ML19291B947
| ML19291B947 | |
| Person / Time | |
|---|---|
| Site: | Berkeley Research Reactor |
| Issue date: | 12/11/1979 |
| From: | Baldwin W, Martino I FRIENDS OF THE EARTH |
| To: | Harold Denton Office of Nuclear Reactor Regulation |
| References | |
| NUDOCS 7912140425 | |
| Download: ML19291B947 (21) | |
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FRIENDS OF THE EARTH 124 SPEAR SAN EnANctsco CAuronNr s 941o5 415;495-4770 December 11, 1979 Dr. Harold Denton Director of Nuclear Reactor Regulation, U.S. Nuclear Regulatory Commission Washington, D.C. 20555 RE: TRIGA Reactor; University of California, Berkeley Docket NO. 50-224
Dear Dr. Denton,
.
Pursuant to 10 C.F.R. Section 2.206, Friends of the Earth hereby files a Request for Action to *he Nuclear Regulatory Commission. Specifically, Friends of the Eal':5 requests that the Nuclear Regulatory Commission order the foll.owing:
- 1. Suspension of all activities under Docket NO. 50-224 at Etcheverry Hall, University of California, Berkeley;
- 2. Removal of all plutonium and all other radioactive materials and wastes from the Etcheverry Hall site;
- 3. Permanent revocation of the Regents of ,the University of California's operating license under Docket NO. 50-224;
- 4. Holding of public hearings in the City of Berkeley before any reactor operation is resumed.
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. I. INTRODUCTION On August 10, 1966, the TRIGA Mark Three pool-type nuclear reactor achieved critical fuel loading after the Regents of the University of California were granted an operating license by the Atomic Energy Commission. The University research reactor operates at a steady power of 1.0 megawatt, and'is capable of a peak pulsed-power of about 2,000 megawatts. The reactor is located in a large laboratory beneath the patio adjacent to Etcheverry Hall on the Berkeley campus. Directly above the reactor is a campus patio and volleyball court. The reactor's cooling water and ventilation sys-tems flow through Etcheverry Hall, a six-story structure. Exhaust - from the reactor is also released on'the patio level. The Etcheverry Hall-reactor complex occupies about one-half of the city block on which it is located. Directly south of the reactor lies the University campus. Surrounding the reactor on three sides, to the north, east, and west, is one of the more densely populated neighborhoods in Berkeley, consisting of a large student population and many multi-unit residential dwellings. In the same city block as the reactor are several restaurants, small shops, a grocery store, and other businesses. The southeast corner of the block is a busy intersection where Hearst and Euclid avenues cross at the North Gate of the campus. This Request for Action is based upon the following consi-derations: (1) the reactor's seismic design is inadequate according to current seismological data and analysis; (! ' the potential threat to public health and safety posed by the reactor is greater than previously estimated; and (3) evacuation plans, in the event of a reactivity accident and/or natural disaster at the reactor site, are inadequate considering the reactor's site in a densely populated urban area. 1582 002
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. , t II. INADEQUATE SEISMIC DESIGN The .nain surface trace of the Hayward fault is roughly 40 yards from the reactor site.1 Hayward fault is an active, right-lateral strike-slip fault. According to U.S. Geological Survey analysis, the active zone of the fault extends out about 300 feet on either side of the main surface fault trace. This active fault zone represents the area in which ground surface ruptures may occur in an earthquake generated by the fault system. This may be a conservative estimate, for data gathered from worldwide studies indicates that the maximum zone width for strike-slip faults may be much greater, capable of producing surface faults in a zone as wide as 3,000 feet.2 . When the original Safety Analysis Report for the reactor was written, the main trace of Hayward fault was thought to lie within 300 to 1,000 feet east of the reactor. Current fieldwork and analysis by U.S. Geological Survey and the University itself has shown that the main fault trace is, in fact, about 40 yards east of the reactor site. The reactor therefore lies within the active surface rupture zone of the Hayward fault. There is also a newly discovered surface. fault trace within the active zone which runs directly under the reactor. This fault trace is estimated as having been inactive for 100,000 years, and it runs parallel to the presently active trace.3 The seismology section of the 1964 Safety Analysis Report states that Berkeley is relatively free of earthquake damage. To
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quote the S.A.R.; ...no locally severely damaging earthquake has ever been recorded in Berkeley."4This statement is misleading. The last large earthquake produced by the Hayward fault was in 1868, estimated at a 7 1/2 Richter magnitude.$ N o severe damage to man-made structures occurred in Berkeley as a result of that quake for the obvious reason that in 1868, the University campus had not been built, and Berkeley at that time was a sparsely populated rural area. The 1868 quake caused surface fault displacement in the Berkeley hills area, and damage to structures due to the 1868 quake was re-corded as far away as Santa Rosa, Sacramento, and Santa Cruz. 1582 003
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_3 Damage was' extensive in San Francisco, and in Hayward many buildings were completely demolished.6 The Safety Analysis Report relies on " good building design and construction" to insure protection of the reactor structure in the event of a large earthquake. Current seismological analysis of the potential magnitude, ground acceleration, and ground surface rupture which could result from an earthquake generated by Hayward fault have now rendered the 1964 estimates used for design and building of the reactor complex obsolete. A. RICHTER MAGNITUDE The U.S. Geological Survey now estimates that an earthquake
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generated by the Hayward fault could reach a Richter magnitude of 7.5 to S.5.7 B. GROUND ACCELERATION The reactor was designed to withstand a horizontal ground acceleration of 0.2 g, and in critical areas (areas in which a failure could cause a loss of pool water) the design was calculated to with-stand a force of 0.3 g.8The firm of Holmes and Narver, which designed and built the reactor structure, state that a vertical acceleration of 0.25 g would cause "...(a) considerable quantity of water (to) be ejected from the reactor pool".9 The AEC reviewed the TRIGA design in 1965 and concluded that the facility would be damaged if subjected to earthquake forces of .5 g:
"(we) have been advised that an earthquake with a maximum ground acceleration of 0.5 g might be ex-pected to occur during the lifetime of the facility and that the possibility of shear displacement at the reactor location cannot be disregarded. Accordingly, we have evaluated the possible consequences of an earthquake with these maximum effects, and have con-
- cluded that while certain parts of the reactor fa-cility may reach or exceed yield point stresses, it is unlikely that the stresses produced by ground vibrations would be sufficient to rupture the reactor structuyg or pool tank. Thus, core meltdown would not occur.
I; is obvious that the reactor structure was neither designed nor built to withstand the stress that may occur at the reactor site. According to seismology Professor James N. Brune, for earthquakes 1582 004
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of a magnitude 7 or more, "we do not have a sufficient data base nor physical understanding to predict ground accelerations very near fault breaks (less than 10 kilmetres distance) with confidence. But available data and physical understanding indicate that accele-rations of greater than 2 g are possible, and accelerations of greater than 1 g may be common."11 Accelerations far in excess of .5 g have been recorded during several recent earthquakes:
- 1. The 1971 San Fernando earthquake, magnitude 6.6, recorded 1.25 g horizontal at a distance of 8 km (approximately 5 miles) from the epicenter;
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- 2. The April 6, 1977 earthquake in Iran, magnitude 5.5, recorded .95 g and 1.08 g, vertical and horizontal com-ponents respectively;
- 3. The recent October 15, 1979 Imperial Va] ley earthquake, magnitude 6.4, recorded .81 g horizontal acceleration and 1.74 g vertical acceleration 26 km (20 miles) from the epicenter.
All three of these earthquakes were smaller than what we may expect from the Hayward fault. All three acceleration measurements were taken farther from the epicenter than the 40 yards from the Hayward fault to the TRIGA. Nevertheless, all three earthquakes produced accelerations far greater than the .5 g which is expected to damage the TRIGA. C. GROUND SUFFACE RUFTURE Although the TRIGA is within the rupture zone of the Hayward
, fault, the Safety Analysis Report ignores the possibility of ground surface rupture near or directly beneath the reactor.
According to most structural engineers, it is impossible to design a structure to resist the effects of surface rupture. The U.S. Geological Survey's 1974 analysis of this danger has been clearly stated:
"Another major earthquake originating in the Hayward or Calaveras fault zones is almost a certainty. If it is accompanied by surface rupture in the fault zone in a built-up area, the damage caused by shearing of struc-tures directly on the line of rupture would no doubt be very great, in addition to the damage caused throughout the San Francisco Bay area by shaking."12 1582 005
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The U.S. Geological Survey calculates that ground rupture - of as much as 30 feet is possible in a magnitude 8 earthquake on a strike-slip fault such as the Hayward fault.13 Contrast in this regard the design calculations of the U.C. Nuclear Engineering Depart-ment that the maximum amplitude of motion of the reactor core in an earthquake coulm . no more than 3 inches! 14 A map produced by the U.S. Geol-ogical Survey l5 takes into ac-count 3 active fault systems (the Hayward, San Andreas, and Calaveras) which are expected to cause damage in this area. The reactor is mapped as within " Zone A" intensity. " Zone A" is the highest damage rating represented, and is defined as "very violent", comprising the " rending and shearing of rock masses, earth, turf, and all structures along . the line of faulting; the fall of rock from mountainsides; numerous landslides of great magnitude; consistent, deep, and extended fis-suring in natural earth." Therefore the complete destruction of the TRIGA and its sur-rounding structures appears to be a certainty in a major earthquake along the Hayward fault in Berkeley. The earthquake could collapse the entire concrete shield structure (the patio and the volleyball court) above the reactor. Giant chunks of concrete and other debris would fall onto the reactor core, crushing the' fuel elements and causing leakage of core materials from the building, and the possibi-lity of a landslide beginning underneath the structure itself cannot be ignored. D. ETCHEVERRY HALL No mention is made of the seismic design estimates used for Etcheverry Hall in the Safety Analysis Report. Since pool water is recycled through Etcheverry Hall and the reactor's ventilation system is also dependent upon that structure, it is apparent that the safety
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of the TRIGA depends on the seismic stability of Etcheverry Hall. III. A LOSS OF COOLANT ACCIDENT AT THE TRIGA It is an accepted medical fact that radiation causes cancer in humans. Doses of ionizing radiation can cause leukemia 5 years 1582 006
, after exposure; cancer, 12 to 40 years later; and genetic diseases and abnormalities in future generations. Most researchers believe that even the smallest doses can cause cancer and genetic defects. Fetuses, infants, and young children are the most sensitive to radiation. The TRIGA is small in comparison to a nuclear power plant. It contains, however, a huge amount of radioactive materials. These could be released into the densely populated environment of the East Bay if an earthquake damaged or destroyed the reactor and its con-tainment structures. Contained in the reactor core are at least 10 grams of plutonium, and an estimated 250 grams of total radioactive
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waste products, of which 14.5 grams are strontium-90. The amounts of radioactive strontium and cesium in the TRIGA are approximately as much as was released by the 1945 Hiroshima bomb. Release of core materials via any possible route from the reactor structure has lethal implications for the people of the Berkeley community surrounding the reactor site. Plutonium could be transported by atmospheric currents and be inhaled, lodging in the lungs. It is generally accepted that one millionth of one gram of plutonium can cause lung cancer. Once deposited.in the lungs, smaller particles may break away to be absorbed into the bloodstream. Because plutonium is chemically similar to iron, it is combined with the iron-transporting proteins in the blood and conveyed to iron storage cells in the liver and bone marrow, inducing liver and bone cancer and leukemia. Plutonium can also cross the placental barrier, reaching a developing fetus. Plutonium is concentrated by the testicles and ovaries, where it causes cancer and genetic mutations. Once released into the atmosphere, plutonium enters the food chain. Plutonium-239 has a half-life of 24,000 years. Decay to safe levels will take as much as ten half-lives, or 240,000 years (10,000 human generations). Strontium-90 has a half life of 28 years, and cesium has a half-life of 33 years. Once released, strontium and cesium remain dangerous for several hundred years. Strontium-90, like calcium, is absorbed into the bone structure, inducing bone cancer. Cesium is concentrated in the reproductive organs and muscles of the human body. 1SS2 007
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IV. EMERGENCY REPONSES TO A TRIGA ACCIDENT Following a major earthquake on the Hayward fault, all roads in the vicinity of the reactor would be blocked with debris. All emergency vehicles and personnel would be immoblized. A substantial proportion of the nearby population would be injured. Immediate
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evacuation of the area would be impossible. V. CONCLUSION The NRC's continued licensing of the TRIGA reactor in the
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middle of a densely populated urban area is irresponsible. The reactor presents an extremely high risk to public health and safety. The reactor's site in the active zone of the Hayward fault and the outdated seismic design of the reactor's protective structures makes possible a serious radiation accident. The inevitable result of such accidents is generous public exposure to radiation, causing cancer, mutations and birth defects for years to come, and possible permanent evacuation of what is presently much of the University campus and the city of Berkeley.
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The reactor, operating at its present location, poses a clearly unacceptable threat to public health and safety. VI. RELIEF REQUESTED
- 1. Suspension of all activities under Docket NO. 50-224 at Etcheverry Hall, University of California, Berkeley;
- 2. Removal of all plutonium and all other radioactive materials and wastes from the Etcheverry Hall site;
- 3. Permanent revocation of the Regents of the University of California's operating license under Docket NO. 50-224;
- 4. Holding of public hearings in the City of Berkeley before any reactor operation is resumed.
Respectfull submitted,
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< Ilene Martino,~ Legal Assistant Fpi4hds of he Earth g g', g 1582 008 W. Andrew Baldwin, Legal Director Friends of the Earth
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REFERENCES CITED IN THE TEXT
- 1. " Map Showing Recently Active Breaks Along the Hayward Fault Zone and the Southern Part of the Calaveras Fault Zone, California";
1974 U.S. Geological Survey, Map I-813; by D.H. Radbruch-Hall.
- 2. " Studies for Seismic Zonation of the San Francisco Bay Region";1975 Geological Survey Professional Paper 941-A; p. A-25.
- 3. " Area Fault Map, University of California, Berkeley Fault Hazard";
1978; by Ben Lennert and Associates.
- 4. 1964 Safety Analysis Report; p. 1-12
- 5. " Studies for Seismic Zonation of the San Francisco Bay Region";1975 Geological Survey Professional Paper 941-A; p. All.
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- 6. " Hap Showing Recently Active Breaks along the Hayward Fault Zone and the Southern Part of the Calaveras Fault Zone, California";
1974 U.S. Geological Survey, Map I-813; by D.H. Radbruch-Hall.
- 7. " Predictions of Maximum Earthquake Intensity in the San Francisco Bay Region, California, for Large Earthquakes on the San Andreas and Hayward Faults'; accompanying Map MF-709; 1975 U.S. Geological Survey; p.2.
- 8. August 20, 1964 Letter to Mr. R. Silver, AEC, from Hans Mark, Chair-man of UCB Nuclear Engineering Department.
- 9. September 12, 1964 Letter to Mr. R.H. Peters, General Dynamic Cor-poration, General Atomic Division, from Holmes and Narver; signed R.R. Alvy, Chief Engineer.
- 10. Hazards Analysis by Test and Power Reactor Safety Branch Division of Reactor Licensing; January 13, 1965; p. 3.
- 11. April 6, 1979 Letter to Mr. John Farmakides of the U.S. DOE from Dr. James Brune, Professor of Geophysics, Institute of Geo-physics and Planetary Physics, Scripps Institution of Oceanography.
- 12. U.S. Geological Survey Map I-813; 1974.
- 13. U.S. Geological Survey Professional Paper 941-A; 1975; p.A-30.
- 14. August 20, 1964 Letter to Mr. R. Silver, AEC, from Hans Mark, Chair-man of UCB Nuclear Engineering Department.
- 15. U.S. Geological Survey Map MF-709; 1975.
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%b 1 STUDIES FOR SEISMIC ZONATION A25 that at least locally extended as far as 1 km to several geomorphic features (controlled largely by climate a,nd kilometres (thousands of feet to several miles) from the local geology and topography). Recent fault traces along main fault (Lawson and others,1908). Data from this strike-slip faults such as the San Andreas can be map-and numerous other historic faulting events in the ped more confidently than those on faults with dip-slip world give a basis for estimating the location, character, movement. Consequently, dip-slip faults with youthful and maximum amount of ground deformation along movement are only now being recognized in regions many of the faults in the San Francisco Bay region. where active strike-slip faults have long been known.
Of principal concern in fault-related ground deforma- . tion are (1) detailed prediction of the pattern of surface ZONE WIDTH faulting, especially the width of the zone,(2) the amount Although the most obvious fault displacement tends of displacement across the surface traces of faults, and to be localized along recognizable and mappable fault (3) tectome distortion of the ground, including uplift, lineaments, some permanent ground deformation from subsidence, and horizontal distortion, fault movement extends outward from the main fault trace. This deformation, manifested as fractures, PA'ITERN OF SURFACE FAULTING relatively small surface faults, and local warping, , The pattern of surface faulting, especially along the defines an irregular zone that parallels and includes the strike-slip faults, involves a main fault zone of varying more obvious and more continuous traces of the main but generally narrow width along which the principal fault. offsets occur and lesser branch and secondary faults The width of this zone of surface deformation varies that extend to, or occur at, considerable distance from with the type of faulting, earthquake magnitude, the the main zone (figs.12,15). Reverse faults commonly local geologic setting, and perhaps other factors. An produce more complex rupture zones, and the zones example of this variation for strike-slip faulting typically are broader and less regular in plan (fig.16). associated with the Borrego Mountain earthquake is Major displacements can be expected along linea- shown in table 3 (Clark,1972). Because the zone width ments defined by recognizable fault-caused topographic is so variable and because it seldom can be well defined features (figs.12,15). Studies of severni surface faulting by surface morphology prior to a major fault event, events indicate that historic ground ruptures closely detailed site studies are usually required for accurate follow mappable geomorphic features that delineate delineationof the zone. Such detailed site information preexisting farit traces (1857 Fort Tejon-Wallace, is not yet widely avail *able. In its absence, estimated 1968; 1906 San Francisco-Lawson and others,1908, zone widths are often based on comparison with known Wallace, 1969; 1966 Parkfield-Brown and Vedder, patterns of deformation associated with well-1967; 1968 Borrego Mountain-Clark and others,1972, documented modern fault geometry accoinpanying Clark,1972; 1971 San Fernando-Yerkes and others, major earthquakes. 1974; 1973 Managua- Brown and others,1973); these Data on zone widths for North American earthquakes observations suggest that patterns of surface faulting in the magnitude range from 5.5 to about 8.5 were are predictable. Clark (1972) estimated, for example, analyzed by Bonilla (1970). The data are sparse because that along about 50 percent of the length of the surface only a few events are well documented, but they rupture from the Borrego Mountain earthquake of indicate the general range in width of zones that can be 1968, the position of the main surface fractures could anticipated. _For strike-slip faults, the maximum half-have been predicted to within about 100 m (300 ft) width of the zone, from the centerline of the main lault before the earthquake. In the San 1 rancisco Bay region, zone to the outer edge of the Mnrmation zone,is about the San Andreas, Hayward, Concord. Antioch, and a few 92 m (300 ft). For dio-alio faults the zone is as much as_ other faults are mapped in sufficient detail to accurately 900 m (3.000 ft). These values are probably conservative show the location of fault traces and of the expected estimates except for very large eart.iauakes. They have future displacements (Brown and Wolfe.1972; Brown, been suggested as the basis for some kinds of planning 1972; Radbruch,1968a; McLaughlin,1971; Sharp, decisions (B rown,1972; Hall and others,1974), but they 1973, Burke and Helley,1973). Much of this map should be used cautiously and where possible should be information is adequate to influence decisions on supplemented by site investigations. Some evidence structural design and land use. from studies of worldwide data suggests that maximum' ,/ The confidence with which surface traces can be zone width for strike-slip faults may be signincantly mapped at a scale of 1:24,000 (1 cm=240 m; 1 greater than that cited above and that deformation inch =2,000 feet) varies considerably depending on fre- zones of strike-slin faulta may be as wide as those quency and amount of Quarternary displacement, the associated with dip-slip faults (U.S. Geological Survey, style of fault movement, and rate of destruction of 1971b, p. A169). . 1582 011
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maximum values to the local damage from earthquakes assigns a
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modified Mercalli index of- VII to VIII to Serkeley while the town of Hayward (lying about 17 miles to the southeast from Berkeley) has a value of IX. The value of IX is also assigned to the low lying filled ground in the northeastern part of San Francisco where the major damage during the 1906 San Francisco earthquake cccurred. The hill area of San Ir,ancisco, where the
' age was much less severe, has a value of VIII. During the San Francisco earthquake of 1906, Eerkeley received only modest ,
damage even though most Berkeley buildings were then not con-structed with earthquake resistance in mind. Modern earthquake resistant design favors basing a building' resistance to horinontal loads on the larzest expected local earthquake damage. rather than a frequency vs. magnitude, risk acceptance concept. For California cities, this frequency is
- i higher than for many other states, but th Expected maximum values are not.. Based on actual local damage experienced during.
earthquakes in historical times, the fcilowing major cities also are rated VIII: Buffalo, New York City, Washington D.C., Chicago, Tulsa, Seattle, Portland, San Diego and the San Francisc. hill areas. It is interesting to noto that cities considered by Richter to be eligible for the higher value of IX local damage
. are.Charlesten South Carolina, Long Island towns, Kansas City, Los Angeles, and the San Francisco filled areas. 4 -
Although ,n ice'lly severely damaging earthquakethks ever /
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been recorded in Berkeley, its proximity to the cities of N
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*The meaning of the Modified Mercalli indices is given in Richter' article. but is best outlined in TID 7024, pp.63-70.
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?00R OR80 Er STUDIES FOR SEISMIC ZONATION All Quaternary displacement Additenal factors for asecoming earthquase potentie.
Quaternary displacement Estimated recurrenew ' Total known tault interval Im yearsi for length un kilometress Present abdity to maximum eartaquame. Magnitude of larunt vestimate of er.asimurn predict pattern of haasone earthquake Commenta Offset Quaternary miermd from geologit magnitude earthquake surface faulting deposita slip rate' m parentheses" Yes inee Cummings 100-1 A0 6.3 see tawson and 1.20018v Generally . locally Rur%t. lateral stnkwlip i 1964 n. tfor magnatude 7 6e a otners i190s.i a,a verv Tauit, maaunum displacement in 1906.6 m _ (20 th Yee . . 10.;00 72's ince Slemmons 72 i7 On i f Generally good, locally
'for magnitude 6-71 i1%7as. very good.
1 Yes iR. D. Brown and E. J. . S 7 esce McEvilly t1970 5).* 72 i7 0 Generally good, locally Helley aunpub. datan. e very good. R9ht lateral etnke-elip 163 17 5, inulta. Nane observed .. .... .. 3-4 inee Lee and 35 <6 6, taally very good, others i1972a.b.ci; abundant avidence. = Weemon and others faust not well mapped i!972a.b: 1973o None observed . None known* 13 e'e termily verv anod Fault
/ ( not well mapped.
Yes iR McLaughlm None knownas . 64 Locally verv good unpub datan. Yes 10 100 6 115 iHoll.ater to Generally sir. lacally i
'for magnstisde 6.7 San Ramoni 6 7 3: sery goua to very pnor Yes ece Gibom and 4 3 6ece lee and 9 t?i ....-...........
Wodenberg e lvbe others 1971 ** Rm.austa North =srdht lateral strike lip 5 4 <=ce sharp i1973t > estensen of Green Va;tey None ob.erved . l's i? locally very good. goanie. Ernen and Cloud 22 includen etterteson il957n
- acrwe Cargumes atraits.,6 31 Yrs .M G liondia and 2-3 esce Ise and 34 66 61 cally very good. /
C. M. Wentworth others f 1972a,b.c t tunpua. data t Weaaon and others Daview s1973a
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i1972a.b; 1973 m* 4-5.on anna ble northward entension ilt 1 Weeson sunpub data.it Yee esee Fos and 2-3 inee tae and others If <?1 her. othervil973,. E.J Helley < 1972a.1: cr. sunpun datan. Waason and others
- il972a b 1973m*
Yesime Dibblee . .. . 3 5 iR L Weeson and 20 am nimum estimates l'nor Northward entenamn i nw?24.o.c o. others t unpub. data a
- i6.2 tower's San Jose not meil knoen.
Yes . . Not known s2 47.4i Poor. 200 emcludes Yes isee Greene and 61 <*ee Richter s 195M
- ia 135 (7 4 e pasu inie north- Inally very good. R.gtit. lateral strike 4tip othere i 1973 *; ward entennion lault. Southward Brabb a 19706 to ban Andreas s tiensen.
fault, ennnect. Yn esce Jack e 196Mt . . . None knownia . 3 i?) ing at Dolmass tecalty very good. Cooper i1971 a; K. R tene. <7 6W J. Tmalev. and G Weber innpup. datait Yes sere Cummmgs None knownia . .. .. 43 e6.7i .............. t Db8 9. Yes sere Greene and 6.1 isee Rrhter t1958 a.*.i* 42 lacross entire boys t6 71 .............. Southward entension on others 1973m shore probable. Yn. Mct.aughlm . . $ 0 <see %: Evilly 11966 m* 96 iPortola Vallev to Steep southiseetdepping i1973 m Hollisters si 4i right-lateral fmuit up on 33 < Mount Madonna to locally good. touthwest side. dip Hollistere i6.7i decreases te northwest. SS iLake Eleman to Hollisteri < 6 9e Yeaisse Dibblee 1966c. . . 3 6 i ee I,e and 31 'Portata s nuev to t'nor Westward 4ippmg thrust Pampeysa il370s others t1972n
- tes Gate 6* fault.
R. McLaughlin iumpub. data o. Yn a J. Melaughlm and . . . 4 5'(R. L Weeson 33 ilee Catne le Pnor Westward 4ippmg thrust D. Sorg sunpub. datan. s unpub. data n.* Mount Madonnae i6 7e feu4t. Yes suis Banalla 11965e . None knownia 4 i'i Very gond. Westwarddippeg thrust ta ust. Pose.ely . . 2-3 sees t,e and 14i? 1%nr
- others il9724.b.cn Wesena and others a 1972a.b.1973 a. *
*/
1582 04ta Yen nose Reiche (1960iA .... None known's . 5 i'l Pnne Nolonger espnaed.buned by dredged matenal. Yee some Burke and . . . 4 9 iese McEvilly and 14<?i lecally wry good. R $ ht-lateral stnke.alip Helley 41973* Canadav i twt 7 e 37 uncludmg en echeson fault laps earthqueW. n.atewerd esienname
.
-- __ _s . _ , .__---- -
--n. = _ - - - - _ _ - __ .
e'as a ryar$up esame where they cross the W
- Ng* maceq4g . s . . , -
p9 a fantas are also known, Dist histencaay these p ** *
- pend to naht shp. -
. * .
,
0F FAULT BREAKS 'N
'
M4 ,,
+ 4..
on thu map were located by laterpretation 5
- g _ ,j ! ,
,,'1 ,,
+
--..(***'**9
'
ivesugation.enammanos of histencai recosda
'
C",**" ,I.r
.ad fross the work of othee mvesugatort Traces a the Oakland East quadrangle, from Know-vensty of Cahfornia titnpa A and 8), were
, k L -- N '
a I, I D.
*
/
.
Da ., V N, J' Traces between the Unrwrsity of Cahf arsua p Ak are pnmanly from a mesis by Case 1963h [' , e'
.
[N f esamanaues of senal photographs and field se ce csiy offlaats of Berkeley and El Cerntix
!
'k ( ' . ..' .)\w'.
-
'
est of me Calaveras fault zone from south of d { "" pe Lake (stap C) are from maps, by as. N $\, r es most conspiceous and topographcally C di S r,e a sown between San Febpe Lake and isi1%7b) han mapped numerous addinonal
. ,, hJf s
shows from San Febps Valley to the Calaverne Some of the fault traces which have been recoemzed (many more probably amat) mark the posanon of surface pipture at the tune of the 1368 earthquake;
;3p y ifromCntienden(1951L Data from the reested by the study of aenal photographs. chrs, lake $e m smmediately southwest of the Oak KnoQ hlaval HostMial, seem ,
at of the Calaveras fault tone, from San fehpe to be the result of much cartner movement. In 1964 an escavation along the fault 63 Valley 4smps E Gt, were located by meerpretation trace northwest of the hospital exposed a peat bog that fhied a depresson which {Q \,, 4 by onahe-ervund observation of phystographic probably was an old ug pond. The remams of alate Flentocene bison were found \ reasurci as esposed gouge zones;no systemaue la the peat,whach andwates that the depression was formed,probably by fault \ M fr
,,g,, * ""'* Pnor tolate P!eistoceu ume.addiisonal movement may or may not W8 we and propetuun was used to transter hnes ta e p me unce n. ement a Hayward fauh am has appaready \v m the office or used fot compdmg data m the e et onaontalan wnscal ymmes accounu of the 1868 eanhquake p' 3, os the topographas base maps are generally desenbe wencal mumas along the fault rop (Lawson,1908, p. 433,443,447,
-t, bot may be as mush as 130 feet off where ar , ,A1 omag data also imply verocal movement. Where
,smaB4cale fault features. Geologists and me Hayward fault am bes at me baW W Berkeley h the steep Mstward.
f thens maps should confirra the location of facing fr at of the hdis appears to be a dassected fault scarp tBewalda.1929, p. (90A a control points on the ground and shotdd then & knnmg e appandy wed upward M mW M those epropnate means whether they are truly the west of the scarp. South of redes. an eastward-faang fault scarp can tie seen south-test of Tule Pond and Suvers Lagoon IGark,1924), mdwaims that 46ong this streich the west side of a fault has moved up relauve to the east ude, whereas m ATING RECENT FAULT BREAES the wKtasty of Irvington a westward-facmg scarp ind6 cates the revene. OtYset
- as faust tone =sa the cause of the catasiropNc 'ucama, usa as Strawberry Creek on the campus of the Umveruty of C4fomia
. Sudden movement along the Hav=ard faalt 18u*4 AM p.1941and numerous nalloffset ravmes hetween Haywerd and
< curred a 1336 and asaan m I868. Both move, Niles tRusseu,1926 p. S0d A indgate that gLojvement As.g,h_ faults has3 2akes;in 1%8 most buildings la Hayward were e lateral,that is, rocks on the northeast uJe of the faults have moved southeast
.cd (Lawson,1908). Old records moscate ha mth se. I to most a h sou$ west ude, a fault gone north of the Calaveras Reservoer gement alone fautes et Nn the Hay werd fault zone has cauwd two msg e carthquake m 186 5 (Radbruch,1968, p. 5 2-53 k . #,rw earthquates with accornpanying surf ace rupture, one m 1536 and one,tn
~
tg the San Andreas fault gone near Hofhster is O aJalas sa acuve fault is t*te fault tone (Tocher, smrallocaun of surface breakase recorded dunns earthquakes ortsmat.
. along the San Andreas fault tone between mg withse the fault tone is fairly weu k news, but uformanon regarding the direc.
j by the deformance of fences and by the te. tion and magmtude of displacement is scanty, a paved roads awe and Wanace,1968 A arr4hete of 1836. - % 1836 earthquake a thought to have had aa latensty fault goes is dislocaans radroad tracks, a culwrt, of X on the Rossi-Forel scale (Lawson,1908; Louderbs6k,1947k Howe.er, the
$ buddings aRadbruch, Bondia, and others, IM6; area su sparsely populated at the uru, and httle evidence a avadabie regardug 1swalks, walls, and buddmss are being of fact in either the kmd or amount of damage to manmade structures,or the nature o(s,ir-
.terp ia the Caiaveras fault sone (Rogers sad Nanon, face breakage associated with the quake. Cracks reportedly opened between San ing fault bleeks that are recogruzable by their Pablo and Misnon San Jose (Louderback,1947).
Earr4uske ofl%#. - N populauon along both the east and west udes of frees fault zone dunas the 1966 Parkficid<holanu San Francasco Bay had grown substannally by I863, and the earthquake of that a melkiefined fault traces aBrown and Vedder, year caused greater property damage than the one in 1836. However, very httle
' ace rupture that formed along the Hayward fault Nance agardmg surface rupture was pubbshed at t he uma of the earthquake, mpanyms map, an most places apparently followed and any that vnay have been compded at the time was subsequendy lost (Lawson, Geomorpluc studica of the San Andreas fault tone 1908, p. 434). After the 1906 earthquake, whtch ongmated on t!.e Saa Andreaa w 19681 show that displacements there have re, fault, the Cahforma Siate Earthquake Invesuganon Commuson prepared a report
, g,,ce. on Ge 1906 esame Rawson,1908L This report contams a renew of other severe
.at ruptums which form at the ume of any futurs earthquakes in the San Francisco Bay repon, including the earthquake of October axompanytag slow tectomc creep are likefy to II 1868. In the course of gathenne facts relanns to the 1365 earthquake, a re-
-ovement 11tus, the rnost recently acave breaks pin' entam of the commsen renewed penodacais of the ame, ohtamed eye-ady hazardous by budders, planners, ensneers, wimens accouais from rendents who eapenenced the shock, and vinted the ares defense officiala, and others;or by anyone can. of masamum m'ensity. The results of thn invesuganon were mcluded in the report
- ructures, land utdsauce, or planned construcuun of the 1906 earthquake and consutute the man body of pubbshed information 1:1pteaks. At present, no one can p* edict when regardmg the earthquake of 1868.
#I ase faults edt recur,or whach ones wdl move nest, Damase to strucrures due to the 1964 earequake was recorded as far sear _n ane udi move agam. It should not be tafernd, hom Rosa,ManwntAgndanta Our Dsmate = sir ermMn Francisio, Sned ennrely to these recendy active breaks or Fa Wi%a he gro%I'* aMm Hhused many buh - -y p of them. Surface fractunns may develop any. der"oi i shed. Ac6ordmg to the 1906 report,"D.e fault. trace was(flaractented for os branching or otherwise related faults b yond the most part by a crack whxh in places, parucularly on th4 tower ground.ses seines along fault traces or lHank spots eithm the suMcsady sapmg. Awared *ph ins mam crack there were austitary Dranchms it stab 6e or unfaulted segments or undisturbeJ craan.and on the alluvui bottom-lands about f an Franctsco Bay there were numer-
;they are merely pla6es where no endence for ous secondary cracks which were usuady not ducnmmated by the observers of that day from the fauP trxe* f Lasson,19n8. p 447). Accordmg to lawson i1908, warm
- p. 4341, a crack esiended from the viemity of Mdia Caliere,oakiand,io JN OF MOST RECENT FA!!I. TING Springs, but endence of t*n esterence north of San Leandro eas obscure. Loader- g faults can generaDy be recognmed by topograpNc ba6k i1937, p. 5; stated that it seems quite cenain that no rupture or the ground ,
anoe that reflect varyms ground-water depths or 1 ok place in the vicmity at the Temescal Dam (Oaklandlin 1868. However, , The most common features are riarps, trenches hht
, accordmg to Mr % alter T. 5teJberg, architect torsicommun.,19451in 1925 or ges, offset drasnase c'innnels, saa ponds, ponded 1930 Joseph LeConte, professor of mecharucas ensmeenns at the I'niverniy of "
ul shutter ndges. These features have been devel- , Cahforrua, told him that his a LeConte'st father had taken him to ace tne (ault a a repeated movements and the contmums eifects of trace of the 1868 earthquane, enKh estended across the weste'tv end of the ""U e fault. Honzontal shifts and verucal displacements Cahforma School far Blind and Deaf and along what is now Warnas Strest. or *", few feet result from successive suddea shifts accom- g between Warnne and Prospect, m Berkeley. LaConte need that he was a small boy "MW
- tervak of slow tecton c creep between ennhquakes. i at the time, and that the trace looked hke a plowed furrow. ,Jersnedtry 8 se o. their origm, the displacements pro- From San Laandro to Warm Spnvin. neveral crassa were reported. The masa usuaDy nor as en .atr if the fault traces shown on the fault trace, trending N. 37* W lay m general near the base of the hdis and ta most widuo se Hs s faup 1cate selected esamples ci these places was wthm the hdl slope, although in other places et cut acrois the edunurn raltona
,+ed ces;arndar features are present w "'I I'*#"'" -
-
. As oppoems fault blocks shde An mmens account by Mrs. Wdham Raywards igiven m the 1906 invesuga-app *
. to form sags or sag ponds, or elongate { ,est of the hills. as caemns ers vuly s n t oa reportl desenbed in detad* the course of the mam fault rup ure through"""*I crack past dissonally up the Haywards tha theI 83*"'
;Ist breaks. Other strees are raned, tdud, or shd nter of Hayward as Mio*C M
a shattet ridges;clongate borsts may be uphfted an et t m the wh com- of the old horet pasr stest east of the Odd - saches of trout sh along the fault may rettect in- ~ 'u"*nt a-h ae c--S em- < =e a-- ;"mu" sed a w sa . bro- res me s.ne ot , -, be whicti stead where the sad now is, on through Walpe t'slidl .Decotas. *By ICinff and St q-J 0l4
P00R D H" M1 -
- -
g6. 7 . at ,, etc th. -.oo.s. , 31ee < - r,r.e .1eree 4.rm .. e. E.e -re.o ,aem e.d eherdt.1970s Ctbhe and torcherde,1974). e 1 erne eseegguese se the me,werd f ault is shows se Analyste of these recordtase stems that certate sheet 1. The see eusseets that a future earthgeste ce freqJamelee of the 161w=etrete grened ettene are either cf the f ehlte cestd steee se eure demoge at
'
amplitted demelderatif s certate typee of local ettee seet distance free the f aulte se et estee 14 the
'
ette eseditions. Bereneret (19N) ehewed that spee. teSeetate tones of peteettal surf ase feuattaa. Alem tral esplificettee curves essented =tth respect to e the earthquake sacerd is met ; the esp
=1f =1e,sseeste thattatowshat the lee erencine so dt.trib.ted :
stwo medese a to mesete.tt.e intate too eetena ree ,eees a.roctw1.etre fleet of the letal restes ad that 1ersevatauan t 4 ese mehthe . ette esedittene. To teolate the dependeece of the esserted ever reist1welp short distances The esp = eteerved 1936 intensities at Leesi otte conditiosa providea settestee of eentoaa earthgsise totemotty for - the specif!s ettee showe. ! ifree the d Etate), latmier increaset e of the 1stessit tee as die. ere denhed for och
-
To c=are the tredicted lateuttlee for se arts. i et the recordieg ette.1er .e hie i anos latement, data .<ees se t se ese 4edress with the ceserve 1,0 intee-
-
.
for each ett see f table 1 cete. O and 95, two types of record. ett %et11a81e. The inteeeitV 18c r ette wee esfined as the dif ferene.resset 6 las estee were cene14.ted.
===rved latewit, and the tatmit,etweee the produced by 190* intensities reeerdl.a. Theee et the .aut,attee =1th escrined et e,tdesce t
-
e se sepitazal relagtes for ettee et the sees dis
- were considered as see sample and these with latesel.
taste et the Preacteees Foreettee (fig. 3). etes ascribed en the t.ese of *.segelvecal" evt.ence i
'
The istemetty testemente are pletted as a fuesttee were cemeteered as emet %er emple. (no intensis ' of the aversee sorteestal Spectret emellficaties values predteted free the empirical relattees heaed se .
-
(&E5A) values computed with respect to the Frametscem entf the rettable 1steesity date era pletted as a Fetentlee free tae receedings of low-otrata treed fweettee of the steerved seluos (fls. Sp.) The esae j eettee (fig. 4) (Gibbe end Sercherdt 1974). tapart. and standard aestattee of the dif ference between the E cal reist1ees were deteralmed (estag the method of ,ateelsted and ebserved walwee for the ettee with "e* ! least eewares) f ree ea17 the esta for ektee la the oestence1* evidence are 0.03 and 0. 39, respectively, , and for all ef the ettee they are 0.06 and 0.71, to- ! eity of San Freaciece fet which there weg *esquige= cal
- evidence for the degree of sectthed 1906 Lates. e,ece tvely . h seas and etandard destattee for tae .
Sit? and f ree the eeeplete date set. Se tus espirle meselste value et the dif ference between the predicted [ tal relat18ee are ela11er with inteestly lacreenste eed cheerved weless are 0.29 and 0.24 respect 1,ely, ! predicted by either telettes dif ettag by less thee for the imeewiwocal* data sad 0.50 e4e 0.43 restsc-tWe=teetha f ece flg. 4) . The espirical relettaa tivelf. Isf all tw date. The 1Mget votese fef the (f1 e 0.27 e 2.?O Les(AP5A)) based es sely the relie. seesle teclading oli et the dets are ceastetest with ble tareasitt data La Oe etty of San Franciece is the 'f act that the quality of the toteesite evidence ; preferred. The esses and steederd deviettees for IS leet for this esepte. h mese velee of 0.29 and I the standard destatten G.24 est be 1sterpreted as ta= ! the emeples are gives La table 1. The standard effet - Si tee regresetos coef f1ctest for the teatriated date 41 cat 19e of the meertaisty esteelsted with the pree dicted setenettv values et the ettes for whteh Inw.
-
set to 0.29 and for the complete data ett le 0.33. otrata esplaticettene have been esseured. The correlattee coef f talent of 0.95 casested for the preferred espirical reistles. 81 = 0.27
- 2.7g The mestam earthevose latenettles see shows se j legt4ASA). shame that a essene estrelattee calate she*E 1 for the sites et ehtch 1du-strate esplifice* r Stees esve beet 884eered. Se areal domstry of the ;
betweoe tDe eesputed 1stemetty 1screusete and the esplificatiosa eteerved at law *ettsia levels. The sitee la set suf ficieet te drew accurate femteure of PhFelsel meanlag af t&ta say1rical correlation te equal te?onetty fs r the entire egsaal however, the camelsa and does not f.ecessarily Lepit that empl1+ predicatase can be eattapelsted to a regional scale meist aestlable geolegte sata. ; Il&atione eweerved,at traseisted directi to low-etrata haga-etrate leveLe c es se levels. be e,er, es. there are two poselble teasete for tala correlattee; 3TTMITT NetM TS. leCAL GEGin1C JITS 13 fet le# ele of grened Sheblag that did Mt c ages greed f allere the mighet esplificettana'tadicate The spunto af Jamese free euserous past earth = thoet sites that espertenced the highet levela of guesee 46*e base oteerved te deseed strongly se tse greed shakleg and 2) for levele of greed ensking geologic charactet af the ground f ees Duas,1955, for e compreae=1** miteerase,s. n avestigete Em cut estad.u 1. ducethete a 1=1cete greedeues I.itere. th. := highee
.ete emot spuf,t.
e.ne - dmedence f ee the i+o ur_use. tw inteau, Elble ta st.+and ' allure. le either case, the higher terremente eseewted at each of the reeerding ettee aspitfications indicate these ettee t'iet espertenced are greersed accoretag to the type of meerif ngigee = greatet manunte of dsasse sad, hence, were assigned teent *1t (taale 1, col. 3) teee oectime se geology h1gner degrees of AstemattF. et and of report).
'he seen et the tateestty Ameressate f ar each group F3EDICTfDit or MAXIct gAgTHQUAE2 Ilfftt31TT eheme t%st a etteS$ Cetfelettee estete between the At 1FECIFIC EITES abeerved 1996 teteesittee end the type of geolagic ett. The essa Latensity 1stressets tactsese utrh de*
'
31st *1 cal 19 large earthquakes have sceurred sloeg steestag "firemees of the geoloeic mate emeweeg that La geestel the greatest ascete 2f easese, escludiat p ett the See nadreas ad hw a r d ' mu lt s 9,.t _d tee (e . g. , weemas un a e ey v D e-e= t 1 . that 14 the twdtste some af earf ate f eeltisg. eeterred on the sof test sitee. These sites are la _ e r . ort %..ee "as.n a s e. , ~-4 5 h.de- t u . e types general the eset likelf to eigetitcastly esplify or .a-t .y eaus. . tene tu.a s er fet.re enth. grond massat (settmerdt d othere.1975). la gunnes se the See Asdreas and netward femite are sto. aadittee, these attee are the met suecapttble to 11st, the etteemattes eurve let the 1904 inteesttles ground f ailure ieduced by laquef acties (Youd and f f13. 3) est be seestdered aseful fet predictieg ta. ethere . 19 731. teosities of e large earthquake se the gafwerd fosit N essee for the camplee of eesseret latessity la-as well as ese ce the $4m Andreas feuig. Seth pre. stenests cogeuted for the varieue eselegte ette
= were bene the tatsosity dictises f <fis.
ree the ne_*teneettee
.uid ie, curve
.uesfor o.th_e 190,6re to.
to. (tatie f ree au1._cel,. 3)-erdas su.d ete reseru..e of _ data que _, _aiuse et evidesee. le the eethers' opiates, as Leproved eas Foresttee, fet sites met es the Freactecan Fores, CLee, intensities res be y-edicted by e4&ag the ee= quantificattee of the Lateatty Jependetes se the pirical relattee between latematty tarrement and the geologic weit le obtataed be ceneiderlag the 1stessity Leu-et rata esplificattee (fig. 4) . Meste for each of lecteneste pt<dicted at each of the recetding sites the attee with esasured Lee" ettsin esplifiestiene ta= estag the emparttal inteestty 1serement we. sep1151te= tene t tide es_ (Mt *e* _ tlea can be1.re. predicted from 4), un_ich is .taped e es
. ce_ly those
_hg_. e. the_two
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1 _ 1582 O hr= _
. -- -_ g ._ -;1 _. IY UNIVERSITY OF CALIFORNIA BERKELEY, CALIFORNI A August 20, 1964 3r. Rot t .w . sein Divisi- Si Ci itian Application U. S. As eic '.n..cgy. Commission Washington 25, D. C. Attention: Mr. Richard Silver
Dear Mr. Silver:
The following information is supplied as Amendment No. 1 to our Applicatior. for a Construction permit Relating to a Class 104 Facil-ity License for a Nuclear Reactor at the Berkeley Campus of the University of California, Berkeley, California (Ref. Docket 50-224). As stated in the previously submitted " Reactor Safety Analysis":
"A horizontal seismic design coefficient of 0.20 g with a 33 per cent increase in allowable stresses has been adopted for the TRIGA Mark III reactor structure. In order to provide additional safety in the design of the structure as a whole, critical areas (areas in which a failure could cause a loss of water from the reactor pool) will be designed with a higher 3erizont al coef ficient of 0.30 g with a 33 per cent increase in allowable stresses."
Based on this criteria, the core and support structure have been designed to the 0.20 g value. The calculations for this condition took the following form:
- 1) The reactor tank full of water (but without the core and support structure) was analyzed to determine the response to a 0.2 g horizontal force. The result was a calculated frequency response for the tank water.
- 2) The cc re and support structure in the reactor tank (without waterj were analyzed to determine the response to a 0.2 g horizontal force. It was found that the major part of the weight acts at the lower end of the support structure with conditions approaching that of a pendulum. Damping is provided by the restraining force through the coLpling to the bridge. A frequency response was determin6 *.
- 3) The core and support structure were analyzed in the reactor tank (with water) for a coupled response. The maximum stress was calculated to be 18,400 psi. The yield stress on non-welded 6061-T6 aluminam is 35 to 40,000 psi, giving a safety factor of roughly 2 over 1582 016 s;;;g.2 7 (f ~ e?%k:,.3
$ ff ys w gld 1, .
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-__ -- __ - . . _ _ _ _ _ _ - . . . _ . _ . . -
_ . _ _ .
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Mr. Robert Lowenstein August 20, 1964 the calculated stress. The maximum amplitude of core ' motion is about 3 inchesi For your reactor conditions,' -
-tt'was concluded t~lial-~the period of the reactor core and support structure in water does not attain reso-nance with the water in motion. Even if resonance were to occur and the structure exceeded the yield stress, no f ailure would occur because as the material yields, it would relieve the stresses and unsynchronize the response of the structure with the water in the tank.
Very truly yours, Hans Mark Chairman, Department of Nuclear Engineering HM:IR:bjd State of California)
) ss.
County of Alameda ) Before me personally appeared to me known to be the person described in the above application, who signed the foregoing instrument in my presence, and made oath before me to the allegations set forth therein, on the day of , 1964. 1582 017 E
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SITE EVALUATION The " proposed site for the TRIGA Mark III reactor does not present any special problems'from a hydrological or meteorological viewpoint. However, the site is located:within several hundred feet of the Hayward Fault System and within about 20'ailes of the San Andreas Fault. / We have discussed the seismological and geological characteristics of this location with representatives of the U. S. Coast: and' Geodetic Survey and U. S. <;eological Survey, and have been advised than an, earthquake with a maximum ground acceleration of 0.5g might lbc expected to occur during the lifetime of the facility and that lity of shear displacement at the recctor location cannot be disregarded. Accordingly, we have evaluated the possible consequences of an earthquake with these maximum effects, and have concluded that while certain parts of the reactor f acility may reach or exceed yield point stresses, _ it is unlikely that the stresses produced by ground vibrations would be sufficient to riipture
- The reactor structur, nr nool ennk. @iv a core mel down wo la riot occur.
FErther, should core cooling be lost by a rupture of the reactor pool due to , differential ground _ motion, our calculations indicate that natural convection air cooling would be sufficient to prevent core melting due to decay heat. A%M ven it it is assumed that the ground displacement due to an earthquake la evere.enough to cause rupture of a large number of fuel elements by mechani- Q MEMI cal damage and also results in rupture of the walls and ceiling of the reactor s room, the resulting calculated exposures to the public are within Part 100 guidelines. On the,, oasts of these considerations, we have concluded that the sit's [ is suita e for a reactor of this type and power level.
'
REACTVR HAZARDS EVALUATION A TRIGA reactor which is considered a prototype of th's TRIGA Mark III reactor has been operating since December .of 1961 at the General Atomic Laboratory in San Diego, California. .In addition, many other reactors of the 1RIGA designs have been constructed and are operating in a manner similar to that proposed by the University of California, Berkeley. The operating experience with these reactors 'has demonstrated that the important reactor parameters, can be confi-dently predicted. The applicant has analyzed various potential hazards asso-cisted with the operation of the reactor. They include (1) release of argon-41 (2) reactivity' accidents (3) fuel element cladding failure, and (4) a loss of
..oolant. ace ident.
Radioactive argon-41, which is produced from neutron activation of the air in various exposurs facilities, could be released to the reactor room and to the environment. The applicant's calculations and our independent analysis indicate that, release of argon-41 will not exceed the concentrations specified in 10 CFR 20 limits for restricted areas and for non-restricted areas which could be.occupiad. The reactivity accident considered by the applicant is assumed to occur af ter deliberate violation of operating procedures and several interlocks and scrams. In effect, the accident consists of inserting the full worth of the transient rod while the reactor is operating at a high stesdy power with all control rods 1582 018
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hh. \ l UNIVERSITY OF CALIFORNIA. SAN DIEGO DERKELEY
- DAY 13
- IRVINE
- LOS ANCELE5
- RIVEE$1DE
- 5AN DIECO
- SAN FRANCISCO i SANTA DARDARA
- SANTA CDUZ
'
Cit .l s_ / INSTITUTE OF GEOPHYSICS AND f.A J4 H.I.A. cal.lf0RN! A 92093 PLANETARY PHYSICS, A-025 SCRIPPS INSTITUTION OF OCEANOGRAPHY April 6,1979
.
Mr. John Farmakides U.S. Department of Energy Washington, D.C. 20545
Dear Sir:
I am responding to a request by Mr. Andrew Baldwin, representing - Friende of the Earth, that I comment on the seismic design appropriate for the Lawrence Livermore site. My comments are based on the geologic situation as presented in the LLL report by L. H. Wight, "A Ceological and Seismological Investigation of the Lawrence Livermore Laboratory Site", and on present knowledge concerning peak ground accelerations expected very close to earthquakes, as presented in my recent testi-mony before the NRC concerning the Diablo Canyon Nuclear Power Plant. This testimony is attached. The essential conclusion of my testimony before the NRC was that
' for large earthquakes (M > 7) we do not have a sufficient data base nor physical understanding to predict ground accelerations very near fault breaks (< 10 km distance) with confidence. Available data and physical understanding indicete that accelerations of greater than
, 2 g are possible and accelerations of greater than 1 g may be common.
One aspect of the problem discussed in some detail in my testimony, and which may be of crucial importance to the Livermore site, is the phenomenon of directivity focussing of energy in the direction of fault propagation. Rupture along the Tesla fault, as well as along other mapped faults in the region (in the direction of the Livermore site), could result in anomalously high accelerations (> 2g). It is not possible to accurately assess the probability of such an anomalously high acceleration, but the effect is well established and commonly observed in rupture propagation (see pp 3-10 to 3-14 of my testimony). Also of particular importance to the Livermore site is the conclusion of Ambreysey's that accelerations of greater than 1 g will probably be recorded for even low magnitudes (p 3-8). On April 6, 1977 a magnitude 5.5 shallow earthquake in Iran generated peak accelera-tions of .95 g and 1.08 g, horizontal and vertical components respectively. (S - T % 1 sec.) 1502 019
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i J. Farmakides
- 4/06/79 page 2 Another part of my testimony which is of critical importance to the Livermore site is the reported results from the Victoria Baja California earthquake swarm of March 1978 (Appendix II of my testimony, pp II-l to II-7). One event of magnitude 4.9 produced accelerations of about .64 g at a distance of about 10 km. Although final informa-tion on the depth, location and mechanism of the event are not yet available, it nevertheless shows that even relatively small events can generate accelerations of over .6 g in an environment of very thick alluvium. This result indicates that the acceleration value of .5 g taken in the L..lf.. Wight report is not conservative.
Sincerely,
/
gt;ggf/ tMLC jfJames N. Brune e/ Professor of Geophysics J JNB:sd
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1 [ N&,'k'g.c .M,,fg ap 4 envcwgainen, and aan gensaal escnJ es uthes enananade sisu suece noeth of ih 11hus, en the San is lepe qu,Js.agic a R.. core matJ ta it aux,lsom Saa faldo to I uni..ae.m now hea aly si.h u. v popuhas.1 and wscoed turu en mons pLsn. Ik ifie.d seat te,ce en &yma J. Irom Wyma:J. g 4 A.{ and Neon 8%1.196h.1911) N.n.g6 t.a the spaumat ..I Cuposs Dans tesor I e lidl to Halh et a thie passes siisuugh ehe senter of she aura baeancia distn.I Sume l fr6' d{ %g ',[ Mg.id f4 alt grases fue pas og its kngth, muy be Joe to fauls anwement tiladtwush. 49t>5), ased sne On.hrane bisJS c.I sac paen ut te.c Calavesas souh conc, ein it as lloilastsa ase *.so bcswdy pups.leecJ. artJ
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'9) jfIyk 1.*wn,19136) finisher states "Ihi ! t c ib.o cJ l'y seJJcn snovenuas.oh-a seJ ruptisse as she 4.me el en easthqu.ke
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A30 P00RONIWb REDL'CTION OF EAdTHQUAKE HAZARDS. SAN FRANCISCO BAY REGION ment a program of earthquake hazard reduction, but be re-evaluated with the availability of new geologic they also indicate a need for further efTort and for data at the site. attention to new discoveries. Regional or subregional deformation of the earth's About 30 faults in the bay region are potentially crust commonly accompanies major earthquakes. It is capable of producmg damaging earthquakes. Most of manifested predommantly as upwarping or subsidence these can be accurately located, and those that are the for dip-slap faalta and predominantly as horizontal largest and 'potentially most destructive can ba very distortion for strike-slip faults. In the bay region welllocated. Detailed maps, suitable for - tost plannmg horizontal distortion appears to be the predominant and de : sionmaking purposes, are available for many of process. although some local vertical warping ( about 0.5 these faults. m or 1.5 ft) accompanied the 190t> earthquake on the Magnitudes of historic earthquakes are known for San Andreas. The magnitude of this process and its more than half of the recognized faults. These data potential hazard for the bay region are not completely indicate that at least eight moderate or large- known, but it appears ta be leas important in evaluation magnitude events have occurred on known bay region of earthquake hazards than other earthquake effects, faults and that one very large earthquake imagnitude The frequency of recurrence af earthquakes is 8.3) was located on the San Andreas fault. Current perhaps the most difficult to amess of all these topics. methods of estimatmg maximum magnitude in the Until more geologic data are available, recurrence absence of historic data are still crude, but they provide estimates are tentative at best and , depend heavily on an approximate measure of the size of earthquake that our knowledge of recurrence of historic earthquakes. can be expected on faults that have no historic record of The historic racord in the bay region is little more than dam iging earthquakes. 150 years old, a woefully inadequate . ample for faults Fault displacement of as much as 5 m (16 ft) was that have been active for millions or tens of millions of recorded after the 1906 earthquake on the San Andreas, years. But wen that record shows a crude pattern of a.n_d maximu_m horizontal daptaceme.nt o_f an nuch as 10 damagmg earthquakes on major bay region faults. m 130 ft) is jud h Attempts to determme recurrence intervals for bay earthquake ~on~a'ged_ strike-slip fault.posdbh EstimatedwA ~_a_m4 upper nitudeis. region earthquakes are further complicated by the
- -
, bounds for'dislacement thorizontall accompany:ng unresobed relation between fault creep and damagmg smaller earthquakes on strike-slip faults in the bay earthquakes because several bay region faults exhibit region are 6 m i20 ft) for magnitude 7,2 m (6 m for fault creep along parts of their length. Despite the need magnitude 6. and 0.5 m (2 ft) for magnitude 5. Vertical for more accurate data on frequency of recurrence, the displacements associated with earthquakes on strike- phenomenon of recurrence is well established.
Many important questions are still unanswered, Jut l slip faultsdisplacement. horizontal are likely to be less than Displacement one-third associated with of the is known now to move positively toward enough dip-slip faults is more difficult to evaluate, but these reducing the hazard from future earthquakes. Some evidently are fewer and shorter in the bay region than steps in this direction are obvious. All residents would strike-slip faults. agree that schools and hospitals should not be located The nature and areal distril,ution of deformation astride the traces of major faulta; most would .ccept related to fault movement includes (1) permanent requirements for geologic sue st. iies in the deforma-ground deformation localized as a zone along the fault tion rones along major faults: and many would agree en and 12) sptematic deformation of the earth's surface on siting restrictions that would locate major highway a regional or subregional scale. interchanges, dams, or power plants away from faults Accurate delineation of the width of the zone of that may generate earthquakes. These kinds of actions deformation along the fault is best accomplished are ultimately a product of the democratic prneess, and through careful geologic site studies includmg, where they depend as much on social and economic values as necessary, trenching, excavation, or other subsurface on our scientific knowledge. investigations. Where such data are not available, zone Other steps toward reducing earthquake harards width can be crudely estimated by ar.alogy with cannot be ta ken without more information 'han is given measured zones of deformation that have accompanied here. Building codes, for example, are an important historic faulting. This method suggesta that, for mechanism for protecting life and property fYom stnke-slip faults, permanent ground deformation may earthquakes. But such codes require specific informa. be expected to extend for 92 m (300 lb on either side of a tion on the nature of seismic shaking, possible modes of recognizable strike-slip fault trace and 425 m (1400 fu structural response, and other factors that go far beyond on either side of a recognizable dip-slip fault trace diall the initial geologic process that causes the earthquake, and others,1974). Designation of deformation zones on These and other problems relating to hazard reduction this basis is admittedly a stop-gap measure and thould are treated in subsequent sections of this report'
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