cordilleran overthrust belt and at the transitional area between the San Rafael Swell and the Uinta Basin. The San Rafael Swell formed 73-58Ma. Northwest trending Laramide uplifts formed in early Tertiary before development of Lake Uinta. The Sunnyside delta complex formed between 50-45Ma. The source area for the sandstones in the Sunnyside delta complex was the Uncompahgre Uplift.
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RECOMMENDATIONS
1. Hydrocarbon leases in Tracts 1, 3, 6 and 7 of Figure 18 contain thin numbered tar zones with 0-4wt% bitumen and are not worth drilling, even for condemnation. These four tracts encompass hydrocarbon leases U-17652, U-17661-A, U-17662 and U-37999. These four tracts contain no significant tar sand acreage and can be relinquished. All surface acreage has no apparent value to the Sunnyside Tar Sands project with the exception of the S/2 of S/2, Section 15, T13S, R14E in hydrocarbon lease U-17652. This southernmost area of Section 15 contains important surface access acreage near the base of the proposed mine dump.
2. Additional field work is needed to define specific aspects of the segmented flexure in portions of Range Creek, Dry Canyon ridge, Mount Bartles and Sheep Canyon. This field data coupled with marker horizon data should be used to define the closure associated with the Sunnyside Tar Sands deposit.
3. Within the Bruin Point subdelta twelve to fifteen detailed measured sections are needed to establish continuity of numbered tar zones at 500-700 foot spacings along the Roan Cliff face.
4. Additional in-fill drilling is needed to evaluate the tar zone continuity in such areas as the North Pilot Mine, NOL, "Lazy L" and "thumb and finger". Relogging of cores from strategically located Mono Power drill holes will help to define specific drill sites.
5. An alternative pilot mine site in the extreme southern portion of the property near MS 6 should be investigated.
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INTRODUCTION
The 1986 exploration program focused on detailed geological and geophysical field work in outlying areas of hydrocarbon leases east of Mt. Bartles. Field work was also completed in the Whitmore Canyon area. The field program extended from June 16 through September 19. During this time geological and geophysical data was gathered from eighteen new measured sections and four old measured sections over a total vertical distance encompassing 15,212 feet. The objectives of the exploration program were:
1. to evaluate the tar sand potential in outlying areas of hydrocarbon leases by numerous measured sections and surface samples from major tar zones;
2. to obtain surface gamma ray data from a portable spectrometer to aid in correlation of major tar zones;
3. to determine the existence of the Mahogany ledge or other marker beds that could be used to correlate the Sunnyside Tar Sands with the regional stratigraphy of the Uinta Basin;
4. to help coordinate removal of 1000 tons of tar sand from Zone 43 in the quarry of the Asphalt Mine for shipment to Chicago;
5. to complete an initial reconnaissance of the proposed conveyor belt route from Grassy Trail Reservoir to the mouth of B Canyon and the proposed plant site in Clark Valley.
The scope of this report focuses on the results of the 1986 field work and serves as an addendum to previous exploration reports. Key photographs are used to highlight aspects of the Sunnyside Tar Sands deposit and are included in Volume I. A large separate mosaic of five aerial obliques provides an excellent view of the Sunnyside Tar Sands area. As in previous reports columnar sections of strip logs were compiled from the field work. The three geology maps are included in Volume II. The eighteen new strip logs are in Volume III. Field work established major and minor environments of deposition and coupled with the surface gamma ray logs were used to correlate and determine the numbered tar zones. These numbered tar "zones (10, 11, 21, 23, 25, 26, 31, 22, 35, 36, 99, 37, 38, 41, 42, 43 and 45) zppear on the strip logs and in Tables 10-12 that contain tar zone data from Measured Sections 1-44. The use of these numbered tar zones has led to a simpler and more comprehension view of the Sunnyside delta complex.
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GEOGRAPHIC SETTING
Location
As seen in Figure 1, the Sunnyside Tar Sands area is near Bruin Point and Mt. Bartles. It is located in northeastern Utah about 120 airline miles southeast of Salt Lake City, 30 airline miles east of Price and 5 miles northeast of the coal mining town of Sunnyside. As seen from Figure 2, the principal physiographic features in the area consist of the Book Cliffs, Roan Cliffs and West Tavaputs Pleateau.
Access
Roads to Bruin Point and Mt. Bartles are from two entirely different routes. Access to Bruin Point is via Sunnyside and up Water Canyon. Access to Mt. Bartles is from Wellington via Nine Mile Canyon, across Nine Mile Creek and up Harmon Canyon (located 32.7 miles from the Wellington turnoff) or up Prickly Pear Canyon (located 8.6 miles down Nine Mile Canyon from Harmon Canyon). Within Harmon Canyon the road travels along the creek bed for about one-half mile and passage can be difficult to impossible unless the BLM has recently completed their annual maintenance. The road up Prickly Pear Canyon is generally clear and of moderate grade as it was used between 1959-1981 to transport oil and gas drilling equipment for nine exploration holes located in the vicinity of the Stone Cabin gas field (abandoned). Most of the oil and gas wells were drilled within 2-4 miles of the abandoned landing strip to depths of 5600-7200 feet. In the lower portion of Stone Cabin Draw (NE 4, Sec 29 T12S, R15E) Chevron completed a dry hole on 7-12-68 to 17,261' TD. About Ih miles east of Mt. Bartles in SE 4, Sec 9, T13S, R14E Mountain Fuels completed a dry hole on 11-19-65 to 9650' TD as located on the Geologic Map, scale 1"=1000'. The road up Harmon Canyon and Prickly Pear Canyon join at a stock pond near the abandoned landing strip at the top of Harmon Canyon as seen in Figures 2 and 3. Final access to the Mt. Bartles area is contolled by a locked gate located near the "W" in West Tavaputs Plateau. The key is at the Sprouse ranch house located about one and one half miles east of Harmon Canyon.
Access to the tar sands in the Whitmore Canyon area is via dirt roads adjacent to Grassy Trail Reservoir and the Right Fork of Whitmore Canyon as seen in Figures 2 and 3. Access to the Grassy Trail Reservoir is via a locked gate controlled by Kaiser Coal Company. Another locked gate exists up the Right Fork of Whitmore Canyon and is controlled by Jay Pagano of Wellington.
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Access to the proposed plant site for tar sand processing in Clark Valley is via Sunnyside, the golf course road, and a dirt road near the base of the Book Cliffs to the mouth of B Canyon as seen in Figure 2. Kaiser Coal Company has submitted plans to Carbon County for surface coal facilities in C Canyon, which is located between B Canyon and Bear Canyon as seen in Figures 2 and 3. The surface coal facilities are to be used for access and development of the north coal lease area of Kaiser Coal Company. The coal will be processed at existing plant facilities in Sunnyside.
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REGIONAL GEOLOGIC SETTING
The late Cretaceous and early Tertiary regional geology of northeast Utah is presented on the basis of structural uplifts, paleogeography maps and correlation charts. This regional framework sets the stage for paleodrainage conditions and the formation of the Sunnyside delta complex in ancestral Lake Uinta. The Sunnyside Tar Sands deposit is located about eighty miles east of the Cordilleran overthrust belt, northeast of the San Rafael Swell and within the southwestern portion of the Uinta Basin as shown in Figure 4. The Cordilleran overthrust belt complex is a major tectonic element in North America and was caused by compression of the westward moving overriding North American plate and the eastward moving subducted Pacific plate during late Cretaceous to Eocene time. That portion of the Cordilleran overthrust belt in Utah is known as the Sevier overthrust belt and is localized along the Wasatch Line as shown in Figure 4.
The Rocky Mountain foreland province exists to the east of the Sevier overthrust belt and contains Laramide uplifts of north-south, northwest and east-west orientation as shown in Figures 4 and 5. The distribution of these three trends and their time of movement is shown in Figure 6 and discussed below based on Greis (1983):
(1) The north-south trending Laramide uplifts are the oldest in age and formed in late Cretaceous (i.e., Campanian and Maestrichtian time of Figures 6, 7, 8) and include the Colorado Front Range west of Denver and the San Rafael Swell west of Green River as located in Figure 5. The San Rafael Swell formed in late Cretaceous during a time interval of 3-15my (million years) and between 73-58Ma (millions of years before present) at low uplift rates of 0.36-0.0 7mm/yr (Lawton, 198 3) .
(2) The northwest trending Laramide uplifts are intermediate in age and formed in early Tertiary (i.e., early to middle Paleocene of Figures 6, 7 and 8) and include the Uncompahgre Uplift in western Colorado as located in Figure 5.
(3) The east-west trending Laramide uplifts are the youngest in age and formed late in the early Tertiary (i.e., early to middle Eocene of Figures 6, 7 and 8) and include the Uinta Mountains that form the north side of the Uinta Basin as located in Figure 5.
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Separate paleogeographic maps of northeast Utah in late Cretaceous and early Tertiary show the spatial distribution of different environments of deposition. Paleogeographic maps in late Cretaceous and pre-San Rafael Swell are shown in Figure 9 and illustrate that from west to east the distribution of environments is from highlands to mountain front fans, to braidplain, to coastal plain, and seaway. Paleogeographic maps in early Tertiary are shown in Figure 10 and illustrate an intermountain area between the Sevier orogenic belt, San Rafael Swell, Uncompahgre uplift and Uinta uplift. These four uplifts rimmed a subsiding basin that formed ancestral Lake Uinta. Figure 11 represents a summary diagram of the Laramide uplifts, paleodrainage and source areas for the Uinta and Piceance Creek basins in late Cretaceous and early Tertiary.
The Sunnyside Tar Sands deposit is located 30 miles east of Price. The Sunnyside delta complex exists within the Green River Formation and formed between 45-50Ma according to the correlation charts of Figures 7 and 8. The area of the Uncompahgre uplift is considered by many geologists to be the source area of the sandstones in the Sunnyside delta complex. Within the Sunnyside Tar Sands area a major northwest trending flexure exists as seen in Photo 1. This flexure and porous sandstones localized the distribution of tar sands. The movement on this flexure is related to reoccurring movement of the northwest trending Laramide uplift system. The numerous gilsonite veins of solid hydrocarbons in the eastern part of the Uinta Basin have a northwest trend. This northwest structural trend represents an important structural element in the Uinta Basin.
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GEOLOGY OF PROJECT AREA
Structure
The Sunnyside Tar Sands area is characterized by (1) uniform low dips of sedimentary beds in a monocline that slopes northeast into the Uinta Basin and (2) a northwest trending flexure that partly controls the distribution of tar sands. The low dips of 3-8°NE are obvious in the upper right portion of Photo 1. The dips in the Bruin Point area of the Roan Cliffs are commonly 6-8 NE, while dips in the West Tavaputs Plateau are commonly 3-4 NE. The change in these dips was noticed in the early part of the 1986 field season and can be seen in Photo 2. In the late part of the 1986 field season views from Measured Section 37 located a distinct lineament in Sheep Canyon. This lineament and associated landslides have not been examined on foot but represent a northern part of the northwest trending flexure zone shown on both the Regional Map (scale 1"=2000') and the Geologic Map (scale 1"=1000'). The southern portion of this northwest trending flexure follows the pronounced topographic lineament associated with Range Creek as seen in Photo 1. In the SE/4, Section 11, T14S, R14E between the "thumb and finger" area dips of irregular orientations were noted by geologists working for Mono Power. This northwest trending flexure has gentle dips of 3-4 NE on the downthrown side and steeper dips of 6-8 NE on the upthrown side. Tar sands of 4-12wt% bitumen persist in the upthrown side of the flexure. Tar sands of 0-4wt% bitumen persist in the downthrown side of the flexure. Clearly the flexure has an important influence on the distribution of tar sands.
This segmented monoclinal flexure may have formed a subtle closure in the immediate vicinity of Bruin Point. Dips and strikes in the eastern and northern portions of the Sunnyside Tar Sands area change from 3-5 to 7-8 . To the west apparent dips are horizontal in the Left Fork of Whitmore Canyon. This data suggests a subtle closure may exist in the northern half of the Sunnyside Tar Sands area. Field data in the southern half is too limited to confirm complete structural closure. The indicated northern half of the closure approaches 500-1000 feet and exists within an area 6-8 miles long and 2-4 miles wide. The area of the suggested closure contains the principal tar sands. The area of closure is updip from the northwest trending flexure. Additional field work to the south will clarify the structural closure and the flexure.
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Green River Formation
The early sediments that formed within Eocene Lake Uinta belong to the Green River Formation and represent one of the largest accumulations of lacustrine sedimentary rocks in the world. The tar sands in the Sunnyside area are confined to rocks within three members of the Green River Formation. These three members consist from top to bottom of the Parachute Creek Member, Garden Gulch Member and Douglas Creek Member. The late sediments that formed within the central portion of Lake Uinta belong to the Uinta Formation or saline facies and do not exist in the Sunnyside Tar Sands area.
Terminology of rock units used within the Piceance Creek Basin and the eastern Uinta Basin is consistent but terminology of rock units used in the western Uinta Basin is not consistent and often confusing. Within the Piceance Creek Basin the Green River Formation was originally separated into three members consisting from top to bottom of the Parachute Creek Member, Garden Gulch Member and Douglas Creek Member by Bradley (19 31). In the Piceance Creek Basin and adjoining eastern Uinta Basin these three members continue to be used to describe the Green River Formation. Cashion (1967) used these three members to describe the Green River Formation within the eastern Uinta Basin extending from Raven Ridge near Dinosaur, Colorado to Desolation Canyon along the Green River some twenty miles east of Bruin Point. Raven Ridge is near the northeast shoreline of ancient Lake Uinta.
The Green River separates the eastern Uinta Basin from the western Uinta Basin and terminology of rock units changes across the boundary. Early common terminology in the western Uinta Basin included the green shale facies, delta facies and black shale facies. The three members of the Green River Formation are not commonly used. Within the western Uinta Basin the Parachute Creek Member is the only member of the Green River Formation with any usage. The green shale facies equates to the Garden Gulch Member. The delta and black shale facies equate to the Douglas Creek Member. In the northern part of the western Uinta Basin a black shale facies exists below the delta facies within the basal portion of the Green River Formation. Fortunately, carbonate rocks dominated by micrites and biomicrites exist in all three members of the Green River Formation (Picard, et al, 197 3) and help to differentiate the Green River Formation from the underlying Wasatch Formation. Recently, Fouch (1975) as well as Ryer, et al (1976) have added more terminology and defined the stratigraphic units in the western Uinta Basin on the basis of three lithologic assemblages that consist of open lacustrine, marginal lacustrine and alluvial with
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no reference to members of the Green River Formation. The open lacustrine rocks were deposited in open lake environments and consist of organic rich claystones and carbonates. The marginal lacustrine rocks were deposited in deltaic, interdeltaic and lake-margin carbonate-flat environments and consist of sandstones, claystones and weakly indurated clay carbonates. The alluvial rocks were deposited peripheral to the marginal lacustrine environments. The terminology of rock units in the western Uinta Basin is' confusing and not uniform. The approach used in the Sunnyside Tar Sands area combines member designation with environments of deposition and helps to present a coherent and simplified terminology.
Within the Sunnyside Tar Sands area geological mapping in 1980 separated the rocks into the standard three members of the Green River Formation. Specific field criteria were used to separate these three members as discussed in previous exploration reports of 1980-1982 and 1984. After the Green River Formation was separated into these three members, it was realized that the Parachute Creek Member represents the lake of gray shale facies, the Garden Gulch Member represents the shore of green shale facies, and the Douglas Creek Member represents the delta of red shale facies. Once these three dominant facies were recognized various aspects of the Sunnyside delta complex became more obvious. These three members and equivalent facies are diagramically shown in Figure 12.
Within the Green River Formation correlation is based on marker beds that include the Mahogany zone, Blue Marker and Orange Marker as used by Dyni (1969) and Ziemba (1974) in the Piceance Creek Basin. The Mahogany zone exists in the upper portion of the Parachute Creek Member. The Blue Marker exists at the base of the Parachute Creek Member. The Mahogany zone and the Blue Marker have now been located within the Sunnyside Tar Sands area. The Orange Marker exists in the Garden Gulch Member and below all the oil shale intervals in the Green River Formation as seen in Figure 13. The Orange Marker roughly correlates with the Carbonate Marker of Fouch, et al (1976) and Johnson (1985)...personal communication R.C. Johnson, 1987. The Orange Marker and Carbonate Marker are suggested to be intimately associated with the carbonate-rich Zones 25 and 26 of the Sunnyside Tar Sands deposit. The Orange Marker is either at the top of Zone 25 or the bottom of Zone 26. The top of Zone 25 is commonly 200-225 feet below the Blue Marker and has a distinct gamma ray peak of 500-600 API units.
Parachute Creek Member
Within the Sunnyside Tar Sands project area two significant markers have been identified within the Parachute
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Creek Member. The "upper marker" is the Mahogany ledge or zone and the "lower marker" is the Blue Marker. Regional correlations with the Uinta and Piceance Creek basins can now be made.
The purpose of this paragraph is to clarify Mahogany oil shale terminology as summarized from Donnell (1961), Cashion (1967) and Dyni (19 73). The Mahogany name is derived from the fact that polished surfaces of dark gray oil shale resemble old mahogany wood. The Mahogany ledge or Mahogany zone represents the mega terminology. The Mahogany zone formed between 45-46Ma (Mauger, 1977). The Mahogany ledge is a 2-60 foot thick outcrop sequence of multiple oil shale beds exposed at the surface. The subsurface equivalent of the Mahogany ledge is the Mahogany zone. The Mahogany ledge or zone contains tuffaceous marlstones at the top and bottom that are characterized on electric well logs by low resistivity values that form a trough-like or groove-like pattern. The A groove exists just above the top of the Mahogany zone and the B groove exists just below the bottom of the Mahogany zone. The A groove and B groove bracket the Mahogany zone or Mahogany ledge as seen in Figure 14. The B groove commonly forms a reentrant below the outcrops of the Mahogany ledge. The micro terminology includes the Mahogany bed and Mahogany marker. The Mahogany bed represents the thick oil shale beds containing the most kerogen and occurs near the middle to top of the Mahogany ledge or zone. The Mahogany bed is 3-10 feet thick and is the most useful widespread key bed in the Green River Formation. The Mahogany marker is a gray tuffaceous bed 3-6 inches thick that weathers to an orange-brown color and is located 3-20 feet above the Mahogany bed. The Mahogany marker is equivalent to the False Marker shown in Figure 14. Two altered volcanic tuff beds serve as additional marker horizons. A distinctive wavy-bedded analcitized tuff bed 10 inches to 5 feet thick exists 55-100 feet above the Mahogany bed and above the A groove. The wavy tuff is light gray to tan in color and weathers to gray and orange-brown colors. A distinctive curly contorted analcitized tuff bed less than one inch to eighteen inches thick exists 25-85 feet below the Mahogany bed, near the base of the Mahogany ledge and just above the B groove. The location of the Wavy Tuff and Curly Tuff are shown in Figure 14.
During the summer of 1986 field work in distal portions of the Sunnyside delta complex defined three common occurrences of oil shale intervals within the Parachute Creek Member. Field terminology of OS, , OS„ and OS., were used to categorize the three oil shale intervals. OS, exists at the base of the Parachute. OS^ exists some 200 feet above OS,. OS., is located some 300 feet above OS,. Well log research coupled with field data from measured sections defined the significance
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of OS-, and 0S ? , OS, is the "lower marker" and represents the Blue Marker of Dyni (1969) and Ziemba (1973). 0S2 is the "upper marker" and represents the Mahogany ledge. Measured sections 27-37 contain the oil shale intervals and exist in the West Tavaputs Plateau near Mt. Bartles, South Ridge and Horse Ridge. The regional topography is shown in Figure 2 and the measured sections are located on the Regional Map (scale 1"=2000'), Geology Map (scale 1"=1000') and Tar Sand Isopach Map (scale 1"=1000').
The lowest oil shale interval (OS,) is commonly weakly exposed in Measured Sections 27-37. OS, is 5-10 feet thick and commonly contains two separate moderate grade oil shale beds each about one foot thick. OS, is found near the characteristic color change in shales of the Parachute Creek and Garden Gulch Members. The shales of the Parachute Creek Member are dominantly light olive gray with a rock-color designation (Goddard, 196 3) of 5Y 6/1 to 6/2. The shales of the Garden Gulch Member are dominantly greenish gray with a rock-color designation of 5GY 6/1. These color differences as well as a change in the gamma ray background values are recognizable in the field. Gamma ray background values in the Parachute Creek Member are between 200-225cps with low values from 180-l90cps. Gamma ray background values in the Garden Gulch Member are between 250-300cps with a number of high peaks from 300-500cps. In the vicinity of the color change the reading interval for the surface spectrometer is decreased to 2-5 ft spacings to make a more detailed gamma ray strip log. With care the gamma ray doublet pattern at the base of the Parachute Creek Member can be established. OS, occurs at the base of the Parachute Creek Member and represents the "lower marker" in the Sunnyside Tar Sands area, it can be found anywhere in the Bruin Point-Mt. Bartles area unless eroded away as in the Whitmore Canyon subdelta and the proximal portions of the Dry Canyon subdelta.
The "lower marker" has been used since 19 80 by John Rozelle and exists at the base of the Parachute Creek Member. Field mapping, drill hole lithology and gamma ray logs from wells and the surface have all defined the same marker at the base of the Parachute Creek Member. The RC marker noted in drill hole files from Mono Power also corresponds to this "lower marker". Clearly this "lower marker" is ubiquitos and has a recognizable signature shown in Figure 15. The "lower marker" in the Sunnyside Tar Sands area represents the base of the. Parachute Creek Member. In the winter of 1986-1987 comparisons of well logs from the Sunnyside Tar Sands project and Rio Blanco Tract C-a project show nearly identical doublet patterns of gamma rays at the base of the Parachute Creek Member as shown in Figure 15. This doublet has the same characteristic peak and trough patterns from both surface and well log data over miles
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of horizontal separation. At Bruin Point the surface gamma log and Amoco No. 63 shown in Figure 15 are one mile apart in a downdip direction. The Sunnyside Tar Sands area and the Rio Blanco Tract C-a area are separated by one hundred miles and the doublet pattern is recognizable as shown in Figure 15. The "lower marker" used extensively at Bruin Point is at the base of the Parachute Creek Member. It is a recognizable major marker and is equivalent to the Blue Marker as used by Dyni (1967) and Ziemba (1974) within the Piceance Creek Basin.
The second oil shale interval (OS-) represents the "upper marker" in the Sunnyside Tar Sands area and corresponds to the Mahogany ledge or zone. The second oil shale interval (0S_) is well exposed in MS 29 (see Photo 4) and near MS 32 (see Photo 5). The best vertical exposures are in MS 29 and prominent lateral exposures over a distance of 2000 feet exist near MS 32. Other good exposures of OS_ occur in MS 30 and MS 36. Poor exposures of OS_ exist in MS 27, 28, 31 and 10. OS2 was not noticed in MS 35. OS- is commonly 20-25 feet thick and contains two prominent rich oil shale beds each 3-6 feet thick. Mono Power drill hole South Ridge No. 1 is located some 1000 feet north of MS 34 and played a prominent role in the initial definition of OS- from gamma-density well logs of BPB Instruments. Once the well log character of OS- was determined, OS- was also found in Amoco drill holes No. 60 and No. 63 and Mono Power drill holes BP-1A, RCT 11, 12 and 13. As seen from Figure 16 the Mahogany ledge (OS-) in MS 32 and Mahogany zone in drill hole Amoco No. 6 3 are characterized by a broad gamma ray low and an inclined three prong pattern over a 20 foot interval in the density curve. The easiest method to look for OS- in the just mentioned drill holes is to look for the inclined three prong pattern in the density curve. The low density values represent rich oil shale intervals. This inclined three prong pattern in the density curve is readily apparent in the Rio Blanco Tract C-a, Amoco Production drill hole Colorado Federal Tract A, CH-2 shown on the right side of Figure 16. This CH-2 well log serves as a standard for comparisons with the Sunnyside Tar Sands area. Within the CH-2 well log the inclined three prong pattern in the density curve exists over a 30 foot interval in the central portion of the 123 foot thick Mahogany zone. Within Amoco No. 63 the inclined three prong pattern in the density curve exists over a 21 foot interval. The true thickness of the Mahogany ledge or Mahogany zone in the Sunnyside Tar Sands area is not known as the resistivity curves needed to define A and B grooves do not exist because of dry hole conditions. The Mahogany ledge or zone in the Sunnyside Tar Sands area is a minimum of 21 feet thick. The Mahogany ledge or zone in the Sunnyside Tar Sands area is limited to areas northeast of the flexure zone with the exception of the immediate area of Mount Bartles.
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The third oil shale interval (OS.) consists of three thin moderate to rich oil shale beds each up to one foot thick that are localized within 30 vertical feet. Exposures of OS, were noted in MS 35 and 37. The OS, interval may represent the R-8 oil shale interval that exists above the Mahogany zone (i.e., R-7 noted by Ziemba, 19 74, p. 127) and shown in Figure 13. The Blue Marker is at the base of the R-2 oil shale interval. Within the Sunnyside Tar Sands area two oil shale intervals can be recognized and represent R-2 (Blue Marker) and R-7 (Mahogany Zone). Oil shale intervals R-3 through R-6 have not been recognized in the Bruin Point area and if present are very thin. The field terminology OS, corresponds to R-2 (Blue Marker); OS corresponds to R-7 (Mahogany ledge or zone). Two significant marker horizons exist in the Sunnyside Tar Sands area and represent the Blue Marker and the Mahogany ledge.
Garden Gulch Member
The Garden Gulch Member represents the shore facies, formed in marginal lacustrine environments and is characterized by fossilferous limestones, poorly bedded greenish gray shales and thinly bedded mixed color shales. Limestone beds dominate the lithology in carbonate-rich Zones 25 and 26 over a vertical distance of 70-120 feet. The limestones weather to a characteristic light brown (5YR hue - 5/6 chroma) to grayish orange (10YR 7/4) color and are readily distinguishable from a distance as seen in Photo 3. The abundant massive green shales have a distinct greenish gray (5GY 6/1) color and are readily apparent in the field. The greenish gray shales were deposited in shallow oxygenated waters as discussed in the 198 4 Exploration Report. The mixed colored shales include shales of purple, olive gray, greenish gray and reddish brown colors and were deposited under alternating wet and dry conditions associated with shallow water environments. The colors formed during long time intervals after deposition. The thickness of the Garden Gulch Member depends on its relative position in the Sunnyside delta complex. Proximal areas near the Roan Cliffs are commonly 200-400 feet thick. Distal areas in the West Tavaputs Plateau near Dry Creek Canyon and South Ridge are commonly 600-800 feet thick.
The Garden Gulch Member contains the most significant fossil assemblage within the Sunnyside delta complex. The limestones contain numerous intervals of ostracods, algal laminated sediments and algal heads. The most prominent algal head zone exists in MS 41 at the base of Zone 32 where a three foot interval with large algal heads are well-exposed along the jeep road that follows the crest of the ridge southwest of the Right Fork of Whitmore Canyon. Black garpike fish scales and turtle bone fragments are common in local
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intervals of intraformational conglomerates. Gastropods and plant fragments are rare occurrences in the green shales.
Two specific occurrences of gastropods were noted in the 1986 field season and were identified by John Hanley of the U.S.G.S. in October, 198 7. These two occurrences are:
1. MS 43-below Zone 35: Fossil Zone I contains two types of planorbid gastropods; a land snail washed into lake sediments, cf. Discus, species indeterminate; and a fresh water Planorbidae, genus and species indeterminate.
2. MS 39-below Zone 37: Fossil Zone I contains 2 species of fresh water gastropods that are both commonly associated in quiet fresh water settings; Planorbidae: Biomphalaria, species indeterminate and Physa: bridgerensid(?). These two gastrods lived in either a small lake within a delta plain or the shore of a large open lake.
MS 39 also contained two other fossil zones:
1. above Zone 99: round fish scales, species not determined.
2. above Zone 35: large quantities of palm fronds; species not identifiable by Jack Wolf of U.S.G.S. as the cuticle (thin film covering surface of plants) is not preserved.
Exposures of the Garden Gulch Member are extensive in the West Tavaputs Plateau and do not contain any significant tar sands. Zones 25 and 26 are thicker in the West Tavaputs Plateau than within the Roan Cliffs. The flora and fauna found within the Garden Gulch Member help to identify the nearshore environment associated with the green shales.
Douglas Creek Member
The importance of the Douglas Creek Member for tar sands in the distal portions of the Sunnyside delta complex and West Tavaputs Plateau is insignificant. Measured sections were commonly started below all tar sands, within a non-bituminous sandstone or at the beginning of the red shales. The Douglas Creek Member and its characteristic red shales was noted for 10-100 feet in thickness in seven of eighteen measured sections. In the proximal areas of the Sunnyside
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delta complex the Douglas Creek Member or delta facies is characterized by large volumes of bituminous sandstones and red shales. More complete descriptions of this member exist in Exploration Reports of 1980, 1981, 1982 and 1984.
Sunnyside Delta Complex
The Sunnyside delta complex is a sequence of laterally continuous stacked bituminous sandstone deposits alternating with red, green or gray shales. The delta system contains fluvial, deltaic, beach and nearshore deposits that formed at the margin of ancient Lake Uinta. The delta system is well-exposed along the Roan Cliffs for heights of 500-1500 feet, distances of 6-8 miles along depositional strike that parallel the Roan Cliffs, and for distances of 1-5 miles along depositional dip in canyons that exist between the Roan Cliffs and the West Tavaputs Plateau (see Figures 2 and 3). These extensive exposures are considered to be unique and offer an excellent opportunity to examine a lacustrine delta complex. In 1986 distal areas of the delta system were examined for the first time and work was largely concentrated in the West Tavaputs Plateau. This experience of work in the distal areas created a different orientation and perspective than work in the proximal areas along the Roan Cliffs. Measured Sections 27-44 were completed in 1986 and generally exist in distal areas of the Sunnyside delta system as seen in the Tar Sand Isopach Map and Table 1.
The Sunnyside delta complex has been defined on the basis of the distribution of tar sands with greater than fifty feet of cumulative thickness. The numerous bituminous sandstone deposits represent distributary channel, distributary mouth bar and beach deposits that form relatively continuous sheets of bituminous sandstones. The lateral continuity of these sandstone deposits is caused by a combination of factors that include: (1) bifurcating distributary channel deposits with high volumes of fine to very fine grained sandstone, (2) shoaled distributary mouth bars and (3) reworking of the distributary mouth bars by waves and longshore currents to form beach and nearshore sandstone deposits.
As seen on the Tar Sand Isopach Map, the Sunnyside delta complex has been divided into three separate areas that include the Bruin Point, Dry Canyon and Whitmore Canyon subdeltas. The Sunnyside delta complex has been separated into these three subdeltas on the basis of field expression, lithology, tar sand distribution and interpreted environments of deposition. An understanding of this delta complex and its subdeltas helps to comprehend the distribution of the tar sands.
The Sunnyside delta complex was formed in river-delta-beach-nearshore environments associated with the margins of
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Lake Uinta during Eocene time some 45-50Ma. As shown on the Tar Sand Isopach Map, the shoreline or depositional strike is parallel to the Roan Cliffs and oriented N40-50°W. The tar sands are distributed parallel to the ancient shoreline over a strike distance of six to eight miles. The tar sands are distributed along depositional dip or downslope from the ancient shoreline for a distance of one to five miles. The tar sands are distributed over a vertical range of 200 to 1200 feet.
During its development the Sunnyside delta complex experienced a major prograding phase in Douglas Creek time within the Bruin Point subdelta and a major prograding phase in Garden Gulch time within the Dry Canyon and Whitmore Canyon subdeltas. The major transgressive phase occurred in Parachute Creek time. In addition numerous minor transgressions and regressions formed cyclic deposition. Eleven to fifteen important cycles or repeated intervals of sandstone-shale-limestone sequences range from fifty to one hundred-fifty feet thick. These repeated cycles formed from alternating wet and dry climatic conditions and result in multi-stacked shorelines in the vicinity of Bruin Point.
Field interpretations suggest that the Bruin Point subdelta is the oldest and the Whitmore Canyon subdelta is the youngest. Within the Bruin Point subdelta the tar sands are largely confined to the Douglas Creek Member. Within the Dry Canyon and Whitmore Canyon subdeltas the tar sands are largely confined to the Garden Gulch Member. The Tar Sand Isopach Map indicates a dominant northwest trend of the bituminous sandstones with the thickest concentrations in the vicinity of Bruin Point. The northwest trend parallels the ancient shoreline and represents depositional strike. The main drainage that formed the delta complex flowed northeast and represents the direction of depositional dip.
Within the Sunnyside Tar Sands deposit the bitumen pay zones are almost exclusively confined to the porous and permeable sandstones deposits. These bituminous sandstones have a dominant sheet-like distribution that thicken in areas of major channel and distributary mouth bar deposits. Sheet sands are ubiquitous throughout the Sunnyside delta complex and formed under different conditions. Thin sheet sands are commonly 10-20 feet thick and represent beach and nearshore bar deposits. Thick sheet sands are commonly 30-60 feet thick and represent dispersed distributary channel and distributary mouth bar deposits. Massive bituminous sandstone deposits often 100-250 feet thick represent localized major channel and/or distributary mouth bar deposits. These massive bituminous sandstone deposits are associated with major influxes of sand during a prograding phase. Beach and nearshore bar deposits
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are more commonly associated with sandstone dispersal from waves and longshore currents or from a minor transgressive phase. The sandstone units are commonly 40-150 feet thick in the proximal portions of the delta and commonly 10-30 feet thick in the distal portions of the delta.
Bruin Point Subdelta
The Bruin Point subdelta is characterized by extensive zones of bituminous sandstones of consistent bitumen content, intervening red shales and four to fifteen numbered tar zones. The thickest tar sand accumulations exist near Bruin Point as seen on the Tar Sand Isopach Map. Large areas of cumulative MSAT's (main saturated zones) up to 300-700 feet thick are localized in the area of Bruin Point and Range Creek as seen on the Tar Sand Isopach Map. The Bruin Point subdelta represents the primary deposition center of the Sunnyside delta complex and contains portions of the Parachute Creek, Garden Gulch and Douglas Creek Members as seen in Figure 12. The Bruin Point subdelta was the area of principal investigation in 1978, 1980, and 1981. Seven of forty-four measured sections have been completed in proximal and medial portions of the Bruin Point subdelta as seen in Table 1 and Table 10. Twenty-four of forty-eight deep Amoco drill holes have been completed in the Bruin Point subdelta as seen in Table 14 of the 1984 Exploration Report. The largest volume of tar sands are localized within the upper portion of the Douglas Creek Member and are contained within a nine hundred foot thick zone on the Roan Cliff face that thins over a distance of two miles to a two hundred foot thick zone in the vicinity of Range Creek. The Bruin Point subdelta contains about seventy-five percent of the total mineable tar sands within the entire Sunnyside delta complex. The tar sands are associated with distributary channels, distributary mouth bars and beach-bar deposits.
The Bruin Point subdelta has a large arcuate or lobate shape as seen on the Tar Sand Isopach Map. The cause of this lobate shape is suggested to be from extensive sediment influx and partial modification by waves in the shore margin of Lake Uinta. The Bruin Point subdelta is considered to be fifty to seventy-five percent fluvial dominated and twenty-five to fifty percent wave influenced.
The lithology of the Bruin Point subdelta based on 17,725 feet of core is: 31.9% sandstone; 47.6% shale; 6.6% limestone; 12.3% siltstone; and 1.6% conglomerate. The siltstones and conglomerates are commonly associated with the sandstones. If the lithology is tabulated by delta, shore, and lake facies the changes in the percent sandstone, shale, limestone and siltstone-conglomerate are dramatic as seen below:
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Lithology Delta Shore Lake
ss% SH% LS%
SL% & CG%
53.4 28.5 1.5
16.6
22.3 53.5 11.4 12.8
4.9 86.1 1.5 7.5
The sandstone content decreases rapidly from delta to shore to lake. The shale content increases rapidly from delta to shore to lake. Limestone content increases in shore environments. The siltstone and conglomerate content decreases gradually from delta to shore to lake.
Dry Canyon Subdelta
The Dry Canyon subdelta is characterized by extensive zones of bituminous sandstones of consistent bitumen content, intervening green shales and three to seven numbered tar zones. The Dry Canyon subdelta represents the secondary deposition center of the Sunnyside delta complex and contains portions of the Garden Gulch and Douglas Creek Members. The Dry Canyon subdelta contains cumulative MSAT's up to 200-400 feet thick as seen on the Tar Sand Isopach Map. The Dry Canyon subdelta was the principal area of investigation in 1982, 1984 and 1986. Twenty-nine of forty-four measured sections have been completed in proximal, medial and distal portions of the Dry Canyon subdelta as seen in Table 1 and Table 11. Twenty-four of forty-eight deep Amoco drill holes have been completed in the Dry Canyon subdelta as seen in Table 15 of the 1984 Exploration Report. The major tar sands are within the Garden Gulch Member and localized within a four hundred foot thick zone on the Roan Cliff face that thins downdip over a distance of one mile to a two hundred foot thick zone beneath the Dry Canyon ridge road. This subdelta contains about twenty percent of the total mineable tar sands within the entire Sunnyside delta complex. The tar sands are primarily contained within distributary mouth bar and beach bar deposits.
The Dry Canyon subdelta is a fluvial-dominated elongated delta system as suggested by the three mile long Dry Canyon distributary-like ridge that extends northeast from the Arco water tank. The elongated type of delta system is characterized by fluvial dominance and weak wave energy. Within the well-dissected Dry Canyon subdelta much of the present topographic expression is an expression of paleo-geomorphology. Present topographic ridges and bulges are underlain by tar sands as determined by both field work and drill hole information.
As seen on the Tar Sand Isopach Map the Dry Canyon and Bruin Point subdeltas have different configurations. They are adjacent to each other and interfinger near their transitional boundary in the "NOL" and "Lazy L" areas. Near this transitional boundary of the Bruin Point and Dry Canyon subdeltas
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there is an abrupt four hundred foot change in elevation at 20,000 NW to 22,00 0 NW as shown on the Regional Map. The Parachute Creek Member has been completely eroded away within the Dry Canyon subdelta but within the Bruin Point subdelta the Parachute Creek Member is commonly 100-300 feet thick. Within the Dry Canyon subdelta the Garden Gulch Member thickens gradually from 400-500 feet near the Roan Cliff face to 800-1000 feet two miles down depositional dip. The lithology of the Dry Canyon subdelta based on 17,8 35 feet of core is: 40.4% sandstone; 40.5% shale; 7.1% limestone; 10.3% siltstone; and 1.7% conglomerate.
Lithologic differences between the Dry Canyon and Bruin Point subdeltas are significant with pronounced changes in percent sandstone and shale as listed below:
Lithology
SS% SH%
All
Dry Canyon Subdelta
40.4 40.5
Members
Bruin Point Subdelta
31.9 47.6
The Dry Canyon subdelta is characterized by 8.5 percent more bituminous sandstone and 7.1 percent less shale than the Bruin Point subdelta.
If only the Garden Gulch Member is examined, the lithologic differences between the Dry Canyon and Bruin Point subdeltas are more pronounced as listed below:
Garden Gulch Member
Lithology Dry Canyon Bruin Point Subdelta Subdelta
SS% 41.1 22.3 SH% 39.9 53.5 LS% 7.7 11.4
Within the Dry Canyon subdelta the Garden Gulch Member has a 84.3 percent increase in sandstone content and a 25.4 percent decrease in shale content. This indicates that the amount of sandstone deposition increased during Garden Gulch time in the vicinity of the Dry Canyon subdelta. It also suggests that lateral accumulation occurred in a northwest direction from the Bruin Point subdelta to the Dry Canyon subdelta and that the Dry Canyon subdelta is younger than the Bruin Point subdelta.
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Whitmore Canyon Subdelta
The Whitmore Canyon subdelta is characterized by extensive zones of bituminous sandstones of variable bitumen content, intervening mixed colored shales and four to six numbered tar zones. The principal portion of the tar sands are localized in the Garden Gulch Member and associated with minor distributary mouth bar and beach-bar deposits. Nine of forty-four measured sections have been completed within proximal, medial and distal portions of the Whitmore Canyon subdelta as seen in Table 1 and Table 12. Limited information from twelve drill holes is available and listed on the Regional Map but the core has not been examined for Amoco. As seen from the Tar Sand Isopach Map the area contains a major tar sand strip 2-3 miles long by 1000-2000 feet wide. This elongated strip contains cumulative MSAT's up to 100-200 feet thick. This subdelta is suggested to contain some five percent of the total mineable tar sands within the entire Sunnyside delta complex and is the least significant area of bituminous sandstones.
The Whitmore Canyon subdelta represents a lower delta plain to delta fringe sequence of distributary channel and distributary mouth bar deposits dominated by intervening mixed color shales and algal-ostracodal limestones formed in interdistributary bays. Red shales of the lower delta plain environments exist near the oil/water contact shown on the extreme left side of the Geologic Map in section 23 and 14 of T13S, R13E. The Whitmore Canyon subdelta represents the wanning stages of deltaic deposition within the Sunnyside delta complex.
In 1980 Great National drilled holes GN-13 and GN-15 as listed on the Regional Map. Limited information on the GN drill holes is available from a May, 1982 report submitted to the U.S. Synthetic Fuels Corporation and data supplied by Chevron Resources to Golder Associates in the summer of 1983. GN-15 contains five bituminous zones 21-77 feet thick with bitumen averages that range from 7.8 to 10.2 weight percent. These five zones total 245 feet. Four of these zones have a weighted average of 8.6 weight percent bitumen or approximately 20 gallons per ton. GN-13 contains five bituminous zones 19-84 feet thick that total 210 feet. Three of these zones have bitumen averages that range from 6.1 to 6.9 weight percent. These three zones total 170 feet with a weighted average of 6.5 weight percent bitumen or approximately 15.5 gallons per ton. The Mono Power files obtained from Morrison-Knudson in the fall of 1986 do not contain any significant additions to this Great National data but do decrease the MSAT thickness in GN-15 from 245 feet to 148 feet and in GN-13 from 210 feet to 170 feet.
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During the summer of 1983 Mono Power drilled nine holes within the Whitmore Canyon subdelta. The location and drill hole information of these nine holes are shown on the Regional Map, Tar Sand Isopach Map and Geology Map. The 5067 feet of core from the Whitmore Canyon area has not been examined for Amoco.
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PERIPHERAL HYDROCARBON LEASES
Field work in the area of Mount Bartles and South Ridge provided three important results:
1. evaluation of the peripheral hydrocarbon leases at minimum cost;
2. location of a significant flexure that represents a mega control for the tar sands in the entire Sunnyside deposit;
3. complete recognition of two important marker horizons and partial recognition of another marker. All three markers exist in the area of the Sunnyside Tar Sands deposit.
Peripheral portions of the Sunnyside Tar Sands deposit exist in an area some four to seven miles north of Bruin Point, one to five miles east of Mount Bartles and within portions of the West Tavaputs Plateau shown in Figures 2 and 3. These peripheral portions exist within the northern half of hydrocarbon leases contolled by Amoco Production as outlined in Figure 18 and encompass 5340 acres within 13 sections. Eighty percent of this acreage exists in Tracts 1 and 3 of Figure 18 and near South Ridge as seen in Figure 17. Investigation and evaluation of Tracts 1, 3, 6 and 7 was the major task of the 1986 field season and accomplished by eleven measured sections located in Figure 17. Alternatively, investigation of the peripheral hydrocarbon leases could have been accomplished by thirteen condemnation drill holes at selected sites shown in Figure 17. These drill sites were selected by John Rozelle, of Pincock, Allen and Holt, and myself using criteria of one hole per half section as suggested by John Hasche of Amoco Production.
Thirteen condemnation holes in the peripheral area would cost at least $50,000 per hole if each hole averaged 1000 feet with a full exploration cost of $50 per foot. The actual drilled footage might have ranged between 600-800 feet, but the remoteness of this peripheral area would increase overall costs. Travel time from Price to the campsite location on South Ridge near Bus Spring is 3% hours. Exploration costs in the less remote Bruin Point area have ranged from $62.08 to $45.03 per foot during four drilling seasons with average exploration costs of $51.50 per foot of drilling. Stone Cabin Spring is located about one mile northeast of Mount Bartles and produces some 5000gpd throughout the summer and represents the only adequate water source for drilling in the peripheral area.
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In lieu of condemnation drilling it was decided that measured sections be used to evaluate the peripheral area. The success of detailed measured sections to determine tar sand reserves goes back to the winter of 1981 when John Rozelle and I were asked for geologic reserves in the North Area (or Dry Canyon subdelta) after completion of the 1981 exploration program. John and I mentioned that the data base consisted of six measured sections with no surface samples and one deep drill hole at Shell No. 1 with tar sand analyses. Reserves were calculated by John Rozelle based on the detailed measured sections and re-evaluated data of Shell No. 1. The reserves were within five percent of the reserves calculated after two extensive drilling programs completed in the North Area during 1982 and 1984. Detailed measured sections with limited drill hole information is an effective method to calculate tar sand reserves within the Sunnyside Tar Sands deposit.
The eleven measured sections completed within the peripheral area of hydrocarbon leases are located in Figure 17 and on the Tar Sand Isopach Map. As shown in Figure 17 the MSAT values of MS 27-31 and MS 34-37 range from 0-23 feet. MSAT refers to Main Saturated Zones that consist of cumulative thicknesses of tar sands which are a minimum of 10 feet thick and contain a minimum of 10 gallons of bitumen per ton. Data on four drill holes was found within the Mono Power files. These four drill holes are Phillips No. 1, Phillips No. 2, Mono Power South Ridge No. 1 and Mono Power Stone Cabin Draw No. 1. The location and data from these four drill holes are included on the Regional Map. The location and MSAT data of these four drill holes are shown in Figure 17 and indicate MSAT values between 0-22 feet. The areas within Tracts 1, 3, 6 and 7 of Amoco's Hydrocarbon Leases clearly do not contain any significant tar sands. John Rozelle and I concur that the MSAT values are so low that it is not worth calculating geological reserves. Measured Sections 32 and 33 exist near the flexure and outside the hydrocarbon lease area. MS 32-33 contain an isolated area of MSAT values from 98-170 feet as shown on the Tar Sand Isopach Map.
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MEASURED SECTION SYNTHESIS
In 1986 eighteen measured sections were completed and field mapping discovered an important flexure. The detailed measured sections helped to locate and define three important markers within the Green River Formation. The 19 86 field season was the first time that the major emphasis was on field mapping and measured sections. In previous exploration years the major focus was on core drilling with minor emphasis on measured sections. Since 1980 forty-four measured sections have been completed over vertical heights that total 33,882 feet. The yearly breakdown is as follows:
Year Measured Section Vertical Height
1980 1- 6 6437 1981 7-11 4184 1982 12-17 3929 1984 18-26 6967 1986 17-44 12365
All locations of measured sections are now categorized by proximal, medial and distal positions within the Bruin Point, Dry Canyon and Whitmore Canyon subdeltas as listed in Table 1. Tables 2 and 3 are a complete listing of elevation and member thickness data for Measured Sections 1-44.
The gamma ray well logs coupled with lithology have been used to establish and correlate specific numbered tar zones in drill holes. The gamma ray logs have proved to be the best correlation tool in the project area. Since the gamma ray well logs are highly effective in the determination and correlation of numbered tar zones, attempts were first made in 19 86 to apply the principle to measured sections. A portable spectrometer was used to obtain gamma ray readings while completing the detailed measured sections. Gamma ray well logs commonly have high values associated with some limestones. In the field it was noted that high gamma ray values were associated with some limestones, local conglomerates and basal portions of sandstone units overlying green shales. Plots of the surface readings of gamma rays along old measured sections were made and compared favorably with nearby gamma ray well logs. The portable spectrometer was then purchased in lieu of continued rental. General log patterns, high value peaks and similar lithology have all been used to correlate strip logs and to determine tar zone numbers. Now tar zone numbers can be established on measured sections and are indicated on the strip logs. The portable spectrometer is necessary to establish numbered tar zones and delineate local marker beds. The portable instrument is of substantial aid in field correlations throughout the project area.
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00670
Important cycles of sandstone, shale and limestone deposition exist in all measured sections and are repeated throughout the Sunnyside delta complex at relatively evenly spaced intervals. These cycles contain a paraconformity (erosion surface parallel to bedding) at the top of limestone interval. Next a sandstone interval is deposited which grades into a shale interval that in turn grades into a limestone interval which is followed by an erosion interval. Then the sandstone-shale-limestone-erosion sequence is repeated. This repeated sequence was previously noted in the Amoco drill core. At least fifteen major and eleven minor cycles of these repeated sequences at relatively evenly spaced intervals exist in the Sunnyside Tar Sands deposit. All unconformities (erosional intervals) in this area are parallel to the bedding planes. The explanation for these repeated cycles is either structural or climatic. Structural evidence is not apparent and the numerous influxes of sand have a consistent grain size. This repetition of sandstone-shale-limestone sequences is suggested to be caused by periodic wet and dry climatic conditions. Influxes of sand are associated with wet conditions and the limestones developed during dry conditions. Major changes in climatic conditions are known to be associated with Milankovitch cycles. These cycles are caused by changes in the earth's orbital geometry and result in climatic cycles of 100,000 year, 43,000 years and 23,000 years (Hays, et al, 1976).
Salient observations from MS 27-44 can be separated into five categories that include bitumen, sandstones, sedimentary structures, carbonates and oil shales.
Bitumen: The best tar sands are located updip from the flexure. Bitumen grades of 4-12wt% are common on the updip side that encompass the Roan Cliffs and Bruin Point. Bitumen grades of 0-4wt% are common on the downdip side of the flexure that encompass the West Tavaputs Plateau and South Ridge.
Sandstones: Sandstones commonly exist above eroded limestones. In distal nearshore environments sandstone units may laterally change to siltstones. Zone 10 commonly exists in the distal portions of the three subdeltas above the second oil shale interval and may correlate with the Horsebench Sandstone. Zones 10, 11, 21 and 23 are commonly separated by 150 foot intervals and represent minimal influxes of sand. Zones 31, 32 and 33 are commonly separated by 30-40 foot intervals and represent minor influxes of sand. Zones 35 and 36 are commonly separated by 40-6 0 foot intervals and represent major influxes of sand.
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00671
Sedimentary Structures:
Carbonates
Oil Shale
The vertical sequence of sedimentary structures within a sandstone interval can be categorized into three types: Type III -all planar bedding; Type II - cross bedding on bottom and planar bedding on top; Type I -cross bedding on bottom, planar bedding in middle and ripple bedding on top. Within Zones 10, 11, 21 and 23 Type III is dominant and Type II is secondary. Within Zones 31, 32, 33, 35, 36 and 37 Type II is dominant, Type III is secondary and Type I is minor to rare.
The limestone intervals weather to a characteristic orange brown color and can be readily recognized from a distance. In the middle to upper portion of the Garden Gulch Member a major carbonate-rich interval averages about 80 feet thick. It contains a lower carbonate-rich zone about 30 feet thick (Zone 26) and an upper carbonate-rich zone about 35 feet thick (Zone 25). Zones 25 and 26 have distinct gamma ray logs and can be correlated throughout the Bruin Point and Dry Canyon subdeltas. Erosion has removed Zones 25 and 26 from the Whitmore Canyon subdelta.
A lower oil shale unit 3-5 feet thick exists at the base of the Parachute Creek Member. A second often prominent oil shale unit . 20-25 feet thick exists some 200 feet above the lower oil shale unit, and is exposed or inferred to exist in MS 27-32 and MS 34-37. MS 33 was stopped near the lower oil shale unit.
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00672
TAR SANDS
The distribution of tar sands in the Sunnyside deposit is related to both structure and lithology. The structural control is associated with a northwest trending flexure within a large monoclinal system that slopes into the Uinta Basin. The lithologic control is determined by porous and permeable sandstones deposited in the Sunnyside delta complex.
The monoclinal structure is vividly seen in Photo 1. The monoclinal structure in the West Tavaputs Plateau dips 3-4 northeast and contains tar sands with 0-4wt% bitumen. The monoclinal structure in the Roan Cliffs dips 7-8 northeast and contains tar sands with 4-12wt% bitumen. The change in monoclinal dips is seen in Photo 2 and caused by a northwest-trending flexure that extends along Range Creek, passes just east of Mt. Bartles and has a distinct topographic expression in Sheep Canyon. The trend and location of this flexure are shown on the Tar Sand Isopach Map. Additional field work is needed along portions of Range Creek, Dry Canyon ridge and Sheep Canyon to better define specific aspects of this previously unmapped structure. This flexure represents a mega control for the distribution of bitumen in the Sunnyside Tar Sands deposit. The extensive, massive and rich (5-12wt% bitumen or 12-28gpt) tar sand deposits along the Roan Cliff face are located 0-2 miles updip from this flexure. Limited, thin and low grade (l-4wt% bitumen or 2-10gpt) tar sand deposits exist 1-5 miles downdip from the flexure.
The Tar Sand Isopach Map illustrates four distinct factors about the Sunnyside Tar Sands deposit. First, the thickest portion of the tar sands exist near Bruin Point. Second, the tar sands are concentrated within a northwest trending belt. Third, erosion has removed portions of the tar sands. Fourth, the Sunnyside Tar Sands deposit formed within a delta complex that can be divided into three subdeltas. In addition, the tar sands of Sunnyside delta complex are concentrated in an area that is eight miles long and one to three miles wide. The long northwest trend represents depositional strike and the short northeast trend represents depositional dip. The outcrops along the Roan Cliffs represent stacked deltaic and shoreline sequences.
The most significant bitumen concentrations are confined to porous and permeable sandstone deposits of the Sunnyside delta complex. These tar sands have an average porosity of 27% and an average permeability of 812md. Minor amounts of bitumen are localized in less porous and less permeable silt-stones and limestones. The bituminous siltstones have an average porosity of 22% and an average permeability of 64md. The bituminous limestones have an average porosity of 18% and an average permeability of lmd as noted in the 19 84 Exploration Report.
30
00673
Specific saturation data from MS 1-44 is listed in Table 4 and shows irregular, scattered differences unless logical separations are made. The location of measured sections is separated into proximal, medial and distal portions of sub-deltas. Proximal portions are within ±0.5 miles of the Roan Cliff face. Medial portions are within 0.5-2 miles downdip of the Roan Cliff face. Distal portions are 2-4 miles downdip of the Roan Cliff face. Separation, tabulation and analysis of the saturation data in Table 4 into subdeltas portions illustrates some significant trends as summarized from Tables 5 and 6 and listed below:
MSAT Thickness
Subdelta Proximal Medial Distal
Bruin Point 430 107 Dry Canyon 231 81 6 Whitmore Canyon 122 32 0
Clearly the proximal portions of the subdeltas contain the thickest accumulations of saturated sandstones. Thinning of the saturated sandstones from proximal to medial to distal portions is pronounced. From the above data the Bruin Point subdelta contains almost twice the MSAT thickness of tar sands in the Dry Canyon subdelta. And the Dry Canyon subdelta contains almost twice the MSAT thickness of tar sands in the Whitmore Canyon subdelta.
Specific data of numbered tar zones in MS 1-44 exist in Table 10 for the Bruin Point subdelta, in Table 11 for the Dry Canyon subdelta and in Table 12 for the Whitmore Canyon subdelta. Thickness values of these numbered tar zones within proximal, medial and distal portions of the three subdeltas are listed in Tables 7 and 8. Tabulation of this thickness data indicates minor differences between these numbered tar zones as listed below:
Average Thickness of Numbered Tar Zones
Subdelta Proximal Medial Distal
Bruin Point 47 21 Dry Canyon 44 23 17 Whitmore Canyon 30 25 17
Note: No measured sections have been completed in the distal portions of the Bruin Point subdelta.
31 00674
The numbered tar zones clearly diminish in thickness from proximal to medial to distal portions of the subdeltas. Within the Bruin Point and Dry Canyon subdeltas the average thickness of numbered tar zones essentially decrease by 50% from the proximal to medial positions over an average distance approaching one mile. Within the Whitmore Canyon subdelta the average thickness of numbered tar zones decreases by 25% from proximal to medial and medial to distal. The thickness of numbered tar zones from proximal to medial portions changes more dramatically within the Bruin Point and Dry Canyon subdeltas than within the Whitmore Canyon subdelta.
Specific saturation data from thirty-five non-Amoco drill holes in the Sunnyside Tar Sands deposit was determined from the Mono Power files and is listed in Table 9 and the Regional Map. This new data from Arco, Great National and Mono Power drill holes has been partially utilized in this report.
32 00675
SURFACE GEOPHYSICS
Surface gamma ray logs along measured sections have proved to be valuable for determination and correlation of numbered tar zones and delineation of marker horizons. The gamma ray readings are obtained from a portable 3.3 pound Urtec gamma ray spectrometer. The idea to use this exploration method evolved from two factors. First, the successful use of gamma ray well logs to establish numbered tar zones at Sunnyside and, second, a short article by Chamberlain (19 84) describing the successful use of surface gamma ray logs for correlations in areas of abundant outcrops and sparse well control.
In the Sunnyside Tar Sands deposit numbered tar zones were established by use of geophysical and geological data. Initially, gamma ray well logs, frequency of intercepts in drill holes and assay data were completed on a hole by hole basis. Specific tar sand intervals were defined by John Rozelle. These intervals were then correlated with detailed lithology and depositional environments of core logs to establish numbered tar zones. From this investigation fifteen tar zones were defined and represent the major mineable tar zones and include Zones 11, 21, 23, 25, 26, 31, 33, 35, 36, 37, 38, 41, 42, 43, 45. Zones 25 and 26 are bituminous limestones and all the other zones are bituminous sandstones. When the gamma ray well log, density well log, lithology and environments of deposition are used in combination, numbered tar zones can be determined. This method works well with subsurface data and was applied to surface data.
Four old measured sections were selected and reoccupied to evaluate the validity of this new surface exploration method. A methodology was developed and correlations of surface gamma ray logs with downhole gamma ray logs from Amoco drill holes was completed. After encouraging results the used Urtec minispec UG-135 was purchased for the project and use in MS 27-44.
The methodology for field use of the minispec was developed by Roger Grette. An over-the-shoulder strap system keeps the instrument suspended and the hands are free while walking and recording data. Check the switch to make sure the batteries are in good condition and always carry a set of spare batteries. Select a base station at least thirty feet from the vehicle and take a reading at the beginning and end of each day. Adjustments to recorded readings should be made if significant differences exist. In 1986 no adjustments were made as the diurnal change was ±10cps. Readings are taken at consistent slope distances of 5, 10 or 20 foot intervals along the 100 foot tape, depending on the desired reading interval, steepness of slope and differences in lithology.
33
00676
The meter mode switch is set to tc(10), which is the 10 second count mode. The audio switch is kept at 250cps for normal background. Any anomalously high or low readings are recorded regardless of the footage. Before the reading is taken the minispec should be placed near the best outcrop or least amount of overburden. Readings are taken 6 inches above the ground or 6 inches away from an outcrop to maximize reliable and consistent results. Gamma ray values are read off the digital readout for the first full 10 second period and recorded in a notebook. High gamma ray readings are often at the sandstone-shale contact and just below the sandstone overhangs. Care should be taken to check for higher readings in nearby outcrops or by digging with a boot heel into loose overburden. High gamma ray values near 400-500cps cause the instrument to release a high pitch sound. When no noise occurs the gamma ray values are below background levels and the audio switch can be put to a lower level.
Strip logs were made of these recorded surface gamma ray values and commonly showed distinct patterns and at least three spikes of high gamma ray values per measured section. The gamma ray patterns, tar sand intervals, detailed lithology and environments of deposition are all utilized to correlate intervals and select numbered tar zones. The minispec is invaluable in this correlation as it establishes definite picks and removes the guess work. The detailed surface gamma ray logs coupled with detailed measured section data are a powerful field method to establish numbered tar zones and locate marker horizons. The lithology serves as a guide to location of the marker horizons. Detailed surface gamma ray readings taken at 1, 2 or 3 foot intervals can form log patterns that are nearly identical to well log patterns as seen in Figure 15 and 16. In Figure 15 the surface gamma ray readings at Bruin Point were taken at 0.5-2 foot vertical intervals. In Figure 16 the surface gamma ray readings near the top of MS 32 were taken at 1-3 foot vertical intervals.
Within the project area gamma ray values in 1986 ranged from 179-1516cps with common values of 250-300cps. Values less than 200 cps are associated with oil shale and values greater than 350cps are considered anomalous and termed spikes or kicks. Analysis by Core Labs of samples with peak values (1153 and 1516cps) indicates that the largest portion of gamma rays are emitted.from the uranium series. The specific peaks are related to Bi and equivalent to radium concentrations derived from uranium ores. The source area for the sands and shales in the Sunnyside delta complex was the Uncompahgre uplift. Significant uranium mines exist on the flanks of the Uncompahgre uplift near Uravan, Colorado and Moab and LaSal, Utah. Low grade uranium ores near Moab were tested with the portable mini-spectrometer and values up to 15,000-20,OOOcps were obtained. Gamma ray values from the minispec are recorded in cycles per second (cps), while gamma ray values from well logs are recorded in American Petroleum Institute (API) units. Calibration of cps to API units can only be accomplished at the API test pit in Houston.
34 00677
REFERENCES
Anders, D.E. and Gerrild, P.M., 1984, Hydrocarbon generation in lacustrine rocks of Tertiary age, Uinta Basin, Utah -organic carbon pyrolysis yield, and light hydrocarbons: in Hydrocarbon Source Rocks of the Greater Rocky Mountain Region (eds., J.Woodward, F.F. Meissner and J.L. Clayton); Rocky Mtn. Assoc. Geol., pp. 513-529.
Bradley, W.H., 1931, Origin and microfossils of the oil shale of the Green River Formation of Colorado and Utah: U.S. Geol. Survey, Prof. Paper 168, 58 p.
Cashion, W.B., 1967, Geology and fuel resources of the Green River Formation, southeastern Uinta Basin, Utah and Colorado: U.S. Geol. Survey, Prof. Paper 548, 48 p.
Chamberlin, A.K., 1984, Surface gamma ray logs: a correlation tool for frontier areas: Amer. Assoc. Petrol. Geol. Bull., v. 68, no. 8, pp. 1040-1043.
Cole, R.D., 1985, Depositional environments of oil shale in the Green River Formation, Douglas Creek Arch, Colorado and Utah in Geology and Energy Resources, Uinta Basin, Utah (ed., M.D. Picard) ; Utah Geol. Assoc, pp. 211-224.
Coleman, J.M., and Gagliano, S.M., 1965, Sedimentary structures: Mississippi River delta plain in Primary Sedimentary Structures and Their Hydrodynamic Interpretation (ed., G.V. Middleton); Soc. Econ. Paleo. and Mineral. Spec. Publ. 12, pp. 133-148.
Crawford, A.L. and Pruitt, R.G., 1963, Gilsonite and other bituminous resources of central Uintah County, Utah in Oil and Gas Possibilities of Utah, re-evaluated (ed., A.L. Crawford); Utah Geological and Mineralogical Survey Bull. 54, pp. 215-229.
Dickinson, W.R., Lawton, T.F., and Imman, K.F., 19 86, Sandstone detrital modes, central Utah foreland region: stratigraphic record of Cretaceous-Paleocene tectonic evolution: Jour. Sed. Pet., v. 56, pp. 276-293.
Donnell, J.R., 1961, Tertiary geology and oil shale resources of the Piceance Creek basin between the Colorado and White Rivers, northwestern Colorado: U.S. Geol. Survey, Bull. 1082-L.
Dyni, J.R., 1969, Structure of the Green River Formation, northern part of Piceance Creek Basin, Colorado: The Mountain Geologist, v. 6, no. 2, pp. 57-66.
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00678
Eardley, A.J., 1968, Major structures of the Rocky Mountains of Colorado and Utah: Univ. of Missouri Jour., no. 1, pp. 79-99.
Fouch, T.D., 1975, Lithofacies and related hydrocarbon accumulations in Tertiary strata of the western and central Uinta Basin, Utah in Symposium on Deep Drilling Frontiers in the Central Rocky Mountains (ed., D.W. Bolyard); Rocky Mtn. Assoc. Geol., pp. 163-173.
Fouch, T.D., Cashion, W.B., Ryer, R.T., and Campbell, J.H., 1976, Field guide to lacustrine and related nonmarine depositional environments in Tertiary rocks, Uinta Basin, Utah in Professional Contributions of Colorado School of Mines No. 8 (eds., R.C. Epis and R.J. Weimer); pp. 358-385.
Fouch, T.D., Lawton, T.F., Nichols, D.J., Cashion, W.B., and Cobban, W.A., 1983, Patterns and timing of synorogenic sedimentation in upper Cretaceous rocks of central and northeast, Utah in Mesozoic Paleography of the West-Central United States (eds., M.W. Reynolds and E.D. Dotty); Rocky Mtn. Sect. Soc. Econ. Paleo. and Mineral., pp. 305-336.
Goddard, E.N., et al, 1963, Rock-color chart: Geol. Soc. of Amer.
Greis, R., 1983, North-south compression of Rocky Mountain foreland structures in Rocky Mountain Foreland Basins and Uplifts (ed., J.D. Lowell); Rocky Mtn. Assoc. Geol., pp. 9-32.
Johnson, R.C, 1985, Early Cenozoic history of the Uinta and Piceance Creek Basins, Utah and Colorado with specific references to the development of Eocene Lake Uinta in Cenozoic Paleogeography of the West-Central United States (eds., R.M. Flores and S.S. Kaplan); Rocky Mtn. Sect. Soc. Econ. Paleo. and Mineral., pp. 247-276.
Lawton, T.F., 1983, Late Cretaceous fluvial systems and age of the foreland uplifts in central Utah iii Rocky Mountain Foreland Basins and Uplifts (ed., J.D. Lowell); Rocky Mtn. Assoc. Geol., pp. 181-199.
Lindsay, J.F., Prior, D.B., and Coleman, J.M., 1984, Distributary mouth bar development and role of submarine landslides in delta growth, South Pass, Mississippi Delta: Amer. Assoc. Petrol. Bull., pp. 1732-1743.
Mauger, R.L., 1977, K-Ar ages of biotites from tuffs in Eocene rocks of the Green River, Washakie and Uinta basins, Utah, Wyoming and Colorado: Contrib. to Geol., Univ. Wyoming, v. 15, pp. 17-41.
00679 36
Picard, M.D., 1955, Subsurface stratigraphy and lithology of Green River Formation in Uinta Basin, Utah: Amer. Assoc. Petrol. Geol. Bull., v. 39, pp. 75-102.
Picard, M.D., Thompson, W.D., and Williamson, C.R., 1973, Petrology, geochemistry and stratigraphy of Black Shale facies of Green River Formation (Eocene), Uinta Basin, Utah: Utah. Geol. and Mineral. Survey, Bull. 100, p. 52.
Picard, M.D., 1985, Hypotheses of oil-shale genesis, Green River Formation, northeast Utah, northwest Colorado and southwest Wyoming in_ Geology and Energy Resources, Uinta Basin of Utah; Utah Geological Association Publication 11, pp. 193-210.
Ryder, R.T., Fouch, T.D., and Elison, J.H., 1976, Early Tertiary sedimentation in the western Uinta Basin, Utah: Geol. Soc. Amer. Bull., v. 87, p. 496-512.
Ryer, T.A. and McPhillips, M., 1985, Early Late Cretaceous paleogeography of east central Utah in_ Mesozoic Paleo-geography of West-Central United States (eds., M.W. Reynolds and E.D. Dotty); Rocky Mtn. Sect. Soc. Econ. Paleo. and Mineral., pp. 253-272.
Wolf, J.A., 1983, Late Cretaceous and Paleogene nonmarine climates in North America in Paleoclimatic and Mineral Deposits: U.S. Geol. Survey Circ. 822, pp. 30-31.
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., pp. 123-129.
37 00680
Photo 7. Northeast View of Clark Valley, Book Cliffs, Roan Cliffs and Proposed Plant Site
Looking northeast for nine miles across Clark Valley to the Book Cliffs at the red dots and for fifteen miles to Bruin Point in the Roan Cliffs at the yellow dot. The blue dot exists above the proposed north area pilot mine site. The right red dot locates B Canyon which is the right-of-way for the lower portion of the proposed conveyor route that will start in the Roan Cliffs. The green dot locates the proposed tailings area. The left red dot locates Bear Canyon. Kaiser Coal Company is currently developing underground coal seams in the area between the two red dots. The orange dot is located at C Canyon and is the area that Kaiser proposes to build surface support facilities. The coal will be processed at the existing plant facilities in the town of Sunnyside located adjacent to the town of East Carbon. Both of these towns are located one to two miles to the right of the photo near the base of the Book Cliffs. The viewpoint is one and a half miles northwest of Sunnyside Junction and off U.S. Route
Clark Valley is at an elevation between 5600-6800 feet and consists of Mancos Shale that is 2000-2500 feet thick. This shale was deposited by a Cretaceous marine seaway. The flat surfaces just above the green dot are 200-400 feet above Clark Valley and represent alluvial surfaces that consist of 20-40 foot thick gravel deposits that locally cap the Mancos Shale. The Book Cliffs are exposed for six miles in this photo and exist at elevations between some 7000-8000 feet. They contain Mesaverde Group rocks that formed during Late Cretaceous in transitional areas of deltaic to coastal environments. The Roan Cliffs are at elevations between 8000-10,000 feet and consist predominantly of rocks of the Wasatch and Green River Formations that formed in early and middle Tertiary. The rocks of the Wasatch Formation formed in continental environments. The rocks of the Green River Formation formed in transitional areas of deltaic, beach and nearshore environments of Lake Uinta and the Sunnyside delta complex.
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Photo 2. Monoclinal Flexure in Sunnyside Tar Sands Area
Looking south at three topographic segments of the northwest trending flexure associated with the Sunnyside Tar Sands deposit. Below the right yellow dot is the TV tower near U.S.G.S. Bruin at 10,184 feet and located about six miles away from this viewpoint on Horse Ridge. The left green dot some four miles away is in the West Tavaputs Plateau and located in Section 23, T13S, R14E. The segment in the area of the left green dot has strata that dip 3-4 northeast and contains low grades of bituminous sandstones of 0-4wt% bitumen. The segment in the area of the middle green dot has strata that dip 7-8° northeast and contains medium grades of bituminous sandstones of 3-7wt% bitumen. The segment in the area of the right green dot has strata that dip 7-8 northeast and contains high grades of bituminous sandstones of 4-12wt% bitumen. These three segments are separated by northwest drainage trends located at the left and middle blue dots. The three blue dots also locate the position of the Blue Marker which exists at the base of the Parachute Creek Member of the Green River Formation. A closure formed from the segmented parts of the flexure zone is suggested to exist over Bruin Point and serves as a mega-control for the distribution of tar sands.
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Photo 3. View of Measured Section 29
Looking southeast across Dry Creek Canyon at Measured Section 29 from viewpoint in Measured Section 30. The excellent outcrops are some 2500-3500 feet away and the photo shows about 1000 feet of relief. The detailed measured section extends for 766 vertical feet from slightly below the lowermost green dot to the horizon above the uppermost green dot. The two yellow dots represent untested nonbituminous sandstone zones suggested to be Zone 35 at the upper yellow dot and Z-36 at the lower yellow dot. Numbered tar zones of bituminous sandstones were determined by correlation of surface gamma ray logs and the detailed lithology shown in the strip log of Measured Section 29. Progressing from the bottom green
' dot to the upper green dot each dot represents a numbered tar zone with its representative bitumen analysis in parenthesis: Z-32 (2wt%); Z-31 (2wt%); Z-26 (nonbituminous limestones and not analyzed); Z-25 by orange dot (nonbituminous limestones and not analyzed); Z-23 (1.8wt%); Z-11 above blue dot (3.1wt%); and Z-10 above red dot (1.2wt%). Lateral continuity is vividly apparent in Zone 10 and 11 and partially apparent in Zones 25, 26, 31, 32 and 35. Zones 25 and 26 show their characteristic orange-brown color and are the carbonate-rich interval in the Garden Gulch Member of the Green River Formation. The orange dot is believed to represent the Orange Marker at the top of the carbonate-rich interval. The blue dot represents the Blue Marker at the base of the Parachute Creek Member. The red dot represents the Mahogany ledge which is the most widespread and definitive marker in the Uinta' and Piceance Creek basins. The area of the red dot and uppermost green dot is shown in greater detail in Photo 4.
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Photo 4. Oil Shale Intervals of the Mahogany Ledge in Measured Section 29
Double oil shale intervals near top of measured section. The lower red dot contains a six foot interval of rich oil shale that weathers to a paper shale. The upper red dot contains a seven foot interval of rich oil shale that weathers to a paper shale. These two rich oil shale intervals define the upper and lower limits of a 25 foot interval that represents the Mahogany ledge. Determination of this significant marker bed is based on (1) mapped exposures in eight other measured sections located in peripheral hydrocarbon leases, (2) correlation of surface and downhole gamma ray logs, (3) correlation of detailed lithology in drill core and measured sections, and (4) comparisons of well logs from the Sunnyside Tar Sands area with those of Rio Blanco Tract C-a area. The Mahogany ledge (i.e., surface exposures) or zone (i.e., subsurface equivalent) is the most widespread and definitive marker bed in the entire Uinta and Piceance Creek basins. Due to erosion the Mahogany Ledge or Zone rarely exists in the Roan Cliff segment of the flexure zone shown in Photos 1 and 2. However, the Mahogany ledge or zone commonly exists in the middle segment and the West Tavaputs Plateau segment of the flexure zone shown in Photos 1 and 2. Detailed field examination of this exposure and correlation of the detailed data in Figure 14 have not been completed. The green dot above Roger Grette locates N65°W, 88°SW joints in Zone 10 that are filled with 0.25 inch thick veins of solid hydrocarbons, probably giisonite. Zone 10 consists of nonbituminous to trace bituminous (1.2wt% bitumen), iron colored, planar bedded, fine grained to very fine grained sandstones with some thin interbedded siltstones and shales that were all deposited as a distal bar of the Sunnyside delta complex. For further detail the reader is referred to the strip log of Measured Section 29.
Photo 5. View of Measured Section 32
Looking northeast 3000-4000 feet across a left to right drainage in the base of the photo at exposures in Measured Section 32. The photo was taken from Measured Section 42, is located about one mile south-southeast of Mount Bartles, and contains 900 feet of relief. The red dot locates the white band with extensive exposures of the Mahogany ledge. Detailed surface gamma ray logs from an area to the left of the red dot are shown in Figure 16 and helped to define the Mahogany ledge. The blue.dot locates the Blue Marker at the base of the Parachute Creek Member. The yellow dot is some 20 miles away in the Uinta Basin and is located on the north side of Nine Mile Canyon near North Franks Canyon. The yellow dot locates the reddish brown colored Uinta Formation that exists above the gray colored Parachute Creek Member of the Green River Formation. Some 10 miles to the left of the yellow dot exposures of the Mahogany ledge exist in Gate Canyon. The green dots are located on numbered tar zones and represent the following zones from bottom to top with analyzed bitumen values in parenthesis: Z-36 (6wt%); Z-35 (7.9wt%); Z-33 (5.6wt%); Z-32 (4.4wt%); Z-31 (6.7wt%); Z-23 (2.9wt%); and Z-10 (4.9wt%). Zone 37 is exposed in the left-to-right drainage below the lowermost green dot and contains 1.8wt% bitumen. The area near Measured Section 32 is shown on the Isopach Map as an isolated anomalous bitumen pod located adjacent to the flexure zone. The flexure zone exists in the left-to-right drainage shown in the lower portion of this photo. In Photo 1 Measured Section 32 is located to the right of the' upper blue dot and lies within the middle segment of the flexure zone. Photo 6 is a close-up of Zone 35 located at the second green dot up from the base of this photo.
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In5 the upper portion weathered gray bituminous sandstones overlie weathered orange-b^pwn bituminous limestones. The weathered coating is only a few millimeters thick but conceals the true bitumen content. The limestone unit contains two characteristic intervals. The lower limestone near the pack is a micrite (microcrystalline carbonate ooze) and contains an estimated 3wt% bitumen. The upper limestone near the hammer head is a biomicrite with abundant ostracods and contains an estimated 3wt% bitumen. An unconformity (erosional interval) separates the biomicrite from the overlying sandstone that contains an estimated 6-7wt% bitumen. The trough and planar cross-bedding in the sandstone continue upward for five feet to an IFC (intraformational conglomerate) above the top of the photo. The IFC is 2.5 feet thick, contains abundant gar-pike fish scales and registered a gamma ray kick of 821cps on the surface minispectrometer. Above the IFC the bituminous sandstone is planar bedded for 12.5 feet to the top of this sandstone interval. This numbered tar zone 35 is 20 feet thick and based on numerous unweathered chips contains an averaged analyzed bitumen content of 7.9wt%. The sedimentary structures and lithology suggest Tar Zone 35 formed as a beach bar deposit. The limestones formed in a nearshore marginal lacustrine environment. This photo represents a characteristic part of a whole pattern that is frequently repeated. The characteristic cycle of deposition in the Sunnyside delta complex starts at the unconformity and sequentially follows from sandstone to shale to limestone to unconformity. Then the sequence of sandstone-shale-limestone: deposition is repeated and terminated with another unconformity.
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GENERAL LOCATION MAP
SUNNYSIDE TAR SANDS
Carbon County, Utah
Scale: 1 inch = A 00696 I 20 miles .
Figure 1
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FIGURE 3 DETAILED LOCATION MAP SUNNYS1DE TAR SANDS
0 1 2 |NORTH i i I
j MILES
FROM METRIC MAP: PRICE, UTAH
S( Rocky Mountain ^ Y? Foreland Province j
""^'SjPtateau
Location of the Rocky Mountain foreiand — west-central part of the North American craton.
00690
MAP Of yTAKSMOVWNC PRINCIPAL. STRUCTURAL Ol V IS IONS
Scale: 1 inch = 1 70 railes
'iaure 4. Cordilleran Overthrust Belt, Rocky Mountain Foreland and Structural Divisions of Utah.
Late Cretaceous and early Tertian.' uplifts of Colorado, Utah, and adjacent areas on north and south. Stippled areas are Precambrian rock exposures: ruled areas of the shelf (eastern Utah and Colorado) are exposures of Paleozoic rocks, and are marked by: IP, mostly Pennsylvanian: P, Pennsylvanian and Permian. Ruled areas of the miogeosyncline (western Utah) are Cambrian exposures. K, major detached slide masses: KC, the Canyon Range slide mass: OR, Oquirrh Range: CU, Cottonwood uplift, M, Mesozoic sedimentary rocks. NFL, Newfoundland anticline. SBY, Stansbury Mountains. Both fold axes and thrusts faults in the miogeosyncline are shown by bold lines.
Eardley, 1963
Figure 5. Late Cretaceous and Early Tertiary Uplifts of Colorado and Utah.
00700
1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18
mya
Tlmtns of upttH on Uremfo* rang** shows *n w<ty LaramMa p»ls» o( oalormaiJon (Campanian through mtoata a tat* Laramida puta* (tatty and mwMta Eocan*)Mpa»1*d'bya law Patoocao* kill,
Palaocana) awtf
<~>
!\ v^vi? -\
N %v
V
<'>
a b c The time of movement on foreland uplifts is definiteiy not the same on ail uplifts.
a. North-soutn-trending arches and uplifts are early Laramide features and are progressively younger from the west (Campanian) to the east (Pateocene). The numbers correspond with uplifts on the graph
b. Northwest-trending features are most dominant in the northern foreland and are associated with Pateocene movement. c. East-west trending structures are the youngest Laramide features (Eocene) and are associated with the strongest period of com
pression in the foreland.
Gries, 1983
Figure 6. Location and Time of Uplift on Laramide Ranges in the Rocky Mountain Foreland.
00701
AGE in
M.Y. THOMPSON CANVON
WESTWATER CANVON
SAN ARHOYO CANYON
AGE
in
M Y .
50
5 5 -
6 0 -
65 -
7 0 -
7 5 -
8 0 -
85
90
95
lA ^THhS^MkB^
H O r t t H HOfiM F O n u A T l O N
MAESTRICHTIAN
CAMPANIAN
W ^ , -/ V < v V r - / v
<>->r» s>~f*>p^ r+jt -*p-
^V/-
W A S A T C H F O f t U A H O N
, , . , . - ' - ' • J " r '
•/>-» /•»^/-^>r->./^.r*>/* /* »^-
CASTIEOATE
^ ^ n ^ M - " tuscxcn
. _ — _, 8ll*CA«TU IOMOUE C.
~r-J*-*f~-j*<t<*t'-J-*-t*-l.i*<t44'<r+j+<t'--f-*4'
zjtiasr:
t onuATioNS
ronuAiiON
2SSHS.3KSHEI
*f*^ r+Z<*f-*4<*r
__ : , ZIIIIlIZlL
* * BtACKHAWK
TONOUC « | U A N C O S S M A l t
SANTONIAN
TURONIAN
CENOMANIAN
A1.8IAN
(part)
5 0 -
55 -
6 0 -
65
7 0 -
75
8 0 -
85
90 -
9 5 " roRUATlOH
o CD
o
Chart I l l u s t r a t i n g s t r a t Igraphlc nomenclature and c o r r e l a t i o n of major Alblan to middle Kocene rock un i t s from the Sanpete Valley of cen t ra l Utah to the Book Cl i f fs of eas te rn Utah (modified from Pouch and o the r s , In p r e s s ) . V e r t i c a l l i n e through s t r a t a Indicated a change In s t r a t I g r a p h l c nomenclature.
Fouch, et al, 198 3
Figure 7. Northeast Utah Correlation Chart.
CORRELATION CHART N O R T H W E S T E R N
U I N T A B A S I N C E N T R A L
U I N T A B A S I N E A S T E R N
U I N T A B A S I N
Correlation chart of Late Crstaoaous and Tertiary formations, Uinta Basin area.
P i c a r d , 1985
Figure 8. Uinta Basin Correlation Chart.
00703
mmtmmzi ^f&:Z:££:&££!:&Smi>» f\5?' >99>
Paleogeographic Map in Late Campanian (75Ma) from Fouch, et al, 198 3
ftC«..OMl *F«&
f^^^^^^SS®^ 7$"~ 7 J
mm
Paleographic Map in Middle Campanian (77Ma) from Fouch, et al, 198 3,
00704
Figure 9. Late Cretaceous Paleogeography of Northeast Utah.
- G E N E R A L I Z E D SESIMENT
TRANSPORT DIRECTION
A L L U V I A L FAN
A L L U V I A L P L A I N
GENERALIZED SEDIMENT ' TRANSPORT DIRECTION
MARGINAL LACUSTRINE
OPEN LACUSTRINE
b. Middle Eocene paleogeography, Upper Parachute Creek Member, Green River Formation, northeastern Utah.
i i ALLUVIAL PLAIN
TACIES
2oPEN LACUSTRINE t--->5 MARSHAL LACUSTRINE
C - Late Eocene paleogeography, saline fades, Uinta Formation, northeastern Utah.
GENERALIZED SEDIMENT TRANSPORT DIRECTION
[ r . ' j ALLUVIAL FAN ( j ALLUVIAL PLAIN ?•"• -' PALUSAL-LACUSTRIN
a . Early Paleocene paleogeography, North Horn Formation, northeastern Utah.
Picard, 1985 Figure 10.
Paleocene and Eocene Paleogeography of Northeastern Utah 007O5*
Inferred paleodrainage and extant source terrenes during deposition of upper part of Price River Formation, pebbly Tuscher Formation, "pebbly beds", and equivalents. Equivalents include the Canaan Peak Formation in southwest Utah {Bowers, 1972), the Ohio Creek Member of the Hunter Canyon and Mesaverde formations in the Piceance Creek basin (Johnson and May, 1980) and the Fniittand and Kittiand formations of the San Juan basin, inferred source areas for Piceance Creek basin from Hansley and Johnson (1980); for the San Juan basin from NLA. Khite (personal communication, 1982). Structural elements of Colorado Plateau and Rocky Mountain regions after Kelley (1955). Bold arrows show relevant paieocurrent localities. . Symbols within source areas indicate derivative grain types: Ls, sedimentary Uthic fragments; Lv, volcanic lithic fragments; F, feldspar.
Lawton, 19 8 3
Figure 11. Summary Diagram of Laramide Uplifts, Paleodrainage and Source Areas for the Uinta and Piceance Creek Basins in Late Cretaceous and Early Tertiary.
G07f?h
LOOKING NORTHWEST SOUTHWEST NORTHEAST
0
© O - J o
GREEN RIVER FORMATION
TAR ZONE NUMBER N°NQrfuMfKon?~o^T-—-—— .
Base of Tor Sands f alls Downdip at ° b A W S T 0 N F . Avorage Rate of 30 Feet Per 1000 Feet
Beds Dip at Average Rate of 100 Feet Per 1000 Feet
IOOOO
9700
- 9 4 0 0
-9IOO
8800
8500
300 FIGURE 12
SCALE
IDEALIZED SECTION OF BRUIN POINT SUBDELTA SHOWING TAR ZONES AND DEPOSITIONAL ENVIRONMENTS
A AMOCO SW 05*
• rn-nw Mr. a
It-H-tt
CAMERON
—~<dfmr
inn n-»-7!
CMKR0*
•u- m nn' m.
W D •-H-J3
A' NE
•w •eicrai.uTOKM * t a w mca
I t I t i t IU! I zauTat m i u •nnatTae am K it:
I t M K U W72
INOtX M * ' UNI Of HCTIOM
T0T3 M8 M& or RICH ***4*C zone*
»I1»TJ IT OJIM.UUUMt. »T0»l»» * wnwftcatc MTIKVJU.
FEDERAL TRACT C-a MO KXlCO CO.. COIOHAOO
SW-NE HISTOGRAM CROSS SECTION lArntox MOmui. TO oo»»c« STKact;
OVTO i* >J MtMCMMU
. SW-NE oil-yield histogram cross section (in ga l / ton) , Federol Tract C-o.
Ziemba, 1974
00708
Figure 13. Oil Shale Zonation and Important Markers in the Green River Formation.
SUNNYSIDE TAR SANDS CARBON COUNTY, UTAH
TOP OF MEASURED SECTION 32 l < -
SUHFACE DATA
GAMMA RAY CPS 200 300
LU
(') Q LU _ l
>-7
< a o T
< £
a. O rr o i -i
o LU _ l
< X CO
_l
o
G A M M A RAY API U N I T S
100 ZOO
AMOCO No. 63 >\<
DRILL HOLE DATA
RIO BLANCO TRACT C-a RIO BLANCO COUNTY. COLORADO
COLO. FED. TRACT A , C H - 2
DRILL HOLE DATA
BULK DENSITY 2.25 2.50
GAMMA RAY API UNITS 200 300
BULK DENSITY 2.0 2.2
B GROOVE
FIGURE 16
Gamma Ray and Bulk Density Log Comparisons of the Mahogany Zone, Sunnyslde Tar Sands, Utah and Rio Blanco, Colorado 0071 1
Detailed measured section of the Oil-shale fades of Parachute Creek Member at DoogM Pass, Cotorada
j ESTIMATED ! -< OIL-SHALE
u •LtTHOLOGY
7 0 M -
6 0 -
5 0 -
30- j
2 0 -
10 H
EXPLANATION
I ' Oil Shale
[ \ Marlstone
: ^ x
1 p
f i
Tuf f
Plant Debris
insect Fossils
UPPER
OIL-SHALE
ZONE
*x
-Wavy Tuff
A GROOVE
-False MAHOGANY Marker
•Mahoaany LEDGE Bed
* Curly Tuff GROOVE
Cole , 1985
Figure 14. Detail of Mahogany Oil Shale Terminology.
00709
SUNNYSIDE TAR SANDS CARBON COUNTY, UTAH
RIO BLANCO TRACT C~a RIO BLANCO COUNTY, COLORADO
BRUIN POINT ROAD 1 mile
SURFACE DATA
GAMMA RAY CPS 200 300
ELEVATION
10,050
PARACHUTE CREEK MEMBER GARDEN GULCH MEMBER
10,025
AMOCO No. 63
DRILL HOLE DATA
GAMMA RAY API UNITS 100 200
100 miles C.E. No. 702
• » |
DRILL HOLE DATA
GAMMA RAY API UNITS 100 200
FIGURE 15 Gamma Log Comparisons at the Base of the Parachute Creek Member (Blue Marker), Sunnyslde Tar Sands, Utah and Rio Blanco Tract C~a, Colorado
M S - 3 3 LOCATION OF MEASURED SECTION
10 WITH MSAT THICKNESS
SELECTED CONDEMNATION DRILL SITE (NOT DRILLED)
0 OTHER COMPANY DRILL HOLES WITH 10 MSAT THICKNESS N
HTMEAVURED SECTION MT. BARTLES-SO. RIDGE AREA
RILL SITE& IN THE
• • • ; • • • • • • • • •
""" ?"
R 14 E
T 12
• S
3 ;6^ •
? ™ " ™ & •A.. .l.hui
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• • • • •d h a d h m i |
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1 0T , 2 )
- — - 28 .'. MOC 0
2-20-82
UJ '5)
, U-17 653 •
' ^ • • • • i
rl
••••••••••^•••••^•••^••••• f :;:':-':;- AMOCO:-
:::; JC::.-'::-vu;::.:::.::: •
?4 IIS T
;S':J^S s
R 14 E
J •
T 13 S
FEDERAL SERIAL NUMBERS
U-17652 U-17653 U-17662 U-25153 U -43997 U•3 7999 U I76SI-A
COMPILED FROM THE FOLLOWING GOVERNMENT LAND PLATS T I 3 S R U E , DATED 1 1 8 - 1 9 0 4 T 14 S R I 4 E , DATED 5 - 5 - 1 9 0 0 T I 4 S R I 4 E , DATED 4 - 3 0 - 1 9 0 9 T I 2 S R I 4 E DATED 1-18-1904 A L L SECTIONS CONTAIN 6 4 0 ACR1$ i CEPT AS SHOWN
LEGEND
TOTAL FEDERAL ACRES
TOTAL FEE ACRES 1119 20
TOTAL 10721 28 1 0 0 0 0 %
00713
• • • • I UNIT BOUNDARY
T RACT BOUNDARY
( ' 2 ^ ' TRACT NUMBER
FIGURE 18
AMOCO ACREAGE
SUNNYSIDE TAR SANDS CARBON COUNTY, UTAH
*** = T12S, ** = T13S, * = T14S,
T13S,
R14E R13E R14E R14E
Subdelta
MS
1 2 3 4 5 6 7 8 9 10 11 Dry
Canyon 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44
Section, quarter
3 10 10 33 29 15 20 33 33 34 28
22 20 29 21 22 21 28 27 27 28 29 33 20 21 29 33, 15, 14 13, 11, 12,
' iv, 16, 16 33 34 6 30 30 19 24 20 19 18
, SW* ,NE* ,NW* , SW , SE ,NE* , SW ,NE ,NE ,NW ,NE
rNE ,SW ,NE rSW ,SE rNE ,NW rNE NW SE NE SW SW NW SE NW SE SE NE SE NW SE SW NE NW*** SE*** NE NE NW rSW , NW** rNW ,NE ,SE
Bruin Point
Proximal P P P
Medial
M
Dry Canyon
Whitmore Canyon
P P P
M
M P P M M M M
M M P P P M P P Distal D D D D M M D
D P P P P M M M
Table 1. Measured Section Locations with Relative Portion in Subdeltas. 00714
Elevation Elevation of Contacts
MS
1 2 3 4 5 6 7 8 9 10 11 Dry Canyon 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44
Top
10040 9885 9920 10125 9733 9670 9585 9845 9815 9607 9280
8820 9500 9510 9398 8989 8800 9260 9085 9106 9440 9510 9845 9635 9326 9610 9580 8725 8480 8320 8350 8170 9480 9030 8920 8418 8300 9215 9720 9850 9810 9954 9565 9685 9965
Bottom
8540 8541 9170 8720 8847 9320 8955 8760 8860 8696 8756
7413 9116 9073 8788 7775 7930 8845 8087 8466 8856 9012 8815 8851 8116 8974 8994 7781 7915 7554 7653 7380 8563 8389 7923 8180 7770 8094 9121 9183 9280 9363 9131 9132 9180
Total Vertical Height
1500 1344 952 1405 886 350 630 1085 955 911 524
1407 384 437 610 1214 870 415 998 640 584 498
1030 784
1210 636 586 944 565 766 697 790 917 641 997 238 530 1121 599 667 530 591 434 553 785
Tgp/Tgg
9929 9786 9753 9986 — --— — —
9453 —
8598 — — —
8729 — —
9026 — — — — — — — —
8487 8235 8062 8155 7874 9232 8918 8645
(all Tgp) 8036 8809 — — --
(all Tgg) (all Tgg)
• —
(all Tgg)
Tgg/Tgd
9601 9372 9535 9571? 9270 9395 9014 9065? 9340 8912 8826
7748 —
9151 8891 8200 8179 8879 8228 8551 8988 9070 9335 9033 8219 9136 9175 — --— --—
8609 8391 7945 — — —
9125 9282 9285
9148
Tgp/Tgg = Parachute Creek/Garden Gulch contact Tgg/Tgd = Garden Gulch/Douglas Creek contact
Table 2. Elevation Data From Measured Sections. 00715
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co to co
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o o co en
co co ^ oo oo tv> h-•
o o o en o en
W O l O O v l U l t O O i t O ^ l O H a > v o c o c o c o * * c n o o K > o o o c o o o o o c n t o v D ^ ^ c n o o
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Bruin Point Subdelta
MS
1 2 3 4 6 10 18
Proximal,
685 400 307 650 108
Medial-
93 120
Distal.,
X 430 107
Whitmore Canyon Subdelta
MS Proximal Medial Distal
0 0
35 37 38 39 40 41 42 43 44
135 190 64 100
23 47 27
X 122 32 0
1 ±0.5 miles of Roan Cliff face 2 0.5-2 miles downdip of Roan Cliff face 3 2-4 miles downdip of Roan Cliff face
Table 5. MSAT Thickness, Bruin Point and Whitmore Canyon Subdeltas.
00718
o
H3
& M fl>
c^
en >
o
fl> W
O
o
o
en tr fl> M rt &>
XI n
O J O J U W W O J l O I O I O I O I O I O I O I O I O I O H H I - ' H H H H i l l O h - 1
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to
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IS en
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- 0 vo
U I en
IS
D i
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CO
rt
CO
Bruin Point Subdelta
MS
1 2 3 4 6 10 18
range
MS
35 37 38 39 40 41 42 43 44
range
Proximal Average(Range)
53(8-143) 45 (19-136) 34 (5-99) 59 (5-120) 42(22-84)
47(12-116)
Whitmore
Proximal Average (.Range)
36 (4-65) 36 (10-86) 17 (8-27) 29(20-51)
30(11-57)
Medial Average(Range)
14(7-28) 27 (5-64)
21(6-46)
Canyon Subdelta
Medial Average(Range)
20(2-35) 32(15-49) 22(4-42)
25(7-42)
Distal Average(Range)
Distal Average(Range)
22(6-37) 12 (2-27)
17(4-32)
Table 7. Average Thickness of Numbered Tar Zones in Bruin Point and Whitmore Canyon Subdeltas.
00720
MS
5 7 8 9 11 Dry Canyon 12 13 14 15 16 17 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 36
X&range
Proximal Average(Range)
41(11-88) 26 (7-65) 31(23-45) 53 (22-88)
44(15-84) 28 (9-65)
33(8-62) 66 (24-146) 46(10-104)
56 (20-88) 60 (38-86)
44 (17-84)
Medial Average(Range)
19 (7-41)
27(13-46)
23 (5-47) 23 (5-58) 11(5-20) 32 (30-33) 17 (5-57) 19 (9-32)
25 (10-57)
25(13-34) 33(10-58)
23(10-44)
Distal Average(Range)
14(3-33) 13(7-25) 19 (3-34) 21(10-41) 16 (4-27)
19 (6-46) 15(2-36)
17 (5-35)
Table 8. Average Thickness of Numbered Tar Zones in Dry Canyon Subdelta
00121
Company and Hole Location Section,Quarter
CE TD TSAT MSAT DSAT BSAT BSAT Elev.
Arco (1964) A-l A-2 A-3 A-5
28, SW 28,SE 29,SE 25,NW**
Great National Corp. (1980) GNC-13 13,SW** GNC-14 11,SW* GNC-15 30,NE
Mono Power (1981-1983) South Ridge No, Stone Cabin Draw No. 1 Sunnyside NW No. 1
2 3 4 5 6 7
No . No. No . No . No. No .
WCT-3 WCT-4
RC-1
B P - 1
BP-1A
Range Creek Tract RCT-1
RCT-2 RCT-3A RCT-4 RCT-5 RCT-6 RCT-7 RCT-8 RCT-9 RCT-10 RCT-11 RCT-12 RCT-13 RCT-14
16, NE
35,SE***
13,NE** 13,SE** 24,NE** 24,NW** 24,SW** 26,NW** 25,NE** 24,SW** 25,SE**
12,NW*
34,SE
34, SE
12,NW*
15,NE* 14,NW* 14,NE* 14,NE* 11,SW* 11,NE* 11,SE* 11,NW* 15,SE* 12,NW* 12,NW* 12,SW* 11,SW*
9584 1295 9340 595 9850 751 9580? 580
9820 675 9916 1200 9720 843
290 109 236 144
172 320 262
8910 620 59
7477 300 57
9720 9926 9744 9746 9611 9343 9380 9720 9400
9414
9815
9822
9680
9666 9824 9746 9689 9772 9386 9548 9793 9793 9411 9454 9699 9492
301 405 420 402 221 250 221 604 145
(aban1
541 (aban' 562
(aban' 1404
208 174 16 8 137 67 130 173 48
d) 11
d) 55
d) 331
184 (aban 424 894 774 805 753 804 794 1114 412 974 1003 1221 733
11 •d) 153 259 140 141 271 259 262 459 168
1 194 181 252 326
188 71
183 128
153 243 148
136 199 43 2
596 8988 378 8962 554 9296 197 9383
75 362 9458 31 791 9125 38 484 9236
0 >620 >620<8290
22 167 280 7197
112 117 105 126 34 26 142 34
0
51 80 66 0 38 45 30 65
383 420 371 202 217 209 279
9543 9324 9375 9409 9126 9171 9441
24 51 —
268 422 1084 8737
0
123 134 85 98 176 179 187 394 138 121 110 166 289
10 204 215 59 186 37 61 158 93 92 480 569 63
287 704 610 582 715 716 760
1068 390 914 917 1194 687
9379 9120 9136 9107 9057 8670 8788 8725 9403 8497 8537 8505 8805
CE =collar elevation in feet TD =total depth in feet TSAT=total footage all saturated sediments MSAT=total footage main saturated zones,
minimum 10 feet thick and 10 gallons per ton
DSAT=depth to top of main saturated zones BSAT=bottom of saturated sediments
***=T12S,R14E **=T13S,R13E *=T14S,R14E
T13S,R14E 1 driller's void 938-974'
00722 Table 9. Other Company Drill Hole Data, Sunnyside Tar Sands.
EXPLANATION FOR TABLES 1 0 , 1 1 , & 12
TE BE T 21 B ND thin NA X bit 4wt% 9.5/22.8 nonbit 114M EOD OS NS DB BB B DMB CMB DC C L
top elevation bottom elevation numbered tar zone, top and bottom not determined less than 5 feet thick no analysis weighted average bitumen content field estimate of bitumen content analyzed bitumen content in wt%/gals per ton nonbituminous 114 thick zone of multiple tar sands environment of deposition offshore nearshore distal bar beach bar beach distributary mouth bar channel mouth bar distributary channel channel levee
QG"?a3
TABLE 10
Tar Zone Data of Measured Sections Bruin Point Subdelta
Sunnyside Delta Complex
Measured Section
o o o tn o oo
H m No. 2
O 00
C* 00
IT) O (M CM r-l r-O 00
u u H DO
No. 6 o o r- CM ID ro c* en
Zone-*-Data +
Elevation Depth Thickness X Bit E0D
Elevation Depth Thickness X Bit E0D
Elevation Depth Thickness X Bit E0D
Elevation Depth Thickness X Bit E0D
Elevation Depth Thickness X Bit E0D
T U B 2 1 B
9 9 4 7 - 9 9 3 0 9 8 3 0 - 9 8 1 2 9 3 - 1 1 0 2 1 0 - 2 2 8
17
DMB
18
DMB
9762-9743 9690-9665 123-142 195-220
19
BB
25
DMB
9899-9877 9760-9738 21-43 22
160-182 22
10095-10090 9997-9986 30-
5
DB
128-139 11
B
9670-9648 0-22 22
5wt% DMB
T 23 B
9748-9740 292-300
8
B
9557-9537 328-348
20
BB
9714-9695 206-225
19
DMB
ND
9628-9589 42-81
39 5wt» BB
T 31 B T 33 B T 35 B T 36 B T 37 B T 38 B T 41 B
9690-9670 350-370
20
DMB
9468-9428 417-457
40
DMB
9644-9639 276-281
5
B
ND
9515-9431 155-239
84 4wt* DMB
9627-9602 413-438
25
DMB
9391-9372 494-573
19
BB
9608-9587 312-333
21
DMB
9742-9711 383-414
31
BB
9 3 6 2 - 9 3 3 9 3 0 8 - 3 3 1
23 n o n b i t
DC
9 5 7 7 - 9 4 5 5 4 6 3 - 5 8 5
1 2 2
DC
9 3 5 7 - 9 3 0 9 5 2 8 - 5 7 6
48
CMB
9 5 3 4 - 9 4 3 5 3 8 6 - 4 8 5
9 9
DC
9 7 0 3 - 9 5 8 3 4 2 2 - 5 4 2
120
DMB
ND
9 4 5 5 - 9 3 1 2 5 8 5 - 7 2 8
143
DC
9 2 8 4 - 9 2 5 3 6 0 1 - 6 3 2
3 1
DC
9 4 5 0 - 9 4 3 2 4 7 0 - 4 8 8
18
BB
9 5 7 2 - 9 5 0 0 5 5 3 - 6 2 5
72
DMB
ND
9 2 6 4 - 9 2 3 0 7 7 6 - 8 1 0
34
DC
9 2 4 5 - 9 1 9 6 6 4 0 - 6 8 9
49
DC
9 4 2 0 - 9 3 8 0 5 0 0 - 5 4 0
40
DMB
9 5 0 0 - 9 4 0 0 6 2 5 - 7 2 5
1 0 0
DMB
ND
9 2 1 0 - 9 1 6 3 8 3 0 - 8 7 7
47
DC
9 1 5 0 - 9 0 8 3 7 3 5 - 8 0 2
67
DC
9 3 4 9 - 9 3 1 8 5 7 1 - 5 8 1
1 1
B
9 3 3 5 - 9 3 1 1 7 9 0 - 8 U
24
BB
ND
9 1 4 1 - 9 0 8 7 8 9 9 - 9 5 3
54
DC
9026-8960 859-925
53M
2DC"s
9322-9262 598-658
60
DC
9283-9208 842-917
75
DC
ND
T 42 B
9067-9033 973-1007
34
DC
8912-8880 973-1005
32
DC
9210-9196 710-724
14
B
9157-9020 968-1105
10 5M
2DC's
ND
T 43 B
9030-8945 1010-1095
85
DC
8841-8758 1044-1127
4 7M nonbit
3DC's
9170-9087 750-833
4 3M nonbit
3B's
9005-8920 1120-1205
72M
BE. DC
ND
T 45 B
8933-8852 1107-1188 - 91
DC
8697-8561 1188-1324
136 nonbit
DC
9054-8968 866-952
66M nonbit
2DC's
8876-8841 1249-1284
35
DC
ND
BSAT
8852 1188
8880 1005
9196 724
8841 1284
9428 242
No. 10 o en oi oo
No. 18
in r-co co o o c co
Elevation Depth Thickness X Bit EOD
Elevation Depth Thickness X Bit EOD
thin 9365-9337 242-270
28
DMB
8950-8925 127-160
33 2wt% BB
9254-9234 353-373
20
BB
thin
<5
NS
9069-9062 538-545
7
BB
8788-8724 297-361
64 3-4wt% DMB
thin
thin
5 3-4wt%
B
8966-8957 641-650
9
BB
thin
5 2-3wt%
B
8924-8912 8850-8840 683-695 757-767
12
BB
thin
<5
NS
10 nonbit
DC
8474-8444 611-641
30 2-4wt%
BB
thin thin 8186-8162 8113-8087 899-923 972-998
<5 <5 24 26 nonbit nonbit
NS NS DC DC
8 9 1 2 . 6 9 5
8352 733
00724
TABLE 11
Tar "one Data of Measured Sections Dry Canyon Subdelta
Sunnyside Delta Complex
Measured Section
ro r-
r- oo
N o . 7
in r-cc o in o~> ch cc
:one-f Da ta ;
Elevation Depth Thickness X Bit EOD
Elevation Depth Thickness X Bit EOD
T 31 B T 33 B
9733-9711 0-22 22
BB
9450-9385 135-200
65
DMB
T 35 B
9656-9606 77-127
50
DMB
9347-9332 238-253
15
BB
T 36 B
9606-9560 127-173
46
DMB
9278-9268 307-317
10
BB
T 99 B T 37 B
9482-9428 251-305
38M
2BB's
9226-9133 359-402
32M
2BB's
T 38 B
9337-9281 396-452
56
DC
9101-9094 484-491
7
T 41 B
9235-9224 498-509
11
BB
9075-9050 510-535
25
9162-9074 571-659
T 43 B
9021-9001 712-732
20 n o n b i t
BB
ND
T 45 B
8942-8908 791-825
34 n o n b i t
DC
ND
9074 659
9050 535
UO O ^r r-co r-& CO
W U E-- 03
:>. 9
E-. a N o . 1 1
O uO co m ( N r-Ch co
H a H a
N o - 1 2
E-t 03
No. 13
No. 15
Dry Canyon
o o (N (N oo ^f
Elevation Depth Thickness X Bit EOD
Elevation Depth Thickness X Bit EOD
Elevation Depth Thickness X Bit EOD
Elevation Depth Thickness X Bit EOD
Elevation Depth Thickness X Bit EOD
Elevation Depth Thickness X Bit EOD
Elevation Depth Thickness X Bit EOD
Elevation Depth Thickness
8713-8699 276-290
14 l-2wt*
BB
8494-8480 326-340
14
8639-8627 350-362
12 3wt% 3B
8456-8440 364-380
16
thin
<5
NS
8381-836 439-452
13
9205-9178 193-220
27 7-8wt%
BB
8404-8389 585-600
15 2-6wt* DMB
thin
9513-9468 332-377
45
DMB
9356-9333 489-512
23
BB
9653-9630 162-185
23
9217-9165 628-680
25M
2BB's
9609-9654 206-251
45
9530-9502 285-313
28
DMB
9125-9084 720-781
32M
2BB's
9482-9420 333-395
62
DMB
9340-9279 475-536
61
DMB
9247-9165 568-650
82
DMB
X Bit EOD BB
9130-9122 150-158
8
BB
9438-9406 62-94
32 3wt% DMB
9505-9495 5-15 10
3-4wt% BB
thin
<5
NS
8301-8281 688-708
20 l-2wt%
BB
8048-8025 772-795
19M
2BB's
9062-9055 218-225
7
BB
9366-9351 134-149
15 5wt% 3C
9468-9458 42-52
10 3-4wt%
BB
8991-8971 470-427
20 12wt%
BB
8259-8201 730-788
58 nonbit CMB
7983-7940 837-880
43
DMB
8957-8916 323-364
41
DMB
9327-9281 173-219
46 lwt% DC
9442-9397 68-113
45 4wt% DMB
8953-8920 445-478
33 4-6wt% CMG
thin
NS
7885-7854 935-966
31 nonbit DMB
9397-9352 113-158
45 8-10wt%
DMB
8888-8841 510-557
47 • l-2wt% CMB
thin
<5
NS
9200-9116 300-384
84 nonbit
DC
9352-9287 158-223
65 5-6wt* DMB
8814-8807 584-591
7 nonbit
C
8072-8051 917-938
21 nonbit
BB
7784-7748 1036-1072
36 nonbit DMB
8797-8759 483-521
3 3M nonbit 2DC's
ND
9260-9251 250-259
9 5-6wt%
BB
ND
8014-7977 975-1012
31M nonbit 2BB's
thin
ND
ND
9229-9182 281-328
28H 4-5wt%
2BB'S
ND
7934-7889 1055-1100
34H nonbit 2BB's
7633-7587 1187-1233
46 nonbit DC
9165-9105 650-710
60
DMB
397-412 15
l-2wt% C
ND
9105-9050 710-765
55
DMB
9065 ND 780
9050-8990 8977 765-825 838
60
DMB
ND 8917 363
9200? 300?
9098 412
8841 557
8281 708
7963 857
00725
TABLE 11 (cont'd) Tar Zone Data of Measured Sections
Dry Canyon Subdelta Sunnyside Delta Complex
Measured Section
No. 16 o o O fl CO <J\ co r-
t) U t< n
No. 17 o m kD ^ (N CO Ch 00
w u E H CQ
No. 19 vO tfl O kD r-1 ^r en co
W K E-t na
No. 20
O vO
T CD Cn CD
DJ W E-t a
No. 21
O <N
in o Oi <T»
w u E-- CQ
No. 22
in LTI
CO CO C\ CO
63 03 En a
No. 2 3 m in
kD CO en co
-.- — =- 3 No. 24
\£> M> CN i—1
M iH a\ co
63 03 E-- 03
No. 25
O T rH r-
yD cr» en co
W W E-" CQ
No. 26 O T CD C*
m a> Ol co
w w E-i CQ
Zone-* Data* T U B
Elevation Depth Thickness
X Bit EOD
Elevation Depth Thickness
X Bit EOD
Elevation Depth Thickness X Bit EOD
Elevation Depth Thickness X Bit EOD
Elevation Depth Thickness X Bit EOD
Elevation Depth Thickness X Bit EOD
Elevation Depth Thickness X Bit ZOD
Elevation Depth Thickness X Bit EOD
Elevation Depth Thickness
X Bit EOD
Elevation Depth Thickness
X Bit EOD
-
-
-
~
• -
—
—
—
T 21 B 23 B 31 B 35 B T 99 B T 38 41 B T 42 43 B
thin
<2
NS
thin
8753-8733 47-67
10 4-6wt%
BB
—
thin
9665-9620 180-225
40M 5-6wt% B&BB
__
9016-8959 310-367
57 2-5wt%
BB
—
—
thin
<5
NS
thin
<5
NS
9274-9265 166-175
9 4-5wt%
B
9510-9472 0-38 38
4-5wt% BB
9577-9520 268-325
57 6wt% BB
9530-9426 105-209
104 6wt% DMB
thin
<2
NS
—
—
thin
<5
NS
thin
<5
NS
9227-9201 213-239
26 6-7wt4
BB
9436-9374 74-136
62 5-6wt% DMB
9505-9481 340-364
24 7wt% BB
9354-9312 281-323
42 3wt% DC
8825-8775 501-551
4 5>;
3-4wt% B&BB
9564-9487 46-123
77 3-8wt% DMB
—
thin
<5
NS
9215-9132 45-78
33 4-6wt% CMB
8838-8781 268-325
57 3-4wt% DMB
9166-9134 274-306
32 7-8wt%
BB
9360-9337 150-173
23 4wt% DMB
9471-9339 374-506
132 6wt% DMB
9289-9227 346-408
62 l-2wt%
DC
8686-8633 640-693
36M 3-5wt% B&DMB
9469-9430 141-180
39 2-5wt%
BB
9566-9528 24-52
38 2-8wt%
BB
thin
<5
NS
9156-9126 104-134
30 4-5wt% CMB
thin
<5
NS
9102-9087 338-353
15 4wt%
B
9322-9290 188-220
32 3-4wt% DMB
9330-9290 515-555
40 4-5wt%
BB
9190-9180 445-455
10 l-2wt%
p
8604-8594 722-732
10 3wt%
B
9411-9368 199-242
43 4-5wt%
BB
9515-9460 65-120
55 4-8wt% DMB
8289-3275 511-525
14 2wt% BB
ND
8754-8741 352-365
13 4wt% BB
9065-9054 375-386
11 6wt%
B
9271-9247 239-263
24 3wt% BB
9210-9152 635-693
58 4-5wt% BB
9150-9137 485-498
13 2-3wt%
B
8540-8530 786-796
10 2wt%
B
9274-9203 336-402
66 2-5wt% DMB
9450-9355 130-225
86M 4-8wt% DMB
8205-8193 595-607
12 lwt% BB
ND
8364-8598 472-508
17M 102wt% 2BB's
thin
M
9178-9170 332-340
8 3wt*
B
9055-9019 790-826
28M 4-5wt%
BB
9118-9081 517-554
37 2wt% DC
8484-8421 842-905?
63? 2-5wt*
DC
9156-9136 454-474
20 2wt%
B
9247-9187 333-393
60 3-8wt%
DC
8129-8111 671-689
18 nonbit
C
ND
8503-8489 603-617
14 nonbit DC
ND
9145-9077 365-433
68 l-2wt% DMB
9001-8855 844-990
146 2-5wt%
DC
9033-8950 602-685
83 l-2wt%
DC
8283-8260 1043-1066
23 nonbit DC
9063-8975 547-635
88 nonbit DC
9142-9082 438-498
60 2-3wt%
DC
8036-8021 764-779
15 nonbit
C
ND
ND
ND
9037-9025 473-485
12 nonbit DC
ND
8915-8850 710-785
13 lwt% DC
ND
ND
ND
T 45 B BSAT
ND 8193 607
ND 9005 255
8581 525
9054 386
9077 433
3855 990
8902 733
8296 1030
9136 474
00726
ND 9082 498
TABLE 11 (cont'd) Tar Zone Data of Measured Sections
Dry Canyon Subdelta Sunnyside Delta Complex
Measured Section
No. 27 l/l t-4 (N CO r- r-oo r^
e m
No. 28
'' o m 00 <-t ««• en oo r-
W W H (Q
N o . 29
O "T
(N in
co r-
W w
frt £Q
No. 30
o <"> m in f> *^ oo r-w w
No. 31
o o r- oo
oo r-
w w
No. 32
o PI CO 40 <r in 0* 03
eg Id
Z
0 T
E 9
03
0 •
BE
838
9 w
N o . 34
o c">
<j\ a* co r~
W W
No. 36
o o o r~ n r~ co r~
W w H (0
Zone-*-Data*
Elevation Depth Thickness X Bit EOD
Elevation Depth Thickness X Bit EOD
Elevation Depth Thickness X Bit EOD
Elevation Depth Thickness X Bit EOD
Elevation Depth Thickness X Bit EOD
Elevation Depth Thickness X Bit EOD
Elevation Depth Thickness X Bit EOD
Elevation Depth Thickness X Bit EOD
Elevation Depth Thickness X Bit EOD
T 10 B
8725-8721 0-4
4 3.7/8.8
DB
8480-8473 0-7
7 3.2/7.6
DB
8304-8286 16-34
18 1.2/2.9
DB
8347-8337 3-13 10
0.5/1.2 DB
8146-8135 24-35
11 2.3/5.5
DB
9442-9415 38-65
27 4.9/11.7
DB
T 11 B
8478-8475 247-250
3 3.4/8.1
DB
8262-8254 218-226
8 4.8/11.6
DB
3145-8129 175-191
16 3.1/7.3
DB
8175-8156 175-194
19 0.5/1.2
DB
7974-7957 196-213
17 2.4/5.8
DB
8928-8918 102-112
10 4.5/10.8
DB
8629-8623 291-297
6 5.0/12.1
B
8131-8117 169-183
14 2.2/5.4
DB
T 21 B
8422-8419 303-306
3 2 wt%
B
8214-6202 266-278
12 9.4/22.5
B
8056-8053 264-267
3 lwt% NS
7901-7897 269-273
4 lwt% OS
8025-8023 275-277
2 3-4wt%
B
T 23 B
8306-8299 419-426
7 3.2/7.6
B
7970-7960 350-360
10 1.8/4.2
B
7810-7792 360-378
18 5.1/12.1
BB
9169-9142 311-33B
27 2.9/6.9
DB
7962-7948 338-352
14 3.S/8.3
DB
T 25 B
8245-8232 480-493
13 2.9/6.9
NS
7967-7942 513-538
25 lwt% NS
7823-7805 497-515
18 nonbit NS
78,32-7817 518-533
15 lwt% NS
7676-7649 494-521
27 nonbit NS
8813-8796 217-234
17 lwt% NS
3387-8371 533-549
16 3-4wt%
NS
7836-7800 464-500
36 trace
NS
T 26 B
8220-8204 505-521
16 2wt% NS
7930-7917 550-563
13 3.0/7.3
NS
7780-7752 540-568
28 nonbit NS
7790-7762 560-588
28 lwt% NS
7624-7603 546-567
21 nonbit NS
8772-8743 258-287
29 lwt% NS
8364-8356 556-564
8 3-4wt% NS
7777-7770 523-530
7 trace
NS
T 31 B
8150-8143 575-582
7 lwt»
B
ND
7682-7654 638-666
28 2.0/4.9
BB
7734-7723 616-627
11 2.2/5.4
B
7582-7570 588-600
12 3.2/2.8
B
8954-8920 526-560
34 6.8/16.3
BB
870108644 329-386
57 4.0/9.6
BB
8281-8261 639-659
20 lwt% BB
ND
T 32 B
ND
7624-7590 696-730
34 2.0/4.7
BB
7697-7656 653-694
41 1.6/3.7
BB
7530-7521 640-649
9 1.9/4.7
B
8886-8857 594-623
29 4.4/10.6
BB
ND
T 33 B
8092-8080 633-645
12 nonbit
R
"ND
ND
ND
7451-7437 719-733
14 2.7/6.6
BB
8818-8804 662-676
14 5.6/13.4
BB
8609-8584 422-446
24 4.8/11.5
BB
8182-8178 738-742
4 l-2wt%
NS
ND
T 35 B
8013-7980 712-745
33 nonbit DMB
ND
ND
ND
7404-7380 766-790
24 0.8/1.8
BB
8759-8730 731-750
29 7.9/19.0
BB
8489-8431 541-599
58 8.3/19.8
BB
8112-8066 808-854
46 2.0/4.8
BB
ND
T 36 B
7888-7861 837-864
27 nonbit DMB
ND
ND
ND
ND
8677-8648 803-832
29 6.0/14.5
BB
ND
8003-7967 917-953
36 0.2/0.6
BB
ND
37 B
ND
7822-7789 903-936
33 nonbit DC
ND
8576-8563 904-917
13 1.8/4.3
B
ND
T 38 B BSAT
ND 8142 583
ND ND
ND 7590 730
ND 7656 694
ND 7380 790
ND 8563 917
ND 8529 501
ND 8066 854
ND 7777 523
00727
TABLE 12
Tar Zone Data of Measured Sections Whitmore Canyon Subdelta and Distal Areas
Sunnyside Delta Complex
Measured Section
No. 35 CD O
Zone -*• Data +
E l e v a t i o n D e p t h T h i c k n e s s X B i t EOD
T 10 B
8408-8402 1 0 - 1 6
6 3 . 3 / 7 . 9
DB
T U B
9 2 3 4 - 8 1 9 7 1 8 4 - 2 2 1
37 1 . 7 / 4 . 0
DB
T 21 B T 23 B T 25 B T 31 B T 32 B T 35 B T 36 B T 38 B
ND 8 1 9 6 ? 2 2 2 ?
No. 37
(N o O) 03
Elevation Depth Thickness X Bit EOD
8795-8785 420-430
10 2wt% B
8742-8725 473-490
17 1.6/3.8 BB
8580-8568 635-647
12 lwt% NS
8557-8530 658-685
27 lwt% NS
8496-8486 719-729
10 1 . 0 / 2 . 5
B
8 4 0 1 - 8 3 9 4 8 1 4 - 8 2 1
7 1 . 5 / 3 . 7
B
8 3 1 2 - 8 3 1 0 9 0 3 - 9 0 5
2 t r a c e NS
8 2 6 4 - 8 2 5 5 9 5 1 - 9 6 0
9 lwt%
B
8 1 8 6 - 8 1 7 5 1 0 2 9 - 1 0 4 0
11 2 . 0 / 4 . 8
B
8 1 5 9 - 8 1 4 6 1 0 5 6 - 1 0 6 9
13 t r a c e
B
8 1 1 2 - 8 1 0 1 1 1 0 3 - 1 1 1 4
1 1 t r a c e
DMB
8 1 0 1 1 1 1 4
No. 38 o .-.
E l e v a t i o n D e p t h T h i c k n e s s X B i t EOD
9 7 0 0 - 9 6 6 8 9 6 3 1 - 9 6 1 4 9 5 7 6 - 9 5 7 2 9 5 2 7 - 9 4 8 0 9 4 2 0 - 9 3 6 1 9 3 2 3 - 9 2 6 0 9 2 6 6 - 9 2 0 1 9 1 6 3 - 9 1 2 5 2 0 - 5 2 8 9 - 1 0 6 1 4 4 - 1 4 8 1 9 3 - 2 4 0 3 0 0 - 3 5 9 3 9 7 - 4 5 1 4 5 4 - 5 1 9 5 5 7 - 5 9 5
32 17 4 47 33M 54 65 38 6 . 6 / 1 5 . 7 8 . 4 / 2 0 . 0 2-3wt% 5 . 1 / 1 2 . 2 2 . 5 / 6 . 0 3 . 6 / 8 . 5 7 . 1 / 1 7 . 1 n o n b i t
BB B NS BB BEiBB DMB DMB DC
9206 514
No. 39 Elevation Depth Thickness X Bit EOD
9850-9754 0-86 86
8.3/19.8 BB
9703-9693 147-157
10 7 . 3 / 1 7 . 4
B
9 6 5 5 - 9 6 4 4 1 9 5 - 2 0 6
11 6 . 2 / 1 4 . 9
B
9 5 7 0 - 9 5 2 7 2 8 0 - 3 2 3
4 3 5 . 9 / 1 4 . 3
BB
9 4 9 7 - 9 4 3 4 3 5 3 - 4 1 6
63 4.3/10.4 DMB
9400-9390 450-460
10 3.9/9.4
distalDMB
9 3 5 5 - 9 3 2 1 4 9 5 - 5 2 9
34 5 . 8 / 1 3 . 8
BB
9 2 1 0 - 9 1 8 3 6 4 0 - 6 6 7
2 7 n o n b i t
BB
9 3 2 6 5 2 9
No . 40 o o r-i CO CO d C* cr»
E l e v a t i o n D e p t h T h i c k n e s s X B i t EOD
9 7 8 6 - 9 7 7 8 2 4 - 3 2
8 3 . 2 / 7 . 6
B
9 7 3 4 - 9 6 9 4 7 6 - 1 1 6
25M
9 6 5 5 - 9 6 2 8 1 5 5 - 1 8 2
27 5 . 1 / 1 2 . 1 1 0 . 3 / 2 4 . 7
B&B BB
9 5 4 0 - 9 5 3 2 2 7 0 - 2 7 8
8 4 . 6 / 1 1 . 1
B
9 4 8 5 - 9 4 6 1 3 2 5 - 3 4 9
24 7 . 7 / 1 8 . 4
B
9 4 0 9 - 9 3 9 1 4 0 1 - 4 1 9
18 1 . 0 / 2 . 4
B
9 3 1 3 - 9 3 0 4 4 9 7 - 5 Q 6
9 2 . 7 / 6 . 4
B
ND 9 3 0 4 5 0 6
No . 41
cri e l o» CT\
E l e v a t i o n D e p t h T h i c k n e s s X B i t EOD
9 9 3 2 - 9 9 1 0 2 2 - 4 4
22 5 . 2 / 1 2 . 4
BB
9 8 4 3 - 9 8 1 7 1 1 1 - 1 3 7
26 6.0/14.5
BB
9774-9754 180-200
20 4 . 5 / 1 0 . 8
BB
9 7 1 7 - 9 6 5 2 2 3 7 - 3 0 2
51M 2 . 5 / 5 . 9 BBEiDMB
9 5 9 1 - 9 5 2 4 3 6 3 - 4 3 0
5 OH 3 . 8 / 9 . 0 B&BB's
9 4 9 8 - 9 4 7 1 4 5 6 - 4 8 3
27 5 . 8 / 1 3 . 8
BB
9 3 7 2 - 9 3 6 3 5 8 2 - 5 9 1
9 9.7/23.4
BB
9363 591
No. 4 2 Elevation Depth Thickness X Bit EOD
9 5 1 3 - 9 4 9 6 5 2 - 6 9
17 0 . 5 / 1 . 2
B
9 3 9 8 - 9 3 6 3 1 6 7 - 2 0 2
35 2 . 3 / 5 . 6
DMB
9 3 0 4 - 9 3 0 2 2 6 1 - 2 6 3
2 lwt% NS
9228-9205 337-360
23 9 . 0 / 2 1 / 6
B
9 1 5 7 - 9 1 3 4 4 0 8 - 4 3 1
2 3 1 . 2 / 2 . 9
B
ND 9 1 3 4 4 3 1
CO CO
E l e v a t i o n D e p t h T h i c k n e s s X B i t EOD
9 5 9 3 - 9 5 5 8 9 5 2 5 - 9 4 9 8 9 4 7 5 - 9 4 2 6 9 3 6 0 - 9 3 2 9 9 2 7 1 - 9 2 5 3 9 2 - 1 2 7 1 6 0 - 1 8 7 2 1 0 - 2 5 9 3 2 5 - 3 5 6 4 1 4 - 4 3 2
35 27 49 31 15M 9 . 5 / 2 2 . 8 8 . 3 / 1 9 . 9 1 . 9 / 4 . 5 0 . 8 / 1 . 9 3 . 1 / 7 . 5
BB BB BB BB B6BB
9 2 1 2 - 9 1 7 9 4 7 3 - 5 0 6
33 1.3/3.1
BB
ND 9179 506
Elevation Depth Thickness X Bit EOD
9959-9955 6-10 4
NS
9918-9897 47-68 21
BB
9853-9828 112-137
25 0-lwt% NS
9800-9768 165-197
32 0.3/0.7
NS
9755-9713 210-252
42 2.4/5.8
BB
9 6 4 3 - 9 6 2 5 3 2 2 - 3 4 0
18 0 . 7 / 1 . 7
B
9 4 9 0 - 9 4 6 5 4 7 5 - 5 0 0
25 9.9/22.3
BB
9430-9406 535-559
24 1 . 8 / 4 . 4
BB
9 3 5 0 - 9 3 3 3 6 1 5 - 6 3 2
17 2 . 4 / 5 . 7
BB
9 1 9 0 - 9 1 8 0 9 1 8 0 7 7 5 - 7 8 5 7 8 5
10 2 . 6 / 6 . 1
B 00728
S - ^ S - i - ??. . i . - - t .
/:<%3
~ ; x ^ — ^ L k * . gr-^aiww' ^agi<i8
Amoco Production Company
WILLIAMS. CALKIN, D.Sc. C0NSULTIN6GE0L0GIST
25200 VILLAGE CIRCLE • GOLDEN,COLORADO 80401 • PHONE (303) 526-0711
May 19, 1987
Mr. Gene E. Tampa Director Tar Sands and Shale Projects Amoco Corporation MC 290 3 200 East Randolph Drive Chicago, Illinois 60680
Dear Mr. Tampa:
This three volume report on the Sunnyside Tar Sands project is a summary of the geological field and office work completed for the 1986 exploration program. The written report represents an addendum to previous exploration reports for the 1980, 1981, 1982 and 1984 exploration programs.
The summary and conclusions as well as recommendations occur at the beginning of the report. All photographs, figures and tables are in numerical order in the Appendix at the end of the written report in Volume I. The Regional Map, Geology Map and Tar Sand Isopach Map are in Volume II. The strip logs of Measured Sections 27-44 are in Volume III.
The support and cooperation of Amoco during both the field and research phases of this tar sands project is gratefully acknowledged. The drafting was completed by Owen Schlipmann and Keith Farmer of Amoco Production in Denver.
Ten copies of this report have been made and will be sent to your office for distribution. If there are any questions regarding the geological aspects of the Sunnyside Tar Sands project that need clarification, please contact me.
Sincerely,
Wm. S. Calkin
00633
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