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7/30/2019 Earthquake Risks

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- -PROXIMAL POTENTIALLY SEISMOGENIC SOURCES FOR SANDIA NATIONALLABORATORIES, ALBUQUERQUE,NEW MEXICO.

J. Duane GibsonSandia National LaboratoriesAlbuquerque, New Mexico 87185-0750P.O. Box 5800, M.S. 0750 RECEIVEDac1 1 1 1995

ABSTRACT O S T IRecent geologic and geophysical investigations within the Albuquerque Basinhave shed light on the potentially seismogenic sources that might affect SandiaNational Laboratories, New Mexico (SNLNM), a multi-disciplinary research andengineering facility of the U.S. Department of Energy (DOE).This paper presents a summary of potentially seismogenic sources for SNL/NM,emphasizing those sourceswithin approximately8 kilometers (km) of the site.Several significant faults of the central Rio Granderift transectSNLLNM.Although progress has been made on understanding the geometry and interactionsof these faults, littleis knownof the timing of most recent movement or onrecurrent intervals for these faults. Therefore, whether particular faults or faultsections have been active during the Holocene oreven the late Pleistocene isundocumented. Although the overall subdued surface expression of many ofthese faults suggests that they have low to moderate slip rates, the proximity ofthese faults to critical (e.g, nuclear) and non-critical (e.g., high-occupancy, multi-story officebght lab) facihties at SNLLNM requires their careful examination forevaluation of potential seismic hazard.

INTRODUCTIONSandia National Laboratories inAlbuquerque, New Mexico (SNL/NM) (Fig. l),lies within the tectonically active Rio Grande rift,a major crustal feature that extends from northernMexico through New Mexico into southernColorado [l]. Included in the faults that cross orlie near SNL/NM (Table 1)is the Tijeras-Caiioncito fault zone (TCfz) with a total length ofat least 93 km [2,3]. The exact role and extent ofthis structure in accommodating differentialextension within the Albuquerque Basin is notwell understood. Quaternary displacement on the

TCfz has been largely strike-slip with differingvertical displacements along the trend of thefault. Normal, down-to-the-west faults thattectonically interact with the TCfz include theSandia fault to the north and the Hubbell Springsfault to the south [4,5]. These faults as well asthe Manzano fault (parallel and to the east of theHubbell Springs fault), the Rio Grande fault [6](parallel and to the west of the Sandia andHubbell Springs faults), and the Coyote fault are

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potential seismogenic sources for earthquakeswithin 8 km of SNL/NM. As is typical in the RioGrande rift, large earthquakes on faults ofconcern for S N L N probably may haverecurrence intervalsof tens to hundreds ofthousands of years [3,7].However, little or nodata are available on recurrence intervals or timesince last movement for major faults on or nearSNLLNM.

Developmentof expected ground motionvalues from potential earthquakes is crucial fordefining a suitable engineering design basis forcritical facilities, such as nuclear researchreactors in Technical Area 5 (TA-5) (Fig. 2), andfor the2,000+ structures that house the 10,000+,on-site S N L m and DOE personnel [SI. Acomparable number of military and civilianpersonnel are employed by the United States AirForce (USAF) n Kirtland Air Force Base(KAFB), such that over 20,000personnel are

TEeadquartered on site.This work was supnorfedby the UnitedStates Department of Energy underC0nfr;c.t !X -P ,C%-94A!J3 ' ' 0 .


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DISCLAIMERPortions of this document may be illegiblein electronic image products. Images areproduced from the best available originaldocument.


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.Various federal regulations and guidelinesgovern the evaluation of seismic hazards atS N L N and the use of these evaluationsin thedesign of facilities. Most buildings at S N L Nhave been designed based on the requirementsofthe Uniform Building Code (UBC) [9] hat were

in effect at the time of design of the building.The UBC has undergone numerous revisions overthe past decades with progressively morestringent seismic requirements for New Mexicoand the Albuquerque area.

,------------! NEW MEXICO ,iALBUQUERQUE,

i BASIN ii w'e? i3'

-------' --ALJI EXPLANATION1 lbuquerque BasinJ iver,*-. Fault-hatchuresd on downthrownside; dashed whereinferred or buried+ Oilandgasexploration wells9 Fault segmentboundary

Fig. 1. Location Map of the Albuquerque Basin, showing SNL/NM (KAFB), the Cities of Albuquerquerequire that all federally owned or leased, new orexisting buildings be brought into compliancewith applicable seismic requirements. Inaddition, the DOE has issued Order 5480.28,

and Santa Feyand major regional faults. (Figure modified from [3], [6], and [lo].)Other federal seismic guidelines includethose of the National Earthquake HazardsReduction Program ( N E W ) [ll]. PresidentialExecutive Orders (e.g., Executive Order 12699)

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"Natural Phenomena Hazards Mitigation,"effective January 15,1993, and related Standards1020-1024for integrating natural phenomenahazards into its facilities design. This Order andassociated Standards use a graded approach

where existing general building codes areacceptable for non-critical facilities, but site-specific seismic hazard analyses are required formore critical facilities.

Table 1 Characteristicsof Proximal PotentiallySeismogenic Sourcesin the Vicinity of SNJL/NM.

Seismogenic Source1

Footnotes to table:12

SeeFig. 1and text for location and explanation of faults, fault zones, tectonic features, andseismotectonic provinces.A: Compelling evidence exists for reueated late Quaternary surface displacement (e.g., "active")B: Compelling evidence exists for Quaternary surface displacement, timing of most recent eventunknown (e.g., "potentially active").Presumed potential surface rupture length based on available data and literature. "N/A" =notapplicable.A 60" average fault dip is assumed for normal faults; a 90"dip for strike-slip faults.These references represent only a portion of the extensive literature available on the AlbuquerqueBasin. The listed references are considered particularly relevant for paleoseismic and seismichazard studies.

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An arbitrary cut-off distance for this studyof approximately 8 km (5miles) follows theapproach ofDOE tandard 1022-94 [12].Among other requirements, this standard requiresdetailed geological, geophysical, seismological,and geotechnical investigations of all faultswithin 8 km (5 miles) of a site with moderate orhigh hazard facilities. This study does not satisfythe detailed investigationsfor SNL/NM asrequired by [12], but represents an evaluation ofthe available data and tectonic models that maybe pertinent to seismic hazard analysis.Significant additional site characterization workwould be required to fulfill the DO Erequirements for seismic hazard analysis atSNL/NM.

SEISMOGENIC SOURCESAn initial step in evaluating site-specificseismic hazards and establishing a basis fordesign requirements is identifying potentialseismogenic sources for a site. As previously

mentioned, S N L m ies within the AlbuquerqueBasin, a major component of the Rio Grande rift(Fig. 1).The Albuquerque Basin has undergoneseveralkm of east-west extension, predominantlyfrom normal faulting over the past approximately30 to 40 million years [13]. Many faults withinthe basin are concave-upward listric faults thatmay merge into a basal extensional or detachment

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fault, The basin is surrounded by fault-boundedbasement uplifts: the eastward-tilted Sandia-Manzano-Los Piiios Uplift on the eastern marginand the Ladron and Lucero uplifts on thesouthwestern basin border. Faults with thelargest displacements occur severalkm basinward

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from the range-front faults adjacent to the rift-border uplifts. Structural relief of the basin isover 10,OOOm, based on the vertical separation ofPrecambrian strata from the top of the easternmargin uplifts to the deepest portion of the basin.

c

h

0,

I464000 State PlaneCoordinates

2 ILOMETERS

cfFig. 2 - Location map of KAFB, showing the location of various technical areas (e.g., TA-1, TA-5) ofSNL/NM. Surface trace of faults near or on KAFB are indicated. Major roads on KAFE3 (e.g.,Wyoming, Eubank) are also indicated. (Figure modified from [5]).

Although the Albuquerque Basin appears asa single, continuous topographic basin, seismicreflection work and exploratory oil and gas wellsindicate that it consists of two subbasins: anorthern eastward-tilted half-graben and asouthern westward-tilted half-graben [4]. Thehalf-grabens arebordered by major Late

Cenozoic faults along either the eastern orwestern margins, by distributed minor faultingalong the opposite margin, and by complextransfer or accommodation zones. The TCfzmay act as such as accommodation zone of theAlbuquerqueBasin (e.g., Reference [141). Moredetailed descriptions of the proximal, potentiallyPage 4


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seismogenic sources for SNL/NM are discussedbelow, in alphabetical order.COYOTE FAULT

The north-south-trending Coyote fault[15,16] borders the northern two-thirds of theManzanita Mountains (Figs. 1and 2). The faultis exposed adjacent to Coyote Springs, near itsintersection with the TCfz. The Coyote fault isnorth- to northwest-striking, down-to-the-southwest, and steeply dipping with at least 400m of documented throw [SI. The fault has aninferred total length of about 7.2km and, locallyas at Coyote Springs, controls ground-water flow.The fault is assumed to have had surface ruptureduring the Quaternary (Le.,to be potentiallyactive: Fault Class B on Table 1). A summary ofthe seismic-source parameters for the Coyotefault @included in Table 1.HUBBELL SPRINGS FAULT15

The north-south-trending, westward-dipping Hubbell Springs fault lies along thesoutheastern margin of the Albuquerque Basin(Fig. 1). It is one of a series of faults that down-drop bedrock in the central portion of the rift asmuch as 10km. The fault is continuous for about58km and is connected by a small graben to theTCfz (Fig. 2) onKAFB. As it crosses thesouthern boundary of KAFB, the Hubbell Springsfault has a strikingly linear trace with twodistinct, parallel fault strands. It is aligned with aseries of freshwater springs in the northem 29kmof its length.Fault scarps related to the Hubbell Springsfault are perhaps the most spectacular in this partof the Rio Grande rift [7] with a prominent 30 to45m scarp along the northern portion the fault.The fault scarp is sharply defined and is incisedby east-west arroyos. Most recent movement onthe fault was probably late Pleistocene to perhapsHolocene, Like several of the other faults in this

study, the Hubbell Springs fault can probably bedivided into discrete fault segments that mayhave moved independently in the past. However,additional work is needed before this division canbe made.MANZANO FAULT

The north-south trending, westward-dipping Manzano fault is a major rift-bounding

normal fault at the base of the ManzanoMountains [7] (Fig. 1). Movement along thisfault probably formed the precipitous range frontof the Manzano Mountains, although Machette[7] found no evidenceof fault scarps developedin Holocene to middle Pleistocene deposits alongthe mountain front. The Manzano fault is markedby a wide zone in which early Miocenetuffaceous sedimentary rocks and andesite (aswell as older rocks) are steeply rotated into faultcontactwith Paleozoic and Precambrian rocks.The Manzano fault probably begins south ofTijeras Arroyo, interacting in some manner withthe Coyote fault, and extends about 54 km southto the Ab0 Pass area, where it may join the LosPiiios fault. Discrete fault segments have notbeen assigned to this fault. The seismic-sourceparameters assigned inTable 1assume that theManzano, Coyote, and Los Piiios faults aredistinct seismogenic sources.RIO GRANDE FAULT

The approximately55-km long, north-southtrending, westward dipping Rio Grande fault islocated several km basinward from thetopographic high margin of the rift. This faultborders the deep, inner graben of the basin andexhibits the greatest amount of vertical separationof the base of rift-fill sediments [4,13]. The RioGrande fault exhibits over 4,000 m of Cenozoicdisplacement and has played a major role in thedevelopment of the Albuquerque Basin. Thefault underlies the Holocene inner valley of theRio Grande [lo, 141.The structural block between the RioGrande and Sandia faults (the latter describedseparately below) likely contains several down-to-the-west normal faults that, with additionalwork, may come to be considered as distinctseismogenic sources. This block forms astructurally high suballuvial bench between therift-flanking Sandia Mountains and the deep,inner half graben of the northern Albuquerque

Basin [171. According to Chapin and Cather [13,this bench and others in the central Rio Granderift may be a result of basin-ward migration ofdisplacement. Considering that the Rio Grandefault is a main rift-bordering structure in. theAlbuquerque Basin and that similar rift-marginstructures to the north (e.g., the Pajarito, LaBajada and Sangre de Cristo faults) and to thesouth (e.g., the Coyote Springs-SantaFe,HubbellSprings, and La Jencia faults) exhibit evidence of

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Quaternary displacement,it is likely that the RioGrande fault is an active Quaternary structure [3,181. Assessment of late Quaternary displacementalong this fault is hampered by the parallelismbetween the fault and numerous topographicscarps that may be terrace back-edges formed bythe Rio Grande [3]. A few historical and well-located contemporary earthquakes have beenlocated near the Rio Grande fault [19], supportingan "active" classification for this fault in Table 1.SANDIA FAULT

The north-south trending, westward-dipping Sandia fault [16,20,21] lies at the rangefront of the Sandia Mountains to the east of theCity of Albuquerque (Fig. 1). The fault is one ofseveral, including the Rio Grande fault describedabove, that downdrop structural blocks to thewest into the axis of the Albuquerque Basin. Thefault extends northward from the southwestextension of the Four HillsUplift (Manzano Areaof Fig. 1) on KAFB, to the Placitas area ofSandoval County, a north-south distance of about45km see Table 1).

Evidence for this fault bounding the westside of the Four Hills Uplift part of the SandiaMountains on KAFB is somewhat subjective.Geologically, a major fault should be present herein order to account for the structural reliefbetween the deepest parts of the rift identifiedfrom well data and the top of the SandiaMountains, a vertical offset of apparently morethan 10km.However, there is littleprominentevidence of late Pleistocene movement on thefault on KAFB [SI. Details of seismic-sourceparameters for the Sandia fault are found in Table1. This fault is assumed to be "potentiallyactive." The Sandia fault dips beneath many ofthe facilities of S N L N with an assumed dipangle of 60"W.TIJERAS-CARONCITO FAULTZONEVCFZ)

As defined by previous researchers (e.g.,Reference [2]), the 93+ km long TCfz trendsnorth and northeast between the TravertineHillsof western KAFB and Caiioncito area of theSangre de Cristo Mountains, about 14 miles (mi)(9km) southeast of Santa FeyNew Mexico [3].Extension of this fault zone to the southwest isdiscussed below. The fault zone consists ofseveral fault segments that have near-verticaldips, exhibit evidence of normal and left-lateral

displacement, and have variable amounts andsenses of separation along strike [2,16,20,22].Lisenbee et al. [2] separated the TCfz intofive sections on the basis of structural style, faulttrace complexity, and sense and amount ofseparation. For ease of description and forpurposes of seismic hazard assessment, Wong et

al. [3] informally named these sections (fromnorth to south) the Lamy, San Pedro/Ortiz, MonteLargo, Tijeras, and Four Hills segments (see Fig.1). Wong et al.'s analysis of the TCfz extendedonly as far as the Travertine Hills in the west-central portion of KAFB, The possible extensionof this fault zone further to the southwest isdiscussed under the Tijeras AccommodationZone below.The TCfz has had as much as 1.5mi (2.4km) f left-lateral, post-Cretaceous offset [ZO].

The vertical Tertiary-through-Quaternary offsetalong the zone is complex. The fault zoneexhibits a "scissoring" type rotation [13] withgeneral down-to-the-northwest net Tertiarythrough Quaternary displacement [14, 15,231.Lisenbee et aZ. [2] nd ConnoIIy et aZ.[24] otethat late-Quaternary colluvium is displaced alongthe fault in Tijeras Canyon. No other evidence ofQuaternary activity is documented for othersegments of the fault, although recent evidencefor late Quaternary orpossible even Holocenerupture has been investigated by J. Abbott [25] ata stream-bank exposure near Golden, NewMexico, that may be associated with the TCfz.Analysis of aerial photography shows thepresence of a prominent tonal lineament along theFour Hills segment of the fault on and to thenortheast of KAFJ3, which may be related to lateQuaternary fault activity [2@. South of the Cityof Albuquerque, the fault strongly influencesnear-surface ground-water conditions [5,10], and,thus, may have had late Quaternary displacement.No additional paleoseismic data are presentlyavailable for the TCfz. Seismicity that hasoccurred along and adjacent to the fault zone ispoorly constrained [19].

The relationship of the TCfz to surroundingfaults on SNL/NM (KAFB), such as the Sandiafault to the north and the Hubbell Springs fault tothe south, has recently been refined (see Fig. 2)[5]. A small graben-like structure connects thenorthern end of the Hubbell Springs fault to theTCfz. Subsidence of the graben (and activity onthe adjacent faults) has continued through late

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Pleistocene-Holocene(?) time. The structuralconnection between the Sandia and Tijeras-Caiioncitofaults is more enigmatic because of therelative inactivityof the Sandia fault.Seismic source characteristics for theentire TCfz are presented in Table 1.All

segments of theTCfz are assumed to haverepeated late Quaternary surfacerupture and areconsidered "active.""IJERAS ACCOMMODATIONZONE

As previously mentioned, theAlbuquerque Basin is composed to two distinctstructural domains or sub-basins with opposinghalf-graben geometries [4,14,27,28]. Within thenorthern part of the basin, dips of units within thehalf-grabens are to the east, similar to the SandiaMountains to theeast of the City of Albuquerque.In the southern portion of the basin, dips withinrotated structural blocks are dominantly to thewest. In addition, extension across the northernsubbasin is at least 17percent while extensionacross the southern subbasin is as much as 30percent [4].

Seismic profiles obtained by Shell OilCompany and deep natural-gas test drillholessuggest that these two structural domains orsubbasins are separated by a narrow zone ofcomplex deformation [4]. This "accommodation"or "transfer" zone appears to follow the overallsouthwest to west-southwest trend of the TCfzpreviously described [1,27]. Whether the TijerasAccommodation Zone is continuous with and anextension of the TCfz is not known. Until furtherwork has been done, the relationship betweenthese two features is equivocal. The twostructures may intersect on the southwesternportion of KAFB. The nature of the TCfzchanges with its intersectionwith the HubbellSprings fault. The fault scarp associatedwith theTCfz at th e Travertine Hills, immediately to thesouthwest of the Manzano Area on KAFB (seeFig. 2), is several meters higher than a parallelfault scarp found to the southwest along thesouthern fence of KAFB. Much of thedeformation along the TCfz is believed to betransferred to the Hubbell Springs fault through amapped graben structure that connects these twofaults [5]. The fault to the southwest of theintersection of the TCfz and the Hubbell Springsfaults may be a continuation of the TCfz, asurface expression of the Tijeras Accommodation

Zone, or a separate, but tectonically relatedfeature. An additional uncertainty in the natureof the TijerasAccommodation Zone is itspossible interactionwith the Rio Grande faultnear the center of the Albuquerque Basin. Forthe moment, the Tijeras Accommodation Zone isconsidered a separate potentially seismogenicsource. Further work is required tocharacterizeadequately this structure as a potentiallyseismogenic source.RIO GRANDERIFT SEISMOTECTONICPROVINCE

Seismic source zones are area sources thatare defined by unique tectonic, geologic, andseismologic characteristics. Following thepresentation of Wong et al. [3], the Rio Granderift is considered to be one seismic source zone orseismotectonic province. The purpose ofincluding the Rio Grande rift as a seismotectonicprovince in this evaluation is to address thepotential hazard from background (random)earthquakes near SNLDJM. The backgroundearthquake is defined as an event that occurswithout an apparent association to a known orrecognized tectonic feature, such as a fault. Inthe western U.S., the maximum magnitude for thebackground earthquakeusually ranges betweenML (Le., Richter Magnitude or local magnitude)6 to 6.5 [29]. Depth for the backgroundearthquake can be within the entire seismogeniczone, assumed to range from 2 to 15kmdepth.In most regions of the western U.S.?events largerthan ML 6.5 are usually accompmed by surfacerupture and, thus, repeated events of this size willproduce recognizable fault- or fold-relatedfeatures at the earth's surface. Wong et al. [3]discuss specifics of the Rio Grande riftseismotectonic province. The largest historicearthquake in the Rio Grande rift was the 1918ML 5.5 Cerrillos event [19], located northeast ofthe Sandia Mountains and not associated with anyfaults presented here.SUMMAZZYPreliminary seismic source characteristicsare presented for the eight known major faults orother potentially seismogenic features within 8km of Sandia National Laboratories inAlbuquerque, New Mexico. Multiple faults andfault segments must be considered for thesesource terms since the timing of Quaternarymovements on these faults is largely unknown.

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Therefore, whether particular faults or faultsegments are active during the Holocene or eventhe late Pleistocene is equivocal. A backgroundor "random" ML 6 to 6.5 earthquake, whichmight be expected anywhere within the RioGrande rift, is also considered in the evaluation.Numerous other faults occur within the centralRio Grande rift but are at greater distances @e.,>8 km) itom the site. These more distal faultswould be expected to produce lower strongground motions at the site because of energyattenuation with distance. Further work onsource-term input for seismic hazard studies atSNL/NM may include: 1) field investigations todetermine timing of last movement and recurrentintervals on the various faults, 2) further work onfault segmentation for the TCfz as well as theother faults under study, 3) identification ofadditional faults that should be included inevaluating seismic hazards for the site, 4) use ofthe seismic-source characteristics presented hereto determine potential earthquake magnitudesusing empirical relationships (e.g., Reference[30]), and 5 ) application of attenuationrelationships (e.g., Reference [31] to thesepotential earthquakes for SM/NM. The scope ofthis additional work on seismic-sourcecharacterization will depend on the needs offacilities managers and design engineers.ACKNOWLEDGMENTS

Discussions with Keith Kelson and ChrisHitchcock at William Lettis and Associates,Walnut Creek, California, were particularlybeneficial in evaluating the lengths and locationsof faults and fault segments as potentialseismogenic sources. Additional reviewcomments were provided by David Borns andKathy Gaither of SNL/NM.REFERENCES[l] Chapin, C. E. and S. M. Cather (1994),"Tectonic Setting of the Axial Basins ofth e Northern and Central RioGrande Rift,"

in G. R .Keller and S. M. Cather (eds.),Basins of the Rio Grande Rift: Structure,StratimaDhv. and Tectonic Setting,Geological Society'of America SpecialPaper 291, pp. 5-25.[2] Lisenbee, A. L., L. A. Woodward, and J. R.Connolly (1979), "Tijeras-Caiioncito FaultSystem - A Major Zone of Recurrent

Movement in North-central New Mexico,"New Mexico G eoloPica1 SocietvGuidebook, 30th Annual Field Conference,SantaFe County, pp. 89-99.[3] Wong, I., K. Kelson, S. Olig, T. Kolbe, M.Hamphill-Haley, J. Bott, R. Green, H.

Kanakari, J. Sawyer, W. Silva, C. Stark, C.Harden, C. Fenton, J. Unruh, J. Gardner,S. Reneau, andL. House (1995), FinalReport. Seismic Hazards Evaluation of theLos Alamos National Laboratorv, February24,1995, Woodward-Clyde FederalServices, Oakland, California (in threevolumes).[4] Russell, L. R. and Snelson, S. 1994),"Structure and Tectonics of theAlbuquerque Basin Segment of the RioGrande Rift: Insights from Reflection

Seismic Data," in G. R. Keller and S. MCather (eds.), Basins of the Rio GrandeRift: Structure. StratiPraDhv. and TectonicSetting, Geological Society of AmericaSpecial Paper 291, pp. 83-112.[5] Sandia National Laboratories (1995),Wide Hvdrogeologic CharacterizationProgram (SWHC). Calendar Year 1994Annual Report. Sandia NationalLaboratories. Environmental RestorationProgram, Albuquerque, New Mexico.[6] Hawley, J. W., C. S. Haase, and R. P.Lozinsky (1995), "AnUnderground Viewof the Albuquerque Basin," in C. T.Ortega-Klett, editor, Proceedings of the39th Annual New Mexico WaterConference. The Water Future ofAlbuquerque and Middle Rio Grande

-YBasin New Mexico Water ResourcesResearch Institute, Technical Report, LasCruces, New Mexico, in press.[7] Machette, M. N. (1982), "Quaternary andPliocene Faults in the La Jencia andSouthern Part of the Albuquerque-BelenBasins, New Mexico: Evidence of FaultHistory from Fault-scarp Morphology andQuaternary Geology," New MexicoGeological Societv. Guidebook 33, pp.161-169.[8] Gibson, J. D., J. Milloy, D. Jones, and M.Chavez (1995), "Ranking of Facilities by

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Potential Seismic Vulnerability for SandiaNational Laboratories," Proceedings of theFifth DOE Natural PhenomenaHazardsMitigation Symposium (theseproceedings), (in press).Uniform BuildinF Code (1991 Edition),International Conference of BuildingOfficials, Whittier, California.Hawley, J. W., and C. S. Haase (1992),Hvdrolopic Framework of the NorthernAlbuqueraue Basin, New Mexico Bureauof Mines and Mineral Resources, NewMexico Institute of Mining andTechnology Open-File Report 387,socorro,NM.NEHRP Recommended Provisions for theDeveloDment of Seismic Regulation forNew Buildinq (1991 Edition), F E U 222,Federal Emergency Management Agencyand Building Seismic Safety Council,Washington, DC, January 1992.Department of Energy (1994), NaturalPhenomena Hazards Site CharacterizationCriteria, DOE-STD-1022-94, U.S.Department of Energy, Washington, DC,41 p.Lozinsky, R. P., Hawley, J. W., and Love,D. W. (1991), GeoloFic Overview andPliocene- Ou atern arv His ory of theAlbuaueraue Basin. Central New Mexico,New -Mexico Bureau of Mines andMinerals Resources, Bulletin 137,pp. 157-162.Lozinsky, R. P. (1988), Stratieaphv,Sedimentology. and Sand Petroloe of theSanta Fe Grow and me-SantaFe TertiaryDeDosits in the Albuquerque Basin. centralNew Mexico, Unpublished Ph.D.dissertation, New Mexico Institute ofMining and Technology, Socorro,298 p.Reiche, Parry (1949), "Geology of theManzanita and North Manzano Mountains,New Mexico," Geolo&al Society ofAmerica Bulletin, vox 60,no. 7, pp. 1183-1212.Kelley, V. C. (1977), GeolomfAlbuquerque Basin. New Mexico, New

Mexico Bureau of Mines and MineralResources Memoir 33,59 p.[17] May,. S. J. and L. R. Russell (1994),"Thickness of the Syn-rift Santa Fe Groupin the Albuquerque Basin and its Relationto Structural Style," in G . R. Keller and S.

M. Cather (eds.), Basins of th e Rio GrandeRift: Structure. StratimDhy. and TectonicSetting, Geological Society of AmericaSpecial Paper 291, pp. 113-123.[lS] Kelson, K. I., and S. S. Olig (1995),"Estimated Rates of Quaternary CrustalExtension in the Rio Grande Rift, NorthernNew Mexico," Proceedings of the NewMexico GeoloPical Society. 1995FallField Conference - SantaFeyn press.[19] Sanford, A. R., K. H. Olsen, and J. H. Jaksha

(1979), "Seismicity of the Rio Grande rift," inRiecker, R. E., ed., Rio Grande Rift: Tectonicsand Magmatism, American GeophysicalUnion,Washington, DC, pp. 145-168.[20] Kelley, V. C., and Northrop, S. A. (1973,Geolom of Sandia Mountains and vicinity,New Mexico, New Mexico Bureau ofMines and Mineral Resources Memoir 29,136 p.[21] Woodward, L. A,, J. F. Callender, and R. E.Zilinski (1975), Tectonic Man of the Rio

Grande Rift, New Mexico, GeologicalSociety of America, Map and Chart Series#MC-ll.[22] Maynard, S. R., L. A. Woodward, and D. L.Giles (1991), "Tectonics, Intrusive Rocks,and Mineralization of the San Pedro-OrtizPorphyry Belt, North-central NewMexico," Field Guide to GeologicExcursions in New Mexico and AdiacentAreas of Texas and Colorado, New MexicoBureau of Mines and Mineral ResourcesBulletin 137, pp. 57-70.[23] Grant, P. R. (1982), "Geothermal potentialin the Albuaueraue area. New Mexico."New Mexico Geolo&cal So ietvGuidebook 33, pp. 325-331.[24] Connolly, J. R., Woodward, L. A., andHawley, J. W. (1982), "Road-log segmentI-A: Albuquerque to Tijeras Canyon,"

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New Mexico GeoloPical Society,Guidebook 33, pp. 2-8.J. Abbott (1995), PersonalCommunication, New Mexico Institute ofMining and Technology, Socorro, NM.Kelson, K. I. (1995), PersonalCommunication, William Lettis andAssociates, Walnut Creek, CA.Russell, L. R.., and Snelson, S. (1990),"Structural Style and Tectonic Evolution ofthe Albuquerque Basin of the Rio GrandeRift, New Mexico, U.S.A.,"in Pinet, B.,and Bois, C., eds., The Potential for DeepSeismic ProfilinP for HvdrocarbonExdoration, Editions Technip, Paris,French Petroleum Institute ResearchConference Proceedings, pp. 175-207.Lozinsky, R. P. (1994), "CenozoicStratigraphy, Sandstone Petrology, andDepositional History of the AlbuquerqueBasin, Center New Mexico," in G. R.Keller and S. M. Cather (eds.), Basins ofthe Rio Grande Rift: Structure,Stratimmhv. and Tectonic Setting,Geologiial-Society of America, SpecialPaper 291, pp. 73-81.dePolo, C. M. (1994), "The MaximumBackground Earthquake for the Basin andRange Province, Western North America,"Bulletin of the Seismolo&al SocietvofAmerica, vol. 84, p. 466-472.Wells, D. L., and K. J. Coppersmith(1994), "New Empirical Relationshipsamong Magnitude, Rupture Length,Rupture Width, Rupture Area, and SurfaceDisplacement," Bulletin of theSeismological Society of America, vol. 84,pp. 974-1002.Joyner, W. B., and D. M. Boore (1988),"Measurement, Characterization andPrediction of StrongGround Motion," in J.L. Von Thun (ed.),Proceedings of theConference on Earthauake EnPineeringand Soil Dvnamics: Recent Advances inGround Motion Evaluation, AmericanSociety of Civil Engineers, pp. 43-103.

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