ML19330A401
| ML19330A401 | |
| Person / Time | |
|---|---|
| Site: | Columbia  |
| Issue date: | 05/31/1980 |
| From: | Farooqui S, Thomas R SHANNON & WILSON, INC. |
| To: | |
| Shared Package | |
| ML17275A455 | List: |
| References | |
| NUDOCS 8007250398 | |
| Download: ML19330A401 (45) | |
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GEOLOGIC EVALUATION OF SELECTED FAULTS AND LINEAMENTS PASCO AND l
WALLA WALLA BASINS - WASHINGTON I
l prepared for l
WASHINGTON PUBLIC POWER SUPPLY SYSTEM under the direction of l
UNITED ENGINEERS & CONSTRUCTORS, INC.
Contract No. 44013, C.O. 43 Task-3 l
B l May,1980 I
B l by SALEEM M. FAROOQUI RICHARD E. THOMS SHANNON & WILSON, INC.
I 2255 S.W. Canyon Road Portland, Oregon 97201 l
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\ %O07250 298
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TABLE OF CONTENTS L
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- 1. INTRODUCTION 1
{ l.1
SUMMARY
AND CONCLUSIONS 1 1.2 PURPOSE AND SCOPE 2 7 1.3 METHODS OF INVESTIGATION 3 1.4 ACKNOWLEDGEMENTS 3
- 2. FINLEY QUARRY FAULT 4 2.1 GENERAL 4
2.2 DESCRIPTION
OF LITHOLOGIC UNITS 4 2.3 FAULTING 6 E~ 2.3.1 Description of Faulting 6 L
2.3.2 Age of Faulting 7
- 3. KENNEWICK-COLD CREEK LINEAMENT 8 3.1 GENERAL 8 L_ 3.2 ANALYSIS 9 3.2.1 Southern Segment (Kennewick Lineament) 9 3.2.2 Central Segment (Horn kapids Lineament) 10 3.2.3 Northern Segment (Cold Creek Lineament) 11 3.3 INTERPRETATION 12 I 4. BUROKER FAULT 16 I
l 4.1 4.2 GENERAL DESCRIPTION OF FAULT 16 16 l
S. GAME FARM HILL FAULT 18 l
- 6. SILVER DOLLAR FAULT 19 l
- 7. BADGER MOUNTAIN FAULT 21 l
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i TABLE OF CONTENTS (continued) 1 Page
> 8. BADGER CANYON FAULT 23
- 9. REFERENCES 24 LIST OF FIGURES Figure Number 1 Index and Location Map 2 Geologic Sketch of Finley Quarry Fault 3 Photographs of South Fault 4 Photographs of North Fault 5 Photographs of North Fault 6 Photographs of Colluvium 7 Lineament Map 8 Geologic Map - Kennewick-Cold Creek lineament area 9 Geologic Cross-Sections 10 Location Map - Buroker Fault 11 Geologic Sketch of Buroker Fault 12 Photographs of Buroker Fault i
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- 1. INTRODUCTION 1
1.1
SUMMARY
AND CONCLUSIONS Seven selected geologic features in the Pasco and Walla Walla basins in Washington State were geologically examined. The features include:
- 1) Finley Quarry fault, 2) Kennewick-Cold Creek lineament, 3) Buroker fault,
- 4) Game Farm Hill fault, 5) Silver Dollar fault, 6) Badger Mountain fault, l l and 7) Badger Canyon fault. The field studies consisted of reconnaissance mapping by traverses, and detailed mapping of a quarry face in the Finley j Quarry.
The Finley Quarry fault consists of a 35-foot wide fault-breccia zone. The fault zone strikes approximately east-west and juxtaposes an older colluvial unit against the fault breccia zone along a high-angle 5 reverse fault contact. The overlying younger colluvial and loess units are not displaced by the faulting. The age of latest movement is estimated to be late Pleistocene.
l The Kennewick-Cold Creek lineament is a prominent linear feature that can be seen on topographic maps, aerial photographs and imagery. The lineament consists of three distinct segments, each with its own peculiar l
geomorphic, geologic and geographic limits. The southern segment can be j traced as a linear feature along breaks in slope on terrace T3 "" **#9 9 i
I cen hal segment consists of an aHgnmed of 6 low terraces T3 "" 4 hills underlain by the Saddle Mountains Basalt. The northern segment trends along the valley of Cold Creek. No surficial evidence could be found for either horizontal or vertical movement along the Kennewick-Cold Creek l lineament. The lineament appears to be of non-tectonic origin.
The Buroker fault is a north-striking reverse fault that juxta-l poses Wanapum Basalt against the Palouse Formation. The fault appears to splay into several fractures that traverse the Palouse Formation. The j
minimum age of faulting appears to be pre-Holocene.
Our reconnaissance of the Game Farm Hill fault revealed that W the basis for identification of the fault is speculative, and that the fault l does not exist.
The Silver Dollar fault appears to be a scissor fault with a I hinge to the east and south-side-down.
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1 The Badger Mountain fault appears to be restricted to the SE-Hill and does not traverse the entire length of Badger Mountain as mapped by Rockwell.
The existence of the Badger Canyan fault is speculative and the mapping of landslide is incorrect.
1.2 PURPOSE AND SCOPE !
This report presents the results of geologic studies of selected structures in the Pasco and Walla Walla Basin areas in Washington. The studies were conducted to evaluate certain fault features mapped by Rockwell and its consulta.ts, and not previously shown on maps in Amendment 23 (WPPSS, 1977a), and to evaluate the Kennewick-Cold Creek lineament described by Glass (WPPSS, 1977b). The structural features selected for field evaluation included: 1) Finley Quarry fault, 2) Kennewick-Cold Creek lineament, 3)
Buroker fault, 4) Game Farm Hill fault, 5) Silver Dollar fault, 6) Badger Mountain fault, and 7) Badger Canyon fault, as shown on Figure 1. Except for the Kennewick-Cold Creek lineament (WPPSS, 1977a), all of these structures 1
are based on mapping done for the following geologic reports prepared for or by Rockwell Hanford Operations.
Geologic studies of the Columbia Plateau, A Status Report: Rockwell (1979) No. RHO-BWI-55-4
- Geology of the southwestern Pasco Basin: Bond and 1.
others (1978) No. RHO-BWI-25 Rockwell Annual Report-Fiscal Year 1979,
)- No. RHO-BWI-79-100
- Geology of the Gable Mountain-Gable Butte area:
Fecht (1978) , No. RHO-BWI-LD-5 Geology cf the Nine Canyon map area: Jones and Landon (1978), No. RHO-BWI-LD-6
- Geology of the Saddle Mountains between Sentinel I Gap and 119 3' longitude: Reidel (1978), No. !
RHO-BWI-LD-4 Field checking began on January 29 and recessed twice - from February 2 to FeOruary 10 and again from February 13 to March 27, 1980 -
owing to heavy accumulations of snow and to freezing rains.
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The objectives of the field studies were to provide information l
on: 1) quality of exposure; 2) existence of faulting in the bedrock and/or surficial units; 3) stratigraphic units involved in the faulting; and 4) probable age of faulting.
1.3 METHODS OF IfNESTIGATION The field studies consisted of reconnaissance mapping by traverses I along the mapped faults, collection of basalt samples for chemical analyses from outcrops critical to understanding basalt stratigraphy and structure; j a review of pertinent published information; and discussions with Rockwell geologists who mapped the structures. The results of the reconnaissance mapping were plotted on U.S.G.S. 7.5-minute series topographic base maps.
Aerial photographs and high altitude imageries were also examined to provide regional information on the Kennewick-Cold Creek lineament.
l The cut-slopes of Finley Quarry were examined in detail to provide I
l a complete study of the exposed geologic conditions. Detailed mapping of the eastern face included examination, description, and tracing of strati-graphic and lithologic units; and a detailed study of geologic structures.
l Measurements were made by a tape survey from an arbitrary horizontal and vertical control. The geologic observations were recorded on a grid base with a vertical and horizontal scale of 1 inch equals 5 feet. A geologic sketch l
of the face was then constructed from these data.
l 1.4 ACKNOWLEDGEMENTS I
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Field work for this project was conducted by Saleem M. Farooqui and R.E. Thoms. H.H. Waldron and R.J. Deacon assisted in the preparation of the report. The report was reviewed by D.D. Tillson.
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r- 2. FINLEY QUARRY FAULT L
2.1 GENERAL Finley Quarry is located at the west end of The Butte, a narrow ridge in sec. 3, T7N, R30E, approximately 2.5 miles south of the town of Finley and 7 miles southeast of Kennewick (Figure 1). The quarry is periodi-cally used for production of crushed rock products.
l The Butte is a doubly-plunging, anticlinal ridge that is underlain by the Saddle Mountains Basalt (WPPSS, 1977a; Jones and Landon, 1978). The anticline is slightly sinous, generally trends eastward, and is mantled by I
l colluvium and loess. The quarry operation, near the west end of the plunging fold, has exposed a complex fault zone in the east face of the quarry. This fault zone is referred to in this report as the Finley Quarry fault. Geologic conditions at the Finley Quarry are shown on Figure 2, and photographs of l the fault are shown in Figures 3 through 6. A description of the lithologic units and structural conditions exposed in Finley Quarry is presented in the l following sections.
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2.2 DESCRIPTION
C .AIC UNITS I
The lithologic units and structures exposed in the east face of I the quarry are shown in Figure 2. The lithologic units, from youngest to oldest, include loess (Unit 1), colluvium (Unit 2), fault-breccia zone I (Unit 3) and Umatilla Basalt (Unit 4). The various units shown on Figure 2 are described below.
I f Unit 1. Iness Light brown sandy silt; grades upward into darker brown soil horizon, and contains scattered, angular basalt fragments l
ranging in size from 1 to 6 inches diameter. Thickness ranges from 0 to 10 feet, with overlying soil horizon as thick as 1 foot.
Unit 2. Colluvium 2a. Young Colluvium.
l Angular, subangular, and subrounded pebble-to boulder-sized basalt and exotic rock types, in light brown, sandy silt l l
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I matrix. Clasts range in size from 1 to 12 inches. Exotic
} fraction includes quartzites and granites. Thickness ranges f rom 0 to 3 feet.
2b. Old Colluvium.
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Similar to young colluvium of 2a, but' lacks exotic clasts, and contains interfingering, wedge-shaped lenses as long as 4 feet and as thick as 5 inches composed of subangular I
and angular pebbles and cobbles to coarse and fine sand.
i Sandy silt matrix is light to dark brown, with limonitic staining in places. Total thickness is unknown, but approximately 5 feet is exposed.
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Unit 3. Pault-Breccia Zone 3a. Clay Gouge.
- Varies frpm dark gray, brittle, slickensided, and 2 to 10 inches in thickness near fault, to greenish-yellow, very t finely granular, plastic, with residual basalt fragments away from fault. Thcse gouge types are separated by a clastic dike of very light terracotta-colored silt, about 1 to 4 inches thick. Short, d scontinuous calicF e i
g stringers occur in the greenish-yellow gouge. Width is approximately 4 feet. Polished surfaces lack stri-ations.
3b. Brecciated Basalt.
i Vesicular, cobble-sized, subangular fragments in a yellowish-stained, pulverized, fine-grained basaltic matrix. C.tasts range in size from about 1 to 10 inches. Width 4 to f feet.
Probably Pomona Basalt.
1 l 3c. Tuff.
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Fine-grained, cemented, somewhat platy, light buff to white tuff. Possibly Selah member. Width 0 to 4 feet.
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l 3d. Brecciated Basalt.
Angular basalt blocks in a light yellow-brown, finely- l 1
crushed basaltic mat :'". Fragments range in size from l 1 to 12 inches. Width 0 to 12 inches. Probably Pomona Basalt.
3e. Clay Gouge.
Brittle, slickensided, platy, dark gray to olive-drab, with scattered angular basalt clasts up to 1 foot diameter.
Clastic dikes of coarse to fine sand adjacent to Unit-3f.
Width 0 to 4 feet. Slickensides lack striations.
3f. Brecciated Basalt.
Angular, dark brown, pebble-sized basalt in a well-cemented, very light brown ground basalt matrix, with thin clastic dikes of sand. Width 0 to 3 feet. Umatilla Basalt.
Unit 4. Umatilla Basalt Fine grained, glassy, blocky-jointed black basalt with scattered, inclined and vertical yellow-brown shear .ones 2 to 12 inches wide. Vertical shear zones strike approximately N60 W.
2.3 FAULTING 2.3.1 Description of Faulting As shown on Figure 2, the Finley Quarry fault consists of a 35-foot wide fault-breccia zone, which includes tectonically fragmented and pulverized slivers of the Pomona (?) and Umatilla Basalts and the interbedded Selah Member (Units 3a, 3b, 3c, 3d, 3e, 3f and 3g). A lithologic description of the fault-breccia was presented in Section 2.2. The fault-breccia zone is bounded by fault planes on the south and north. These 2 fault planes are called the south fault and the north fault, and are described as follows:
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The south fault (Figure 3) strikes N65 W and dips vertically.
[ It separates Umatilla Basalt (Unit 4) from the fault-breccia zone (Unit 3). Although polished surfaces are present along
{ the fault plane, no striations were observed. This fault is overlain by a thin veneer of loess (Unit 1) showing no evidence of a displacement.
The north fault (Figures 4 & 5) strikes approximately east-west and dips 55 degrees to the south. It juxtaposes an older colluvial unit (2b) against the breccia zone. The older colluvium (Unit 2b) consists of angular basalt fray-ments in a sandy and silty matrix (Figure 6) with brown
( and red-brown iron-staining present throughout. Horizon-tally bedded, fluvial sand lenses interfinger with the older colluvium. We estimate the minimum probable age of this colluvial unit (2b) is Wisconsin. The adjoining fault-breccia zone (Unit 3) consists of sheared, pulverized Pomona (?) and Umatilla Basalts. Numerous slickensides are present in the clayey gouge zones, but no striations were observed. Generally, these slickensides are sub-parallel to the fault plane.
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2.3.2 Age of Faulting
{ The Finley Quarry fault zone, and specifically the north fault, is overlain by a thin (0 to 2 feet) younger colluvial unit (2a), which in turn is overlain by 0 to 10 feet of loess (Unit 1). The overlying younger colluvial unit (2a) is not displaced by the north fault; however, some fractures emanating from the fault (Figure 5) seem to dissipate into this
[ unit. The overlying loess also is apparently unaffected by faulting. The l age of this loess is estimated to be approximately 7,000 years B.P. This j estimate is based on the presence of what is probably Mazama ash within similar loess on slopes in nearby areas.
{ The Finley Quarry fault lies along the projected trend of the l Wallula fault (WPPSS, 1977a; Shannon & Wilson, 1979). Latest movement of the Finley Quarry fault is estimated to be late Pleistocene (pre-7000 years).
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I 3. KENNEWICK-COLD CREEK LINEAMENT I 3.1 GENERAL I
l The Kennewick-Cold Creek lineament is a prominent linear feature paralleling the Rattlesnake !! ills-Wallula lineament from the vicinity of Wallula Gap to near the east end of Yakima Ridge, a distance of about 20 miles (Figures 1 & 7). The term " lineament" as applied to this feature l follows the usage of O' Leary and others (1976). It can be seen on AMS and U.S.G.S. 7.5-and 15-minute topographic maps; on both vertical and oblique l low altitude aerial photographs, on LANDSAT imagery; and on various geologic maps. '
Relative resolutions of these imageries are shown on the Lineament Map (Figure 7). The broad, finely-dotted pattern represents the lineament I as it appears on the LANDSAT photographs. The narrower, more coarsely-dotted l'
strips show the three major segments of the lineament on the AMS sheet.
Topographic breaks, readily seen in the field and on 7.5-and 15-minute topo-graphic maps and low-altitude aerial photographs are indicated by broad solid lines (dashed where less distinct).
l The "Kennewick-Cold Creek Lineament" was recognized and described by Glass (WPPSS, 1977b) as follows:
"The Kennewick lineament parallels the Rattlesnake structure from Wallula Gap to approximately Kennewick. The lineament I is characterized by an abrupt vegetation contrast and an l
east-facing break in slope (Figure K-15) . A number of factors have led me to interpret this feature as a terrace.
At its northern end the Kennewick lineament turns to the northeast and joins several similar features originating
( to the west and northwest. At its southern end the lineament gradually (sic) decreases in height and cannot be followed south of Finley. Several older terraces l
appear upslope to the west of the Kennewick lineament and trend roughly parallel to it . . . . The Cold Creek l
lineament extends from Columbia Camp to beyond Benson B Ranch (Figure K-24, Sheet 2). The lineament is eminently detectable on LANDSAT imagery and parallels the Rattlesnake structure."
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- In an earlier report, Glass (1977) described the lineament as I 1
paralleling the Rattlesnake trend, but about 2.5 kilometers east of it, and l as being formed by a 2 to 3 meter-high topographic break combined with a l striking contrcst in vegetation. He also noted several ponds resembling sag ponds along the lineament's trend and suggested the lineament may extend onto the Hanford reservation in the vicinity of Cold Creek.
Although the lineament may appear to be a single, continuous
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feature on high-altitude imagery or on larger-scale topographic maps, our detailed analysis shows that it actually consists of three distinct segments, each with its own peculiar geomorphic, geologic and geographic limits. In addition, these segments display angular alignments of features that can
_ differ from each other by as much as 25 of azimuth, although they are usually
__ nearly coincident. The Geologic Map (Figure 8) and the Geologic Cross-sections (Figure 9) show the details of the topography and geology in the vicinity of the lineament. Geology and geomorphology of the area are based upon this investigation and previous mapping by WPPSS (1977a) and Rockwell
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(1979a). Observations of the physical nature of the three lineament structures are presented in Section 3.2, and the interpretations are given in Section 3.3.
3.2 ANALYSIS 3.2.1 Southern Segment (Kennewick Lineament)
This segment is a distinct feature on topographic maps from scales of 1:24,000 down to 1:250,000. It can be seen plainly as a slope break and vegetative change on both vertical and oblique aerial photographs (see WPPSS, 1977b, Figures 2R K-12 and 2R K-15) as well as on LANDSAT photos of the area.
It is a portion of a broader pattern of terraces first described by Farooqui (WPPSS, 1977a, p. 2R H.5-10), who stated:
"Four Quaternary terraces are mapped along the south I margin of the Pasco Basin. These terraces occur at approximately 340 foot elevation (T y), 370 foot elevation (T ), 500 foot elevation (T * ^"
2 3 foot elevation (T 4). The two lower terraces, T and T2 , are developed on younger glaciofluvial deposits. The higher terrace, T4 is overlain by L
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{ Touchet beds. Northwest of M-liill, this terrace T4 is developed on the Ringold Formation. Locally Kennewick fang 15merate may underlie the terrace
{ southeast of M-Hill."
j on the ground, the lineament can be traced as a linear feature,
[ trending about N50 W, from Piert Road on the southeast to Carlson Road on the northwest, a distance of about 3.5 miles. Throughout its entire trend, it consists of a northeast-facing break in slope on terrace T . From Cadson 3
Road on to the northwest as far as south Garfield Street, a distance of about 2.5 miles, it continues as a linear feature but consists of the north-east-facing break in slope of two merging terraces, 3 T and 4
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{ total distance over which a distinct linear feature can bo traced is about 6 miles. Beyond the southeastern end, the contours along this trend continue parallel to it as far as the Columbia River, but no distinct break in slope can be detected. Along the Meals-Yellepit Road, between Toothaker Road and Goose Gap, a series of low, parallel ridges are crossed, but these do not involve sufficient elevation changes to produce any effect at a scale of 1:24,000.
Beyond south Garfield Street to the northwest, the lineament is lost in the dissected alluvial fan at the mouth of Zintel Canyon. Plat
{ surfaces with elevations equivalent to those of terrace T 3
1 mile to the northeast of the lineament, and which are centered on the low hills where Triangulation Point " Junk" is located (Figures 7 & 8; Figure 9, i sections C-C's and D-D').
Terrace T 3
s r a n ma n y gra e a m r san sm layers, but little distinct bedding can be seen. The gravel is composed of basaltic and exotic (plutonic and metamorphic) rock types, which are rounded to_subangular and range in size from pebbles to boulders. Weathering rinds on basalt clasts average about 1/8". No significant change in lithology
{ could be seen throughout the entire break in slope, nor between terraces T3 and T2, which have similar clast rock types.
E 3.2.2 Central Segment (Horn Rapids Lineament)
Topographically, this portion of the lineament consists of a series of 6 low hills about 600 to 700 feet in elevation, which trend about E
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L N35 W along the southwest side of the Yakima River from Leslie Road on the
[ southeast to just north of Ilorn Rapids on the northwest (Figures 7 & 8; 1#
Figure 9,sectionsB-B{andB-Bj). 2 Attention was initially drawn to this feature, described as the
" Horn Rapids Alignment", by Jones and Deacon (1966). Later (WPPSS, 1974),
it was discussed in more detail:
" Horn Rapids Alignment - The Hot.2 Rapids alignment consists
{ of a series of 6 small elongated domes exhibiting a very low relief of 50 feet to a maximum of 350 feet. Most of the relief occurs on the northeast sides and gentle slopes are common toward the southwest. The hills extend for a distance of about 13 miles in a southeastward cirvilinear (sic) path from approximately one mile north of Horn Rapids on the Yakima River to about two miles south of Richland (Figure 2.5-4 and Appendix 2D). The maximum amount of surface structural relief occurs on the hill
{ adjacent to the town of West Richland. This hill exhibits about 350 feet of relief above glaciofluvial sediment.
Folding of the dome is relatively gentle, with maximum mapped dips of basalt flows being about 35 degrees."
The hills consist of nearly flat-lying flows of the Elephant Mountain and Ice Harbor Members of the Saddle Mountains Basalt mantled by glaciofluvial deposits. In one place along the lineament, in the banks of the Yakima River (NE 1/4 sec. 16, T9N, R28E), flat-lying beds of the Ringold Formation are at the same elevation as an outcrop of the Ice Harbor flow at
{ the southern end of the exposure. A covered interval separates the two units, obscuring their contact relationship. Structure along this trend appears to be very minimal, with shallow dips of 2 to 5 on gentle anti-clinal folds (Rockwell , 1979a) .
3.2.3 Northern Segment (Cold Creek Lineament)
This segment, prominent on aerial photographs and topographic maps of all scales, consists of the N50 W trending valley of Cold Creek, which runs perpendicular to the northeast-facing pediment of the Rattlesnake
{ Hills. On the ground, the only distinctive portion of the northern segment is a low northeast-facing scarp, about 50 feet in height, which borders E
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i Cold Creek to the southwest from its confluence with the Yakima River to a point about 2.5 miles upstream. This scarp, trending about N25 W, is visible on Bonneville Power Administration (BPA) aerial photograph PSLG7E-43 and on the Richland 15-minute topographic map (Figures 7 & 8; Figure 9, section A-A').
Units exposed in the scarp include the lower of the two Elephant Mountain flows overlain by colluvium and glaciofluvial deposits, and valley fills of coarse, poorly sorted, angular material apparently derived from Rattlesnake Ilills. The northeast bank of Cold Creek is composed of glacio-fluvial deposits, chiefly gravel and sand. The pediment was constructed on gently eastward-dipping basalts (WPPSS, 1977a), capped with a thin veneer of colluvium, now being dissected by streams downcutting through valley fills.
The scarp cuts across both the basalt and the old valley fill.
- 3. 3 INTERPRETATION The southern segment (Kennewick lineament), which chiefly consists of the break in slope between terrace levels T and *2, was probably produced 3
as an erosional feature during one of the later episodes of Spokane flooding (Wisconsin age). This is supported by the existance of similar gravel at similar elevations immediately across terrace T to the northeast of this 2
trend (see section C-C' in Figure 9). The linear nature of the feature, although long and distinct, is not unique among erosional or depositional features produced by Spokane flooding. Between Umatilla and Boardman Junction in Oregon, a 400'-terrace can be traced as a near-straightline feature for about 11 miles; while in the Portland area, a 200'-terrace can be traced for about 6 miles. Thus, it appears that the Kennewick lineament may represent a streamlined erosional feature produced by flood waters rushing toward
! Wallula Gap. The dramatic vegetational change along the lineament coincides with' the proximity of groundwater to the surface. In fact, the ponding of spring water issuing from the gravel near the base of the break in slope between terrace T and T was n e yG ss (WPPSS, 1977b), who originally 2 3 thought they might be sag ponds. Ponding appears to be caused, in part, by the impervious lining of the irrigation ditch, which parallels the break in slope. The possibility of right-lateral motion along this trend was hypothe-sized and then discarded by GLASS (WPPSS, 1977b, p. 2R K-10 and -11) :
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"Ilowever, between Terril Road and 27th Avenue (Figure
{ K-24, Sheet 1) the stream channels across the Kennewick lineament appear too large to have been generated by the streams which currently feed them. The major streams from the highlands to the west are located at the ends of the domes on the Rattlesnake structure. These streams are currently cutting relatively deep channels across
[ the Kennewick lineament. A possible interpretation of these apparently anomalous channels is that movement
{ along the Kennewick lineament has progressively displaceu the channels on the right-lateral direction. This would result in a total offset of 3,000 meters. Offsets of this magnitude, however, seems incredible for a feature which can only be traced for approximately 16 kilometers.
The most reasonable interpretation is that the Kennewick lineament is an old terrace of the Columbia River."
It should be further noted that only two major streams, which exhibit the appropriate pattern, occur within the southern segment, while at
{ the very northern end of the segment, Zintel Canyon exhibits exactly the opposite direction in its passage around the northern end of Pipeline Hill.
In addition, Farooqui (WPPSS, 1977a, p. 2R H.5-10) commented on the lack of evidence for deformati,on:
"All of the terraces appear to be free of deformation and show no evidence of tectonic movement."
AGeording to the interpretation given above, the Kennewick lineament would have been produced in late Wisconsin time. Alluvial rans produced since that time, by sidestreams debouching onto terrace T2, show no
{ features that can be considered part of the alignment.
The central segment (Horn Rapids, lineament), consisting of a series of low basaltic hills mantled by glacisfluvial deposits, is tenuously
{ interpreted as a ser.es of very low amplitude folds parallel to and probably produced simultaneously with the Rattlesnake Hills-Wallula lineament (Figure 9, sections B -B' 7 , andB-Bj).
2 These were apparently later modified into erosional scabland remnants by the plucking action of Spokane flood waters and subsequently nearly buried under glaciofluvial deposits. No evidence E
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expressed by Fugro, Inc. (WPPSS, 1974):
"No faults were identified along the Horn Rapids alignment during the detailed mapping done for this investigation. '
Photogeologic lineations appear to be related to differ-ential erosion along basalt joints and commonly are parallel to joint sets measured in the field. Breccia j zones observed at isolated localities are identified as flow breccia based on the scoriaccous and vesicular nature of the basalt. It is concluded that the Horn I Rapids alignment is not faulted. Blume and Associates (Reference 50) arrived at the same conclusion during mapping for the FFTP study."
I Erosion by the Yakima River in post-Wisconsin time has enhanced l l these features.
The northern segment (Cold Creek lineament) consists of two l features related to the action of Cold Creek. The first of these is the alignment of the valley of Cold Creek. '"his is not surprising, as it runs counter to the slope of the Rattlesnake Hills pediment, exactly as it should.
I Such situations are the rule in the arid cycle of erosion. The second feature is the low scarp, seen along the west side of the valley near the confluence with the Yakima River (Figure 9, section A-A').
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This was probably produced by the lateral planation of Cold Creek. Concerning this portion l of the lineament, Glass (WPPSS, 1977b, p. 2R K-10 and -11) has commented:
" Interpretation of low sun-angle photography has failed I to yield a conclusive interpretation."
Both of these features are probably post-wisconsin in age.
j In conclusion, no surficial evidence could be found for either horizontal or vertical movement along the Kennewick-Cold Creek lineament.
The existence of the same stratigraphic horizons at the same elevations I across the lineament precludes any significant vertical movement. These realtionships can be seen along the Kennewick lineament where the gravel of terrace T ccurs on both sides of the lineament. Again, along the Cold 3
Creek lineament, the lower Elephant Mountain flow crops out at approximately 1
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u the same elevation on both sides. Along the Horn Rapids lineament, the upper lacustrine and conglomerate members of the Ringold Formation crop out on the southwest side of the feature (Figure 9,sectionB-Bj),whilethe 2
blue-clay member has been recorded from a well at the Richland Wye, at a depth of 72 feet, on the northeast side of the lineament (Newcomb, 1958).
L Thus, the stratigraphic progression toward the northeast across the lineament is in the normal sense, with no indication of reversal, c-
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- 4. BUROKER FAULT
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4.1 GENERAL The Buroker fault is exposed in a road cut along Russell Creek Road, approximately 6 miles east of Walla Walla in sec. 31, T7N, R37E. The
( location of the exposure is shown on Figures 1 and 10. A sketch of the fault exposure is shown on Figure 11 and photographs of it are shown on Figure 12.
{ The Buroker fault investigation was conducted to evaluate its reported late Cenozoic (post-Columbia River Basalt) movement. The fault was described in Rockwell (1979a), although it was not shown on the map accompany-ing the text. The RocLwell description is as follows:
" Reconnaissance mapping of sediments within ti.e Blue Mountains subprovince showed the presence of two minor faults which cross-cut late Cenozoic sediments
( (Plate II-16). One of these faults is a small reverse fault in a roadcut southeast of Walla Walla on the
{ Buroker quadrangle (T7N, R37E). The fault appears to cut overlying fluvial gravels and an older loess, but does not deform overlying younger loess. The age of these sedimentary units currently is not known; hence, age limits for the structure are not yet established. A second nearby fault, cutting the basalt (Frenchman Springs Member), is probably related
[ to the previously described structure."
Swanson and others (in Rockwell, 1977a, b) mapped a small
{ northeast-striking fault in the vicinity of the Buroker fault. However, from their mapping, it is not clear whether they mapped the Buroker fault, as described in Rockwell (1979a), or some other fault.
4.2 DESCRIPTION
OF FAULT The Buroker fault is exposed in a road cut excavated at the south cnd of a north-northeast-trending ridge. The cutface is oriented east-west and is approximately 20 feet high near the middle.
As exposed in the cut, the ridge is underlain by a soil horizon
{. (A-horizon), tan loess, red-brown loess (Palouse Formation) and basalt
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i (Figures 11 & 12). The A-horizon soil zone, which mantles the ridge slopes, is approximately 1 to 2 feet thick and consists of dark gray silt with abundant organic debris. The underlying tan loess is 2 to 5 feet thick and l
is composed of silt with scattered caliche stringers and nodules. According to Newcomb (1965), this tan loess is derived from the reworking of the l
l Touchet beds. Most of the caliche stringers in this loess are sub-parallel to the topography. The tan silt also mantles the slopes. The Palouse l Fonnation (Newcomb,1965) occurs between the basalt and the tan loess, and ,
consists of red-brown, clayey silt and some scattered angular to subrounded j basalt fragments. The contact between the tan loess and the Palouse Formation '
appears to be gradational and unconformable. Only a small portion of basalt is exposed in the cut; most of it is covered by debris. The limited exposure shows that the basalt consists of highly weathered and altered, greenish-E gray and red-gray, closely-jointed basalt of the Dodge flow (Swanson and l
l others, in Rockwell, 1979a). The contact between the basalt and the Palouse Formation is nearly horizontal.
l The Buroker fault is a reverse fault that appears to strike in a general north-south direction. It dips approximately 26 degrees to the j west and is in sharp fault contact with the Palouse Formation (Figures 11 &
12). The throw is approximately 22 inches. The fault appears to splay into several fractures that traverse the Palouse Formation and vanish in the overlying tan loess. Sorae of these fractures are lined with caliche.
5 The fault cuts both the Dodge finw of the Wanapum Basalt of middle Miocene age and the Palouse Formation of Pleistocene age. The Pleistocene age of the Palouse Formation is based on its stratigraphic position, lying above the old gravel and beneath the Touchet beds of Pleistocene age (Newcomb, 1965). The minimum age of faulting appears to be pre-tan loess, or pre-Ilolocene.
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- 5. GAME FARM HILL FAULT
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Game Farm Hill (Jones and Landon, 1978) or K-Hill (WPPSS, 1977a)
( is located in section 30, T8N, R30E. The hill is underlain mainly )y Pomona and Umatilla Basalts. A small section of the Priest Rapids Basalt crops out
{ above a creek bed along the south slope of the hill. The hill is a doubly-plunging anticline, defined by the distribution of the Pomona Basalt. A small outcrop of the Umatilla Pasalt occurs near the structural culmination (WPPSS, 1977a; Jones and Landon, 1978; Rockwell, 1979a).
Jones and Landon (1978) mapped an approximately 1/2-mile long fault (Game Farm Hill fault) along the south flank of the anticline. A field check was conducted to evaluate the existence of the fault, because
( it lies along the trend of the Rattlesnake Hills-Wallula lineament (WPPSS, 1977a and 1974; Rockwell, 1979a). This minor fault, as shown on the map
{ (Rockwell, 1979a), is within the Umatilla Basalt. Two deep ravines, which cut the inferred fault trend show no evidence of faulting, although some minor shears and altered basalt were observed. Such minor shears, however, are common in tight folds of the Columbia Plateau.
Our reconnaissance of the faulting revealed tl.at the basis for identification of the fault is speculative and lacks direct field evidence.
The ravines cutting across the trend show unfaulted basalt and rule out the
( interpretation of faulting. Therefore, in our opinion, a fault as shown on the Rockwell Map (1979a) does not exist.
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- 6. SILVER DOLLAR FAULT The Silver Dollar fault was originally mapped by Rockwell (1979a) in secs. 1, 2 and 3, T12N, R23E, and secs. 6 and 7, T12N, R24E (Figure 1) along the east flank of the east plunging Yakima Ridge anticline. As shown ;
{ on sheet 4 of Rockwell's (1979a) map, the fault offsets the Frenchman Springs, Roza and Priest Rapids Members of the Wanapum Basalt against the Umatilla and Pomona Members of the Saddle Mountains Basalt in secs. 1, 2 and 3, T12N, R23E, and is mapped solely within the Pomona Member in section 7, T12N, R23E. The total indicated length of the fault is approximately 5 miles. The eastern one-third of the fault is !hown partly in bedrock and partly covered, whereas the western two-thirds of the fault length is shown covered by loess. The Silver Dollar fault extends westward into the Yakima Bombing Range. To the east, it is shown branching into two faults in sec. 1,
{ T12N, R23E. The shorter north branch terminat.es in the Pomona Member; whereas the longer south branch extends for one mile and is shown also terminating in the Pomona Member. Rockwell (1979a) interprets the fault as either a high angle reverse or a normal fault with the south-side-down.
Our field reconnaissance confims the presence of the Silver Dollar fault west of the Yakima-Benton County line. We found no evidence, however, to confirm either the branching of the fault or its eastward extension into sec. 7. T7N, R23E. Evidence of faulting observed during this study confirming the Silver Dollar fault is based on the following field observations:
Dark gray to black, glassy to very fine-grained, closely-
{ jointed basalt of the Umatilla Member to the south is in contact with a dark gray to black, columnar, fine-grained aphyric flow of the Frenchman Springs Member to the north.
I These members occur at about the same elevation (approxi-mately 1800 feet) in a south-draining ravine between secs.
1 and 2. However, the members are separated by an approximately 200-foot wide area covered by colluvium, I which conceals the nature of the fault contact and breccia zone.
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- Northward, the aphyric flow of the Frenchman Springs Member is covered by a sequence of phyric and aphyric flows of the Frenchman Springs Member. This member, in turn, is overlain by the Roza, Priest Rapids, Umatilla and Pomona Members. The Umatilla Member occurs at approximately
[- elevation 2200 feet. Accounting for a slight southward dip off the Yakima Ridge anticline, a 300-foot vertical displacement is estimated on the fault in this ravine.
Based on similar stratigraphic relationships, this estimated 300-foot displacement appears to continue west-ward along the fault.
Eastward, the displacement appears to decrease rapidly.
Apparently the unfaulted Pomona Member lies along the projected trend of the fault in the SE 1/4 sec. 6.
Our field reconnaissance shows the mapping of the thick Umatilla Member by Rockwell (1979a) in a south-draining ravine in the E 1/2, sec. 1, T12N, R23E, south of the fault, appears to be in error. Within a short distance south of the fault, a 40-foot thick tuff bed is exposed in the ravine. This tuff bed, not shown on the Rockwell map (1979a), is underlain by gray, fine-to medium-grained, blocky columnar basalt, probably the Priest Rapid Member (?) . The Umatilla Member occurs north of the fault, as mapped
{ by Rockwell. However, there is no evidence that it occurs in the ravine south of the fault as it is shown on the Rockwell map. Also, an anomolous stratigraphic relationship is indicated in the mapping of the Ellensburg Formation (Tel) by Rockwell (1979a) in sec. 7, T7N, R24E. To the west, the "Tel" unit is mapped between the Elephant Mountain and Pomona Members, but the continuation of the same bed eastward is mapped within the Pomona Member. This anomolous relationship may be real or due to stratigraphic and structural mis-mapping.
{ A small fault segment was mapped by WPPSS (19-"7a) in SW 1/4 sec. 34, T13N, R23E. This fault lies on trend with the Silver Dollar fault, and is probably a continuation of it.
Based on the stratigarphic displacement observed, we interpret the Silver Dollar fault to be a scissor fault with a hinge to the east in the Pomona Basalt (sec. 1, T12N, R23E) and incres=ing displacement to the west.
The western termination of the fault was not determined.
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- 7. BADGER MOUNTAIN FAULT Badger Mountain consists of three elongate hills in T9N, R28E that
[ trend northwesterly across the area between Badger Coulee and the Richland-Prosser Highway (Figure 1) . For this discussion, these hills are named
{ SE-Hill, Mid-Hill and NW-Hill. The SE-Hill is located near the mouth of Badger Coulee and NW-Hill is located near the highway. All three hills are underlain by the Ice Harbor, Elephant Mountain, Pomona and Umatilla Members of the Saddle Mountains Basalt (WPPSS, 1974, 1977a; Rockwell, 1979a; Bond and others, 1978). They are commonly overlain by an extensive loess cover above an elevation of approximately 1000 feet and by undifferentiated loess and Touchet beds below this elevation. The basalt units crop out generally near the crest of the hills, while the flanks are mantled by a mixture of colluvium and silt. Structurally, the hills consist of three elongate, doubly-( plunging, slightly en echelon, sinuous anticlines.
The mapping of SE-Hill for WPPSS (1977a) showed an overturned fold with a possible fault along the north flank. The fault interpretation was based on: 1) the tight geometqr of the fold; 2) steep to reverse dips of the Elephant Mountain and Ice Harbor Members along the north flank; and
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- 3) an escarpment along and near the fold-axis. The mapping of the Mid-and NW-Hille, which are comparatively broader folds, did not show evidence of faulting similar to that observed in the SE-Hill (WPPSS, 1977a).
Rockwell (1979a) and Bond and others (1978) mapped a northwest-( striking fault along the north flank of all three of the Badger Mountain Hills between Badger Coulee and the highway. The mapping of the fault along the
{ north flank of the SE-Hill is in general agreement with the mapping by WPPSS (1977a). However, its northwestward extension beyond this hill (northwest of sec. 34, T9N, R28E) ~ could not be confirmed or substantiated during this reconnaissance. As mentioned earlier, the mapping of faulting in the SE-Hill is largely interpretive, based on the tight geometry of the structure, reversed dips, and an escarpment. Our reconnaissance along the fault in the Mid-and NW-Hill area did not reveal any comparable features that could be attributed to faulting. Our reconnaissance did confirm previous mapping of the Mid-and NW Hills by WPPSS (1977a). Both of these hills appear to
{ be rather broad, slightly asymetrical, doubly-plunging folds. Although the E
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F area across the trace of the projected fault is covered by colluvium and L
loess, the basalt members do not show any stratigraphic displacement across r the postulated fault. The topographic breaks on the north flank of the Mid-I Hill, described by Bond and others (1978) as due to the faulting, appear to be due to stacked and dipping f1cus. Moreover, these topographic breaks neither lie on trend nor do they form an escarpment; they lie en echelon and parallel to the ridge, and rise in elevation in an up-dip direction. i Therefore, these breaks are considered non-tectonic in origin.
The Badger Mountain fault, as mapped by Rockwell (1979a) and
{ Bond and others (1978), could not be confirmed in its entirety during this reconnaissance. The faulting appears to be confined to the SE-Hill, and the j l
geometry of the plunge suggests the fault dies out rapidly in the fold I (WPPSS, 1977a).
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- 8. BADGER CANYON FAULT The Badger Canyon fault (Rockwell, 1979a; Bond and others, 1978) was mapped across Badger Canyon, south of Badger Coulee, in sec. 29, T8N, R28E (Figure 1). As shown on sheet 11 of 12 (Rockwell, 1979a), the one-mile long, northwest-striking fault appears to cut landslide deposits in a right-lateral sense.
I L Based on our reconnaissance, the area in general, and within a 1/4-mile on either side of the fault in particular, is covered by loess and colluvium. , Mapping of the Priest Rapids, Umatilla, Pomona and Elephant Mountain Members within 1/2 mile of the fault, therefore, is highly conjectural, because few basalt outcrops occur in this area. The juxtaposition of the basalt members, as shown on the map (sheet 11, Rockwell, 1979a), is therefore highly conjectural.
In addition, our reconnaissance suggests that landslide depositt occur only on the east side of the canyon, not on both sides as shown on L sheet 11 of 12 (Rockwell, 1979a).
Thus, our reconnaissance indicates the existence of the Badger Canyon fault is highly conjectural, and that the existence of a landslide on the west side of the canyon is incorrect.
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l I 9. REFERENCES Bond, J.G. and others, 1978, Geology of the Southwest Pasco Basin, RHO-l BWI-C-25: prepared by Geoscience Research Consultants for Rockwell Hanford Operations, Richland, Washington.
W Fecht, K.R., 1978, Geology of Gable Mountain-Gable Butte area; Rockwell Operations, RHO-BWI-LD-5, Richland, Washington.
Glass, C.E., 1977, Letter report, prepared for Washington Public Power
{ Supply System.
Jones, F.O., and Deacon, R.J., 1966, Geology and tectonic history of the
' llanford area and its relation to the geology and tectonic history of the state of Washington and the active seismic zones of western Washington and western Montana: report prepared for Douglas United Nuclear, Inc.
l I
t Jones, M.G., and Landon, R.D., 1978, Geology of the Nine Canyon map area:
Rockwell Hanford Operations, RHO-BWI-LD-6, Richalnd, Washington.
Newcomb, R.C. ,1958, Ringold Formation of Pleistocerie age in type locality, the White Bluffs, Washington: Am. Jcur. of Sci. , Vol . 256,
- p. 328-340.
l I
l Newcomb, R. C. , 1965, Geology and groundwater resources of the Walla Wr.lla River Basin, Washington-Oregon: U.S. Geol. Surv. Water Supply Bull. No. 21.
l O' Leary, P:W., Friedman, J.D., and Pohn, H.A., 1976, Lineament, linear, lineation: some proposed new standards for old terms: Geol.
l Soc. Am., Bull., Vol. 87, p. 1463-1469.
I Reidel, S.P., 1978, Geology of the Saddle Movitains between Sentinel Gap and 119 30' longitude: Rockwell Hanford Operations, RHO-BWI-LD-4, Richland, Washington, j
l Rockwell Hanford Operations, 1979a, Geologic studies of the Columbia Plateau:
a status report: RHO-BWI-ST-4, prepared for U.S. Dept. of Energy.
l Rockwell Hanford Operations,1979b, Basalt Waste Isolation Project Annual Report-Fiscal Year 1979: RHO-BWI-79-100, prepared for U.S.
Dept. of Energy.
Shannon & Wilson, Inc. ,1979, Evaluation of faulting in the Warm Springs I
j Canyon area, southeast Washington: by Saleem M. Farooqui, prepared for Washington Public Power Supply System, under direction of United Engineers & Constructors, Inc.
report 1
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{ Washington Public Power Supply System (WPPSS), 1974, WNP-1/4 PSAR, Amendment A, Appendix 2D, " Geologic mapping of the Rattlesnake-Wallula alignment and associated structures", by Fugro, Inc.
Washington Public Power Supply System (WPPSS) ,1977a, WNP-1/4 PSAR, Amendmont 23, Sub-appendix 2R H, " Geologic evaluations of structures in the Columbia Plateau", by Shannon and Wilson, Inc.
Washington Public Power Supply System (WPPSS), 1977b, WNP-l/4 PSAR, Amendment 23, appendix 2R K, " Remote sensing analysis of the Columbia
{ Plateau", by Charles E. Glass.
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e Photograph (a) is just left 3' .,
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;he h d$g?- Q 3 *. 1 'N . N k , p N $ ~; "( %' @y'also be seen in Figure 3a.
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DOCU '- punur I Il A ,Oe I EOO 795089Z ! NO. OF PAGES 2 o versf 2cb yyggs REASON: O PAGE ILLEGIBLE: PDR CF C HARD COPY RLED AT: OTHER
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O BETTER COPY REQUESTED ON [ AGE TOO LARGE TO RLM. O HARD COPY RLED AT: CF h OTHER r O FILMED ON APERTURE CARD NO.398 300 72FCB 7%c of 1
[ [ s A e u A' 1000 - - 1000 [ O 8' b b d Qgf, M [ z ~ ' s ._ _f z
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{- LEGEND: Qal Alluvium Qds Stabilized dune 0 . _ _ 20,00 4000 HORIZ0 EAL SCA M IN FE U gf a o uv 1 deposits Tem Elephant Mountain Member deposits [ Tp Pomona Member WASHINGTON PUBLIC POWER SUPPLY SYSTEM NUCLEAR PROJECT NOS. 1 & 4 [ GE0 LOGIC CROSS-SECTION A-A' SHEET 1 0F 5 MAY, 1980 UE & C CONTRACT # 44013 ( SHANNON & WILSON, INC. Geotechnical Consultants FIG.9 Portland, Oregon
[ b 1000 B1 f B' t 1000 b b I D E E b e 8 5 W F z - T1. o m z L - s .Qgf l l l - z 500 - 09f - Tem * - 500 z 2 _91 _ _ 9 _ -- l __ / Qal 3
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{ g _~ _ q __ _ p _ _- g n w n w F 0 - --- - ------ 0 VERTICAL EXAGGERATION X 4 l l l l d E o 5 E e B' I y g 2000 B1 g g - 1 2000 y 5 $ c l, 5 g I I I g l C i j ; p 5 I 5 w 0-
-0 g l SEE FIG. 8 FOR LOCATION OF CROSS-SECTION I
i 1 LEGEND: I I Qal Ogf Ti Alluvium Glaciofluvial deposits Ice Harbor Member 0
~ - - -'
2000 4000 o HORIZONTAL SCALE IN FEET Tem Elephant Mountain Member deposits WASHINGTON PUBLIC POWER SUPPLY SYSTEM NUCLEAR PROJECT NOS. 1 & 4 l l l GEOLOGIC CROSS-SECTION iB -B1 ' SHEET 2 0F 5 MAY, 1980 UE & C CONTRACT # 44013 l SHANNON & WIL50li, INC. I Geotechnical Consultants Portland, Oregon FIG,9
L [ d r E L B [$ B'2 1000 - yh - 1000 b 3 g b 8 - b E I g E [ z
~
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g 500 _ . ~ . llg31 09 T ) - 500 g j 2~ j [ -? 9If ? _ f_7 /_. ..(7 w $ w b ~ ~~ V5iiTICALlXAGGERATIONX4" [ F d z I \ E e m g I l b y 2000 B2 5, 8 g B' 2
-2000$
r l z m z 5 5 \ Q 4 l\ I G d
" 0------------- --
-0 $
I d SEE FIG. 8 FOR LOCATION OF CROSS-SECTION LEGEND: l Qg(T ) Pasco gravel, Terrace 2 I I Qgf 2 Glaciofluvial deposits 0 _ 2000 4000 QTr Ringold Formation HORIZONTAL SCALE IN FEET Ti Ice Harbor Member I WASHINGTON PUBLIC POWER SUPPLY SYSTEM NUCLEAR PROJECT NOS. 1 & 4 I l GE0 LOGIC CROSS-SECTION B 2 -B,' SHEET 3 0F 5 W.Y, 1980 UE & C CONTRACT.# 44013 l SHANNON & WILSON, INC. I Geotechnical Consultants Portland, Oregon FIG,9 l
r. i
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SEE FIG. 8 FOR LOCATION OF CROSS-SEC~
\,
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l LEGEND: Qt Touchet beds Qg Pasco gravel C' Qf Alluvial fan deposits 1500 (T1 ,T 2,T ,T4) 3 Terraces developed on Qt and Qg Tp Pomona Member E
< H
[ 1000y y a m
$ 5 5 Y N p I w 500 w t i. Q Qg(T )
3 M' g(T ) 2
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-0 VERTICAUEXAGGERATI0iiT4 z w
$ g 0 2000 4000 h -
2000 m HORIZONTAL SCALE IN FEET E S s n a Y w
' 3 k WASHINGTON PUBLIC POWER SUPPLY SYSTEM
---0 k
C NUCLEAR PROJECT N05. 1 & 4 J w lon ' GEOLOGIC CROSS-SECTION C-C' l SHEET 4 of 5 MAY, 1980 UE & C CONTRACT 4 44013 SHANNON & WILSON, INC. Geotechnical Cor,sultants FIG.9 Portland, Oregon
[ [ D E D' 1000 - e $ - 1000 [- e e5 em b >- ef 88 b M $ u 5 z$ M [ 5 x_ -Qt(T4) _@ y8 @j z g 500 f 09(I3) Qg(T ) g p Tp N p'?- ] l
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$5 5
C I I i E/ l C 5 0- -0 5 3 $ w w SEE FIG. 8 FOR LOCATION OF CROSS-SECTION LEGEND: {. Qt Touchet beds 0 2000 4000 Qg Pasco gravel Tp Pomona Member HORIZONTAL SCALE IN FEET (T,T,T,T) 3 2 3 4 Terraces [ developed on Qt and Qg WASHINGTON PUBLIC POWER SUPPLY SYSTEM NUCLEAR PROJECT NOS. 1 & 4 b GE0 LOGIC CROSS-SECTION D-D' SHEET 5 0F 5 MAY, 1980 UE & C CONTRACT # 44013 [ SHANNON & WILSON, INC. Geotechnical Consultants FIG.9 Portland, Oregon
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{ SCALE 1:24000 WASHINGTON PUBLIC POWER SUPPLY SYSTEM p NUCLEAR PROJECT NOS. 1 & 4 { 0 1 l Miles LOCATION MAP - BUR 0KER FAULT 11 0 1 Kilometers MAY, 1980 UE & C CONTPACT # 44013 BASE MAP TAKEN FROM U.S.G.S. TOP 0 GRAPHIC SHANNON & WILSON, INC. ( 7.5' QUADRANGLE OF BUR 0KER Geotechnical Consultants Portland, Oregon FIG, 10
r / c-1 f L , Ei I
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)
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9
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m a) Exposure of the Buroker Fault and lithologic units in a road cut along the r Russell Creek Road. g b) Details of reverse fault juxtaposing the Palouse Formation against the Dodge Basalt. FIG. 12 I}}