pne 1113 Pre-Gondola 2

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PNE 1113 '

UN ITED STA TES ARMY CORPS O F ENG IN EERS

FO RT PECK RESERV OIRMONTANA

Pre-Gondola.P R E - G O N D O L A IIP R O J E C T

CLOSE-IN GROUND MOTION AND EARTH STRESSReproduced From

Best Available Copy Charles E. Joachim 2 0 0 0 0 9 0 8 1 3 1U. S. Army Engineer Waterways Experiment Station

Vicksburg, Mississippi 39180

U. S. Army Engineer Nuclear Cratering GroupLivermore, California


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LE GAL NOT ICEThis report was prepared as an account o( Government sponsored work. Neither the UnitedStates, nor the Commission, nor any person acting on behalf o( theCommission:

A. Makesanywarranty or representation, expressed or implied, withrespect to the accu-racy, completeness, or use(ulness o( the in(ormation contained in this report, or that the useo( any information, apparatus, method, or process disclosed in this report maynot In(ringeprivately ownedrlgbte; orB. Assumes anyUablllties withrespect to the use of, or (or damages resulting from theun of any informaUon, apparatus, method, or process disclosed In this report.

Ae ueed In the above, "pereon acting on behalf of the Commission" Include. any em-ployee or contractor of the Commieeion, or employeeof eucb contractor, to the extent that.uch employee or contractor of the Commleelon, or employee of .ueh coatraetor ...epare.,d1.nmlnatee, orproYtde. aeeee. to, any lDformaUODpur.U&Dto hi. emplOJlD_t or CODtractwith the Comml IOD,or hi. employmfllltwith .ueh contractor.

Printed in the United States of AmericaAv ail abl e f romClearinghouse for Federal Scientific and Technical InformationNational Bureau of Standards, U. S. Department of Commerce

Springfield, Virginia 22151Price: Printed Copy~; Microfiche ~


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PNE 1113

P RO JE CT P RE -G ON DO LA IIA WET MEDIUM, 140-TON ROW-CHARGE CRATERINGEXPERIMENT IN VARYING TERRAIN

CLOSE-IN GROUND MOTION AND EARTH STRESS

Charl es E . Jo achi m

U. S. Army Engi neer Wat erwa ysE xp er im en t S ta ti on

V ic ks bu rg , M is si ss ip pi 39180

October 1968


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ABSTRACT

Stress, particle velocity, and acceleration data wereobtained from a 140-ton nitromethane row-charge detonationin a saturated clay-shale. The charge row consisted of two40- and three 20-ton spheres (first and fourth charges were40 tons) extending S 11 W from the Pre-GONDOLA I Charlie

crater on an 80-foot spacing (first charge 105 feet fromcrater center). The primary instrument line (stress andparticle velocity gages) extended S 79 E from the centercharge (G) with gage stations 100, 150, 200, 300, and 400 feetfrom G. Gage depths were 10 and 50 feet except the 400-footstation which was gaged at 50 feet only. Acceleration measure-ments were made on the slopes of the Pre-GONDOLA I Delta andCharlie craters and at the Control Point (CP).

Peak stress measurements were higher than Pre-GONDOLA Idata. As the charge-to-gage distance increased, the individualcompressional waves from the various charges began to coalesce.The resulting stresses (coalesced wave) scale using combinedcharge weights and cube root scaling.

Initial peak horizontal velocity compares well withPre-GONDOLA I data. Similar to stress, velocities resultingfrom the coalesced shock front scale using cube root.

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A low-amplitude, long-duration acceleration was recordedat the Delta and Charlie craters. The fractured crater materialfiltered out the high-frequency, high-amplitude motionsanticipated at the crater slope and lowered the average prop-agation velocities. CP accelerations compare well with predic-tions based on competent media.

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PREFACE

This study was performed by the U. S. Army EngineerWaterways Experiment Station (WES) for the U. S. Army EngineerNuclear Cratering Group (NCG) during the period May-June 1967.Field support was provided by the Fort Peck Area Office, CE,and the Omaha District, CEo

The work was conducted by personnel of the WES NuclearWeapons Effects Division (NWED) under the direction ofMr. G. L. Arbuthnot, Jr., Division Chief; Mr. L. F. Ingram,Chief, Physical Sciences Branch; and Mr. J.D. Day, Chief,Blast and Shock Section. NWED Project personnel were Messrs. C. E.Joachim and W. M. Gay. Messrs. L. T. Watson and G. H. Williamsof the Instrumentation Branch, Technical Services Division, WES,were responsible for .the instrumentation. COL John R. Oswalt,Jr., CE, was Director of the WES and Mr. J. B. Tiffany wasTechnical Director during this work.

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CONTENTS

A BSTRACT ---- ------- ------ ------- ------ ------- ------ ------ iPREFA CE -- ------ ------- ------- ------ ------- ------ ------- -- 1CHAPT ER 1 INTROD UCTION ----- ------ ------- ------ ------- --- 5

1 .1 Des cripti on of Ev ent ---- ------- ------ ------- ------ 51.2 Objective s ----- ------- ------ ------- ------ ------- -- 61 .3 Backgroun d ----- ------- ------ ------- ------ ------- -- 6

CHA PTER 2 PROC EDURE ---- ------- ------ ------- ------ ------- 92.1 Exp erimen tal Pl an ---- ------ ------- ------ ------- --- 92.2 Pre dictio ns ------ ------- ------ ------- ------ ------- 92.3 Instr umenta tion ------ ------ ------- ------ ------- --- 12

2.3.1 Gages ---- ------ ------- ------ ------- ------ ---- 122.3.2 Gage Ins tallati on ------- ------- ------ ------- - 132.3.3 Record ing System --- ------- ------ ------- ------ 15

C HAPTER 3 RESU LTS A ND DISC USSION ----- ------ ------- ------ 2 03 .. I nstrum ent Perfor mance - ------- ------ ------- ------ -- 203.2 Dat a Reduc tion --- ------- ------ ------- ------ ------- 2 03.3 Arri val Ti mes ------ ------ ------- ------ ------- ----- 213.4 Soil Stress --- ------ ------- ------ ------- ------ ---- 223.5 Partic le Ve locity ------- ------ ------- ------ ------- 263.6 Acce leratio n Me asurem ents -- ------- ------ ------- --- 28

C HAPTER 4 C ONCLUS IONS ---- ------ ------- ------ ------- ----- 41APPEN DIX A STRES S-, ACCE LERATIO N-, VELOCI TY-, AND

DIS PLACEM ENT-TIM E HISTORI ES - ------ ------- ---- 4 3R EF ER EN CE S - -- -- -- -- -- -- -- -- -- -- -- -- -- -- -- -- -- -- -- -- -- -- -- 71TABLES

2 .1 M AIN GAGE LINE: G AGE TYP E AND SET RANG ES -- ------ - 162 .2 A CCELERO METER LOCA TION AN D S ET RAN GES - ------ ------ 173.1 PEAK M EASUREM ENTS FR OM VELO CITY AND STRE SS G AGES

(MAIN GAGE LINE) - ------- ------ ------- ------ ------- 323.2 PEAK M EASUREM ENTS FROM ACCELER OMETER S ---- ------ --- 34

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FIGURES

A.lA.2A.3A.4A.5A.6A.7A.8A.9

A.10A.llA.12A.13A.14

2.12.23.13.23.33.4

Layout of main gage line ----------------------------Accelerometer layout --------------------------------Arrival time versus distance ------------------------Initial peak soil stress versus slant distance ------Peak soil stress versus distance --------------------Initial peak horizontal particle velocity versusdistance -------------------------------------------- 38

1819353637

4445464748495051525354555657

A.15 Computed vertical displacement time history,Station 150 ----------------------------------------- 58A.16 Computed vertical displacement time history,Statton 150 ----------------------------------------- 59A.17 Computed radial displacement time histories,Station 150 ----------------------------------------- 60A.18 Computed vertical displacement time history,Station 200 ----------------------------------------- 61A.19 Computed radial displacement time histories,Station 200 ----------------------------------------- 62A.20 Computed vertical displacement time histories,Station 300 ----------------------------------------- 63

A.21 Computed radial displacement time histories,Station 300 ----------------------------------------- 64A.22 Computed radial displacement time history,Station 400 ----------------------------------------- 65A.23 Vertical acceleration time history onCharlie Crater Slope -------------------------------- 66A.24 Radial acceleration time history onDelta Crater Lip ------------------------------------ 67

3.5 Initial peak vertical particle velocity versusdistance -------------------------------------------- 39

3.6 Peak acceleration versus distance ------------------- 40Stress time history, Station 100 --------------------Radial velocity time histories, Station 100 ---------Stress time histories, Station 100 ------------------Vertical velocity time histories, Station 150 -------Radial velocity time histories, Station 150 ---------Stress time histories, Station 200 ------------------Vertical velocity time history, Station 200 ---------Radial velocity time histories, Station 200 ---------Stress time histories, Station 300 ------------------Vertical velocity time history, Station 300 ---------Radial velocity time histories, Station 300 ---------Stress time history, Station 400 --------------------Radial velocity time history, Station 400 -----------Computed radial displacement time histories,Station 100 -----------------------------------------

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FIGURESA.25 Vertical acceleration time history on

Delta Crater Slope ---------------------------------- 68A.26 Vertical acceleration time history atControl Point --------------------------------------- 69A.27 Radial acceleration time history atControl Point --------------------------------------- 70

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C HA Pl 'E R 1INTRODUCTION

1.1 DESCRIPTION OF PROJECT PRE-GONDOLA IIP ro je ct P re -G ON DO LA II was a row-charge cratering experi-

ment in weak, wet clay-shale conducted by the U. S. ArmyEngineer Nuclear Cratering Group (NCG) as a part of the jointAtomic Energy Commission-Corps of Engineers nuclear excavationresearch program. The primary purpose of this nominal l40-ton5-charge row-charge experiment was to gain row-charge crateringexperience in a weak, wet medium. In addition, this experimenttested techniques for connecting a row-charge crater toan existing crater and for over-excavating to accept throwoutfrom a follow-on connecting row-charge crater.

P ro je ct P re -G ON DO LA II was detonated in Valley County,near the edge of the Fort Peck Reservoir approximately 18miles south of Glasgow, Montana, at exactly 0800 hours (MDT)28 June 1967. Coordinates of the center charge were W106 38'31",N47 55'51". The orientation of the row was along a 10 east

of north to 10 west of south alignment extending throughthe center of the Charlie crater.

The average lip-crest to lip-crest dimensions were 640feet by 280 feet. Individual charge yields, depths, spacing,

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and resulting apparent crater dimensions were as follows:

ApparentEmplacement Configuration Crater Dimensions

(feet) (feet)Depth of

Charge tons NM** Burst Spacing Width W Depth Da aCharlie (existingcrater) 105.5

E (connecting 38.61 59.7 206.5 55.5crater) 79.8

F 19.70 49.4 152.5 37.579.9G (center crater) 19.55 48.8 164.0 36.979.9H (over-exca- 39.5() 59.9 214.5 57.0

vating charge) 79.9I 20.00 48.8 173.0 33.5

1.2 OBJECTIVESThe primary objective of the study described herein was

to obtain close-in (~400 feet) grovnd-motion and earth-stressmeasurements from a row-charge detonation in weak, wet clay-shale. Mot ion meaaurenerrts were also performed for the exist ingCharlie and Delta crater slopes and at the Control Point (CP).

1 .3 BACKGROUNDEfficient use of nuclear devices for large-scale exca-

vations requires reasonably precise predictions of initial** Spherical charges of liquid explosive nitromethane (CH3N02)Actual total charge weight was 137.42 tons.

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crater dimensions and subsequent long-term stability. Suchpredictions can only be made if cratering experience is gainedin a wide variety of geologic media, particularly those whichmight be encountered in excavation projects. The physicalmeasurement of crater parameters together with measurementsof transient, directly coupled ground motions and stresses

is used to evaluate the engineering properties of the excavatedmedia.

Early cratering experiments were conducted by NCG in drymaterials, i.e., basalt, rhyolite, and desert alluvium. Sinceit is highly probable that some portions of any major excavationwill be in material at least partially saturated, crateringdata are needed for wet materials. Also, design for long-term use of a canal requires knowledge of slope stabilitywhen explosively excavated slopes are subjected to wetting.This includes pore pressure effects of water behind theslopes and erosive effects of water flowing in the channel.The Pre-GONDOLA cratering experiments conducted by NCG atFort Peck, Montana, provide data for one such medium, a weak,wet clay-shale (known as "Bearpaw" shale).

Due to a lack of meaningful cratering data for these media,it was necessary to conduct a site calibration test series.Pre-GONDOLA I, a series of four, single-charge 20-ton experiments,

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was conducted for this purpose. Close-in stress and groundmotion measurements were made in conjunction with the Bravo

1*Event of this series The data obtained served as a basis fordesign of this project on Pre-GONDOLA II, a row-charge event.This report describes that portion of the Pre-GONDOLA IIexperiment concerned with measurement of close-in stress andground motion.

* Superscript numerals refer to similarly numbered itemsin References at the end of the text.

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CHAPTER 2PROCEDURE

2.1 EXPERIMENTAL PLANThe main gage layout for Pre-GONDOLA II is shown in

plan and profile in Figure 2.1. A total of nine earthstress gages, and nine horizontal and seven vertical particlevelocity gages were installed at nominal depths of 10 and 50feet and at horizontal distances of 100 to 400 feet. The deepgages (50-foot depth) were located along a line perpendicularto the charge row at charge G. The shallow gages (IO-foot depth)were installed in separate holes located 10 feet north ofand perpendicular to the main gage line. In addition to themain gage line, surface accelerometers were placed on theexisting Charlie and Delta crater slopes (Figure 2.2) tomeasure motion of the slopes, and surface accelerometers wereplaced at the CPo Table 2.1 lists the main line instrumentationby gage type and location and also gives predicted peak values.Table 2.2 lists all accelerometers, and gives peak predictedvalues.

2.2 PREDICTIONSBecause of the uniqueness of the experiment there was no

empirical basis for predicting stresses and motions. Althoughclose-in earth motions from multiple contained bursts in a

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2linear array have been measured , these measurements were madein an entirely different material (dry basalt) and in linewith the charges rather than normal to the array as plannedfor Pre-GONDOLA II. Therefore, predictions were based onstress and velocity measurements obtained from the 20-tonsingle-charge calibration series (Event Bravo). Basedon these measurements, stress and horizontal particle velocityinputs from the individual charges of the row were computedfor each of the nine gage locations. Cube-root scaling fromBravo was used to obtain the 40-ton charge inputs. Applyingthe principle of superposition, peak values which occurredwithin any 10-msec time interval were added. The maximumvalues thus obtained were used for instrument set-range

predictions (Table 2.1). These predictions were consideredconservative because, in this procedure, no allowance or con-sideration was made for the signal decay.

Peak particle velocity predictions were based on radial1measurements from Pre-GONDOLA I. Using these data, vertical

and horizontal particle velocity predictions were computedfrom the following relations:

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whereuR = radial particle velocityuH = horizontal particle velocityUv = vertical particle velocitye = angle between horizontal and charge-gage lineParticle velocities up to 1/3 uR have been measured

perpendicular to the compressional wave propagation althoughwave propagation theory does not predict these motions. Therefore,the minimum vertical particle velocity prediction used was

No acceleration data were available on crater slopes;therefore, predictions (Table 2.2) were made using the

3following equation taken from Newmark, based on continuous

media.

whereAR = radial accelerationuR = radial particle velocitytR = rise time to peak radial particle velocity

This equation is derived for rockf primarily from tests conductedat the Nevada Test Site.

The peak radial particle velocity obtained from the 20-tonBravo Event was used in this equation. It was assumed that the

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single charge nearest the gage would contribute the maximumground motion input at that gage location due to theunsymmetrical gage-charge geometry (Figure 2.2).

The range of rise times given by Newmark is 1/6 to 1/12of the arrival time. A rise time of one-twelfth the arrivaltime was used in making these predictions. This method gavethe highest peak acceleration prediction and was the moreconservative approach. Peak vertical accelerations were predictedusing the same method used for peak vertical particle velocity.

2.3 INSTRUMENTATION2.3.1 Gages. Earth stress measurements were made with

1/4- and 1/2-inch-diameter tourmaline gages purchased fromCrystal Research, Inc., Cambridge, Massachusetts. The 1/2-inchgages were employed in the predicted stress region from2,500 psi to 3,500 psi, and the 1/4-inch gages for pressureshigher than 3,500 psi. These gages had been used successfully

1in previous tests in the Pre-GONDOLA seriesVelocity gages used in this study were Sandia Model DX gages

purchased from Spartan Industries, Albuquerque, New Mexico.These gages operate on the principle of the overdamped acceler-ometer. A variable reluctance sensor is used. A more detailedgage description can be found in Reference 1. Vertical particlevelocity gages used were horizontal gages modified by theaddition of a spring to counteract gravitational forces on the

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. . A cce ler ome ter s use d we re of two ty pes : str ai n gag ea nd va ria ble r elu cta nc e. The a cce le rom ete r des ign ate d "200 AR C L"was a 1,0 00- G-c apa ci ty ins tru me nt ma de b y C on sol ida tedE lec tro dyn ami cs Co rpo rat ion , Pa sad ena , Ca lif orn ia, andt ha t d esi gna ted "150 AR CS" was ma de by E nd evc o Co rpo rat ion ,P as ade na, Cr. lif orn ia. T he r ema ini ng ga ges we re va ria blerel uct an ce ty pe ma de b y Pac e En gin eer ing Co mpa ny , No rthH ol ly wo od , C al if or ni a.

2 .3. 2 Gag e In sta lla tio n. A ho rizon tal and a ve rti calv elo cit y g age wer e mou nte d in a 5-1/2- inc h-d ia met er c ani ste rwi th a sso cia ted c ali bra tio n ele ctr on ics . T he ca nis terass emb ly was fi lle d with p ara ffi n fo r wat er pro ofi ng ands ho ckp roo fin g of the co nte nts . Th e e lec tri cal ca ble was

fed to t he g rou nd s urf ace th rou gh a 3/4- inc h-d iam et er alu min ump ipe thr ea ded i nt o the can ist er li d. The pi pe a lso ser vedas a pl ace men t an d ori ent ati on dev ic e.

Si gna l cab le f rom t he to urm ali ne str ess ga ges wa s pr o-t ect ed wit h l-i nc h rig id p las tic pip e t o th e g rou nd sur fa ce.The g age pro tru ded 1 in ch b el ow th e en d of th e pl ast ic p ipe .For i nst al lat ion the st res s g age a ss emb ly wa s ta ped t o th evel oci ty gag e can ist er so th at i t exten ded 6 inc hes be lowt he b ott om o f t he c ani ste r.

All ma in g age l ine ins tr ume nt ho les we re de ep er tha n

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required gage depths and contained water to within a fewfeet of the surface. These were filled with sand to approxi-mately 1 foot below the desired gage depth. This wasaccomplished by shoveling sand into the hole and allowingit to settle through the water. The entire gage assemblywas then lowered to the desired depth and oriented. Sufficientsand was shoveled into the hole to ensure that the tourma-

line pressure gage and part of the canister were surroundedby sand. A grout mix was then placed by l-inch-diametertremie pipe from the top of the sand forming a 3-foot-longplug. When the grout had set, the remainder of the holewas backfilled with sand.

Horizontal and vertical accelerometers were mounted ina 3-1/2- by 3-1/2- by 6-inch aluminum box which was filledwith paraffin. The box was fastened to a 4- by 4-inch woodpost that had been buried in the crater wall.

Electrical signals from the velocity gages and thetwo variable reluctance accelerometers located in the Charliecrater were carried on four-conductor shielded cable to ajunction box (Figure 2.1) located approximately 500 feet from

the charge row. Connections between the junction box andthe WES instrumentation van were made with a 50-pair telephonecable. The two strain gage accelerometers required individualshielded cables and were not connected to the junction box.

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Four-conductor shielded cable was used for all gages in theDelta crater.

Piezoelectric gage signals were carried on coaxial cable.A piece of "low noise" cable, approximately 100 feet long,was used at the gage. The remaining cable was standard coaxial.The low noise cable was utilized to prevent cable noise fromobscuring the portion of the pressure-time history of

interest. It was not necessary to bury any surface cable runssince the data of interest would have been retrieved beforedamage from crater ejecta.

2.3.3 Recording Systems. All instrumentation outputs,except from the tourmaline stress gages and strain gage acceler-ometers, were recorded on light-beam galvanometer oscillographs.The high-frequency outputs of the tourmaline stress gagesand strain gage type accelerometers were recorded on an FMmagnetic tape recorder. Signal conditioning equipment variedwith the type of instrument; velocity gages and variablereluctance type accelerometers used a 3 kcps carrier-demodulatorsystem; strain gage type accelerometers used a solid-stateDC operational amplifier system; and the tourmaline stressgage used a cathode follower system.

All electronic recording equipment was housed in theWES recording van located approximately 2,100 feet south ofthe Pre-GONDOLA II row charge.

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oWES .] W ES 2 W ES 3 W E~4t000 $..-50~50 ..$ 100-_'''~$1--''f-l00~n-s n.7 IIS n9 n] 0 o

PLAN

LEGEND0 10-FOOT DEPTH$ 50-FOOT DEPTH 20-TON NM~ 40-TON NM0 JUNCTION BOXa EARTH STRESS

U R RADIAL VELOCITYU V VERTICAL VELOCITYNOTE: ALL DIMENSIONS ARE IN FEET.

10 0 15 0 20 0 30 0a 0 IT 0 a 0 a 0

U R U R I U R I U R IU V I U V I l I V U V II Ia $ a $ a $ a $

U R U R U R U RU V U V U V U V

SECTION

40 0 o

Figure 2.1 Layout of main gage line.

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LEGEND 20-TON NMQ 40-TON NMo ACCELEROMETERS

(HORIZONTAL AND VERTICAL)NOTE: ALL DIMENSIONS ARE IN FEET.

C HA RL IE C RA TE R

I

D EL T A C RA TER

Figure 2.2 Accelerometer layout.

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CHAPTER 3RESULTS AND DISCUSSION

3.1 INSTRUMENT PERFORMANCEAll timing and sequence-initiating signals were received

and properly translated, resulting in all recording equipmentoperating as planned.

Of the 35 gages installed for Pre-GONDOIA II, 32 were'operable at shot time. Gage 100 S 50 apparently faiLed priorto detonation although resistance readings had given noindication of this condition. Equipment in the WES vansustained damage when the site transformer bank was hit bylightning, and lightning damage is suspected in the preshotfailure of gage 200 AR CL, a strain gage accelerometer. Afterequipment repairs, a gage check revealed this gage to beinoperable. A resistance check, upon removal from thecanister, showed all leads open. The cause of failure in200 AV CL is not known. Three of the remaining gages(100 UV 10, 100 UV 50, and 200 UV 50) were overdriven andrendered only qualitative data.

3.2 DATA REDUCTIONThe oscillograms and tape playbacks were read on an electro-

mechanical digitizer, and the data converted to card form. Thesedata cards were then processed through a digital computerwhere a temperature correction and an integration were performed

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on the particle velocity records to yield displacements. Alldata were then automatically plotted.

Peak measurements of particle velocity and stress aresummarized in Table 3.1. Acceleration peak values are presentedin Table 3.2. Time histories of particle velocities and theirassociated displacements, soil stresses, and accelerationsare presented in Appendix A.

3.3 ARRIVAL TIMESCompressional wave front arrival times at all main line

gages are plotted versus slant distance in Figure 3.1. Theaverage propagation velocity based on gages at charge depthwas 6,600 ft/sec. Gages at a nominal 10-foot depth yieldedslightly longer arrival times and, consequently, a slowerpropagation velocity. The higher velocity at depth is probablydue to more competent material at charge depth compared tothe weathered zone near the surface.

The average compressional wave velocity (6,600 ft/sec) forthe main gage line was lower than the value reported for the

1Pre-GONDOLA I Bravo Event. The Pre-GONDOLA I value was basedon gages spread over a greater distance. The shock wavetraveled through deeper, more competent material to reachthe farther gage stations. The result was a slightly highervelocity. The accelerometers located at the CP yielded avelocity comparable to the Pre-GONDOLA I value of 6,800 ft/sec.

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More precise arrival times were obtained from the piezo-electric gage traces than from the particle velocity recordsbecause of the ability of the stress gages to respond faster.

3.4 SOIL STRESSInitial peak stress versus slant distance is plotted in

1 4, 5The 20-ton Pre-GONDOLA land scaled graniteFigure 3.2.data are shown in this figure for comparison. The firstdisturbance sensed by all pressure gages in the main gagearray was caused by charge G (with the exception of stations300 and 400 feet from G, both at 50-foot depths). Thecompressional waves from charges F, G , and H coalesced aftertraveling approximately 290 feet and are not separatelyidentifiable 300 feet from charge G. The compressional wavesfrom charges E and I still lagged the coalesced wave slightlyat the 400-foot station (see Figure A.l2). Data from thedeep gage stations 300 and 400 feet from G are presented atboth actual (80 tons) and scaled distances (20 tons) in

.1/3The scaling factor is S = (Wl/W2) where:igure 3.2.= combined charge weight (F, G, and H)= charge weight being scaled (20 tons)

Initial peak stress data from the deep gages are consistentlyhigher than those from shallow gages. The deep gages werelocated in stronger, saturated, more competent material whichtransmitted stronger shock. The shallow gages were apparently

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located above the groundwater level which is estimated tobe between 10 and 20 feet below ground surface in the Pre-GONDOLA II

6area. In addition, wave forms recorded by shallow gagesat stations 200 and 300 feet from charge G (gages 200 S 10and 300 S 10, Figures A.6 and A.9) indicate the presenceof an unloading or tensile (rarefaction) wave which furtherreduced peak values at these stations. The gage station150 feet from charge G yielded initial peak stress datasignificantly higher than the general trend (gages 150 S 10and 150 S 50, Figure A.3). That both deep and shallowgages responded in this manner indicates some cause otherthan gage error.

When a compressional wave impinges on a free surface oran interface of lower acoustical impedance, it is reflected

7as a tensile or unloading wave. Tension is not recorded assuch but is manifested as a decrease in compressive stress.When a gage is located in a medium with a sufficiently closeboundary such that the difference between direct and reflectedray paths is small, tensile relief resulting in lower peakvalues can occur. The shallow gages were located close

23

enough to the surface that tensile relief must be investigated.Consider the following:


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Appa rent ris e ti me(f ir st p ea k)

0.3 m sec 0 .9 msec 0.5 m sec 0 .9 msec

Gage10 0 S 10 150 S 10 20 0 S 1 0 300 S 1 0

(F igure A.l) (Figu re A.3) (Figure A.G) (Figu re A.9)Co mput ed AT(reflected-direct)

1 .5 ms ec 1.4 m sec 0.7 mse c 0.3 m sec

The shock wave fro m a s pheri cal so urce eman ating into ah omog eneou s, co ntin uous medi a, suc h a s B earpaw clay- shal e,. 7d1sp erse s and at tenu ates This ca uses a rou ndin g o f t he

s hock fr ont, r esul ting in l onge r ris e t imes with d istan ce. Thecom pari son prese nted ea rlie r shows a rise ti me incr ease withdist ance o ut to t he l50 -foot s tati on (gage 1 50 S 10) while asho rter a ppare nt ris e ti me was me asur ed at t he 200 -foo ts tati on (gag e 2 00 S 10). The comp uted dif feren ce be twee nre flec ted and di rect arr ival t imes at the 20O-f oot st atio nis ve ry clos e to the ap pare nt ris e time valu e, m aking te nsilerel ief at thi s sta tion a di stin ct pos sibi lity. A si milarco mpar ison a t t he 30O -foot stat ion (g age 30 0 S 1 0) i nd ic at esth at tens ile re lief had taken plac e, resu ltin g in a lowerin itia l peak str ess valu e.

Peak soil str ess data a re plo tted ver sus sla nt di stanc ein Fig ure 3.3. One g age (100 S 10 ) was da mage d af ter r ecord ingthe i niti al peak s tres s, res ulti ng i n loss of add itio nalst ress data from th is gag e. T he dee p gages r ecord ed hi gherpeak valu es t han the shall ow ga ges. T his was p arti ally d ue

2 4


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to the stronger, saturated, more competent material found atdepth but primarily was the result of the gage-charge geometryused for the shallow gages. Placement of these gages 10 feetnorth of the main gage line resulted in longer traveltimes for the stronger compressional wave from charge H (40 tons)than for charge F (20 tons). This difference decreases atgreater distances. It is particularly evident when comparingdeep and shallow gage data at the l50-foot station (gages150 S 10 and 150 S 50, Figure A.3) as follows:

Charge Gage 150 S 10 Gage 150 S 50Weight, Slant distance, Travel time, Slant distance, Travel time,

No. tons feet msec feet msec

G 20 155 24.1 150 21. 9

F 20 170 25.6 170 24.4

H 40 182 26.4 170 24.4The wave form at the deep l50-foot station (gage 150 S 50)

shows that, as expected, the charge F and H compressional wavesarrived almost simultaneously but the charge H compressionalwave lagged the F wave by almost 1 msec at the shallow gage

(150 S 10). This results in three distinct peaks (compressionalwaves from F, G, and H) with only a small increase in totalpeak stress at the shallow gage.

25


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E xami nati on of time -his tori es f rom the dee p gage s (F igur es A.3,A.6, A.9, an d A.12) indi cate s that the ga ged a rea is in atra nsit ion zo ne. Pe ak stre ss a t the 15 0-fo ot stat ion (Figu re A .3)is the su m of a p arti ally dec ayed pul se fr om a 20- ton char ge(G) and the con tribu tion of a 40- ton (H ) and a 20- ton (F)charg e. As th e d ista nce in creas ed, thes e comp ress ionalwave s t ende d t o coa lesc e. The wav e fo rm reco rded at the400 -foo t st atio n (g age 40 0 S 5 0) ind icat es t hat ch arge sF, G, a nd H h ave co ales ced and inpu t f rom char ges E a nd Istill l agged sl ight ly.

The ini tial peak pre ssur e att enuat ed as the -2 powe r ofdi stan ce as was fo und for the Pre-G ONDO LA I s eries . T otal peakstres s a lso att enuat ed as the -2 powe r of d ista nce at th e300 - an d 4 00-f oot s tati ons. It must b e note d th at the effe ctiv ei nput c ontin uall y chang ed over t he g aged re gion du e tocoale scen ce of shock waves fro m t he se para te char ges. Alth oughthe com press iona l wave s f rom al l five char ges h ad n ot coa lesc edat the 400- foot sta tion it i s pr obabl e t hat after co alesc enceatten uati on wou ld c onti nue as th e -2 power of d ista nce.

3.5 PART ICLE V ELOC ITYIni tial horizont al parti cle ve loci ty d ata a re pres ente d

i n Fi gure 3.4. H ere (as with th e str ess meas ureme nts) th e26


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ini tial peak valu es a re i nput s f rom char ge G (20 tons) exceptthe deep ga ges (30 0 UR 5 0 an d 4 00 UR 50) at sta tion s 300 an d4 00 fee t from G. Data f rom th ese ga ges are pr esen ted i n Fi gure3.4 at both ac tual an d s caled d ista nces . An effe ctiv e cha rgewe ight o f 80 ton s was as sumed fo r s cali ng. W ave forms re corde dby th e sha llow gage s (200 UR 10 and 300 UR 10) at s tati ons200 and 300 fe et from G i ndica te t hat tens ile re lief hastaken pla ce. In addi tion , the s hall ow g age at 200 fe et fr om Gwas ti lted wit h the arri val of the i niti al comp ress iona l waveand re gist ered a hig her than n ormal pe ak valu e. Th is d atapo int is ques tiona ble.

Pr e-GO NDOL A I data (horizonta l p arti cle ve loci ty) a reincl uded in Fi gure 3.4 f or c ompa riso n. Th ese d ata were no tcorr ecte d for te mper ature in t he o rigi nal re port l The g agecali brat ion proc edur e wa s p erfo rmed at 65 F . As sumi ng thesame grou nd t empe ratu re as a t Pr e-GO NDOL A II (50 F), a tem pera turecorr ecti on fac tor of 1.18 is ap plied . The t hree clos estP re-G ONDO LA I me asur ement s a re in dica ted a s low i n Re fere nce 1.T he ga ge lo cate d at a sla nt di stanc e of 97 fee t was ov erdri ven,whil e t hose at slan t di stanc es of 1 00 a nd 133 fee t experi encedtens ile rel ief. Th e rem aini ng P re-G ONDO LA I dat a p Oint s co mpar ewell wit hin th e usual d ata sc atte r (i.e. 2 0 perc ent) w~th thePr e-GO NDOL A II d ata.

Vert ical part icle velo city dat a ar e prese nted in Fi gure 3.5,an d exh ibit consi dera ble sc atte r. Wave for ms reg iste red at t he

27


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shal low s tatio ns 200 and 300 feet from G (g ages 20 0 U V 10 a nd300 UV 1 0) i ndic ate tha t th ere has bee n s ome ten sile rel ief ofpe ak val ues. Th e ga ge at the st atio n 20 0 f eet from G (ga ge2 00 UV 10) a lso ind icat es ear ly t iltin g, making t he init ialpea k v alue quest iona ble.

Par ticl e ve loci ty-ti me hi stor ies a nd f irst in tegr als(di splac emen t) ar e pr esen ted in A ppen dix A. No b ase lin ec orre ctio ns were appl ied to the ve loci ty da ta. Th erefo re,the i ntegr al-t ime hist ory (di spla ceme nt), r elat ive data atb est, mu st b e re garde d as onl y qua lita tive .

3.6 AC CELER ATIO N M EASUR EMEN TSPeak a ccel erat ion dat a are pl otte d versu s hor izon tal

d istan ce in Fig ure 3.6. In re tros pect , t he p eak a ccel erat ion

p redi ctio ns were ov erly co nser vativ e. Th ey were b ased onthe assu mptio n of co mpete nt ma teri al an d d id not take intoacc ount the pr esen ce of t he i nter veni ng cra ter (in t he case o fmeas urem ents on the Ch arli e c rate r lip). Mo reov er, onl yemp iric al info rmati on was av aila ble pre shot. The co mbina tionof these fa ctors (eff ect o f crat er b ounda ries and rub ble)stro ngly in fluen ced the maximum s urfa ce acce lerat ions a tth e cl ose- in stat ions . H owev er, e stima tes fo r the C P moti onswere mu ch bett er, an d excel lent m easu remen ts we re obt aine d att hi s l oc at io n.

28


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Based on arrival time data at Delta crater (gages380 AR DL and 425 AV DS), a propagation velocity of 4,000 ft/secwas computed using the distance to the closest charge (I).This value is much slower than the 6,600 ft/sec value computedfor the main gage line instrumentation. The discrepancy isexplained as follows. Propagation velocity computations arean average value for all the material between two pOints, in

this case between the closest charge (I) and the Delta cratergages. Two distinctly different materials are encountered bya shock wave traversing this line; crater rubble and a morecompetent clay-shale. Consider the gage located on the Deltacrater slope (425 AV DS) with an arrival time of 106.6 msec.Assuming a propagation velocity of 6.6 ft/msec in clay-shaleand 1.5 ft/msec in the rubble, a path approximately 80 feetlong through the rubble would result in an average velocityof 4,000 ft/sec at this gage. Delta crater rupture zonemeasurements were not made. Excavation of the Bravo crater(also a single-charge 20-ton experiment in similar material)gave the following information*:

* PNE-ll03, in preparation.

29


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Radius from Charge,feet

Depth to Base of RuptureZone feet

125 60175 43225 21375 o

Gage 425 AV DS was located approximately 10 feet below theoriginal ground surface at a 50-foot radius from the centerof the Delta crater. Based on the above information, an80-foot-long path in rubble appears realistic.

The accelerometer (150 AV CS) located on the Charliecrater slope was situated on the far side of the crater awayfrom the closest charge (E). The shock wave reaching thegage had to travel under or around the intervening craterthrough the rubble. This resulted in a longer compressivewave ray path to the gage and a higher average velocity thanthe 2,000 ft/sec computed using the horizontal gage-chargedistance. Charlie crater is located at the edge of the FortPeck Reservoir which had a pool elevation at Pre-GONDOLA IIshot time of 2,243*6 This was 5 feet above the pool elevationat the end of the Pre-GONDOLA I series. The bottom of the Charliecrater is at elevation 2,220 which is 18 feet below the poolelevation at the end of Pre-GONDOLA I. Therefore, the rubble* Elevations are in feet referred to mean sea level.

30


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under the Charlie crater was probably saturated, which wouldresult in higher average velocities at this location than atthe Delta crater.

31


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oz

.~til0.

C)Q)til : > : >Q) C D Q).~.~.~r - t r - t r - tC D C D C DJ . < J . < J . ~U l ; : : : J ; : : : J U l0 0 0 00 0 0 0r - t r - t r - t r - t

>~; : : : J ; : : : J U l0 0 0o o I ! ' ). . - I . . - I r - t

32

ooor - tM

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or - t00

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< : f < I ! ' ) C \ I < : f < ( o M M I ! ' ) < : f < l ' - l ' -C \ l C \ I C \ I < : f < M O O O ( o O O O OC \ l C \ I M M M M M M < : f < < : f < < : f ~ > e < :; : : : J ; : : : J U l ; : : : J ; : : : J U l ; : : : J ; : : : J0 0 0 0 0 0 0 0I ! ' ) l t l O O O O O Or - t r - t C \ l C \ l C \ l C \ l C \ l C \ l

> e < :U l ; : : : J : : J0 0 00 0 0M M M


38/81

UlUl 0 00) 0 0H .~ t- t-O) . . . , Ul: :s en . 0. ':!' C\ IS r-l"" ' : :s t1l'0 S > -0) .~ 0) t> :: s ~ . ! < ! r-l . . . , o e n t-, : : : : t1 l t1 l o .~ 0) C\ I r-l.~ ~ 0) .~ o Ul."... . . , :J. . . . . , 0 t1 l 0) 'HC) C 1 l :J. . > -. . . . , ;s :"" ' . ! < !r . : : ! C) UlZ 0 Ul 0 0H .c (j) .~ 0 0. . . : I en . H Ul t- t-O) . . . , 0.r . : : ! :: s en . ':!' C\ It :: l r-l r-lt 5 C 1 l t1l.~> -. . , J . . ) >.Z .~ .: 4 rl . . . , 0H , : : : : d o .~ Q) e n t-~ H0) .~ o Ul C\ I r-l0. . . . . , 0 < 0) "-' 0e n e n C O H H '0 r-l~ Q l!j ':!' ':!' ':!' :: s cO H oH .w ::: cO 0C,) cO 0. ~ . . . ,S H : : s . . . ,0) 0) : :s 0)r . : : ! b f\ 0. 0 H:> (iJ ;., S cO0 ell 0) 0):g . . . , ~ .c . . . , :>.. . cs C c: U 0000 .~ 0) : ; : :cO -l- D 0000 H . . . , :> 0r > : . . rl U; S 'H MM ':! ' ':! ' 0 .~.~ .cen . .~ 0 'H Ul . . . , Ulen . Q . . . 0 . .. ,~ 'H '0 0. ,e n Ul0) 0) 0 Q)r . : : ! bD . . . , 0. 0~ til 0 C co 0) 0) 0 ell~ r-l b D H .~ I= ! . . . ,:: > til (j) ;., H . . . , 0 [/Jen . . . . , .: d 0 0 'M .~~ C .c o S .w '00 dU 0000 0:g N w . . . , 0000 Ul r-l S r-l.~ u : '" 'H MM ':!' ':!' 0) cO: : . : : H ... , 0 .~0 r-l cOD~ 0 Q . . . . . . , .~ c;j c: : r : : 'H .~ . . . , 'M 00. . o H '0 N0 0) cO . . . .r-l > - p: : Hr-l 0 0 0) 00l!j 0l!j > - : : r : :M l!j l!jp:: p ::~ 0 en . :: > en . :: >z w~

0000 ~0000 f i tM ':!' o : j . s : :til til til til r-t r-tr-t r-t s : : s : : . . . , O M (J)C I . l . s : : . s : : . s : : . s : : Q) Q) (1) Q) 0 0 o M . . . ,E -< U U U U O O O O U U (J) O M (J)Z o (J) (1)~ Q)

0.0 0bD 0. s : :til (1) tilIl:: o r-t bD s : : . . . ,;::l til Q) ~ 0 s :: (J)C I . l . . . , 0 til O M 0 O M~ s : : s : : . s : : . . . , 000000io tn 00 . . . , O M '00 til U 'H 00tn tn 00 00 N N 00 0 . . . ,:g t'I . . . , N N r-t r-t M C) ' : : t : :M >1l::>1l::>1l::>1l::~~~ 0 ~~~~~~~~OOZ r . : : : I!X l 00 0000tntn 00 E -


40/81

U 40W(J)~u i~I-.J 30< t>ita:< t

20

70

60

50

Cs:: 6,600 FT/SEC

100 200 40000SLANT DISTANCE FROM CHARGE G, FEET

Figure 3.1 Arrival time versus distance.

35

500


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OlD-FOOT DEPTH 50-FOOT DEPTHo PRE-GONDOLA I6. SCALED(BO-TON SOURCE)~ TENSILE RELIEF

V i PRE-GONDOLA Ia.IIiI/)w 1,000a ::I-

GRANITE~\I/)_j0 (HARDHA T AND SHOAL) \I/) (SCALED) \: . : :

O~0

\100

o

100 1,00020 L-L-~-L~ -L__~~~ __-~L-~~ -L__~50

SLANT DISTANCE FROM CHARGE G, FEET3,000

Figure 3.2 Initial peak soil stress versus slant distance.

36


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100,000

UlD .viUlU J0:f0 -sn.J(5UllI:U JD .

10,000

1,000

l- I I T T T 1 I -I- -I- LEGEND -I- -I- 0 . to-FOOT DEPTH - SO-FOOT DEPTH~ J) TENSILE RELIEF -l- -I- -

0

I- -I- -l- -I- -I- -- -- -- -

~

I- -* -f- -f- -

I I f I , , J0060 tO O

SLANT DISTANCE FROM CHARGE G, FEET600

Figure 3.3 Peak soil stress versus distance.

37


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uwVI -I-U0..J 100W>W..JS !I-0: :a ...JI-Z0N0: :0I~wa ...J 10I-~

LEGENDo 10-FOOT DEPTHo 50-FOOT DEPTH

PRE-GONDOLA ISCALED(SO-TON SOURCE)TENSILE RELIEFOVER DRIVEN

2 ~ - - ~ ~ - - ~ ~ ~ - - - - - - - - - - - - - - ~ - - - - - - - - ~ - - - - ~ - - ~ ~ ~ ~ ~ - - ~ ~ ~50 109 1,000

SLANT DISTANCE FROM CHARGE G, FEET

Figure 3 . 4 Initial peak horizontal particle velocity versus distance.

38


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50 I I

LEGEND -0 la-FOOT DEPTH0 50-FOOT DEPTH~ TENSILE RELIEF -

UU JI/)< 0I-I J . .> - l-- -U0.JU J>U J.JUI-a:-cQ..Jc(U 10I-a: I-U J ->! I i : : - -c(U JQ. - -.Jc(l- I- -~

I- -0

I- -

3 I I100 400SLANT DISTANCE FROM CHARGE G. FEET

Figure 3 . 5 lnitial peak vertical particle velocity versus distance.39


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30 I I I T I I I I I

- 0 -CHARLIE CRATERSLOPE

- -- -~ -~ 0 -D E LT A C RA TE RLIP -r-r- -- -

- -0D E L T A C RA TE R 0SLOPE CP

- -- -- LEGEND -- 0 RADIAL -0 VERTICAL- -I I I I I I I I 1

10

zoI-0: :w_JwoolI:-cwu

0.4100 1000

HORIZONTAL DISTANCE FROM CLOSEST CHARGE, FEET3,000

Figure 3 . 6 Pea k a cce ler ati on v ers us di sta nce .

40


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CHAPTER 4

CONCLUSIONS

The computed Pre-GONDOLA II propagation velocity was6,600 ft/sec. This is lower than the value reported forPre-GONDOLA I. The Pre-GONDOLA I value is an average valueover a longer distance. The shock wave reaching the farthergages travels through a deeper, more saturated, more competent,d en se r m at er ia l.

Initial peak stress data are the result of input fromcharge G (20 tons) at all stations except the deep gages 300and 400 feet from G. These exceptions scale using the combinedcharge weights of F, G, and H (80 tons). Wave forms indicatetensile cutoff of peak values at shallow stations 200 and300 feet from G. Although higher initial stresses were measuredfrom Pre-GONDOLA II than I, both attenuated as the -2 power ofdistance.

Peak stress measurements were obtained in a transitionzone where the effective charge input was changing withdistance. As the charge-to-gage distance increased, individualcompressional waves began to coalesce, resulting in higherstresses with distance than found for initial peak data.Pulses from charges F, G, and H coalesced approximately290 feet from charge G, but all five charge inputs had notcoalesced at the 40D-foot station. Placement of the shallow

41


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gages 10 feet north of the main gage line resulted in a lossof symmetry. Thus, greater distances were required for theindividual compressional waves to coalesce. Where coalescenceis complete, scaling using combined charge weights of thecoalesced pulse is effective.

Initial peak horizontal velocity similar to initialstress is the result of input from charge G (20 tons) at allstations except the deep gages 300 and 400 feet from G.Peak values at these stations scale using cube-root scalingand combined charge weights of F, G, and H (80 tons). Thesedata compare well to Pre-GONDOLA I data.

Peak acceleration predictions for the crater slopes werebased on competent material and did not take into account thepresence of the intervening crater rupture zone. This methodresulted in good predictions at the CP, but did not predict thelow motions on the Charlie and Delta crater slopes. Maximumsurface accelerations on the crater slopes were strongly influ-enced by the effects of crater boundaries and rubble.

42


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APPENDIX A

STRESS-, ACCELERATION-, VELOCITY-,AND DISPLACEMENT-TIME HISTORIES

43


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o o z '0 ' o o z - '00"J 3S ll ~ - l l I J 0 1 3 A

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oor-I

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Z..d

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en L & J tilW en :II: tila :: Z - Q)Q.. . . . . ' "~ W of.). . . . Ul0 MU :I: :I:06 . . . :u.. Q)' ": sb .O.r-!" ' "

. ~ o o o o ~ o o o o t 0 o o o o t - O O O ( J C J O O O l o o o o t 0 o o o o t -I S d - SS3~lS l I D S I S d - SS3~lS l I D S

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o e t :Q)r- .;jb DoMIii

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m.~a >lot;:lb. O.r-!r . . .

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o '0008 '0009 'OOOh 'OOOlI S d - SS3~lS l I D S

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pne 1113 Pre-Gondola 2

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