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( ( GeoIogic and Seismologic Study af Bodega Head by Pierre Sain>Amand 1 l 4 INTRODUCTION Dr. Saint-Amand's previous publications are many. The most recent, Los Terremotos De ' Mayo--Chile 1960, has been published as Tech-nical Article No.14 by the Naval Ordnance Test Station, Michelson Laboratories , China Lake and ' ' Pasadena, California. It is the first eye-witness I account of a major earthquake by a recognized expert seismologist who was there to ride it out. Dr. Saint-Amand's interest in Bodega Head began in late 1962, when David Pesonen of the Northern California Association to Preserve Bo-dega Head sent him several aerialphotographs of the area for study. Subsequently, Dr. Saint-Amand, accompanied by Dr. Oresti Lombardi, al-so from China Lake, made a two-day field trip to' the headland. He enjoyed the advantage in gath-ering his data of seeing the proposed reactor site
" opened up" by Pacific Gas and Electric Compa- Mf 4 - 7> 'c,3 '7 ny's initial excavation. In addition, the reports of the utility's experts (both close friends of Dr.
Saint-Amand), Dr. Don Tocher of the University of California and Dr. George Housner of the Cal-ifornia Institute of Technology, were made avall-able to him by the Association. This report is Dr. Saint-Amand's analysis and conclusions concerning the hazards posed by the Pacific Gas and Electric Company's anticipa-ted construction of a 325 megawatt nuclear reac-tor at Campbell Cove on Bodega Head.
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4 N i PO gr so or > ls% s 4 EXPLANATION xaf. 0 l OUATERNARY SEDIMENTS I lT l TERTIARY SEDIMENTARY ROCKS , e l xaf l FRANCISCAN FORMATION a RELATED ROCKS 5* lSr l GRANITIC ROCKS .s\ N CONTACT, APPROXIM ATELY LOCATED 6 s- *
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( kg FAULT ZONE, DOTTED WHERE CONCEALED I Generalized geologic mop of Bodego Head and Pt. Reyes (of ter Son Francisco and Santo Roso sheets of the Geologic Map of Californi,o). The oreo shown in dashed lines is the oreo shown on* new f f *"Je. (Reproduced from "The Geologic Setting of Bodega Head, "Koenig, J.B. , Calif. Div. of Mines and Geology, _M_ ineral Information Sve. , July 1963.)
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i' TABLE OF CONTENTS page
- 1. Introd u cti on . . . . . . . . . . . , , . . . . . , , . . . . . . . I j
- 2. Geology . . . . . . . . . . . . . . . . . . . . , , . . . . 1
- 3. Possibility of a Severe Earthquake at Bodega Head and the Possible Consequences . . . . . . . . . . . . . . . . . . 14 4 . Con clu s io ns . . . . . . . . . . . . . . . . . . *. . . . . . . . 20 5 . Refe re nce s . . . . . . . . . . . . . . . . , , , , , , . . . , , 21
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, GEOLOGIC AND SEISMOLOGIC STUDY OF BODEGA HEAD l By Pierre Saint-Am'and*
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- 1. INTRODUCTION l
l 1-1. Field Work. The author visited Bodega Head on 6 and 7 April 1963 in ordet to make an examination of the geology of the Head. The area was traversed on foot in company with Oreste W.' Lombardi. The study consisted esser.tially of mapping on both aerial photographs and on a topographic map. Special attention i was paid to faulting, condition of the terrain as foundation' material, probability j of landslides, and other aspects of engineering geology applicable to the con- l struction of an atomic power plant on the Head. I 1 - 2. Previous Work. V.C. Osmont (1905) included a discussion of Bodega Heac in a paper on the regional geology. Johnson (1934,1943) presents a general geo-logic study of the region. Tocher and Qualde (1960) present the engineering geol- ( ogy and seismology, and Housner (1961) discusses criteria for engineering design j based on the work of Tocher and Qualde and on his own observations. Koenig (1963), of the State Division of Mines, has summarized the geology of Bodega Head. A study by Dames and Moore, concerned with foundational aspects, was not available to the author at the time of writing.
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- 2. GEOLOGY 2-1. Geography of Bodega Head. A general view of the region is shown in Fig.1, a close-up of the Head in Fig. 2, and the topography in Fig. 3 (from a f j
map taken from Tocher & Quaide). The Head is an erosional remnant of an elongated ridge lying along a SE-NW line seaward of and parallel to the main San Andreas fault zone and in the i I general area of deformation marginal to the fault. It is connected to the main-land by a tombolo of san'd dunes lying over a mixed collection of littoral deposits i and wind-blown sand. The long sand spit of Doran Beach State Park extends southwestward from the mainland to enclose the south side of Bodega Bay. A protected channel hs been built to prevent sanding of the entrance to the bay, which is used as a harbor by fishing and pleasure craft. l P. - 2 . Structure. Bodega Head is part of a long, thin ridge of rock, interrupted-
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I ly connected to Tomales Point (4.5 miles to the southeast) by a line of sub- l l marine hills. The ridge bounds the western edge of the San Andreas fault zone, and is composed of a line of horsts, or uplifted blocks, squeezed up by move-ment on the fault. Similar ridges border the San Andreas and other strike-slip faults in many places. These ridges are slowly and continually being forced up-ward at a rate somewhat faster than that at which the forces of erosion can re-move the extremely crushed and broken rock. The presence of such ridges is a diagnostic aid for estimating the activity on a fault. l l 4
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2-3. Bedrock. The bedrock is a medium to coarse-grained granodiorite, called " Bodega diorite" by Osmont (1905). It is probably a part of the coast range batholith and is similar to other granitic rocks found along the coast and offshore . It is generally thought to be middle to upper Cretaceous in age; j radiometric dating indicates an age .of 80 to 90 million years (Curtis, et al. , 1958). It is occasionally injected by acidic dike rocks. Rock crops out on -I the higher parts and along the seaward sides of the head; in one or two places 'l It is exposed along the shore on the bay side of the head. . 2-4. Weathering and Soil. In newly exposed outcrops, where the sea is ac- ! tively removing material, the rock is relatively fresh but is broken into small l fragments. Where erosion is less active the granodiorite is covered by a deeply weathered clay-rich residual soil derived from weathering of the granodlorite. The residual soil is usually covered by a well-weathered sand, , in part of aeolian origin. A sample of the upper sand from the reactor-pit excavation shows angular to sub-rounded grains of quartz and feldspar. l Horizons of the soil may be readily seen in the reactor pit and on the south l side of Horseshoe Cove. J Near Horseshoe Cove,1 meter of dark humic soil overlies 2 meters of coarse orange sand, which in turn rests upon 4 to 5 meters of light-gray arkosic sand. This material is somewhat different from that in the reactor pit. 1 None of the sediments are in any way cemented or indurated. They are in ' part Recent Marine or Estuarial deposits. I i Tocher and Qualde express the view that these are terrace deposits, l l pointing to the presence of mussel shells in the soil. Koenig (p. 6) describes l these sediments in some detail, concurring in general with the other observers. ' i They are probably correct, because although definitive evidence for these being terrace deposits seems hard to find, a series.of what appears to be raised shore lines can be seen on the flat, grassy surface just west of the sand dune area (see Fig. 2, and Fig. 3, Point A). Along the inland shore at Point D, Fig. 3, about 10 meters of coarse red sand unconformable overlies a blue-gray sand for the remainder of the exposure. Bedrock is not seen here. The sediments at this point are deeply gullied, are l scarred by small slumps and ooze' water from many small springs. , 2-5. Ground Water. The sediments are loosely consolidated, porous, and permeable . At the time of this study the sediments were saturated, and numer- ' ous small springs could be seen at the water's edge. At Point E, Fig . 3, a - fault cuts the cliff and a good spring has developed. Here bedrock is just visible at about sea level. As Tocher and Quaide point out, the soils are saturated during rainy seasons and probably dry out somewhat in late summer. 2-6. Pra cturinc . Tocher and Qualde describe the rock of Bodega Head as extensively sheared and broken. Johnson (1934, pp. 24-25) reports the same. The rock is indeed severely fractured, as Figs. 4 and 5 show, the fracturing being most intense near faults. In many places it is difficult to find sound ! rocks larger than a man's head. Often, in shear zones and in the vicinity of faults, the fragments are augen-shaped or rudely tabular and are aligned along the general trend of the fa ult s . In such regions the "soi-disant" solid rock has the consistency of a vertically stratified alluvial deposit. Many of the surfaces have thin mylonite zones. In some places the rock is a tectonic or cataclastic breccia. A combination of the fracturing, mylonitization, deep weathering, and an abundance of ground water render the bedrock far less stable than similar rock
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" 2 - 7. Faulting. Minor faults abound on. Bodega Head 'and a few major faults can be clearly seen. The best way to appreciate the degree of faulting is to walk along the sides of Horseshoe Cove. .
The Cove itself is a rentrant cut by the erosive action of the waves-from the zone of a large fault that trends about N450E. The crushed and broken , rock of the fault zone has been more easily excavated than the relatively harder ! surrounding rock. The Cove is bordered on both sides by faults parallel to its: l northwesterly and southeasterly shores. The faults on the northwesterly side l (Point F, Fig. 3) are very well exposed. ' A good-sized fault is exposed every hundred feet or so along the south-westerly side of the Cove. Short canyons have been elaborated along these fa ults . In the bottoms of some of these canyons are granodiorite boulders covered by alluvium and slope wash. Six steeply dipping faults of consider-able size, measuring 1 to 5 meters wide, are found between Points C and G. These faults trend between S45 E and S60 E, and are sub-pars 11el.to the San Andreas . Occasional thmst faults, steep reverse faults and normal faults can be seen between the high-angle faults. In fact, each rentrant along the coast is determined by a fault. One ) of the more notable ones (Point H) can be traced easily on air photos, and with. only a little difficulty on the ground, to the southwest of the hill crest marked 238. Between Points F and H, and as a matter of fact clear to Windmill
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The wave-cut platform that surrounds the seaward side of the Head dis-plays faulting very clearly. At several places the platform is at a different l altitude on either side of a fault, indicating differential uplift across the fault. In places the platform is destroyed'or completely, missing--for example, where the fault shown by Johnson enters the sea. At Point J the platform is at different elevations on-either side of the fault, and the 100 meters 'or so of-missing platform heads against a cliff so fractured (Fig. 6) that it is actively landsliding along the upper edge and face. Near Point K a rentrant channel has developed in the wave-cut platform (Fig. 7). At the head of this channel a fault zone--50 meters wide, consisting of septa of rock caught between shear zones and curtains of gouge--is exposed in the cliff. Figure 8 shows a portion of this fault zone. Horizontal stria may 1 be seen by exposing any of the mylonitized surfaces. At Point L a landslide is developing in the zone 'of a very large fault. l Material is being removed by mass movement, slope wash, and gullying. -t One spectacular fault is exposed on a bedrock high on the northwest face of the excavation for the reactor, the approximate location being at Point : M; the original banks on the northwest and southwest sides of Campbell Cove have been removed by the excavation and precise location was difficult, l especially in the rain. The fault lies near a temporary road,' a temporary ; drainage culvert, and a stake marked " Top Bench 55.0". The fault extends up. ! and down the road for at least 50 meters, strikes N450 W, and dips vertically, , as nearly as can be seen in the partial exposure. Numerous small' fractures
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( ( . 1 10. delineate the zone; these are interspersed with septa of crushed rock and cur-tains of mylonite and gouge measuring 2 meters wide. The majority of the stria indicate dexteral strike-slip displacement, but some clearly indicate vertical j movement. Figure 9 shows a section of one wide gouge zone. This fault alone might well concern the builders, and is ample reason to recommend against the use of the site because of the possibility of movement thereon during or following an earthquake. I 2-8. La nd slid ing . Numerous examples'of soil creep and mass wasting are to be seen along the coast. The rentrant at Point D has been the scene of several small slides . The sediments here are now extensively gullied and show small slumps, i terracettes, springs, and a topography indicative of an unstable terrain. An old ' landslide, on a gentle slope in " solid" rock, is found at Point N; the debris that l l flowed out is overgrown by gorse. I The water-soaked condition of the soil', the looseness and lack of com- ; paction, and the broken state of the rock all suggest that landsliding could be ' expected following a major earthquake during or just after a normal rainy season l
--especially following extensive construction work that will redistribute masses l of earth and change the ground loading.
The former Campbell Cove'is now being filled to make a dock area and to 1 dispose of the dirt removed in excavation. Unless an excellent sea wall is placed on the bay side this deposit will be unstable even in the absence 'of earth-quakes, and even with a sea wall the situation would be difficult in the event of an earthquake. A similar installation in Puerto Montt, Chile was destroyed in 1960 by liquefaction of the soil (Saint-Amand,1961, p.19, and Duke and Leeds, 1963). 2-9. Recent Uolift. Severa! lines of evidence point clearly to Recent uplift of Bodega Head: Soil now fcund above sea level is in part a tenace deposit (Tocher and Qualde) that was originally emplaced below sea level, as indicated by the mussel shells . Absolute age of the deposits and hence a maximum age for the uplif t could be determinable by Carbon-14 dating of wood and shells found in the de-posits . Carbon 14 dates for wood from the reactor pit, taken at about sea level, yield ages in excess cf 42,600 years; dates are not yet available for shells and other debris from higher in the section. A careful study of these materials will be very important and interesting from an academic point of view. Elevated shorelines, shown in Fig. 2 and in the plain at Point A, Fig. 3, are subdued but nevertheless visible in the field. The soil is soft sand, and al-though Jt is stabilized by grass cover one would expect erosion to have pro-ceeded so rapidly, because of the abundant rainfall, that these marks would not be very old. This bespeaks a very recent uplift. The wave-cut platform around the head is also diagnostic of Recent up-lift. It is apparently a local effect, not caused by a custatic change of sea level I as postulated for uplift of the terrace deposits by Tocher and Qualde (page 7[. This platform is quite' young, is at different elevations in different places / and is clearly offset vertically by some ' faults. A similar platform was found around Isla Mocha and near Lebu, Chile, following the great earthquakes of 1960. At that time Isla Mocha was elevated-about 3 meters and Lebu 1.5 meters (Sain't-Amand,1961). 1
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1 I f - 12. On the southeast shore of Campbell Cove there is a concavity cut by > storm waves, probably before the mole was built. This is now elevated about a meter above the level at which it was formed. It was probably uplifted at the i same time as the wave-cut platform. Several of the canyons produced by erosion of fault zones now have old bottoms exposed at a height of 3 to 5 meters above present sea level (Fig.10); 4 they have wave-rounded boulders in the bottoms, and are filled with slope wash ' and soil. The same sort of boulders may be seen at the present sea level in the heads of channels produced in the same fault zone, where the sea is now fash- 1 foning them from joint-blocks and fragments. The soll in the old canyons is ! quite young, loose, and uncemented. This situation also indicates a Recent up-11.f
- l The rather surprising depth of alluvium reported in Campbell Cove is sug--
gestive of a tectonic origin for that bedrock depression. It is difficult to see how i it could have been cut to that depth by erosion.. Hence it is possible that it was produced by the down-dropping of a small graben; however, other explanations-could probably be found as well. 2 - 10. Recency of Tectonic Movement. Although fresh fault scarps are scarce, , several were noted, and abundant other evidence such as cited abeve indicates ' vigorous Recent tectonic activity on the Head. The fault lying along Points P and B,' Fig. 3, on the northwesterly side of Horseshoe Cove, clearly offsets the pattern of the old shorelines, as may be l seen in Fig. 2. Another fault, at Point C, leaves a faint scarplet running sub-parallel to the shorelines. i The relative lack of fault scarps is deceptive. This is almost certainly be- l cause of the failure of the soft-soil overlying portions of the Head to reveal move-
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ments in the bedrock, and because rapid. erosion caused by the heavy rainfall on the soft soil would quickly destroy any such scarps. For example, in 1906 the San Andreas fault moved about 16 feet in the vicinity of Bodega Bay. Lawson (1908), p. 65, quoted by Tocher and Quaide, pp.1-3, clearly states that even this considerable movement was not visible in the sand dunes nor across the Doran Beach sand spit. Pault movement effects produced by earthquakes have always been easier to follow over bedrock than over even the shallowest alluvium. Furthermore, the San Andreas fault and the majority of the fractures on Bodega Head undergo mostly horizontal movement, and this sort of displacement does not produce scarplets as conspicuous as an equal amount of vertical movement. Scarplets do not long endure under the climatic regime at Bodega Head, nor in the type of soll found there. The trace of the 1906 earthquake is now quite modified. A similar example was shown in the Kern County earthquake of 1952 which broke a series of scarplets along the trace of the White Wolf fault (Buwalda and Saint-Amand,1955); today these scarplets are scarcely visible. Far less rain falls in Kern County than at Bodega Head, and the soil is much firm-er. The scarp of the 1872 earthquake in the arid Owens Valley is now so smooth and modified that it is in places difficult to recognize. 1 Hence, one must observe considerable caution in estimating the state of present or Recent tectonic activity on the basis of vertically displaced scarplets alone. C________.__ ___ _ - - _ _ _ _ _ _ _ - - - - - - - - - -
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- 3. POSSIBILITY OF A SEVERE EARTHOUAKE AT BODEGA HEAD AND THE POSSIBLE CONSEQUENCES >
3-1. Estimates of Frequency of Earthquakes. Tocher and Qualde, p.12, in. l regard to Bodega Head, estimate that "at least one and perhaps two major earth-- I quakes can be expected near the site within the next century. These may be at s lea,st. as strong as or even stronger than the California Earthquake of April 18,- j 1906." Housner, p. 3, says "It has been estimated that a large earthquake, such - as the 1906 shock, may be expected to occur along the San Andreas fault perhaps . three or four times per 1,000 years. .Less intense ground motion can be expected- ; to occur with greater frequency, it being estimated that ground motions at least i sufficiently strong to cause damage to poorly designed structures may be expected 1 at the site several times during the next hundred years." The author's pe.rsonal guess would be almost the same as that of Tocher and Quaide. Small earthquakes do not often occur on the San Ahdreas fault. Large San l Andreas earthquakes have occurred in the San Francisco region'in'1838 (Louder-back,1947) and 1906 (Lawson,1908). The 1857 earthquake (Wood,1955) took . j place a little further south and is cited to indicate the general activity.. j A great earthquake in 1836 was tentatively assigned by Louderback to the l Hayward Fault, Fig.11, a branch of the San Andreas fault at the western foot of ' the Berkeley Hills, and another great earthquake occurred on that fault in 1868. 'j Each time the San Andreas Fault has moved it has jumped a distance of 4 ; to 8 meters. Strain is estimated to.be accumulating at a rate of about 6 to 7 I meters per century across the fault. Hence one could expect at least one great earthquake per century.- 1 Other similar fault systems have had a similar history. The great . 1 Yakutat Bay earthquakes of 1899 (Tarr and Martin,1912) were probably on the l same fault as those of 19S8 (Tocher,1960). In southemChile the Arauco Fault had ' ! a great earthquake in 1835 and another in 1960 (Saint-Amand,1961). ' Smaller earthquakes on nearby faults may be expected oftener. These will ; probably cause no serious trouble unless they occur on or near Bodega Head as aftershocks of a larger event. 3-2. Intensity to be Expected at Bodega Head. The intensity (severity of shaking) will be about the same as for other earthquakes of magnitude 8 to 8.4 at similar distances. Tocher and Quaide estimate a Mercalli VIII or IX for an earth- ! quake equal to the San Francisco earthquake of 1906. The author's own observations'made in other earthquakes would incline , him to guess that MM IX would be the least expectable intensity. MM X might be. noted if landsliding of consequence were to occur, or if one of the faults on Bo-dega Head were to move. If a large fault on the Head were to move during the ' main earthquake the intensity could easily reach XI. It is difficult to give a good' opinion for intensities above MM IX because the scale itself is not too precise and the intensity assigned depends upon the presence of certain diagnostic ; structures and conditions. 1 Richter (1958, p. 353) gives the following table for average Mercalli iri-l- tensities to be expected for metropolitan centers in California and for ordinary ' ; ground conditions: l l l
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1 Magnitude- 2 3 4, 5 6
, 7 8 1, Maximum intensity M.M. .I- H III V- VI-VII VI!-VIII IX-X XI Radius (Kms) (felt) 0 15 80 150 220- 400 600 These values are in good agreement with those observed in actual earth-quakes.
The author's own estimate for.the severity of shaking at Bodega Head would be, for an earthquake of magnitude 8.2 - 8.4, something like an average ! maximum acceleration of about'0.4 g for about 1 minute, with peaks 'in excess of 1 S and with a vigorous shaking' continuing for perhaps 3 minutes.. This is somewhat larger than the intensity predicted on the basis of'the strong motion recorded in the El Centro Earthquake, as recommended by Hous-ner. The basic idea of using actual accelerograms is quite sound and is far superior to using Mercalli intensity alone. . The El Centro earthquake is the only one for which such information is avallable for a position near a fault. The-earthquake occurred on the Imperial fault, a branch of the San Andreas system; l it was originally estimated to be magnitude 6.7, but.was subsequently upgraded to 7.0.' The accelerograph was located about 5 miles to the west of the surface 4 { expression of the causative fault, or about 7 miles from the epicenter,- the-exact location of which.is in some doubt. .'Not only did~the thick alluvium alter. the power spectrum by attenuating the high-frequency effects and probably aug-
.menting the lower and middle frequencies, but also it probably does not show clearly the effects of the " fling"--an effect discussed in the next section.
Further, the intensity at a point depends on the location of the point 'with respect , to the fault and the direction of propagation of the faulting. The faulting begins - l at a point and progresses, usually in one direction. The' shaking is much harder in the direction in which faulting progresses, with.both the. frequency and ampil , tude being changed (Benloff, ~1954, p. 201). Hence' the record of the El Centro accelerogram probably indicates a lesser intensity than it would have had; ! it been located further south. ! The historical record shows very clearly that higher intensities go with larger earthquakes, and thus the use of the El Centro record will!not guarantee- ,i adequate design factors for the maximum accelerations produced by a shock of magnitude 8 or more. -f For example, Gutenberg and Richter (1942, p.170 et seq.) relate In-tensity I and maximum' acceleration, a, for various earthquakes. They derive the semi-empirical relation: log a = f - f This yields accelerations of 1 g at a Mercalliintensity of Ten and'one half. ~ Accelerations in excess of 1 g have been noted in several large earth-- quakes (Oldham,1899). -
s ( ( 17, 3 = 3. Meehantes of Eartheuake Mot'i on. . Une n ovement near a fault is quite different from that at a distance; in fact, the oscillatory motion near a fault may
., ivell be a little less.
" .There is one movement, however, that is at maximum near a fault and diminishes rapidly with distance--this is the permanent throw or fling. '
During the inter-earthquake period the blocks of land on either side of a fault move continuously and slowly with respect to each other. It is most probable that the oceanward side of a fault undergoes more absolute movement than the continental side, but this makes little or no difference regarding the in-tensity of the impending earthquake as it affects opposite sides of the fault zone. The gradual drift of the land deforms'the blocks (see Fig.12) bending the rocks and storing energy in them in the form of elastic strain. The strain. accumulates until the forces generated in the rock are great enough to overcome - the frictional forces on the surfaces of a fault that prevent slippage. When this happens the rock on either side suddenly snaps back into its unstrained straightened condition. In'the zone near the fau?t, up to say 30 km, the land on both sides at this time undergoes a permanent sudden displacement. The total displacement across the fault zone may be as much as 5 to 8 meters. This takes place as a sudden high acceleration, followed by a slower deceleration) the time. involved lis of the order of seconds. Effects of the fling are most noticeable on or near bed-rock. Most of the extremely-high-intensity effects in epicentral regions are the resuk of such action. The total fling may be ameliorated somewhat by drag in the fault zone, in the case of a very large fault, but this carries the penalty of-movement on a variety of subsidiary faults, freference line, for example, a fence fa ult -~ I L 1
, a b c FIG. 12. Process of Strain Accumulation and Release (not to scale)
- a. Field cut by a strike slip fault, before strain accumulation.
- b. During strained condition and before an earthquake.-
cs After an earthquake. The Bodega Head reactor site is located in the zone of fling of the San Andreas fault and will probably undergo some-3 or 4 meters permanent horizontal displacement. 3-4. Possible Fault Movement on the Head. The most serious cause for con-cern at the reactor site would be the possibility of movement on a fault passing either through the power plant area or across the cooling-water system. : This possibility is quite high. When a fault such as the San Andreas moves, it moves not on a single plane but on many fractures. There.is usually one main plane of movement, but in many major earthquakes faulting has been found to have occurred over a large area. Some of the faults move during the main event while others move during tne aftershock sequence. Numerous examples could be given
(' 18. where movement took place on more than one fault. Richter (195 8', pp. 47 6-- 487), in discussing the 1906 earthquake, shows rather clearly that that event
* . was much more complex than a simple fault movement. Although the 1906 earth-quake was accompanied by displacement along a fracture to the east of the Head it must be remembered that during an earthquake energy is suddenly re-leased from a large volume of rock and movement can and does take place across many faults and fractures over a wide zone. Pre-existing faults, often considered " dead," joints, bedding planes and similar structures participate in the readjustments. The Chilean earthquakes of 1960 (Saint-Amand,1961) pro-duced movements on a plurality of faults spread over about 100 km of longitude.
The Kern County earthquake of 1952 (Buwalda and Saint-Amand,1955) had a zone of faulting of considerable width, with many minor faults and some clear-cut traces as far as 5 to 10 miles to the side. The list could continue indefinitely. The hazard from movement is carefully pointed out by Housneri. page 3, wherein he says that "Since it.is quite impossible to design a power plant to survive without damage the large permanent ground surface displacements that might must be occur if the given earthquake special fault slippage consideration. " occurred on the site, this' possibility
/
While the whole slippage from a major earthquake will probably not occur on any one fault going through Bodega Head, it is quite likely that movement may occur on the big fault in the plant site, or on any of the several faults that cross the site of the cooling-water system. 3 - 5. Possible Changes of Land Elevation. One phenomenon that has been ob-served following all large earthquakes, when an attempt has been made to notice it, is a widespread change in elevation on both sides of the causative fault, even when the movement is mainly strike-slip. The land on either side is either quakes. raised or lowered, usually a matter of a meter or more for the larger earth-Examples are the 1835 (Fitzroy,1836) and 1960 (Saint-Amand,1961) earthquakes in Chile, the Kern County earthquakes of 1952 (Whitten,1955, p. 79), and the Yakutat Bay earthquake of 1899 (Tarr and Martin). This list could also be continued almost indefinitely. These changes are widespread and involve inore than mere displacement on one fault. Many faults are involved, together with uplift and downbowing.on a regional scale.
'Ihis raises the serious question of the effects of a change of level on an installation that draws cooling water from a shallow estuary.
Attempts were made in the year following the 1906 earthquake to detect changes in the level of Bodega Head on the basis of barnacle growth, but these were unsuccessful. The study was largely confined to the eastern shore, where such evidence would i>e difficult to find or to assess. The negative findings do not indicate that the Head will not change elevation--it has done so in the past, as evidenced by the wave-cut platform and by the elevated shorelines. In fact, the very existence of the promontory is due to continued uplift; no mass com-posed of such easily erodible rock could long withstand the assault of the sea I were it not for continued rejuvenation. 3-6. Tectonic Movement in the Absence of a Major Earthouake. Even if no major earthquake occurs in the area concerned, the possibility of large-scale warping or slippage is present and should be considered. While there is no clear-cut evidence at Bodega Head for other than catastrophic changes, it seems appropriate to recount one or two cases of this sort. Perhaps the most notable case is that of the W. A. Taylor Winery, near Hollister (Steinbrugge, et al. , 1960), where damage has occurred from a slow slippage on a portion of the San Andreas fault. Concrete floors have been broken and walls displaced at a rate
( 19. - of one centimeter per year. a l A thrust fault in the Buena Vista Hills, near Bakersfield-(Wilt,1958), has been moving without earthquakes for a number of years, deforming roads and bending pipelines. J y On another scale, widespread changes of considerable rapidity are taking place in many places, such as across the San Andreas fault near Cajon Pass or j along the southern and southeastern coast of Alaska (Saint-Amand,1957, pp.13 60-1364). J' l Changes of this sort are large enough to cause trouble, and a study to identify any such changes should be made before construction begins. 3-7. Foundation Considerations . It is generally thought that it is better to ; build upon solid rock than upon alluvium. This is certainly true at a distance j from the causative fault. However, at near-fault distances, where fling is im-l portant,' rock may be as bad or worse. Clearly the worst possible situation is to build upon a combination of the two. At the Bodega Head site the rock is severely crushed, broken, and mylonitized. It could scarcely be classed as ) { good foundational material. It will transmit well high-frequency vibrations, and ! then elastically deform in response to regional readjustment of strain; it will { probably also undergo mass movement due to its own weight during the long- I period oscillations . In addition, the alluvium, a loosely aggregated clay-rich soil, will certainly yield at a different rate than the rock, subjecting the in-stallation to widely varying dynamic loads and permitting the several parts of ; the installation to settle different amounts, probably resulting in serious damage from changes in level and position to interconnecting structures, to the cooling system, and to the reactor itself. A worse foundation situation would be difficult to envision. ( j 3-8. Transmission Lines. The transmission lines which will stretch across the fault zone will probably be destroyed by the fault movement, after first possi- I bly having been shorted by swinging together. While damage to the power lines could be repaired easily enough, sucn' activity is certain to put a severe load on the power plant. 3-9. Tsunamis. Since California has never suffered extensively from tsunamis (seismic seawaves) produced by its own earthquakes, this does not seem a serious cause for concern. 3 - 10. General Observa tions. It is difficult to conceive all the trouble that a great earthquake can cause. . Accounts of these events are always condensed, and hence a mere perusal of the literature, often after it has been digested and edited in the interests of economy, does not convey a very graphic impression of the extent of disruption of the normal human activities. Not only are there the usual concomitant of fire and occasionally flood, but widespread disruption of water supply and sewage disposal occur. One of the most serious losses is that of electricity; this loss is invariably felt during the period it is most needed for emergency service. / Loss of electricity leads to shortages of water, hospital facilities, elevator service, street signals, lights, etc. The most serious loss is in com-munications--especially radio, television, and the press, which in turn leads to j public panic and the spread of groundless rumors and exaggerations. The latter l tend to include misinformation regarding installations known to have a damage-
n , e-y\ ( -; .(- 20, 7 . ' -- producing potential s$ch as desms, and in the future would inevitably involve atomic reactors--especially any known to be precariously located.
, For the above reasons it is absolutely essential that electrical power l'
plants be so situated that they are as invulnerable as possible to disruption by scismic causes . The presently announced plans for the PG&E installation in- L clude eventual construction of several units on Bodega Head. Consideringlthe j extreme vulnerability of any plant on the site, it seems highly imprudent to lump l such an essential service in such e poor locality . Eventually the United States will have to turn to atomic energy to fulfill its power requirements. The future developmaat of atomic energy will hinge upon the safety of the first reactors 1 Reactors mtht%e carefully sited in order that an accident does not so alarm, discourage, and d! shear:en the public that wide-spread mistrust will prevent the deliberate, careful, and competent development of this energy sour:':e. ('
- 4. CONCLUSIONS
?
rea sons: Bodega Head is a very poor location for a rea'ctor for th'e following p
- a. The probability of a great earthquake is at least one per century; over half e century has elapsed since the last one, hence another may be ex-pected within the lifetime of the plant.
- b. The extensive faulting on the head has rendered the rock a poor foundational ' material. The combination of an unstable alluvium'and crushed -
rock is especlally unsuited to heavy construction.
- c. The plant is located in the region of permanent distortion, or fling- -
a region where exceptionally high earthquake intensities will develop.
- d. The probability of actual fault displacement on or near the site is high. The large fault exposed in the present excavation is of specisl concern,-
and is itself sufficient reason to discontinue construction. The presence of faults crossing the site of the cooling water tunnelis another serious aspect.
- e. The abundant evidence for recent uplift causes concern for the cool-ing water system because of the possibility of change in elevation of the plant with respect to the water source.
It is surprising, in view of the expert advice given by Tocher and Quaide, and by Housner, that another site was not chosen and that construction has gone ahead. The erection of a device not in itself dangerous except to its occupants is not a cause for great public concern. The erection of a device that in itself is, hazardous to others is a matter for public concern, and the builders have a grave moral responsibility to be certain that harm to others will not result from failure of the device. The location on Bodega Head is hazardous from'e. geological and seismic point of view. Because the San Andreas fault runs parallel to and forms the coast from San Francisco northward, it seems that the nearest safe locality near the sea would lie north of Point Arenas or south of Monterey Bay, and even then the site selected should be carefully ard prudently examined from all points of view before beginning construction. '
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21. REFERENCES b,
*t . ,,'
V Benioff, Hugo (1955), Meshaaism.and Strain Characteristics of the Whik Wolf Fault as Ind!,cated by the Aftershock Sequence, Chapter 10s , pp.199, 202.< Earthquakes in Kern County',195 2, ' Bull.171, Cali-' fornia Division of Mines,;1955. ./
...g Bugalda, J.P. and Pierr[ Saint-Amand (1955)','GeolbgfmEffects of the Arvin 7Tehachapi Earthquake, Chapter 4 of Earthquake's in Kern County,.
. Ca!!fornia During 1952, Bull.171,JCalifornia Division of Mines, San, 4 Fp nciscon pp. 41-5 6. p ,
Curtiss, G., J.F. Evernden, and J. Lipson (1958),' Age" determination of some-granitic rocks in California.by the Pottasium-Argon method. ' Calif. Div. . ' of Mines, Special Report 54,16 pp. - Duke, .C. Martin and David J. Leeds (1963), Response of Soils, Foundations 'd-and Earth Structures to the Chilean Earthquakes of 1960,1B.S.S.A'. , s V61. 53, No.2, pp. 309-357, 1 .
\
Fit::roy, R., Sketch of the Surveying Voyages of His Majesty's Ships Adventure ' and Beagle, 1825-1836, Geograph. Journal, Vol.' 6 (1835), pp. 311-14.- H I Housner, George W. (1961), Earthquake Hazards and Ea.rthi luake Resistant '
' Design Bodega Bay Power Plant Site , Pacific Gas and Electric' Company, o
Typewritten . Manuscript. Johnson, F.A. (1934), Ph.D. Thesis, Univers!.ty of California at Berkeley. Johnson, F.A. (1943), "Petaluma Region," California Division of Mines, Bull . 118. i Koenig, James B. (1963), The geologic setting of Bodega Head. . State of I ' California, Division of Mines and Geology, Mineral Information
, S ervice, Vol.16, No. 7, July 19 63, pp.:1-10. '
1 Lawson, A.C., et al. (1908), The California Earthquake of April 18, 1906, ' Report of State Earthquake Investigation Gommission, Carnegie l Institute of Washinpton, Vol.1,1908. > Louderback, G.D. (1947), Central California Earthquakes of the 1830's, B. S . S . A . , Vol . 3 7, pp. 3 3-7 4.
, ,, Oldhum, R.D.,'Rpport on the Great Earthquake of 12th June 1897, Member of l Geological Survey of India, Vol. 29, 1899. i
+
e) Osmont, V.C.,(1905), a geplogic section of the Coast Ranges) north of San ! Francisco Bay, University of Calif. , Department of Geology, Bull.
~
; . Vol. 4, pp. 39-87.
Richter, Charles F. .(1958), Elementary Seismology, W.H. Freeman ~ Company, .; San Francisco, pp. 768. Saint-Amand, Pierre (1957), Geological and Geophysical Synthesis of the Tectonics of Portions of British Columbia, The Yukon Territory, and Alaska , B. G.S . A. , Vol . 68, pp.1343-137 0. , f ____j___m_..i__---.--_---------------**~ '
a . ( 22. Saint-Amand. Pierre (1961), Los Terremotos de Mayo, Chile 1950, Technical Article No.14, U.S. Naval Ordnance Test Station, China Lake, Calif. Steinbrugge, Karl V. and Edwin G. Zacker, Part 1; Don Tocher, Part 2; and C.A. Whitten and C.N. Claire, Part 3; 1960, Creep on the San Andreas Fa ult , B . S . S . A . , Vol . 5 0, No . 3 , p p . 3 69-415 . Tarr, Ralph S. and Lawrence Martin (1912), Earthquakes at Yakatat Bay, Alaska l in September 1899, U.S.G.S. Prof. Paper 69,135 pages. Tocher, Don (1960), The Alaska Earthquake of July 10, 1958. . A Collection of Articles by Several Authors is Included, B.S.S. A. , Vol. 50, No. 2, pp. 217- 322. Tocher, Don and William Quaide (1960), Report on Earthquake Hazards at the i Bodega Bay Power Plant Site, Pacific Gas and Electric Company, Typewritten Manuscript. I , Whitten, C. A. (1955), Measurements of Earth Movements in California, Chapter 8, Bull.171, Division of Mines, State of California, Earth- l quakes in Kern County, California During 1952, pp. 75-80.- ! Wilt, James W. (1958), Measured Movement Along the Surface Trace of an Acti,ve s Thrust Fault in the Buena Vista Hills, Kern County, California, , B. S . ' . A . , Vol . 4 8, pp. 16 9-17 6. l J Wood, Harry O. (1955), The 1857 Earthquake in California, B.S.S.A., Vol. 45, No.1, pp. 47-67. f 1 l t
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BEFORE THE UNITED STATES ' ATOMIC ENERGY COMMISSION In the Matter of PACIFIC GAS Docket No. 50-205 AND ELECTRIC COMPANY Amendment No. 4-l- Now comes PACIPIC GAS AND ELECTRIC COMPANY (the l Company) and amends its above-numbered application by submitting i herewith Amendment No. 14 This amendment sets forth further details with regard to the earthquake design criteria for Unit No. l'of the Company's Bodega Bay Atomic Park and supersedes the material set forth on page 8 of Section V of the Preliminary Hazards Summary Report (PHSR), paragraph 21 of' Amendment No. 2 I to the application, and paragraphs 2 and 3a of Part III of Amend-ment No. 3 to the application. The Company has established earthquake design criteria for the Unit based upon the recommendations of Dr. George W. Housner. In general, the usual methods of earthquake resistant' design will be followed except that the lateral-force factor i which will be assumed as a basis for designing e g critical-g g,j structure, equipment or system will vary with the natural-period
', and damping characteristics of the particular structure, equip-ment, or system, ( "" M # "' b The earthquake design criteria for all critical ,jg j e g structures, equipment and systems are based on the maximum t YA
*C credible earthquake ground motion on the_ granite _ at Bodega Head .
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'[,1.AssetforthinthePHSR,thisisequalinintensitytothe ;
j ground motion recorded on deep alluylum,at El Centro, California, e' k- on May 18, 1940, which had a maximum acceleration of 33% of j I gravity. (Thisisestimatedtobeoneandone-halftimesthe intensityofthe1906SanFranciscoearthquakeatBodegaHead) l The specific earthquake ground motions upon which the { design of critical structures, equipment, and systems will be ]
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' ; based are, for acceleration, the spectra shown in Figure 10, i ]
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-! Appendix V, of the PHSR, converted for the maximum credible l
4 earthquake ground motion at Bodega Head by multiplying by 2.7. The corresponding velocity and displacement spectra are obtained by multiplying the acceleration spectra by T/2 pi and T 274p12 , respectively. (T : natural period.) Stress levels to be used ) in design will conform, where applicable, to the ASME Boiler and Pressure Vessel Code, Section VIII, including applicable nuclear code cases, the ASA Code for Pressure Piping, and the Uniform Building Code of the International Conference of Build-ing Officials, 1961 Edition (except that the usual one-third IW , allowable over-stress for structures during earthquakes will not be applied). The above design will be based on the following l 2
t I s I damping factors: Structure % of Critica? Damping Steel frame structures 2.5 l Reinforced concrete frame structures 4.5 Reactor structure (See attached curve)
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j ,,,,4v In the event of earthquake ground motion equivalent 1 d k to 66% of gravity critical, equipment and systems will be capable of bringing the Unit to a safe shutdown. For example,
, ,'s' Q' Il' particular items of equipment important to safety shall be
( . A b designed to withstand such earthquake ground motion without l 3, , jt f"fi s-deflection or distortion which would impair their functioning. 4, u. - Critical structures (referred to as Class 1 Struc-tures in Appendix V to the PHSR) include the reactor containment structure, reactor refueling building, control building, and ventilation stack. Critical equipment and systems include the nuclear steam supply system inside containment, isolation valves, liquid poison system, emergency cooling systems, emergency electrical power system, and the necessary associated instrumentation and controls. All noncritical structures, equipment, and systems l will be designed in accordance with applicable Company seismic l l 3 1 1 l l l
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. design practices.
Subscribed in San Francisco, California, this 9th 1 day of August, 1963 . l Respectfully submitted, PACIFIC GAS AND ELECTRIC COMPAFI By Robert H. Gerdes ! President i l RICHARD H. PETERSON I FREDERICK W. MIEIJ{E, JR. l PHILIP A. CRANE, JR. J Attorneys for Pacific Gas and Electric Company By Philip A. Crane, Jr. Subscribed and sworn to before me l this 9th day of August, 1963 RITA J. GREEN (SEAL) Rita J. Green, Notary Public in and for the City and County of San Francisco, State of California My Commission Expires July 16, 1967. 14 1 l I
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DR AWING hiU M B( H Daft .. f OK mtN' m $ f sts
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R. Xavenstein, Director .... . ..:A U G 5 1963 ; ) Division of Licensing & Regnistion d;I, - ?, ; R. L. Price M 8' L. Prie, by. I Director of Reguistion {/. j paEpAIATION FOR BODEGA EIAD urAR M.' i f 9 4 I have en my desk a draft hasards analysis on the l Bodega Esad case dated June 21, 1963. It uses up l 56 pages. i {_. Without projedice to any changes that may need to be made in this draft I went you to have prepared p
-JJ a separate saneary statanant which deals with the-
$% merits of this case la the manner described in the Q 11 censing board precedures disenssed with the licensing M... board panel at the recent meeting. ,
. .a - :- What the Commission wants from the boards is very i '
elear en this point, but there is no hope that the P~d licensing boards can, as a practical matter, carry M ' est the Commission's wishes unless the staff work puts them in an easy position to do se.. gg - W W Preparation of a safety analysis along the lines . N.. described above should be began ismiediately so that k;58 it will be ready in sugle time for the hearing. F~i Q' por your guidance, I enclose a rough outline prepared F '.'. by Dr. Beck of the basic elements to be considered in .s this case, sad at least some, or most, of the judgment ~ positions we must support. What we eventually decide J to say on earthquakes een very logically follow the - treatment of the itens contained herein.
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Enclosure:
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