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J l ENGINEERING GEOLOGY OF THE PROPOSED NUCLEAR POWER PLANT SITE ON BODEGA HEAD, SONOMA COUICY, CALIFORNIA 1
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i UNITED STATES i r DEPARTMENT OF TE INTERIOR
- . Geological Survey Washington, D. C.
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ENGINMING GEOLOGY OF TE PROPOSED NUCLEAR POWER PLANT SITE ON ,
j BOIEGA HEAD, SONOMA COUNTY, CALIFORNIA .;
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CONTENTS
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,, Abstract . . . . . .:. . . . . . . . . . . . . . . . . . . . . 1 tl.h p i Introduction . . . . . ... . . . . . ... . . .'. . . . . . .- .
. 2' Mt .
6(J Geology of reactor shaft and vicinity . . . - . . . .- . . . . .
6 a "j
.'l Granitic rock. . '
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l Weathering . . . . . . . '. . . .-. . . . . . ... .
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Faults and joints ................ 8 l I Li Strength properties . . .. . . . . . . . .; . . . . . 11.
e Pleistocene deposits . ................ 13 Fossils and age . ................ 15 1 Shaft fault . . . . . . . . . . . . . . . . . . . . . . 17 .
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, :j Ori gi n . . . . . . . . . . . . . . . . . . . . . . . 23
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- ' I l Surface ruptures west of the San Andreas fault zone . .. . 28 i
Conclusions ........................ .
.33 .i
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j Significance of the Shaft fault . . . . . . . . . . . . 33 l l Possible future faulting on Bodega Head . . . . . . . . 34-References cited . . . ... . . . . . . . . ... . . . . . . . 36.
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ILLUSTRATIONS c (Plates and fi6ures are at end of report)
Plate 1. Map showing reactor shaft, San Andreas fault zone,
- . lineaments, and localities discussed in text.
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- 2. Map showing contours on the bedrock surface, reactor shaft, Shaft fault, and exploratory trenches.
3 Map of reactor shaft showing location of faults, Joints, j and dikes.
, 4 Geologic section of the walls of reactor shaft.
Figure 1. Strike (bearing)-frequency dia6 ram of faults and joints l on valls of reactor shaft. ~
- 2. Contour dia6 ram showing faults on valls of reactor shafts.
- 3 Shaft fault on south vall of shaft, elevation -75 feet.
f l 4. Shaft fault on floor of shaft, elevation -42 feet.
5 Shaft fault in granitic rock on south vall of shaft, elevation -41 to -51 feet.
- 6. Shaft fault on south wall showing sediment lying on
,i granitic bedrock.
, 7 Shaft fault on south wall showing sand filling and
, variation in dip.
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- 8. Shaft fault in floor of shaft, elevation -20 feet, showing dip and branches.
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., 10. Shaft fault in exploratory trench 1, looking southwest.
.>+.,W N 11. Shaft fault in exploratory trench 2, looking southwest. .
- 12. Close view of the Shaft fault on elevation 25 feet level.
13 shaft fault on elevation 25 feet level.
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- Table 1. Strength measurements on granitic rocks fim the' s: . u. o . ..
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- ENGINEERING GEOLCGY OF THE PROPOSED NUCLEAR POWER PIRIT SITE ON BODEGA HEAD,.SONOMA COUNTY, CALIFORNIA
., by .
Julius Schlocker and Manuel G. Bonilla-
,fy , ABSTRACT y ,
1 This report sinnmarizes the geology of a shaft excavated for the
+
) proposed nuclear. reactor and discusses geologic features on Bodega Hsad and on Point Reyes penin'oula that relate to geologic aspects of earthquake-resistant design.
The reactor shaft exposed Pleistocene sediments overlying granitic bedrock. The sediments are as much as 43 feet thick, dip gently' south-l eastward, and consist of nonmarine, gray massive, gravelly sandy clay.
l The granitic bedrock is mostly a foliated, biotite-hornblende, quartz 1
diorite. Faults and joints are common in the granitic rock, and one !
i complex fault displaces the overlying sediments as well as the granitic j rock. The age of the latest faulting cannot be determined.
, \ .
1 .
! Faults that occurred on Point Reyes peninsula in rock similar to l that of Bodega Head as a result of the earthquake faulting that occurred d
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in 1906 indicate that if some future earthquake, in which fault displace-
. ments comparable to those that occurred on the San' Andreas fault zone in 1906, took place near Bodega Head, rupturing of near-surface granitic
- bedrock would be expected somewhere on Bodega Head.
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- m. crgkfkhtch. iwr w,%duka .DE w ?- y- 7 77 M nb6E5uewsssH&tnczw:~LMlh05.%?.k.s d alkdi,k A b- ^'O-t INTRODUCTION The Pacific Gas and Electric Company (PC42) has applied to the ,
U. S. Atomic Energy Comission for permission to construct and operate . "
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1 a nuclear-powered electricity generating plant on Bodega Head, Sonoma i
9 County, California. Questions have been raised about the potential
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i hazards to'the plant posed by its nearness to the San Andreas fault
'l i zone. The plant mi 6ht be damaged by shaking from seismic waves or by rupturing due to earthquake-produced faults that might pass through the site.
Geological and seismological aspects of these proble=s have been investigated by the Geological Survey. Some of the results have been presented in $EI Report 837 (Part I-Schlocker, Bonilla, and Clebsch; I -
PartII-Zaton,1963). The present report discusses tihe specific pointe '
brought out in TEI-837 that could be resolved only by dete.iled field study at the site itself, as well as by study of the relationship between surface ruptures resulting from the. 1906 earthquake and the San Andreas fault zone. To that extent the present report supplements TII-837 It includes a detailed geologic description of a shaft excavated for the reactor foundation. The examination of the shaft was undertaken to determing whether tectonic faults cut Pleistocene and Re' cent sediments that overlie granitic bedrock. One of the main purposes of this report is to evaluate the probability of future surface faulting at the site. Because such faults at the reactor site vould 3
d lie west of the main San Andress fault zone, data on surface ruptures
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vest of the San Andreas fault zone, particularly historical events, are pertinent in predicting future surface rupturing at the site.
., Surface rupturing that developed during the 1906 earthquake west of the San Andreas fault zone was investigated on Point Reyes Peninsula, 17 to 30 miles southeast of the site.
The report has been prepared in response to a request from
, Chairman Seab'org to Secretary Udall dated Octnber 3 Close contact with the AEC regulatory staff has been maintained in order to apprise 1
] the Commission staff of work progress as it might affe,:t studies of I
the site by other Government agencies and consultants.to the staff.
The continued cooperation of officials and employees of Pacific l
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- Gas and Electric Company and their contractor, Peter Kiewit Sons Co.,
l greatly facilitated this phase of the investigations. Their help is
'I appreciated.
The location of the shaft for the reactor foundation is shown
, on plates 1 and 2. The term " plant north" as used in this report i
refers to PG&E's plant coordinate grid and'is 32 6' vest of true
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north. The shaft is 11+0 feet in diameter. The bottom is at j approximately -73 feet (mean lower low water datum, MLLW).
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- . j A concrete collar two feet thick, about ten feet deep, and
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slightly larger in diameter than the shaft proper was first con-structed. The elevation of the top of the collar ranges from +0 75 to +3.88 feet. A bulldozer and a loader excavated the shaft. The
/:, a granitic rock below the weathered zone vas loosened by blasting.
l ~ j. . The excavated material was removed from the shaft by a clamshell
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' bucket working from outside the collar. Horizontal ring beams, generally spaced 4 to 5 feet apart vertically, were used for vall support. Gunite placed on heavy vire mesh was used to prevent ~j
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spalling and aloughing of the vall. A 48-foot sector of the vall l on the south side is supported by. sheet piling to about elevation t
-20 feet. l I Geology of the vall of the reactor shaft was mapped during the actual excavation because the vall was generally covered I shortly after it was exposed. In the vicinity of the plant south line, poorly consolidated vet sands had to be ' supported immediately I
after excavation; consequently structural features of the sediments were not seen in these areas.
' The site is adjacent to Campbell Cove on Bodega Head (pl.1 i
and2). Details of its topographic setting and a summary of previous Beologic investigations are given in TEI-837 BodeEa Head is a :
granitic body that lies vest of the San Andreas fault. The granitic rocks are partly covered by Pleistocene unconsolidated marine j l
sediments and partly by such continental deposits as slope debris, j l
vind-blevn sand, lake deposits, and alluvium. i 1
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The power plant site 10,on a buried. valley system that was
. eroded in granitic rock by a surface" stream and its tributaries, when sealevelwasrelativelylower(pl.2). The valley was subsequently
, filled with marine and nonmarine deposits. The main buried valley
.l crosses Bodega Head in a more or less east-west direction. At its ,
1 deepest point on t,he east side of the Head at Campbell Cove (pl. 2)
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' it is more than 80 feet below' sea level (reported in TEI-837 as more 1
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' ' than 60 feet below sea level as based on Dames and. Moore map of f contours on granitic rock surface).
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e wdnu. .:axechs en:.-Ams.n wMi5E.uc&hbdun;ssamEm.wm.cuma%dein a u:rmb= ' -- L GEOLOGY OF THE REACTOR SHAFT AND VICINITY e
The center of the reactor shaft lies about 325 feet north of the northeast-trending axis of the main buried valley and on the northeast :
flank of a southeast-trending tributary (pl. 3). Granitic rock is exposed at the collar on the north side of the shaft at an elevation i
l of +5 feet (MLLW), but in the southeast quadrant unconsolidated i
j deposits extend to elevation -41 feet. In the southwest quadrant of
, the shaft the irregular surface on the granitic rock is et an elevation' i
slidh tly deeper then -35 feet and slopes gently southwestward. Farther i southwest, ner. the shaft m'.11 the buried s>:rface of the 3rnnitic rock ;
rises on a southeastward-trending spur whose exis lies chout 200 feet j southwest of the center of the shaft. .
Sedimento in the shaft reach a maximum thickneoc of about 43 feet ,
'! in a sa_rll buried valley cut in granitic rock on the southeastern vall (st vertical control line 32, pl. 4; also see pl. 2). Northward the sedimenta thin toward the granitic rock spur, but vestward they lie on a slight rise in the bedrock .ind then thigken to about 41 feet on ;
tha southver.t vall of the shaft.
Plate 4, a r.ap of the reactor shaft vall, shovs the great irregu-larity of the btried granitic rock surface. Note the overhang between l 1 l
vertical control lines 1 and 7 Thy nearly horizontal surface on the.
granitic rock at elevation of -29 feet over part of this well area and l near vertical control line 28 suggests that it is a remnant of an old s .
J vave-cut nearsbore terrace. A narrow terrace at about -20 feet is 1 '
also indicated by the profile. ,,
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l l The large rock masses resting on a clay bed above the bedrock surface between vertical control lines 23 and 25 may represent an ancient landslide.
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. The predominant granitic rock in the shaft is a foliated,
. coarse-grained, biotite-hornblende quartz diorite. Dark constitu-
' 'ents,mostlyi>1otite,mak'eupIdto30percentoftherepresentative .
, quartz diorite. A few pieces of granitic rock as much as 10 inches in diameter contain both foliated dark-gray biotite-hornblende quartz ;
diorite and a light-gray to pink, unfoliated, coarse-grained, j hornblende-biotite quartz monzonite. The two types are separated by
. a short but unfaulted, irregular to straight, intrusive contact. A !
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dike of unfoliated, fine- to medium-grained biotite-horr.blende
!" leucodiorite (light gray, little quartz, no potassium feldspar, An43 plagioclase) was exposed in several places on the final floor of the shaft (pl. 3). Where seen, it followed the south side of a 2- to 6-inch-thick zone of gouge and cylonite. Pegmatite dikes are common in the quartz diorite of the shaft. Foliation in the quartz diorite is fairly uniform in the valls and floor of the shaft and
.J strikes N. 100 to 200 E., and has a vertical or steep eastvard dip (pl. 3). Additional information on granitic rocks of Bodega Head is given in TEI-837 a
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1 Weathering P
A zone at the top of the granitic rock is gederally weathered to a brown color. The zone is about 8 to 18 feet thick where exposed in the shaft (pl. 4). .It is thinnest on the flanks of the bedrock i
spur and probably is as much as 30 feet thick at the top of the spur.
] The bottom of, the zone is generally controlled by gouge and breccia zones and nay follow a steeply dipping shear zone 10 feet or more below the general bottom of the zone of brown weathering. In some 4
j places the granitic rock near its buried surface is anomalously gray in color, though the rock is highly altered. ,
Faults and joints i
Faults and joints are abundant in the granitic rock exposed 1
during excavation of the shaft. The number and orientation of faults ,
and joints in the shaft between elevations -66 and -73 feet are more or less typical of the granitic rocks exposed at all levels in the wall of the shaft. Where faults and joints are closely spaced, only the preferred orientation is indicated. Most faults are marked by plastic clay gouge (pulverized and chemically altered rock) 1/8 inch to 2 inches in thickness. Some faults are marked by a plastic gouge zone nearly 1 foot in thickness. Breccia (brokenrock)zonesare also common along faults; the pieces in such zones are co=monly streamlined slivers elongated parallel to the fault walls. Mylonite '
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, (pulverized and streaked out, but firm rock) is relatively rare. ,
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j more than 20 feet wide. The shape-of the shaft in the northwest and' 1
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~. north part of the well between -37 and -51 feet was controlled only- J 01th difficulty due to excessive overbreak from blasting. Those 3
9
.t areas occur in ' vide zones of crushed, sheared, and chemically altered
.t';**',
[ rock.
Another way of describing the. abundance of faults and joints in
- % .il .. ... ...
... ' ~tic rocks is to give the size of block s bounded by these the grani - . . . _ . . . . . .
!. ~
1 fractures. . The range in size of the blocks from place to' place on :
I 4l the wall and bottom of the shaft is great, but generally the blocks I
are 0.5. to 1 foot across; the maximum diameter is 6 feet. Within some parts of the shear zones most of the blocks are less than 0.1
. , , , foot.
.1 Shearing 'is also evident from microscope avandnation of thin-r.
sections of granitic rock from the shaft. Many microscopic shears cut the quartz and feldspar crystals and are in turn filled with-quartz or feldspar. )
The orientation of faults and joints in the granitic rock exposed-on the shaft wall is shown on plate 4 and in figures 1 and 2. Figure i
J l shows the percentage of faults and joints having various strikes' !
l4, ,
e (bearings) grouped by 10 degree arcs. That is, all faults and joints whose strike is within the range N. 200 to 30 W. were considered as
, .l one group. One of the diagrams on figure 1 shows the ' distribution of 1,120 measurements made of the strike of faults and' joints at all' 2 '- levels in the shaft.' Thus if a fault or joint persists from one le. vel ' .
v.
9 1 ,
J
'.,7, s
Q O E---u M 49K60E9_5E9R W F,a ._
5 ?_G w3 ,,o@ m'> ns.,#-z
< t 9p.;9. . : gg..g,;,
- p. .yng
. 1. 2, ,
.,....,7, s..- r. .. , , .. ,,. ;. , w. .
wgw Jw.M a wm:rvad,da.c I E d u ,c M E N P
., U
# WA Um aa L: uhmWH;. . _. --
1.1' ' 1 --
.;I
.~ ~
I.. . . .,' .
.- .. 7 n.O . ..-
.,. e ,.
~
~
t'o a lower level'its orientation was measured at each level. Vse of ~
.,r.epeated measurements on'.the sabe feature at several levels in figur$s' -
, .l'and 2 tends.to weight the. data in the direction of. persistent,; con-- -
.'co tinuous' features.; Another diagram on figure l'shows strike-frequency.
j' 4 9 .
. . ., f .
7 of,only the faults included in"the 1,120 measurements used-in the other Ecth diagrams abow that the predominant . strike of.'fahlta i$tud 4 c>
- [^ .
. diagram.
h.- , joints is in a.narrov zone 10 degre'es on eithei side of east-west and . . i' , . . .
~
i - 'that the least-favored strike is between north .and'N.100 W. . The - 1 The '
. second mast-1'avered[ strike is 'between N.1700 V. and N. 800 W.
i averaBe dip of all the fa' ult and joint measurements is 63 degrees. . . t
- . Figure 2 shows both dip and strike 'of the faults in ti:e form of
~
c a contour map of the concentration of poles to the fa61ts. A' pole is
~
./
' a line drawn perpendic.ular 'to a fault plane. It confirms what is shown in figure 1 and,'in addition,.shows that the predominant' dip i i direction of the vest-trending faults is 500 to 75 S. , but .the general range is 650 N. to 450 S. Many fault surfaces seen in the-vall bend in open curves through large angles. Slickensides or striations caused by
~ - relative =ovement on fault surfaces are ec=non and generally plunge at
.large angles thou6h on some faults they plun6e at low-an61es or are a
nearly horizontal.
.L
.i -
3 l
- e . .
. .[
];, .
1
)
i 10 ~
"r - .
'J. l i
'1, P, K.
i s'Y',i. e . . .f . .. q 6 At . . . . ',., $ * .. , 49 W 8 'a ,. *
+ "'~ ~ ""- '
' ;knidi1EiliGLOCI.~l.14Z'E~
"" .uC' T~ ' J ~~~L'
- ~'"N '
i ny:c .s . 1
.1
-! i, i
j , Strength properties ; I
'. The values for the ultimate unconfined compressive strength of j t
the granitic rock from the shaft are given in table 1. They show a i
, range from 1,037 to 16,800 pounds per square inch The strength values r,
l determined by the Geological. Survey were made on core taken from a
~
; 10 x 10 x 14-inch piece of bEock, typical of the fresh. unsheared
} rock in the, shaft. It is a foliated, coarse-grained, biotite-hornblende
~ ' ~ ~ ~
-I' quart'z'diorit.e t'hEt i:onsairisInfoEt'iO percent biotite and hornblende. ~~ ;
i The granitic rock core from borehole 14 is described by Dames j and Moore (1962, pl. AlC) as follows: " White and black quartz diorite (severely jointed into mod. fresh blocks up to 3") with numerous small l
*< 1 l
shearzones(jointsandshearzonesalteredtoclay)". The same descriptionisgiven(DamesandMoore,.1962,pl.AlD)forcore'from 3' ~ borehole 16, with the following addition in the zone in which the 2 deeper of the 3 tested cores were taken: "(grading into harder and l i fresh blocks up to 8") (little or no alteration in joints) (few shear I l zones)". 1. t 5 I
.t
*q
'a I
r, y
)'
. 2 .,,
e
..,,1
. .- f ,
f r.). l ,
\
k s.. 11 1 i -. . . . . . _ _ . . _ . _ . . . . . . . . . . _ . . ., 1 i
'Mf .J$..m%.m.V<sMn%r?
m h _m - . m .__tM dpn_:n.W_.8_?,t_ sn>W:. 4 @ d igd _._., __ .. __ .x : Q ?,p ,;mn)c6.gp &._g m sju.Z_5EG?
.__. .. _ _~ Q 5_
1 a
-,- % i ._ , .._.,,-a.... -. i
- m. . .rm. a. w .. _i., .w . . . ,, . .L.. nc Ja .- ' ' * * *d . , . , . . - - ..v.~.-
. -. ~~ = l ' in -u : =W . -
1
- l l
i i d 1 Table 1.--Strength measurements on granitic rocks from the shaft, Bedega Head reactor site, Sonoma County, California. I l i Sample location Ultimate, unconfined Analyst and. remarks compressive strength,. I pounds per square inch , , 4 i l j Core-borehole 14(pl.2): Dames and Moore (1962, pl. AlC); 10 feet " below bedrock surfac'e 2,108 NX-size (2-1/8 l 31 1,861 inch in diameter) l 34 2,k48 core pieces 2 74 to 3 25 inches in length. 1 Core - bore hole 16: '~ Dames and Moore (1962,pl.AlD); j 16 feet " below bedrock surface 1,037 XX-size core *
; 23 -
3,673 pieces 2 5 to 26 " *" " " ' 3,953 3 4 inches in . length. ' 1 l F.ock - at vall, northeast side U. S. Geological of shaft near vertical control Survey, Denver, line 21, elev. -31 feet. Colorado Laboratory Approx 1=ctely 27 feet belov NX-size cores, k.3 bedrock surface; 15 feet below inches in length. brown weathering zone. I Perpendicular to foliation 16,800
! Parallel" "
10,000 12,800
! but perpendicular to last core 1 .
i
' .[
\ .
l . i i 0 1 ; i I 1-1 ,:yI... -
'. b l* YD%%d Ca i + Ot&d%%? '
~ %T. a 2 s2L Wh W- RLY L*L"-%im m
- d&'"'*- " " ' * ' * - ^ I -
$~j5&$iSi&%'46.2G,;51C&" M YEt~'r' y r R ;. _ - + y - - , . , . - .. ,,
*+,, y ,
f),W 7 ., l. I Pleistocene _ deposits. 1 The predominant sedimentary materir1 overlying the, granitic rock It is in the shaft area is a maseive g, ray,x grr?/elly, sandy clay. c, thickest in the southwestern part of the shaft, reaching a maximum of 32 feet ir.cluding a few thin beds of other lithologic types on the
.s.Y .
i 2, . perimeter of the shaft at the plant vest Idne (pl. 2). The gravd in - i thu sandy clay consists of. granitic rock fragments. In plaue; the 1
;,1., - -
1 amount c.f granitic fragments increases ...;_. in the clay forming a g7adaticnal , , _ ,
;.J contact rith tbo underlying granitic rock. This evidence suggests the i a
4 t sediment formed in place. Rounded detritd wood f.iagments, bwever, ; indicate that some movement occurred prfor to deposition. fhe gravel 4 in the ss.ndy clay varies in size and amount. In most placea gran21es . 1 _1 , 4.}t By .
- 2 ,t o 4 sa in diameter make sp about 5 to lo percent' of the sediment
, 4.,o
-i In some placts a sandy clay layer one inch to one foot thick and- 1 1
containing pethic.s as large as 3 inches instaaeter occurs within ]
'-j *l I,
themassive$ediment. The gravelly, sank clay is mottled brown and. - y gray in many p'. aces alorig th? vestern and southwestern vall of the 4 1 p i shaft. Mottling is especie.lly ec.mopin the southwest sector cf the , 7 , . . s l l shaft vall. It t,
..b , --
j
'y. .
Southwal*1 fra about the cbter of the shaft <the nonmarine, gravelly, _( , 3 , f eendy clay fe'interbedded with layers of sands and c1Ays, O to 1 foot
' ' ~,1 -
iri t.hickness, probably of marico origin. The interbe&Nng probably e
'-;n: .
resulted from north-south shoreline oscillations.* Above about ekvatic.h
'V .,'
g.
-20 near vertical control line 34,.the sediments consist of' gray and
- N
.e ( j kh '
yeasvish-orange sand, pt,de.bly of beach or near-shore marine origin. -' ' ( [
* ~
k
-/q a h 9 '
, y , ,
S- , fy 5 j p s f 1 7" (6 ,. 13 t t .5 % l'
.b.* ,
,e 3' i .,
1
,-.7 -- + . . , _ _ , , , , , , , , , , , , ,,
n' 's \'( .' "
)- - <
'(
i, i j g
, . . .-o i i k
* , .(gg, wY ,, Q.* g b.'. 5 ,f ffsj Y.@ ftf5h *'f , 5 -% f f ;;;g g g, y
a .- , .w . n , g- m ., 4. e . . ..y,,... . . , . . . , _ . _ . . . . , . . , , , . . ,
~ - . . mte wwax.w .vu,.h.;.xL wmwLL9MV'huid14:& waam,ma =.u O Ph Lk *
'f I
9 The sand appears to thicken south of the reactor shaft toward the axis , of the main buried valley. The sand lies unconformable on the older - sediments. i I The variations an characteristics of the sediments are well . I J illustrated in the valls of the shaft. As would be expected in deposits l
.; such as these, details of the sedimentary sequence are complex. Before u
l deposition of the ss.nd at the top of the shaft, channels were cut into the nonmarine gray, gravelly, sandy-clay and later filled with clayey mand (pl. 4). The north side of the cut channel is shown between '1 vertical control lines 27 and 29 Alaterchannelwascut(see verticalcontrollinesP9and40pl.2)andfilledwithunconsolidated, fairly clean sand. Part of this; sand is gray and part is dark yellowish-1 j
- orange. The two color varieties are almost everywhere separated by a 1
i black or dark brown zone of sand that is rich in oxides of' iron. At t- . places these ironstone bands follow the surface of.. fossil tree limbs. The fossil wood appears to occur only in the gray sand. Though fossil wood is abundant in the other sediments, it was not seen in dark' yellowish-orange sediments.
, Sands and clayey sands in the shaft generally contain, in addition t
t to a large proportioh of sand grains of granitic origin, rounded sand grains of red chert and greenstone presumed to have been derived from
; the Franciscan Formation. This formation is. exposed in the Bodega 4
Head' region only on the east side of.the San Andreas fault zone and 3 sand from it was probably moved across the fault by ocean currents.
- . s V
j i '
; 14 It ..
1 , i, ' j. , 5 1 _E[X.'ddf$QW32$$yn{CnD.1%hrQya2G.::.EAWMFct2,d'.2,4%di.2d@yM@
,7% Q (j 2 *T:, -CC ...@u:.2.- ,*~.T rt;q.*. *ih .22*.x"~~&s 7 *.77~~ 'w" . - nww,w=we 1
~ ~ - ' ~ r :v+-~m,mwamu._
s . . . .nw%- i
.e '
%s .1
... )
1, .
.p .
j , Bedding is discernible in most parts of the sedimentary section other than in the gray,' gravelly, sandy clay and in parts of the thick j send deposits. Bedding in sands is marked in places by 1 to 2' mm-thick layers of black heavy minertis or by a change in average grain size. j 3q y In many places, color banding in orange, brown, and gray, is parallel to bedding, though color banding in many other places lies at steep
]4 y angles to the bedding. Alternating beds,1/8 to 2 inches in thickness, 1
1 are especially abundant on the south side..of the shaft. Beds in the - j 1 reactor shaft are generally flat lying or dip gently eastward or southward. Rarely does a thin bed or group of beds dip northward i or westward. t -
-5 4
Fossils and aBe Fossil wood is abundant in the' sediments. Limbs 4 to 6 inches I 1
- l
. in diameter are commonly seen. Fieces1/4to2incheslongareabundant. (
l
' A tree about 2 feet in diameter and more than 10 feet long was found in :)
I 4 the northeast quadrant of the' shaft at about elevation 5 feet. l 1
. Cones,' frdit, seeds, and needles of the following species vere 1 4
l found in sediments near the shaft between elevations 5 and 21 feet and
'a a
identified by Jack A. Wolfe, U. S. Geological Survey (written communication,
.f.
4 December 4,1963). i l '?l
- 1
; 3
, 'm '
j
,a ,
9 I (
..c4 1 s. ,m ;
'.. J C j m,$!ikqpen w g F W W+ m & M'U p w K p<.e .n~.;e,.w.m m W n wpareme.m T
"~
_NE I_^ I_7~_N Y _ _ __
' ~
Y g
- r b p, ,
' ~ =w:.w=&nvnnwa-m.Ma$cigggf[. .
j;'"[';'((g
- ~~- . -
Monterey pine (Pinus radiata) Bishoppine(Pinusmuricata) Sitka spruce (Picea sitchensis) ,.
,' Westernvaxmyrtly(Myricacalifornica) l Red elderberry (Sambucus callicarpa)
J l Manzanita (Arctostaphylossp.) l l Bedstrav(Galiumsp.) Wolfe also states that the flora here is similar in composition to the Pleistocene flora from the northeast shores of Tomales Bay (pl.1) and suggests that their floristic similarities indicate that the beds in which both floras are found were deposited at about the same time and - under the environment of the closed-cone pine forest.
' The exact age of both the beds at Tomales Bay and Bodega Head is '
i not certain. A radiocarbon date of greater than 42,000 years was * . obtained from 3 fossil veed samples obtained 102 feet S. To o W. from - the center of the shaft at elevation 49 feet, 197 feet N. 320 W. of the cent.cr at elevation 55 feet, and 240 feet N. 35 W. of the center at elevation 77 feet.N Thus, the sediments in and near the shaft between elevations 5 and 21 feet are considered to be Pleistocene in age. i i
- O The age of these samples was reported in TEI-837 as greater than
- 38,000 years. This preliminary age determination was later refined to greater than 42,000 years (Meyer Rubin, U. S. Geological Survey, written communication, August 8, 1963). ',
-)
=l
'I
-l b
l 16 , l I I d.
.+ , ). .
s ??E&AO]']kbM5)-f$$tf;> j;j,5j- Q
,;;.3
. 3 ,
x
l
'I
$ h'Y S 5'h"+ N A d 5 M S A USA '~ - E a L.w.Z4idhL:n i M fLyw_. .. :- :a'; . . a --g
.)
. Q..d .. .
..
- 1
- k. . -i l
, 1 Shaft fault The Shaft fault is the major structure in the reactor shaft area and in this report is named for the fault' complex that has been traced i
*L frost the' Pleistocene sediments near vertical control line 39, at the l %. ' ,
@ approximate elevation of -12 5 feet, downward into the granitic rock '
]
, a- '
near vertical control lines 40 and 41 to the bottom of the shaft (pl. 2). i l [I Southwestoftheshaftthefaultisexposedinexploratoiytrenches1
~ ~ M2 dtii!ITn~ Pleistocene sediments-(pl. 2). - -
~
l i ' J The Shaft fault in the granitic bedrock is a well-developed con- il o l spicuouszoneoffaults2to10feetwide(pl.2and4). Individual
- l faults within the zone have various characteristics. Some are tight, l l f paper-thin, clean fractures in fresh rock; others are wedges 1 td 2 1 feet vide, and elongated for as much as 5 feet along the dip or strike.
rn . . .
.. Some of the wedges are composed of brecciated slivers of hard granitic
.; rock whe-eas others are composed of soft, clay gcuge zones. A zone l
i of plastic gouge in the fault at elevation -67 feet at vertical i
' controlling 40isnearly1footinthickness(fig.3). Individual
~
' faults b$abch and ' bend, within' the* zone, but most can be fonoved for tens of feet. The fault zone is a complex array of intersecting Q)ij t em=11ar faults, but elsewhere only a few strong subparallel ruptures can be seen and the rock between them is relatively unbroken.
}'E sa
! .e The well-developed fault zone on the south wall near elevation >
. .e
, Ii c; .
i -55.(fig.5)consistsofnumeroussubparallelfaults. on the north-
. i.t
.[ % east vall, however, the fault zone is not as well developed. At the c w . -
floor (elevation -73) and for about 7: feet above, the zone consists
,/.
n
# of two faults separated by about 2 feet of fairly intact rock.
- ---~--- _.
i _.._ 17.,, . . a e a:k(, 1 , f?! w , y . ,??@Z M:% n K g gpts.n Q . n p; Qi.pt n g m m,_.;.
.Q.;y.u.;
4 ,,, ,, .w.99ge,p; y
,p q q p g.gs p o. g ;w g,y,x x py g ;g Q
, n a; m.m.4p.wanug
a- - - .
- . , - . . . - ,. . . . . %:,,. a. . ~ . .: =. _ a. .: t
.. n.w.. .
~
"mk.r.:w:n a ,c.:-w_ru.s.:~.~r~..ne. .csg.u;.&h;p v.e Q % M .h & 6 w.g,a Q ,,,393 g.gy_
At this locality each fault is a gouge and breccia zone 1 to 2 inches vids. From elevation -55 to -51 the fault zone is a foot vide and made up of gougs and breccia. Between elevation -41 to -46, the fault. vas ,. l tracedfromthesouthvalltothenortheastvall(pl.3andfig.4). i l At this elevation the fault is 2 to 12 inches wide and consists of
'}
i several intersecting and branching faults separated locally by breccia. Near elevation -24 between vertical control lines 25 and 26 the fault splays out into several branches about 5 feet below the top of the f granitic rock (pl. 4). No rupture was seen in the overlying gravelly sandy clay. The Shaft fault strikes N. 400 E. and dips 650 to 800 W. Slichensides on individual faults of the zone range from vertical to horizontal, but i
! most are steep, indicating a dip-slip component of movement. ,
I
,' Field evidence for horizontal (also called lateral, or strike-slip) movement is seen on the floor of the shaft at final grade. The evidence '
is conflicting with respect to direction of horizontal movement. A steeply dipping pegmatite dike that is aligned at a high angle to the Shaft fault appears to have been dragged northeastward along the Shaft fault for 11 feet (pl. 3). If the isolated pegmatite shown in plate 3 east of the fault is the same dike, it indicates left lateral movement i of the Shaft fault in the granitic rock of about 37 feet. A steeply dipping leucodiorite dike is also offset by the Shaft fault proper I and two vest branches of it (pl. 3). Direction of offset of this dike also suggests horizontal movement of the Shaft fault, but of a right ' d . lateral nature. We believe the field evidence for right-lateral movement .; 4 f i 18 l i y 1 . It [ { '9dsa m . . . .* ., 5.,p d,r.4:.b d.Q Q g - y,, . , . , , .
r/ .nMahat ado..'4 jua' Sea J .ars* * ' -- .shf;/Mw.w.'a mu k s' - ' -
- ann- 2 ,ie h -^ - " - ' - - I.A:
.x. .
i, . . I suB6ested by the offsetting of the leucodiorite dike is somewhat more l t; i reliable than that for left-lateral movement 61ven by the pegmatite dike.
; . The Shs.ft fault intersects the Granitic rock surface on the south l i l sideoftheshaftatelevation-35 feet (fig.6). At this locality the '
j sediments-granitic rock contact appears to be offset about 1-foot dorn-s
] vard on the vest but field relations do not clearly establ$ sh this
.] relation. At several temporary positions of the floor of the shaft )
,n !
-j (about -35 to -40 feet), as shown on plate 3, the direct connection j between the Shaft fault in sediment and in Sranitic rock is well I l
l established. The fault is the contact between the two rock types. It dips 820 W. and was followed by hand trenching into the underlying Sranitic rock. The Shaft fault in the overlying sediment is easily traced from the surface to about elevation -26 feet. It is nearly vertical about 10 i 2 feet above the granitic rock but at a point within about 8 inches of I the Branitic rock surface it is distributed a=ong several thin clay 1 gouge zenes, the most prominent of which bend to the west, parallel to t the rock surface and about 1 to 3 inches above it. One small gouse is vertical and appears to join a gouge zone in the rock.
} The geolo61c map of the reactor shaft vall, plate 4, shows the dip of the Shaft fault at various levels. Above elevation -28 feet .
, the Shaft fault complex dips steeply eastward; below this level it j
! l dips mostly vestward. In the granitic rock it dips vestward. From
.L..' .
- .t
-28 feet to -26 feet the Shaft fault is 1 to 2 inches wide and is filled
; , with gray, medium- to coarse-grained, clayey sand and with pieces of 19 i
t I f'
.e' t
- h .
pger e . , I
'k b95
- h * '}-
- 4" d e*
sw .ny~,. :r & n.;ys.zy+yu&+ gy.s m w wy+poygeg' I . f $
- g. ~ ,. . . rmy:nym;p%
- . . . . . . . . ~ . . . . . ..t..-..;m.....-.-,..: .s. ,. .. .a .,. - ~. , ,c, ,s a c.;. .c e ci.
.y p ,1 .
p ah -eg.w y * =,. g.g . jegwp.; ~y, , a j pjp,, .. j [n; .hg 3,[g h.e .k .. ;,, , . ,. ~.
. ,.7 g .E, . ..g q.
^
,,.g hj.y .,, .3,.3 . .
' the sediment from the valls, gravelly, sandy clay (fig. 7). Between ~
-26 and -23 it passed through in a massive, dark gray, gravelly, sandy ,
~i clay of higher clay content than the underlying unit and could not be ~
4 seen. When the floor of the shaft at various levels was still in l similar sediments, it was impossible to trace the fault across a horizontal surface (pl. 3).
.( l l From elevation -23 to about -12 5 feet the fault cuts a well- l I
i bedded section. Near the perineter at the south it appears either as a thin, clean break, or as a fracture about 1 to 2 m:n vide, filled . 1 with sand or clay. About 15 feet to the northeast and elsewhere it l l forked into 2 branches that vere separated about 1 foot (fig. 8). {
, In some places the main branch ended and the other continued. In
\ '
other places branches recombined to form a single break. The sediment ' j between branches did not appear to be greatly disturbed. The line of I the fault was either a sharp, clean break or a break with valls 5 to 15 mm apart and filled with sand or clay. , i Beds at about elevation -16 feet appear in cross section to be { I folded into a menocline. The Shaf t, fault complex cuts tP s fold. ' Beds are 2 feet lower vest of the fold and fault. The continuity of the Shaft fault from the south wall was established by cleaning off j the bottom of the shaft with a strong jet of air along the fault at I 4 elevation -41 to -46 feet. The fault was followed to the northeast vall. Gunite panels vere removed at higher elevations in order to l examine the" fault in the vall. 1 q 4 i 20 s' g, z . . . . .
. . mm :..~ amm ~ - x - .mu
+ ~
' @% 5.% @ 4,M M a L :d:rz.1 d kE E G L:.2 ki!.k C M d % E ; ^ J u u k :- - n
- 4 = * " z'
.gb . .
.e ,
l The amount of vertical separation of beds on the two sides of the
, fault varies from place to place on the south wall, though it is every-I. where down on the vest side, except along two minor faults near eleva-
.> tion -12 feet. From the granitic rock surface to about elevation -29
$. . feet, some uncertainty in matching beds was encountered. The apparent Y_ . vertical offset of the basal two feet of sediments may be about one foot.
j' From about elevation -32 to -29 feet, the vertical sepe. ration may be as g -
- -much as 19-inches. . From about e.levatioL-29 'to -26. feet, it may be only about 6 inches. Vertical separation at. elevation -20 feet is about one I
i foot. Above elevation -19 feet several lines of rupture ran out. The middle line shows the greatest well-established vertical separation, j 14 inches (fig.9). The easternmost fault is marked by a one-quarter inch thick plastic clay gouge that follows beds and also breaks across beds (pl. 4). Ruptures can be followed to about elevation -12 feet,.
- t. )
~
j Beds here show a vertical separation of two inches across the western-most fault. Above elevation +10 the concrete collar r.akes up the vall of the shaft. Conditions of observation in the collar trench in the
, vicinity of the Shaft fault were poor. This work was done after dark i
by' flashlight before adequate lighting had been installed;
-g Exploratory trench 1 vas made to intersect the Shaft fault so as
- l; c
/ -
to permit examination above its highest level in the shaft. Plates 2 and 3 show faults in Pleistocene sediments southwest.of the. shaft. a
;# Two faults were found in the , trench at elevation -16 feet that are j
.. a .
- N believed to be an extension of two in the shaft vall.. They dip eastward e .,
. [f. / . and show vertical offsets of about 1/2 inch, down on the east. .They 4 could not be seen above about elevation -16 feet. Another fault was t j
~
. ,.. l
.. . ., , 4 h l . - ~ . - . . . .
,$1 f rE '
nob $$YM'$bb [NbI.[NbU'((L.I 9# '#"N N'4 /D#[b"'Y N" @bN# hbh
,p y ...,.,e sA ,, ..*- *
,s - , m. .->4 7 7 -- vp~
- A*s . J y . - typ E ' * .e p t e ,%-*fmap M ;*j (--*
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found about 9 feet to the east. It dips 70 to 850 eastward, strikes
., i N.'350 E. to N. 420 E. and shows a vertical separation of about 1.8 )
inches,downonvest(fig.10). A fault believed to be this one (see f I j plates 2 and 3) was found in an embankment to the southwest. It was 1 . . i traced upward to the elevation +25 feet and followed by bulldozer j
\ l across this level to the asphalt ' drain at the base of the' embankmant ]i below the elevation 55 feet bench. It was well developed where last t
l seen near the asphalt drain 170 feet southwest of the shaft... Exploratory trench 2 van dug in an effort to intersect the Shaft l t . I
.i fault branch seen in the south wall of the~ shaft at elevation -12 feet. ;
It could not be found. Trench 2 also crossed the Shaft fault branch found at elevation +25 feet. In the trench its strike is N. 240 E., dip 83o E. The amount and direction of movement could not be determined 1 1 , I (fig.11). On the +25-foot level the fault appears mostly as a black , f 1
~
band of discoloration,1/8 to 1 inch vide in pale brown sand (fig.12). It splits and reconnects creating lens shaped areas a few inches l l wide (fig.13). Exploratory trench 3 was dug on $he elevation 55 feet bench in an 1 4 effort to follow continuation of the fault at the elevation 25 feet i level. It reached to about elevation 51 feet. No faults were seen in
. 1 a .
the well-developed sand beds in the trench. I An unsuccessful search was made for a possible continuation of the Shaft fault northeast of the shaft. A bulldozer and hand scrapers were i . used for this purpose. Embankments northeast. of the shaft were' scraped
.]
L.
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., clean (fig.13). ;
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.I The She.ft feult is the only structure at the proposed power
;i . -
plant site that transects both the younger sediments and the under-
.I i
.lyin6 older granitic rock. Moreover, the origin of this fault is ]
fa fundamentally important in any evaluation of its significance to
, site acceptability and plant desi6n. The three mechanisms that have en been considered as contributing 'to the ' origin of the Shaft fault are (1) tectonic faulting, (2).. ... lands , . .._11 .. .ding,
_ , ,.and (3) sub'sidence from'~ - compaction'of the sediments. I l Tectenic' faulting is used in this report for the rupturing of l
)
. rocks caused by crustal stresses of deep-seated to shallow origin l l l
l l sach as those..that produced the 1906 earthquake. The hypothesis l l that', the Shnft fault in the granitic rocks was formed by tectonic j
,'. faulting'io supported by the horizontal' displace =ent evidenced in j
the dike rocks. Although the field evidence is conflLctin8 with respect to direction of horizontal movement on the Shaft fault, the i
~
zone is Eeners.lly vide and consists of many intersection 6 faults separated ' locally by breccia and gouge, features that vere formed during repeated movement along this zone of weakness. The stron8est evidence supports a right lateral' movement a minimum of 2} feet; the j amount of vertical displacement is unknown.
. ~]
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The extension of the Shaft fault into the overlying Pleistocene u sediments indicates that .the displacements measured' in the sediments . i
~~
along this fault are also the result of tectonic activity.'. In'the. sedimentsi-a maximum vertical separation of lk inches was measured - across the Shaft fault. ~The amount of horizontal movement in the [ sediments was.not measured in the field though the many changes in. i dip of the fault in the sediments as seen in the south wall'of .the 1 da~f(particularly the rightainP4 bends of the easternmost and -e I highest branch (see pl. 4), suggest the reement on the: fault had a - strong horizontal component. 'The differences'in thickness of beds and1 inability to match beds across the Shaft fault, as seen in the routh j vall of the shaft, is evidence that strike-slip faulting has ' occurred. The amount of strike-slip displacement of.the sediments is satinated .. I to be about 13 feet. Thie value is required to produce the vertical .' separation of 14 inches measured across the fault that displaces through horizontal shear movement beds that. dip 50.' At the site the
~
Pleistocene beds generally dip southward and/or eastward at angles'.as, high as 100 thou6h the average dip is about 50 s. The horizontal-i displacement on the Shaft fault in the sediments is right lateral,
' the same relative movement as indicated by the offset on the
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e leucodiorite dike on the floor of the shaft. -l
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s ; i j- j 1 i i The scarcity of more or less horizontal slickensides and the i I
.j . abundance of those that plunge steeply along the Shaft fault both ,
.]
- . 1 I in the granitic rock and in the Pleistocene. sediments, suggest that I
.i i 1
j the last' movement was predominantly vertical. ~Slickensides, however,' I J i can form by-very = mil movements, particularly in soft gouge or soft ]
-J l
.sedinients, .so that the vertical slickensides may not reflect the principal direction of movement on the fault'.
1 The abs.ence..o.f .the Shaft fault,,in exploratory trench 3, about i i 250 feet southwest of the reactor shaft (pl. 2) can be attributed - i to(1)dyingoutoffaultingupwardand/oralongstme,or(2) 5 deposition of the younger sediments after faulting. ; Tectonic faults of lateral movement are characteristically discontinuous, en echelon, and branching. Surface ruptures'within j; the San Andreas fault zone produced during the 1906 earthquake t illustrates these characteristics. (See description by Higgins, 1961, p. 53 of the ruptures at Fort Ross, 18 miles north of the , reactorsite.) It is to be expected, therefore, that the Shaft fault, a tectonic fault, cannot be traced continuously along the l y strike for long distances and that its absence in trench 3 is due
.l . .
! to its dying out between trenches 2 and 3 i
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If the sediments were deposited'atter the youngest movement ' on the Shaft fault, then faulting of the sediments took place more' l than 42,000 years ago, the age of the oldest dated sediments, according i j to radiocarbon measurement of fossil wood. The Pleistocene beds on Bodega Hesa may be younger than a crustal disturbance that is esti- ! 1 j nated by Louderback (1951, p. 86) to have taken place from about 2W,000 to %0,000 years ago. Thus the Shaft fault in the Pleistocene beds at the site may have originated between h2,000 and 400,000 years-.ago. The Shaft fault in the sediments might reprisent the left flank. of a landslide which moved in a southwesterly direct, ion.; The topography of the bedrock surface as depicted on plate 2, hovever, precludes this
! possibility because such a landslide would have had to move across a
{ .
! narrow valley and up the bedrock ridge on the opposite side of the: !
valley. Ccuceivably the bedrock topography as shown in plete 2 may ; be incorrect in detail; even so, in order to produce .a landslide that could create the Shaft fault, a southwesterly slope at' least as long ' .
, as the known extent of the Shaft fault would be necessary. It seems 1
very unlikely that such a long southwesterly slope would have formed i l contrary to the general bayward slope of. the ground surface. If the Shaft fault is the result of landsliding, deformation and disruption of sedimentary features should be greater in the sediments of the landslide mass than in the adjacent ground. This would especially I
! be true of subaqueous landsliding. No marked differences, however, S.
]
i < d in disturbance of sediments were seen on the two sides of the Shaft ., I
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.i An ori6in by compaction 'is favored by T.he location and trend of I the Shaft,faalt ale:g the northwestern flank of a ridge of granitic bedrock at,the reacter shaft (pl., 2). The sediments are somewhat-thicker vest. cf the Shaft fault over a low place on the granitic bedrock.
- surface and greater subsidence by compaction would be expected here. ,
A fault caused by compaction of sediments should' dip everywhere toward l' ,
.y
- the area of, compaction, vestward for this place, and the fault move -
- i. ._~ .p.e..n..t. Aqu.i.d. k.e o. f .t. he .nor.:n..al..t.yp,e.. in _w_h__ic_h. ..th.e.. .dow..n moving block lies I
above the fault. On the south vall of the shnft at about elevatica -
-16 f,.eet, theoretical displacement on the Zhaft f* Alt is icvn en the west about 2 feet--a condition that favers the sceidence theory.
! However, the Shaft fault dips both eastvard and vestward, but where
.j 1 ' it shows its. greatest apparent vertical offset, it dips eastvard,
.]
or movenent was reverse to that required for compaction. Furthermore, the appsrent dovrmovin6 block is belev the fr. ult. Also subsidence northwest of the fe. ult vodd leave unsupported sediments abcve the east-dipping part of the fault. This sho21d result in additional faulte near elevation -20 tetween vmical control lines 33 and 39 None was seen. The undivided continuity of the Shaft fault southwest i of the shaft across an area of thick sediments filling a valley cut
'; in the bedrock surface, and onto an area of thin sediments above the adjcining ridge of bedrock, makes the origin of the Shaft fault by l
i
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cor.paction highly.unlikely.
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c ,, l SURFACE RUF:'URES WEST & EE SAN ANDREAS FNJLT ZONE \y J
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1 The structural features in bedrock a W g the west side of the A y ' t .;' ) . San Andreas fault were examined to deterisina their genetic relation ] t i l g to the Ses,Andreas fault zone'for comparison with similar features , j vi ) 1 at the px y sed reactor, site on Bodaga Headn The, areas studied
, ,- .t inclwid Inverreau, Mt. Mittenburg7i and Mu$ Lake. (pl.1).
3 9 . Gilbert (inLewsonandothersg1908,p'.6Nandpl.453and 47A)describesend.11'iNratesiurfmerupture',inthetohnof r
~
.,, 3. . , >
0 1 f , , l Invermas' that resulted fion the 19C6 'arthquake. .Althou6h ,the I 93 ^ l i f j .
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1 exact loc .11ty vas, not given by Gilbert, .we were shown by Mr.. Thomas ; 3
) ,
Drew, a resident of Inverness, 3, feature which his fath?;r, who 31ved 3 4+ ., ; l there i 1906, referred to as "the earthquake crack." This feature l' , ' i *
, .I j ~ (locality 1, pl. Ih gonnists of two ; carps' hbree or four feet high
~
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bounding a small ridge 10 to 25 feet wide;yhat strikes L 180 L ;! 4i ,, The ridge and the bounding scarps look very much like th5pe shown fI in plate 47A of the Lswson report. The ipograph/ tin the immediate d 1 vicinity of the ridge also is similte to'that, shown 'on plate 47A ' (Lawson,1908) and the skyline, nov, obscured by trees is, according to Mr. Drew, the swe as in thej photograph ipl. 47A). ' Sqnnants of I the fence visible in the photspaph were also found in the trees leaving little doubt tnet the locality we visited is the Une pictured ,"
. < .c
- in the Lawson report. Gilbert, states (in Lawsch,1908, p. f,r)) that ;
' 'i i the horizontal displa ;er.ent alosg this crack ve.s:El feet.( This '4 l a.
'l undoubtedly is tectonic) fault movement. .
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4 l l j Locality 1 is at the top of a rather flat ridge and according ; i to the Gilbert description and plate 45B (Lawson and' others,1908) the rupture extended down both sides of the ridge and across part - I of a flat.-bottomed valley and trends at nearly right angles to the f
.1 l 2 ridge and. valley. At locality 1, the rupture is about 2,000 feet y , '
' vest of the projected edge of the San Andreas fault as shown on
.l published geologic maps (Weaver,1949, pl. 9; Koenig,1963).7 l > .
-. However,, Gilbert ,(Levson and,others,1908, p.194), probably influ , ,, , -
enced by, the surface rupturing,he saw there in 1906,' considered l I Inverness to be within the fault zone. ( Gilbert (in Lawson and others,1908, p. 75) described cracks _ j r j resulting from the 1906 earthquake that cross a spur on Mt. Wittenburg , i (Locality 2.on plate 1). The authors accompanied by Alan J. Galloway, t a geologist who has recently mapped the geology of this area,- inspected ~ the spur in an attempt to find the cracks described by Gilbert. 1 Although we were unable' to locate the cracks, the spur is a broad ridge and landslide movement is very unHkely to have caused the , l cracks. We believe Gilbert was correct in ascribing them to fault
' movement. A subsequent study of selected aerial photographs of
,, Nt. Wittenburg revealed a' dense network of lineaments, some of which
, 2 i are shown on plate 1. Several of these lines extend toward the spur a
- on Mt. Wittenburg and the fault movement described by Gilbert may s
have ,been on one of these. 1 b~ r., Jl . n
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i 3; - 9... e The lineaments appear in various forms on the photographs. Some - are prominent straight stream valleys; some consist of the alignment of short tributaries, of notches in ridges, and of trees of different height than their neighbors; and come are extremely fins dark lines.
] They occur in quartz diorite, shale, grayvacke, and greenstone. Those
,{
shown on plate 1 are merely a sample obtained by a brief study of a 1 few photographs and with additional study many more could be plotted.
~ Results of our brief study have shown that some of the lineaments-are joints and faults, a few may be ' igneous dikes,[but many of them ere zones of weak rock along which erosion had been greater than' elsewhere. According to A. J. Galloway (bsd cc:=unication,1963)'
i l some of the lineaments are faults having~ measurable offset. The genetic relation of the lineaments to tid San Andreas fault
- l zone has not been definitely established. . Some of the more prominent. .
lineaments curve northward from the San Andreas fault and probably are branches of it (Galloway,1961, p. 31, and oral communication, 1963). On the other hand, examination of aerial photographs of an area approximately five miles east of the San Andreas fault indicates
,j that the lineaments are just as prominent there as they are within Jl t
. one mile of the fault. Even if the lineaments observed in the Mt. Wittenburg area cannot be related to the San Andreas fault a
genetically, they indicate that the granitic rocks have prominent
't 1
zones of weakness along which fault movement has and could occur.
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The distribution of many lineaments in the Mud' Lake area (near locality 3) are shown on plate-1. Mud Lake is about 3,000 feet west of the San Andreas fault and it' probably resulted from subsidence of l a block bounded by faults. It lies in an elongate steep-walled depression.whose topographic position and shape preclude origin by-
.,landslidin6* . It .is estimated from the. Double Point quadrangle 1[
3
] topographic map that the block has. subsided' more than M feet. The rate 'at' which this type of movement ' occurs is not known. [
l -Vertical movement of as much as five feet,'which Gilbert-(in'
, Lawson and others,-1908, p. 75) ascribed to faulting, occurred at locality 3 south of Mud Lake. The authors accompanied by Alan Galloway and Don Tocher, were able to positively identify locality 3 lc as the one that Gilbert described (op. cit.,1908, p. 75). This
'l movement was probsbly caused by landsliding rather than faulting.
~
Very large landslides are prominent just west of the locality, and' study of aerial photographs reveals that an irregular scarp formed-by a landslide joins the fractures described by Gilbert (1908). Moreover, the stream valley down hill from the site has been blocked
.s. ..
.by the landslide moveme'nt, causing ponding of the valley and deposition
'. j e of sediments. 4
- q ,e .
Additional information on the structural features resulting.from' the movement along the San Andreas fault during the 1906 earthquake
'i .
- g. .
6 was obtained in a railroad tunnel at Wrights Station, about 100 miles . j south of Bodega Head (Lawson and others, 1908,'p. 111-113). The
.1 .
1 ,* . tunnel is in bedrock of sandstone and chert, and makes an angle of I
, 800 with the San Andreas fault. As a result of the 1906 earthquake. .
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the tunnel was offset'(horizontal 4 ) about five feet along a fault and , damag'e over much of its length consisted of crushing of the: timbers, .
. -i l.
breaking of ties, and caving.- The' tunnel vns also bent out'of line,- ^ the amount decreasing away w from the fault. At a distance of 4,000 feet
- from the fault the horizontal deformation was 14 inches.:.The report- i 8
1
, does not state whether the fault in the tunnel was'in the main San Andreas' 'I j si t
fault' zone or was a secondary branch fault, but in either case, the ground '. I
; was strained for a distance of at least 4,000 feet from the place where 1 the tunnel was offset five feet.'
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i 9 CONCLUSIONS i . On the basis of the geologic information obtained during the detailed geologic study,of,the proposed power plant site and the study of the faults developed by the .1906 earthquake on the vest side of 7! the San Andreas fault zone southeast of Bodega Head, the following
.I j
conclusions are presented. , 4
~ ~~
-- Significance of the Shaft fault The Shaft fault is one of the principal faults cutting the ;
granitic bedrock in the reactor shaft area. Its size in the granitic. l rock indicates that it has been the locus of stress relief at many l s .. 1
, times in the past. Drag and offset of igneous dikes by the Shaft fault indicate.: that its movement may be primarily horizontal like
]:
; that of the San Andreas. The ruptures in the Pleistocene sediments evidently formed during the latest movement along this fault. The abrupt changes of dip with depth and the variation in offset magni-tude and direction with depth also indicate that movement of the Pleistocene sediments was largely horizontal.
Whether the Shaft fault should be considered as an active or in-
; active fault cannot be determined. Geologic evidence bearing on the 1
age of the latest movement of the Shaft fault is inconclusive. The field data may be interpreted to indicate that the last movement took place more than 42,000 years ago, On the other hand, it is just as
. reasonable to postulate that displacement in the granitic rock at some more recent time ruptured the lovest of the sedimentary deposits 33
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by shearing, vbereas the sediments higher in the section absorbed the differential movement. That is, the intensity of shearing diminished upward and the unconsolidated sediments adjusted to the strain by J intergrariular movement, compaction, or displacements so small. and diffuse that they left no visible evidence of shear.
, 'i'he Shaft fault in the granitic rock of the reactor shaft is an l important zone of weakness that could undergo differential movement if f
stressed to a degree comparable to the stresses applied to granitic rocks on Point Reyes peninsula during the 1906 earthquake. In this respect it is no different from myriad other faults in the granitic rock of Bodega Head and there is no basis for saying that it vould move f in preference.$g other faults. Possible future faulting on Bodega Head ' i, The commonly accepted outer limits of the San Andreas fault zone ' are the boundaries of the zone that has been the locus of the majority of surface ruptures. The same stress field that causes ruptures along I . the San Andreas fault zone is also present in the crust adjoining the zone. As was seen in Point Reyes Peninsula and at other places along l 6
-l the San Andreas fault zone during the 1906 earthquake, the ground
'l surface was ruptured by sympathetic faulting at places as much as a j mile from the commonly accepted border of the fault zone.
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.." If in some' future earthquake surface rupture comparable in
; , severity to that produced in 1906 occurs'on the San Andreas fault,
- 3; .
[ the near-surface granitic rock of Bodega Head would be expected to' :- j i rupture. The nature, di.rection, and amount of displacement cannot
, w. .
4.1 be predicted, nor.can the location.of.such ruptures. . Judging from
. .t, . . .
Ej the, surface rupturing observed on Point Reyes Peninsula after.the
..y
'i 1906 earthquake, displacement on the order of a few feet, either horizontally or vertically, should be anticipated. . - -
An earthquake appreciably less' severe than the 1906 earthquake,
]
under the conditions stipulated, would not be expected to cause '
- rupturing outside the San Andreas fault' zone. There is no voy to relate this rupturing outside the main San Andreas fault zone to cf
, earthquake severity except in the most general way; thus, -it is !
impossible to define some " threshold severity" above'vhich faulting , i a 'l outside the main fault zone would be predicted. ' 8 m. I e
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, REFERENCES CIIED .
l Blair, B. E.,1955, Physical properties of mine rock, Part III, Bureau ., l
.j ot' Mines Report 'of Investiga'tions. 5130, 69 p.
39'5k 'Pitysical propertie's of mine' rock, Part IV, Bureau of Mines
, ' Report of Investigations 5244, 69 p. -
j 1 Bureau of Reclamation, 1953, Physical properties of some typical ! l 4 l fou'ndation rocks, Concrete" Laboratory Report SP-39 (nopagination) l
.; .. . . . . .. . . . . . . . . . . - . - . . . .. 1 Dames and Moore,1962, Foundation investigation, Bodega Bay Atomic Park, i
Unit'no. 1, Bodega Bay, California: Unpublished report for Pacific l I
- Gas and Elec ric Company, April 30, ~ L962, 25 p., 26 plates, appendix A, 7 p.; a;;endix B, ? p. l l
Galloway, A.'J., 1961, GeoloEy of the Point Reye3 Peninsula: p. 30- 34 . j
] in Land use' survey, proposed Point Reyes National Seashore, National )
' Parit Service, 57 p. I hie 61ns, C. G.,1961, San Andreas fault north of San Francisco, C tlifornia:
)
l Geol. Soc. of A= erica Bull. , v. 72, no.1, p. 51-68 Koenig, J. B., 1963, The seolosic setting of Bodesa Head: Calif. Div. Mines and Geol. Mineral Information Service, v. 16, no. 7, p. 1-10. l I Lawson, A. C., and others, 1908, The California earthquake of April 18, i 1906. Report of the State Earthquake Investigation Commission: . I \ l Carnegie Inst. Washington Pub. 87, v.1, pt.1, 254 p.; pt. 2,
; p. 255-451; atlas 25 maps and seismograms.
q l Louderback, G. D.,1951, Geologic history of San Francisco Bay: Calif.
- Div. Mines and Geology Bull. 154, p. 75-94.
l 36 a4
. );. W 1%S s 8,@rJAMs ctes::. d;Nschg+qM, m.t.- ygen,in-wa.!wh.m wMgrwegv.y w.j;g . g:d
3, .. . ,. w . .
. . . , , . . . . . . . , ;, ,, :,.. . ,4.
4~.
,. s -ds,.mm.uam . . %.:. g. -.
.,. .we ; j <,.n.-mu.-.w_- _.m. < . . _ .. - .y...
; .a w an..es.:
.1,=w eru w asss ux w u.a -
I .
.y y 9 .- .'
i i 1956, Wrench-fault tectonics: Geol. Soc.
~
.. Moody, J. D., and Hill, M. J.,
. America Bull., v. 6T, no. 9, p. 1207-1246.
Schlocker, J., Bonilla, M. G., and Clebach, A., Jr.,1963, coologic 1
- I l.
investigations of a proposed nuclear power plant site on Bodega i 1 Head, Soncina County, California: 'U. S. Geol. Survey' report TEI-837;- . a pt. 1, 43 p. ' I J Weaver, C. E., 1949, Geology of the Coast Ranges immediately north of. . J the San Francisco Bay region, California: Geol. Soc. America ! l Mem. 35, 242 p. 1 Windes, S. L., 1949, Physical properties of mine rock, Part I: Bureau of Mines Report of Investigations no. 4459, 79 p. l
. .. 1 1950, Physical properties of mine rock, Part II: Bureau,of Mines d'
4 Report of Investigations no. 4727, 3 p. l 3 y
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E io b o . s io PERCENT (Faults and jomts, total 1120) PERCENT 4 I N 1 to 1o j
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; PERCENT PERCENT Figure 1. - Strike (bearing)-frequency diagrama of faults and joints observed 'in well of reactor shaft, showing
. percent mapped within 10 degree intervals of strike. Includes repeated obser' v ations of faults and joints
, i + th'at persisted from. level to level.
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e9 on r-Figure 2.- Dl'AGRAM SHOWING ORIENTATION OF FAULTS Contour diagram of 568 poles of f aults on wall of reacter shaf t. j Plotted on lower hemisphere of equal-arco not. Includes repeated observations on f aults that persist from level to level. i l' Contoured on I, 3, 6,11, and 17 pole concentration intervals; unit creo l for counting poles is one percent. G Indicates pole to Son Androos f ouitzone, which for this diagram is
.] osausned to be vertical strike N37 W. 3 indicates pole to Shof t fault, i
s dip 77 degrees N. W., strike N 40 E. 3 i
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Fig. 4.--Shaft fault on floor of shaft, elevation -42 feet. i
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I Fig. 5.--Shaft fc. ult in Branitic rock on south wall of shaft, h '. . elevation -41 to -51 feet. l .) 1 i t 9 i j
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Fig. 7.--Shaft fault on south wall showing sand filling and 4i g . variation in dip. t J I i p 41 6 - p- h f
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showing 1Linch vertical' separation.
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