STATf OF CALIFORNIA-THE RE50URCl:S AGENCY DEPARTMf;N1 OF CON$CRVAl10N DIVISION OF MINES AND GEOLOGY SAY AREA REGIONAl OFFICE 114.l MARKET STREET, 3RO FLOOR SAN FRANCISCO, CA 94103-1!513 PHONE. (415) 557-1500 ATSS 597-1500 Jarnes R. Hogg Engineering Division Chief Planning & Developrnent Services Department 2700 "M" Street, Suite 100 Bakersfield, CA 93301 Dear Mr. Hogg: • •. PETE WILSON. March 23, 1992 We are placing on open file the following report, reviewed and approved by the County of Kern in compliance with the Alquist- Priolo Special Studies Zones Act: Geological hazards investigations, Tent. Parcel Map No. 7959, Kern Co., CA, Feb. 1992. EWH:ra cc: A-P file,,,,. Sincerely, EARL W. HART, CEG 935 Senior Geologist & Program Manager
Transcript
STATf OF CALIFORNIA-THE RE50URCl:S AGENCY
DEPARTMf;N1 OF CON$CRVAl10N
DIVISION OF MINES AND GEOLOGY SAY AREA REGIONAl OFFICE 114.l MARKET STREET, 3RO FLOOR SAN FRANCISCO, CA 94103-1!513 PHONE. (415) 557-1500
ATSS 597-1500
Jarnes R. Hogg Engineering Division Chief Planning & Developrnent Services Department
2700 "M" Street, Suite 100 Bakersfield, CA 93301
Dear Mr. Hogg:
• •. PETE WILSON. GQ~mQr
March 23, 1992
We are placing on open file the following report, reviewed and approved by the County of Kern in compliance with the AlquistPriolo Special Studies Zones Act:
Ml'. Earl Hart, Senior Geologist Division of Mines and Geology 1145 Market Street, 3rd Floor San Francisco,Ca 94103-1513
Re; Alquist-Priolo Special Studies Zone Report for Parcel Map 7959
Dear Mt'. Hart;
Enclosed is a copy of the Alquist-Priolo Special Studies Zone Report for Parcel Map 7959. As required by the Alquist-Priolo Act this report has been reviawed and found to be in COllpliance with the applicable laws and standards by Kern County's contract geologist BSK & Associates. This report is therefore being transmitted in order to be placed on open file with your office as outlined in the AlquistPriolo Special Studies Zones Act.
If you have any questions please contact Aaron Leicht of the Floodplain Management Section of this Division.
Very truly yours,
Ted James, Director Planning and Development Services
fo-.o-- ..C~/ ~-James R. Hogg,
Engineering Division Chief
JRH:al
Enclosure
2700 "M" STREET, SUITE 100 BAKERSFIELD, CALIFORNIA 93301
PRINTED ON RECYCLED PAPEH
(805) 861-2615 FAX: (805) 861-2061
!
117 'V' Street • Bakersfield, CA 93304 (805) 327-0671
& Associates (805) 324-4218 FAX
February 28, 1992
Aaron J. Leicht Kern County Department of Planning and Development Services 2700 ''M" Street, Suite 100 Bakersfield, California 93301
SUBJECT: Review of Geologic Hazards Report Tentative Parcel Map 7959 Kern County, California
Dear Mr. Leicht:
OUR JOB B92054
I have reviewed a Geologic Hazards Report for Tentative Parcel Map 7959, located in Sec. 16, T29S R29E, MDB&M, prepared by Duane R. Smith and Associates and dated February, 1992. In conducting this review I have applied criteria outlined in Minimum Requirements for Submilfal of Geologic/Seismic Hazard Reports to Kem County, which BSK prepared for your Department in March, 1990. I reviewed the Special Studies Zones map and the Kern County Seismic Hazard Atlas sheet for the Rio Bravo Ranch Quadrangle. Since I have conducted geological investigations in the general area, am quite familiar with areal geology, and have discussed the site with Mr. Thomas Gutcher, preparer of the report, it was not necessary for me to visit the site as part of this review.
The report deals with major points listed in the Minimum Requirements including literature search, airphoto analysis, geologic mapping, trenching, seismic data, seismic hazards, conclusions and reco=endations, and certification. It includes a plat map, a geologic map compiled on an airphoto enlargement, several trench logs from adjacent parcels prepared by Park and Smith in 1977 and 1979, and regional and local fault and seismic data maps. The report contains seven plates (folded in pockets at the back of the report), 14 figures, and three tables.
Tentative Parcel Map 7959 is situated south of Highway 178 northeast of Bakersfield in the western part of the Ant Hill Oilfield. Present within TPM 7959 are two fault traces, reportedly active in 1952 during the Kem County Earthquakes, for which 50-foot seismic exclusion setbacks have been established.
Relationships of the two fault traces are shown on the Special Studies Zones map. However, the Kern County Seismic Hazards Atlas map shows only the southwesternmost of the two faults. The Geologic Map (Plate 2) shows close agreement with the Special Studies
Review of Geologic Haz.ards Report Tentative Parcel Map 7959 Kem County, C.alifornia
• I OUR JOB B92054 February 28, 1992 Page 2
Zones map. Seismic trenching for adjacent tracts, performed by Park and Smith in 1977 and 1979, provides adequate subsurface data for verification of fault relationships.
The literature search is adequate; the more important published reports and maps have been cited.
An analysis of stereo airphotos was used and contnbutes vital data for fault interpretation.
Geologic mapping, presented on an airphoto enlargement, shows adequate detail.
Geophysical methods were not used in this study and appear unnecessary.
Presentation of available seismic data for the area appears adequate. The report includes Maximum Credible and Maximum Probable earthquake magnitudes, rock acceleration, and velocity for ten major active or potentially active faults in the region. Values presented appear reasonable.
Conclusions, recommendations, and certification as presented in the report are acceptable.
I find this report to be in substantial compliance with the Alquist-Priolo Act and recommend that you accept it as adequate.
I appreciate the opportunity to be of service.
IDS:wp
Respectfully submitted,
Ivan D. Sanderson, Ph.D. Registered Geologist No. 4514
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GEOLOGICAL HAZARDS INVESTIGATION
TENTATIVE PARCEL MAP NO. 7959
KERN COUNTY, CALIFORNIA
FEBRUARY 1992
DUANE R. SMITH AND ASSOCIATES
Consulting Geologists 7201 Fruitvale Extension
Bakersfield, California 93308 (805) 589-7861
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Introduction,
Conclusions .
Recommendations
Geography . . .
Geologic Setting.
Historical Geology
Stratigraphy
Structure.
Faults. . • •
White Wolf Fault
San Andreas Fault.
TABLE OF CONTENTS
Pond-Poso Creek Fault.
Breckenridge-Kern Canyon Fault system.
Garlock Fault ....
Sierra Nevada Fault .
Pleito Fault .
Big Pine Fault
Santa Ynez Fault
San Gabriel Fault.
Local Surface Faults
Geologic Hazards .
Seismicity . .
Potential for Liquefaction, Seiches, and Tsunamis.
lifornia, Geo ?g 1 Fault Map of ;a Calif. Div. Mines Data Map No. '
MAP
and Geol.' 1975 •
Figure 4
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SAN ANDREAS FAULT ZONE IN CALIFORNIA
Northern Colif. ·"'~- active area
Copt! Mt!ndocino
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NORtH AMERICAN PLATE
Son
PACIFIC PLATE
0 100
Break I
"' Break "'-
Bt!rnordino
200 300 400 500 km
(from All@n, 1968)
Figure 5
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folding and faulting of the thick section of sedimentary beds and
the underlying basement complex .
Deformation of the sedimentary rocks in the area has not been
restricted to faulting. Localized folding has also occurred
within the geosyncline forming entrapments for oil and gas
accumulations. The general structure underlying the property is
a west-southwest dipping faulted anticline •
FAULTS
In the general area of the property there are literally thousands
of faults that have been created during geologic time. Many of
these have been mapped and studied but most are unmapped and have
yet to be discovered. The major fault systems in the area are
the White Wolf, San Andreas, Pond-Paso Creek, Breckenridge-Kern
canyon, Garlock, sierra Nevada, Pleito, Big Pine, Santa Ynez, and
San Gabriel. Figure 4 shows most of the known faults of signifi
cant length within a 62 miles radius of the property. Table 1 is
a catalog of named faults in the south end of the San Joaquin
Valley. Figure 6 shows the property with respect to the major
faults in southern California .
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FAULT CATALOG OF THE SOUTH END OF THE SAN JOAQUIN VALLEY
HISTORICALLY ACTIVE FAUL TS
Name of Fault Last Known Movement Faujt Tyoe Evidence of Existence Buena Vista creeping thrust surface Kern Front creeping normal? surface New Hope creeping normal? surface Pond-Paso Creek creeping? normal surface White Wolf 1952 reverse surface Unnamed (Bruer, 1952) 1952 normal? surface
Length (mites)
1 3/4 6t u
45 33±
6±
Possible Magnitude
7.0 7.4
6.0 to 6.5
QUATERNARY DISPLACEMENT, WITHOUT HISTORIC RECORD
Na me of Fault Deepwell Edison East Edison West Elk Hills Jasmin Mount Pose McVan Pleito Wheeler Ridge
Name of Fault Ai do Bacon Hills Greeley-Rio Bravo Jewett thrust Jewett Kern Gorge Polonio Tejon Canyon Trice
{6 miles or more in length)
Li!§l Known M gvement Fault T;.:ee Evidence of Existence ~~ngth imi I e§ ! Quaternary normal surface 10± Quaternary normal surf ace 8± Quaternary normal surface 6t Quaternary normal surface 6± Quaternary normal surface 9± Quaternary normal surface 9± Quaternary normal :surface 10± Quaternary thrust surface 18+ Quaternary thrust mostly subsurface 15+
FAULTS DISPLACING ONLY PRE-QUATERNARY ROCKS (6 miles or more in length)
Last Known Movement Fault Type Evide nee of Existence Length Im ile s I Cretaceous normal surface 6± upper Miocene normal? surface and subsurface 9t Miocene normal subsurface 7± Miocene thrust subsurface 10± Miocene norm.al surface and subsurface 7± lower Miocene normal surface and subsurface 18± Miocene? thrust? surface and geophysical 14± Mesozoic normal surface 7± Miocene normal geophysical 10±
Table 1
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FAULT MAP OF SOUTHERN CALIFORNIA
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:FauU cn1.p o-f sou.Lb em Ca..Hfo:mia. ..!.now a ten ta tiveiy indicate pri:a.ei:pai component of :relative- .mo•em.eJJ.t..
(from Hill, 1955). Revised June 1976.
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White Wolt Fault
The White Wolf fault is a major active fault located about 14
miles southeast of the property. It traverses the southeast end
of the San Joaquin Valley from Wheeler Ridge to northeast of
Caliente, a distance of at least 33 miles. It is generally
believed to be a high angle reverse fault with a left-lateral
component. Data from oil wells in the North Tejon area indicate
total vertical displacement to be in the neighborhood of 10,000
feet .
On July 21, 1952, the well-known Kern County Earthquake occurred
as a result of movement along the White Wolf fault. The initial
shock was a 7.4 magnitude (Bolt, 1978) event with the epicenter
near Wheeler Ridge about 28.5 miles south of the property. The
ground ruptured discontinuously along most of the length of the
fault with maximum vertical displacement of about 3 feet. Subse
quent to the main event of magnitude 7.4, 19 aftershocks of
magnitude 5.0 or greater occurred from July 22 through August 22,
1952 (see Table 2) . Surface ruptures associated with these
events occurred on and near the property (discussed in a follow
fHl~.2?. 3:41:23. e atn 35°2u· 118°~5' 5.8 "lh~ "Di\kerRfh?ld Shock'' !P.:t.RI of ~:1kersrlC'.h1}.
'th~ follnwlng shock: ocr.urred In 1951. 'tlnul! l:!i Pacific Sl:tnd:trd Tln1e (orlrl I hour fnr l~yllght S~vhl~ TlmP.)_ Data •u·e prellmlnn.ry at tlri1e of wrHh1g.
NOTES: -·-Tfi'ii 1952 ~0~1lhPn1 C~llfornl:w e:'l.rthqoo.kc~ have bP-en r3l:tlo~ul'!d by the Scli:11uoloi;::lr.:1l L:wbor:t!nry ol lhi:!' C111llfOl'lll~ lnRlllute of "l"er.hnology In Pa!l!::t.clf'n:t. 'tab!@ Is bR~('d on !heir infnrn1:-illnn .
T:,hlf' ltH·h1"1f':R only :-iFler~hock!'!. having :t. 1~1:1gnlt1.1d,. of 5 or gr~ott('t 011 lh~ Gul.f':nherF?;, ntc11lrr M:1r.11t111rle Sr.=ile 1 ::i.nd tht:!refote scvet:il hundred Rnli:lll@r shuCk.!'i ';111'1:!'.f':llmln::iterl.
TltnC!<: ~lnlf'(I !!'Ive lhP. lnRl::inl of r.ommenccn1ent ol f':1r.h Rhock in l~(.'lrle 0<1yH1it;ht S:tvlng ·r-tm~ wht("h wns In eHcr.I ~t lh~ llme or th~ shocks. For Pnclflr. St:-ind=itd 'time sub-1.-~~1 nn(> hour, And lot Gt!'.'enw~i:'h Civil TimP. add 7 haura.
Loc~tlon~ glVl"ll illt(" "l'li:'e11tcl'~fpolnt on P.::irth'~ surrace dltectlyal>ov4:! lheinRtrument:-il latallon of flr:"il ,round ITHJvetnetil).
Mni:;t of theFie f!l'lrthquakes ortglnal~ nc:;ir the avP.r:t.KP. rlepth for- sovlh<""rn CaHfon11::1 ll;'!~rlhqn:'lkt:'!'I, l:1kf!n :1!'1 18 kl1omP.lf!'rS (10 tntles); those on July 25th are ~h~llower~ but that 011 Joly :ll.':11 rlPt>pPr.
(from Steinbrugge and Moran, 19511 I
Table 2
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san Andreas Fault
The San Andreas fault, located about 39 miles south and west of
the property, extends from the Gulf of California to at least as
far north as Cape Mendocino (see Figure 5). It has a northwest
southeast trend parallel to the crest of the Coast Ranges. It
has been active in Historic time along this entire length.
Movement along this fault is in a right-lateral direction, with
the western block or Pacific Plate being displaced northerly in
relation to the eastern block or Continental Plate. The average
rate of movement is about 1 1/2 to 2 inches per year. It has
been estimated that total displacement since late Cretaceous time
is in excess of 300 miles .
In 1857 the historic "Fort Tejon" earthquake occurred along the
San Andreas fault with an estimated magnitude of 8.0. Ground
rupture occurred along the fault over a distance of about 200
miles (see Figure 5) with maximum right-lateral displacement of
possibly as much as 30 feet. Destruction was total in the Fort
Tejon area approximately 5 miles north of the fault .
Pond-Poso Creek Fault
The Pond-Paso Creek fault extends in a northwesterly direction
from the Sierra Nevada foothills east of Bakersfield to north of
the Kern-Tulare County line. It is an active fault which trends
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to within about 12 miles to the northwest of the property. It
has a length of approximately 45 miles. Work in the Pond area,
by Fugro, Incorporated of Long Beach, indicates 9 inches of dis
placement along its trace at a depth of 10 feet, 35 feet at a
depth of 250 feet, and approximately 1,000 feet at the top of the
Acoustical Basement. It is a normal fault, downthrown to the
southwest, and dips at about 70 degrees. Repairs to county roads
crossing the trace of the fault indicate that creep movement is
occurring on the fault.
Breckenridge-Kern canyon Fault System
The Breckenridge-Kern Canyon fault system is located in the
southern sierra Nevada about 16.5 miles east of the property. lt
trends northerly from the south end of Walker Basin to north of
Mount Whitney, a distance of almost 100 miles. Seismic activity
during historic time attests to its active nature. It is a high
angle reverse fault system with a total displacement of probably
as much as 4,000 feet .
Garlock Fault
The Garlock fault is located about 32 miles southeast of the
property. It extends for a distance of about 150 miles to the
northeast from its intersection with the San Andreas fault, near
Lebec. An a.pparent offset of dike swarms along the zone
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indicates left-lateral displacement of as much as 40 miles
(Smith, 1962). Recent movement of up to 2,000 feet is indicated
by offset streams, fresh-appearing escarpments, etc. Although
few earthquakes take place along the Garlock fault, triangulation
data indicate that deformation is occurring along the zone a few
miles east of the San Andreas intersection.
Sierra Nevada Fault
The Sierra Nevada fault is located about 45 miles east of the
property. It intersects the Garlock fault near the southern end
of the Sierra Nevada Mountains and shows vertical displacement of
large magnitude. It trends northerly along the eastern face of
the mountain range. Vertical displacement has been estimated to
be 3,000 to 4,000 feet since Late Pliocene. Evidence for active
fault movement consists of recent escarpments in alluvium and
damage in an abandoned aqueduct tunnel along the trace of the
fault.
Pleito Fault
The Pleito thrust fault, located about 28 miles south of the
property, delineates the northern base of the San Emigdio Range
at the south edge of the San Joaquin Valley. It extends from
Live Oak canyon east of Interstate Route 5 to 2 miles west of
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Pleito Creek, a distance of approximately 18 miles. It dips at a
low angle to the south beneath the San Emigdio Range .
The Pleito fault was recognized as a south dipping thrust fault
of probable low angle dip by Hoots (1930), who also postulated
displacement of 10,000+ feet along the fault. South of Wheeler
Ridge, the average recurrence interval for moderate to large
earthquakes has been estimated to be about 500 years (Hall,
1987). Hall (1984) estimated an average uplift rate of 0.5
mm/yr .
Big Pine Fault
The Big Pine fault is located about 40 miles south of the proper
ty. This fault joins the San Andreas in Cuddy Valley and has
been mapped for a distance of approximately 50 miles in a south
westerly direction. An earthquake occurred on the Big Pine fault
in 1852 that resulted in ground rupture. Poyner (1960) suggests
strike-slip displacement of approximately 12 to 15 miles. The
Big Pine fault is commonly believed to be the western extension
of the Garlock fault, having been offset in a right-lateral sense
by the San Andreas fault .
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Santa Ynez Fault
The Santa Ynez fault is located about 55 miles south of the
property and trends east-west for a distance of more than 80
miles. Movement on the fault is oblique-slip with the southern
block uplifted to form the Santa Ynez Mountain Range (Dibblee,
1950). Total vertical offset is believed to be on the order of
two miles. The fault has been active in the Pleistocene and
possibly in Holocene time (Rodgers, 1979).
San Gabriel taylt
The San Gabriel fault, located about 46 miles south of the
property, is unconformably overlapped by the Pliocene Hungry
Valley Formation. The trace probably extends on to the northwest
at depth. From the point of surface exposure it can be traced
for about 90 miles to the southeast. It is a right-lateral fault
with a total displacement of as much as 30 miles. The San
Gabriel fault shows evidence of Quaternary displacement
(Jennings, 1975) .
Local Surfaoe Faults
Numerous northwest-southeast oriented local surface ruptures were
observed in the area following the 1952 earthquake and after
shocks (see Bruer, 1952, for example). Reports prepared for
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adjacent properties exposed two fault zones which cross the
property (Park, 1978, Park and Smith, 1977, Park and Smith,
1979). The locations of the adjacent properties and the perti
nent trenches are shown on Plate 3. Plate 4 shows the profile of
the trench excavated across Parcel Map No. 3044 (Parcel 4) .
Plate 5 shows the profile of Trench No. 1, Parcel Map No. 3044
(Parcel 1). Figure 7 shows the profile of Trench No. 2 1 Parcel
Map No. 3044 (Parcel 1). Plate 6 shows the profile of Trench No .
1, Parcel Map No. 4646. Figures B, 9, and 10 show the profiles
of Trench Nos. 2, 3, and 4, Parcel Map No. 4646. Plate 7 shows
the subject property relative to the Special studies Zone in
which the property is located. Note on Plate 7 that a 1952
surface rupture crosses the property and that another short fault
trace trends onto the northeast corner of the property .
The fault trace exposed in the trench across Parcel Map No. 3044
(Parcel 4) is a sharp vertical break with the southwest side
displaced upwards relative to the northeast side (see Plate 4).
Two fault zones were exposed in Trench No. 1, Parcel Map No.
(Parcel 1) as shown on Plate 5. The southwestern fault zone
developed as a small graben. An offset trench also exposed
fault zone (see Figure 7). The northeastern fault zone was
clearly identified in Trench No. 1 1 however, the geomorphic
expression of the zone is distinct (see Plate 5) .
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3044
this
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SW
PROFILE OF TRENCH NO. 2 PARCEL MAP N0.3044
PARCEL I Animal Boring I (__ - - ···~"·--·FAULT ZON E--•'-1
-~--• - -=-----
--. -
.. - -" E '! . -. -
'-...:_ . -..
-----....:._-~-----: ...
Horizontal Scale Vertical Scale
J 11 - -- .. - ____:: ... ..:·
UNIT A
UNIT C
UNIT E
]. II 5' . . . ' ' . .
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----...:....··· -·
BAR Soil mantle, clay, sandy, dark brown, SCALE very fine to coarse grained, friable, roots abundant.
Sand, whitish tan, =ine to very coarse grained, pebbles and cobbles common, poorly indurated, animal borings common, roots common.
Animal n.11""=-_,Borings
WILLIAM H. PARK, GEOLOGIST NOVEMBER 1978
(from Park, 1978)
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The northeastern fault zone was clearly identified in Trench No.
1, Parcel Map No. 4646 (see Plate 6). lt was not identified in
Trench No. 2 (see Figure 8), but was observed in Trench Nos. 3
and 4 (see Figures 9 and 10). This fault zone appears to be
about 50 feet wide and consists of a series of fault blocks
progressively downthrown to the northeast (see Plate 6) .
Aerial photographs taken in 1956, 1975, and 1981 were reviewed
during this investigation. The 1956 photographs are not in
stereo and were not very informative. The 1975 photographs show
the subject property and most of the surrounding area prior to
development. Geologic mapping was conducted on the 1975 photo
graphs and transferred to an enlargement of a 1981 photograph
which shows the property essentially as it exists today. Geo
morphic expression of the two fault zones discussed above is
clearly visible on the 1975 stereo photographs. The presumed
center of each fault zone was mapped on the photographs and
transferred onto Plate 2. The two fault zones, as mapped on the
1975 photographs and as shown on Plate 2, are in good agreement
with the faults shown on the Special studies Zones Map (see Plate
7). The northeastern fault zone is shown as a short trace at the
northeastern corner of the subject property. However, on the
1975 photographs, it appears to join with a longer fault trace
near the northwest corner of Section 22 southeast of the property
(see Plate 7) .
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Since the two fault zones are clearly active, seismic setback
zones have been established for each zone. The setback zones are
150 feet wide (75 feet on each side of the center of each fault
zone) because the faults exist as a series of breaks up to 50
feet wide. No structures for human occupancy should be built
within the setback zones.
The setback zone shown on Plate 1 is an approximation taken from
a straight line projection based on the report for Parcel Map No.
3044, Parcel 4 (see Park and Smith, 1977). It should not be used
for planning purposes. The setback zones shown on Plate 3 are
also approximate and should not be used for planning purposes.
Only Plate 2 should be used for planning .
GEOLOGIC HAZARDS
seismicity
The principal geologic hazards to the area are those related to
seismic disturbances. Because of the pervasive nature of the
stresses being applied to the general area as a result of activ
ity along the major fault systems surrounding the valley, future
earthquakes can be expected. Based on historical data, the White
Wolf fault area, as defined on Figure 11, is one of the more
seismically active areas in the continental United states.
Figure 12 indicates that a magnitude 6 earthquake can be expected
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,_ftKl"l!LD
SANTA IAPllAftA CHANNtL
SITE
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+ + 3!5"
SOUTHERN CALIFORNIA
+ 34°
LOS ANGELES AREA~ ~
IMPERIAL VALLEY
I I 120 +
119 118
AREAS FOR RECURRENCE CURVES
t --.. -·
NORTHERN MEXICO
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111• 116°
-·· . -'
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11!5"
OUTLINE OF THE VARIOUS AREAS FOR WHICH RECURRENCE CURVES ARt PRESENTED IN FIGURE 12. NOTE THE HEAVY OUTLINE FOR THE ENTIRE SOUTHERN CALIFORNIA AREA OF COVERAGE, EXCLUDING
NOl'tTHERN MEXICO,
33°
SOURCEl HILEMAN, JAMES, ET. AL., SEISMICITY OF THE SOUTHERN CALIFORNIA REGION, JAN. 1932 TO 31 DEC. 1972, NO. 2385, DIV. GEOLOGY AND PLANETARY SCIENCES, CALIF_ INST . OF TECHNOLOGY, PASADENA, 1973 .
- LOS ANGE' LES ARE A ..:. !':'!.,2 1971 ?l;,6;>;;- KM~
1iri FV~l\il~ M~30 ~·O<JJ
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IQ .:: WHITE WOl..F FAULT AREA IO WOLF F'A AR A SANTA BAABARA CHANNEL .. 1932-191"1 10,;ioo 1"=PJ2 : 19.32 19~1 1!1,400 "l~l
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-~SO. SIERRA NEVADA :- !932-t971 6,'150 11M'°
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orn
0.001? .. 1 I • ' •o ·: PARKFIE;LD ARE:A
- 19~2'-1971 15,000 kM'° 4'.><i<I ~ v£r-.i rs M) J..O b' 0130
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0001.., L ... l ) 0()0! l . ..... 1 .. J 0001 l _ . .l._.L_L I • > • ' • ' • > " ' ' ' " ' • MllGNlTUDE
Interval recurrencl! curve& for f!ach of th" areaA Ahown in Figure 11. Note th&t the ordin&te scales are identical for all curvf!e except for the curves for the eouthern California network and north Mexico areas.
Hilemon,Jomfts, el ol, 1932 to 31 Oecemb"
Sei9micily of the 1972 1 Calif. Ins!.
Southern California Re9ion, I January of Technology, Pasadena, 1973.
Figure 12
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within the area on a frequency of about once every 33 years per
1,000 km2 • A strain release map, Figure 13, constructed from
seismic data collected for the period 1934 to 1963, shows the
number of equivalent magnitude 3 earthquakes per year per 100 Km'
to have been in the range from 64 to 256 .
Earthquake epicenter data compiled from 1900 to 1974 shows that
70+ earthquakes of magnitude 4.0 to 4.9 have occurred within a 30
mile radius of the property during that period (see Figure 14).
The closest of these was a magnitude 6.1 event located about 1.3
miles southeast of the property which occurred on July 29, 1952 .
This event is listed on Table 2.
Geological conditions in the area which are of concern when
earthquakes occur consist primarily of those associated with
ground shaking. Because of the thickness of the sediments
overlying the basement complex and the unconsolidated character
of the Quaternary deposits, the area is subject to possible
surface readjustment during severe shaking. This can result in
structures being moved from their foundations, foundation fail
ures, damage to water wells and pipeline systems, disruption of
power facilities, roads, etc .
Table 3 lists the relevant faults in the general area along with
the closest distance to the property, estimated maximum credible
and maximum probable magnitudes, estimated peak horizontal
I . The estimotcd maximum c~ible magnitude (Richter ocale) earthquake tMt oppears capoble of occurring under the present tectonic framework Little ~g=r is given to its proboi:>ility of oocurrence ond the timo factor is not a parameter. The so<Jtce• of the estimated magrlltud09 are (a) - Gn=llfekier (1974) ond (b) • Bolt {197g). When> no source is given, the magnitude wu cstimllted bued on similoritie• to olnor faults. 2. The estimated moximum pro bob lo magnitude (Richter scale) eartO<juako thal is likely to occur during • 100 year interval. Tho postulated me.gnitudo man not be lower than thc maximum chat has occumod in Historic timo. 3. The estimated peok oorizontll! acceleration (gBvity) based on thc maximum c~ible mognitude. 4. Tile clltimoled peak horizoootl accclcration (gravity) bolled on t0o maximum probable mognitude. 5, The estimated .epeatable high ground acceleration (gravity) based on the maximum c~ible magnitude. 6. The estimoted repeatobie high groond oeeelenlion (gravity) based on t0o maximum probable magnitude. 7, The estimated peok horizor<al velocity ( cm/o) based on the maxirrwm credible magnitude. g. Tho estimoted peok oorizontll! velocity { cmlo} baaed oo the maximum proboble magnitude. 9. The Olllimated Modified-Mercalli intensity baaed on the estimoted peok horizontal velocity of tbc maximum probable mognitude using Table 11.4 of Hunt (19114).
Sourcu: Peak horiz.ontal .acce~cor11tion and ,,.elocity c.a.ieulllliona b.flllCd on method of Joyner- and Film.al { 198.S). Repc.at11ble high ground .11cccler111Cion -citlcuiati.ons hued -an the mi:tbod of Ploes&el and Slouon (1974 ).
Table 3
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accelerations, estimated repeatable high ground accelerations,
estimated peak horizontal velocities, and the estimated Modified
Mercalli intensity of the maximum probable event. The property
is located on the Seismic Risk Map of the United states in Zone
No. 4. This zone was determined by the proximity of certain
major fault systems which include those mentioned in the above
discussions .
Accelerations discussed in this report are calculated from the
maximum probable events since they represent the most reasonable
values based on the use and life of the property and the geologi
cal conditions. Due to the thickness of the sediments underlying
the property a slight amplification of the accelerations given in
this report may occur. Appendix A gives an explanation of the
ground motion calculations used in the preparation of this
report. Appendix B gives a description of potential earthquake
damage based on the Modified-Mercalli intensity scale .
Maximum probable ground motion at the property would likely
result from movement along the White Wolf, San Andreas, Pond-Poso
Creek, Breckenridge-Kern Canyon, or Garlock fault. The estimated
peak horizontal acceleration at the property resulting from a
maximum probable event of magnitude 7.4 along the White Wolf
fault is 0.20 gravity. The estimated repeatable high ground
acceleration of such an event is 0.13 gravity. The estimated
peak horizontal acceleration at the property resulting from the
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magnitude 6.1 event which occurred on July 29, 1952 is 0.33
gravity. The estimated repeatable high ground acceleration of
this event is 0.21 gravity.
Considering all factors, it is believed that the San Andreas
fault is the most likely to produce a maximum probable earthquake
during the lifetime of the development. The estimated peak
horizontal acceleration resulting from a maximum probable event
of magnitude B.25 along the San Andreas fault is 0.09 gravity.
The estimated repeatable high ground acceleration of such an
event is also 0.09 gravity .
If a maximum probable magnitude earthquake were to occur from
movement on the White Wolf fault, intensities could be as high as
VIII on the Modified-Mercalli intensity scale. Damage could
include: fall of stucco and some masonry walls; twisting, fall
of chimneys, factory stacks, monuments, towers, elevated tanks;
frame houses moved on foundations if not bolted down; loose panel
walls thrown out. A maximum probable magnitude earthquake along
the San Andreas fault could produce similar intensities. The
estimated intensity of the magnitude 6.1 event which occurred on
July 29, 1952 is also VIII .
Faults not yet identified may exist in the general area that are
capable of producing earthquakes that could be damaging to
structures located on the property .
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Potential for Liquefaction, Seiches. and Tsunamis
Case histories of earthquakes where liquefaction occurred in flat
terrain indicate that generally the conditions of cohesionless
surface material accompanied with relatively shallow water tables
existed underlying the problem areas. In such cases ground
vibration increases the pore pressure resulting in water moving
upward turning the sand or silt into a "quick" condition. The
surface manifestations include the development of sand boils,
surface cracks, ground settlement, and differential compaction.
The conditions. underlying the property do not appear to present a
hazard from such activity. The depth to groundwater renders near
surface liquefaction improbable .
The potential for seiches, tsunamis, and earthquake-induced
flooding at the property is negligible due to the absence of
large bodies of water in the vicinity .
Subsidence
Local subsidence is not expected to present a hazard because of
the generally coarse-grained sediments and absence of shallow
groundwater. Significant subsidence in the vicinity has not been
noted. Regional subsidence could occur as a result of the
withdrawal of fluids due to the extensive exploitation of oil
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fields in the area. Regional subsidence should not threaten
structures on the property .
Flooding and Erosion
The property is not located within a flood hazard zone as defined
by the Federal Emergency Management Agency. There are no large
bodies of water in the area that might endanger the property from
inundation. Rapid erosion is not likely to present a hazard to
the property .
Landslides and Rockfalls
There are no steep natural slopes on or near the property; there-
fore, no natural landslide conditions exist. Rockfalls are not a
factor on the property because there are no hills or cliffs .
It is the opinion of this investigator that the property is
geologically suitable for the intended land use .
Submitted by:
Thomas F. Gutcher Registered Geologist State of California No. 5010
GEOLOGICAL HAZARDS INVESTIGATION TENTATIVE PARCEL HAP NO. 7959 ~ERN COUNTY, CALIFORNIA FEBRUARY 1992 TPM79S'!l.llA.Z
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SELECTED REFERENCES
Allen, C.R., 1968, The tectonic environments of seismically active and inactive faults along the San Andreas fault system in Proceedings of conference on geologic problems of the San Andreas fault system: Stanford University Publications in the Geological Sciences, v. XI, p. 70-82 .
Allen, C.R., Saint-Amand, P., Richter, c.F., and Nordquist, J.M., 1965, Relationship between seismicity and geologic structure in the southern California region: Bull. Seism. Soc. Am., v. 55, no. 4, p. 753-797.
Bartow, J.A., and Doukas, M.P., 1978, Preliminary geologic map of the southeastern border of the San Joaquin Valley, California: U.S.G.S. Miscellaneous Field Studies Map MF-944.
Bartow, J.A, and Pittman, G.M., 1983, The Kern River Formation, southeastern San Joaquin Valley, California: U.S.G.S. Bull. 1529-D, 17 p .
Bolt, B.A., 1978, The local magnitude ML of the Kern county earthquake of July 21, 1952: Bull. Seism. Soc. Am., v. 68, p. 513.
Bolt, B.A., and Abrahamson, N.A., 1982, New attenuation relations for peak and expected accelerations of strong ground motion: Bull. Seism. Soc. Am., v. 72, no. 6, p. 2307-2321.
Bruer, W.G., 1952, Earthquake fissures in central and southwestern Kern County, California: unpublished report, 12 p.
California Division of Oil and Gas, 1973, California oil and gas fields, volume I, north and east central California: Calif. Div. Oil and Gas.
Campbell, I., 1971, Geologic map of California, Olaf P. Jenkins Edition, Bakersfield sheet: Calif. Div. Mines and Geol., second printing .
Campbell, K.W., 1981, Near-source attenuation of peak horizontal acceleration: Bull. Seism. Soc. Am., v. 71, no. 6, p.2039-2070.
Davis, J.F., 1985, State of California special studies zones, Oil Center quadrangle: Calif. Div. Mines and Geol., revised official map.
Davis, J.F., 1985, state of California special studies zones, Rio Bravo Ranch quadrangle: Calif. Div. Mines and Geol., revised official map .
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SELECTED REFERENCES (Continued)
Dibblee, T.W., Jr., 1950, Geology of southwestern Santa Barbara County, California, Point Arguello, Lompoc, Point Conception, Los Olivos, and Gaviota quadrangles: Calif. Div. Mines and Geol. Bull. 150, 95 p.
Federal Emergency Management Agency, 1986, Flood insurance rate map, Kern County, California (unincorporated areas), panel 1050 of 2075.
Greensfelder, R.W., 1974, Maximum credible rock acceleration from earthquakes in California: Calif. Div. Mines and Geol., Map Sheet 23 .
Hall, N.T., 1984, Late Quaternary history of the eastern Pleito thrust fault, northern Transverse Ranges, California: unpublished Ph.D. dissertation, Stanford University.
Hall, N.T., 1987, Late Quaternary history of the eastern Pleito thrust fault, San Emigdio Mountains, California: Geol. Soc . Am., Abstracts with Programs, v. 19, no. 6, p. 385.
Hileman, J.A., Allen, C.R., and Nordquist, J.M., 1973, Seisrnicity of the southern California region, 1 January 1932 to 31 December 1972: Seismological Laboratory, Calif. Institute of Technology, Contribution No. 2385, 83 p.
Hill, M.L., 1955, Nature of movements on active faults in southern California, in Oakeshott, G.B., ed., Earthquakes in Kern County, California during 1952: Calif. Div. Mines and Geol. Bull. 171, p. 37-40 .
Hoots, H.W., 1930, Geology and oil resources along the southern border of the San Joaquin Valley, California: U.S. Geol. Survey Bull. 812-D, p. 243-338.
Jennings, C.W., 1975, Fault map of California: Calif. Div. Mines and Geol., Geologic Data Map No. 1.
Joyner, W.B., and Boore, D.M., 1981, Peak horizontal acceleration and velocity from strong-motion records including records from the 1979 Imperial Valley, California, earthquake: Bull. Seism. Soc. Arn., v. 71, no. 6.
Joyner, W.B., and Furna!, T.E., 1985, Predictive mapping of earthquake ground motion, in Ziony, J,I., ed., Evaluating earthquake hazards in the Los Angeles region - an earth-science perspective: U.S. Geol. Survey Professional Paper 1360, p.203-220 .
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SELECTED REFERENCES (Continued)
Kern County Council of Governments, 1974, Seismic hazard atlas, Oil Center quadrangle, Kern County, California.
Kern County Council of Governments, 1974, seismic hazard atlas, Rio Bravo Ranch quadrangle, Kern County, California .
Oakeshott, G.B., 1955, The Kern County earthquakes in California's geologic history, in Oakeshott, G.B., ed., Earthquakes in Kern County, California during 1952: Calif. Div. Mines and Geol. Bull. 171, p. 15-22.
Page, R.A., Boore, D.M., Joyner, W.B., and Coulter, H.W., 1972, Ground motion values for use in the seismic design of the trans-Alaska pipeline system: U.S.G.S. circ. 672, 23 p.
Park, W.H., 1978, Geologic investigation of parcel map no. 4646, parcels "A'' and "B", Kern county, California: William H. Park and Associates, November 1978, (unpublished), 7 p .
Park, W.H., and Smith, D.R., 1977, Geologic investigation of parcel map no. 3044 (parcel 4), Kern county, California: William H. Park and Associates, August 1977, (unpublished), 4 p •
Park, W.H., and Smith, D.R., 1979, Geologic investigation of parcel map no. 3044, parcel 1, Kern County, California: William H. Park and Associates, April 1979, (unpublished), 6 p.
Ploessel, M.R., and Slosson, J.E., 1974, Repeatable high ground accelerations from earthquakes - important design criteria: California Geology, v. 27, no. 9, p. 195-199.
Poyner, w.o., 1960 1 Geology of the San Guillermo area and its regional correlation to Ventura, California: unpublished M.A. thesis, Univ. Calif., Los Angeles, 119 p .
Real, C.R., Toppozada, T.R., and Parke, D.L., 1978, Earthquake epicenter map of California: Calif. Div. Mines and Geol., Map Sheet 39.
Rodgers, D.A., 1979, Vertical deformation, stress accumulation, and secondary faulting in the vicinity of the Transverse Ranges of southern California: Calif. Div. Mines and Geol. Bull. 203, 74 p.
Smith, G.I., 1962, Large lateral displacement on the Garlock fault, California, as measured from offset dike swarms: Bull . Am. Assoc. Petrol. Geol., v.46, no. 11, p. 85-104 .
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SELECTED REFERENCES (Continued)
Smith, T.C., 1984, Faults east of Bakersfield, Kern County: Calif. Div. Mines and Geol. Fault Evaluation Report FER-145 (unpublished), 11 p.
steinbrugge, K.V., and Moran, D.F., 1954, An engineering study of the southern California earthquake of July 21, 1952, and its aftershocks: Bull. Seism. Soc. Am., v. 44, no. 2B, p. 201-462.
U.S. Department of Agriculture, 1967, Report and general soil map, Kern County, California: U.S.D.A., Soil Conservation Service, 71 p ..
Ei\STBAKE.AEF
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CALCULATION OF GROUND MOTION PARAMETERS
The ground mo1ion paramelers presented in the text are based on the predictive equation in Joyner and Fumal (19851:
logy~ c0 + c,(M-61 + c,IM·6)' + c,logr + c,r + S,
where r ~ Cd' + h')"', S ~ 0 for rock sl1es, S ~ c, for soil sites, Mis the moment magnitude, dis the closest distance to the surface projection of the faull rupture in kilometers, and y Is 1he ground motion parameter to
predict. The equations are based on a two-slage regression analysis of strong motion data which yields tho following:
loge~ 0.43 + 0.231M-6) - logr - 0.0027 r,
where r ~ Id" + 64) 11' and a is the peak horizontal acceleration in gravity; and also
log v ~ 2.09 + 0.49(M-6l - log r - 0.0026 r + S.
where r ~ Cd' + 16) 11', S ~ 0 for rock sites, S ~ 0.17 for soil sites, and vis the peak horiwmal velocity in
centimeters per second. The data from which the equations were derived contained only even1s with magnitudes between the range 5.0 s M :!i 7.7. Note that the peak horizontal acceleration Is independent of the positioning over rock or soil, but the peak horiwn1al velocity is not.
For Iha ground motion parameters presented in the taxi, the computations are based on 1he assumptions that dis the closest distance to the fault trace and that the equations are valid for events outside the magnitude range 5.0 :!i M,,; 7.7. Figures BB and 89 lbelowl from Joyner and Fumal 11985) show that be1ween the magnitude range 5.0 s M ,,; 7.7, the curves are magnitude-independent and evenly spaced. Therefore, we assume that these equations are valid outside the magni1ude range 5 .0 :!i M s 7. 7. However, no data is available to verify this assumption .
"' ;!; z 0
~ 0.1 w _, w u '<i
-------
M
15
6.5
5.5
0.001 J I 1 .. J.111 ' t ' •' "'' ..L ... 1 .... L!.~"--'--'-'CJ 1 10 100
DISTANCE, IN ~ILOMETERS
FIGURE M.-~icl.-:1 vt.lu& of peak acceleretioo for the fl!ITM:iomly oriimt~ hotlmnta* compoMint 11111 111 fun1::lii:m Qf db;t1nc11 and moment me~lrud1111. C11rvtr.11 ilrW duhlfd where no4 conftl'lllned by i:l•IA. .
ZD _z .o
<':OJ Qvo 9 0: ~:!' _,"' <("' ~w z:;; §:li <Ci= oz I t'l
FIGU:Rt lt!l.-l"'tedleted value of P'1"'1r. vtilocity rot the randomly orfe111ed horW:tnt~ r;i;imJ)otlll!nll as a Funcllon of d!staw::e "nd 1111)' TJ1fl'J:il tt118f1ltude al rock sll911 lhMVf linnl 111nd ~II sllcit (lhln llhel. Cuf"ll!!ll ani d1Hhed wh~ llQI (:n~lrabwrl by data.
The repeatable high ground accelerations (RHGA) presented in the text are based on the method ol Ploessel and Slosson 11974). It has been noted (Page and others. 19721 that a single peak ground acceleration may not be as damaging as several cycles of lesser shaking. Analysis of strong motion data was found to indicate that within about 20 miles of the epicenter, the RHGA typically averages about 65% of the peak ground acceleration . For distances greater than about 20 miles from the epicenter, the RHGA rapidly converges to the peak acceleration. Therefore, Ploessel and Slosson 11974) feel that the RHGA may be a better appro•imation of tho ·design acceleration· than peak ground acceleration. The RHGA as presented in the text are based on the peak horizontal acceleration values .
Ml I, N1JI r~ll. Marginal 1!md 11'.ln~-Jt@rlod eft'8(:1t; of large e111rlhq1to\lr.t!!1 lfor det1til1!1; u.e text).
__ .,._ ... , .... _ _,
' II. felt by ~rsons et rest on 1111~ ftoon1, !fr f:iv~r21hly placed. -·--
Ill. l'eU hnltnJt!I. HAn!lng oblvett hlllng. Vibn1llon !Ike p&'!Slng of llghl lrnck!I. DuraUon ~:11tlm11IP.d. Mey m:it l:"'1 rlf;'cognlzed El~ ein e21rthquake.
0.0035-0.007
1----··· ---··· -IV, f111nglng obJect~ swine. Vibration 11\t pa!!!lng ol hei:iivy !ruck~; or n.001-0.015
' t11.1n.allon of a Joli ll~tJ fl heavy ball strildn9 the walls. S1i:iindit113 motor cars rock, Wlni'tl()ws, db1he!, dl'.l(ltl ranle. ClaM-tl!I e11nk. Crockery tln~lit!!I. In lhl!I tippet r~nRf! of tv wooden w111l11111nd lr11otne ert.11k. ···-----·--
VI. f'dt by 1111. Many fdghl~nf!d and n1n (1\Udoor11. l>enion:t w"'lk un,llteadily. 3-7 0.0::15·-0.(17 5 Wh1dow!I, dl11h1B11, ghi.~er~ brokl!!!n. Knkltk11acb, boob, eh;:., off !!helves.
l'k:l\ll"t' Qff w11!1s. ~un1Ut1re moved or ov11t1"llltntfl_ Week plal!llfJr ftnd mll1MJ11ty O erecked. Small beH:1 rlns lchun::h, iw.l!.ool). T ree11, bt1~l1~ 111ht1l:en (\ll~bly, or he11rd t1J 11.'Mle-CFR).
~ --vu. nlfficult I<' l!lt&111l Noticed by drivieH of motor uu. Hnng\nR oblect11
qulv!!!r. FurnUure btt)1ten. Dami;tge lo m111sonry O. lncludll'IJ et11cks. Week chhnnieyi broki!!!n 111 rog[ lln~- Fall ol pl~~~t, !OMl!!I bricks,. 11tonc~. llle111, comloet l"'l~ unbraced p&f&pttt; •nd erchltectqrol nrn11menl11-CF"-l-
7-20 0.0?-IJ,Hi
• Same!! Crt'ck$ In ma!onry C, Wl!llVC!ll on pondti; 'M'!ll)r lutbld with mud . 6m11ll 11llde11 ond c:11vlnR In alon@: l!;llnd or gravel bettks. 1.arge hells ring . Cc:mcrelP.! lnl@:Blltin dll~hi'!11 rlam11ged, _,_,_
VIII_ Ste1BJIP8 <if molor c:an1 effll!(;tc(I, n11mege lo n'l1'1$(Jt11'Y C: partlel colh••1~1'!. Som111 d~1rt;;i.9e lo ma11onfJ 9; tiOl'ii& lo me!IOnry A. Fall of stucco end 1!11'.ltfll'!
2.11 .. f!IJ 0.15-0.:JS
me110T1ry woll~. Twl!llng. lull or clilmnctya. fsclocy totac::k..1, monumenl~. 1ow111r11, elevl(lil~ lanka. Fr11m1J hoO~!I moved on fo\lrnh1llon!l 1f not bolled down; loo11e r-ne1 wal1s lhrown o\11. Decayed plllng broken off. Bfenchci: broken from Int~- Ch11np.s In flow i;t lemperalufe or tiptll'I~ 11nd well11. Cncb In wet 11:rou11.d •nd on ll111111p iltlJ'e-'· -· ·- ,.
IX. Cenefel penle. M11!0nl')' [J deSIJoyf!d: me11onty C he111vl1y. damaged, 60-21JIJ 0.35-0.7 "'ml!!llml!!ll wltti C<)mpli'!li!!! collapse: ma1onry B seJloul!l1y d•1n11ged_ , (Gen~ral clamage h.'1 fo\1nd11llon11-Ct-R.I frame structures, H n~I holled, sldflied oft foundetlonf.. F111mea taeked. S"rkn.1.!ll damaBe lo rm1etwoh1\. U11d€ltgto11nd r•re11 bJoken. Con.!llJ1lr.uou11 Cfecks II\ 9ro11nd. In slh.1vl"'l(!d area1111&nd an nu.id !!!lecled, l!!!'lirthqu!lllre foonlslnl!I, send eraler!I.
• damage lo dems. dllr~s. l!!!11lbank111111n1~. l.aJe land11lldes. W111ll'!r tluown on banb ol c:enals, tlvt'.!n. lak~. tile:. Sand en m11d 11hlhed hofh:.t'.llill'llly nn beeehes and ft111 land. R•lls ~nl 11llf!htly.
