USGS-474-184

UNITED STATES DEPARTMENT OF THE INTERIOR

GEOLOGICAL SURVEY

PORTIONS OF THIS REPORT ARE ILLEGIBLE. lt has been reprodt~c~d from the best available copy to permit the broadestpossible avail-ability. ,

Seismicity of the Pahute Mesa Area, .,;: -:;.

Nevada Test Site -:;: -:: :""

8 October 1975 to 30 June 1976

by

A. M. Rogers, G. H. Wuo11et, and P. A. Covington

1977 .

Prepared under Agreement No. E(29-2)-474B

for the

Nevada Operations Office

-----NOTIC£-----.

1bl& ...,. .. - prepmd ..... ICCOIII\1 of work sponoored by the Unltod Sta,., Gowmmcnt. Nelthor the Uni,.d Sta,.l nor the Unitod Slatel Deparlllllnt of Ene'l)', nor any or their employlel, nor any of th<l• contractors, subconuacton, or their liD!~• makes any wuranl)', exprtll or Implied, or _,... any lepl U.bUII)' or mpontlbUII)' ror thelCCIIfiCY,comple,._ or usdulnca or lilY mrormatlon, appantut, prod.t&et 0t proceu dllcloled, or repmentl thet irl ue wolll4 not lnfri¥ priVIltly owned rtaltta.

Environmental Research ar.d Development Administration

DISTRlBUilON QE tHJ.S D.OCtlMfl'l.t IS tJNClMITED

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TABLE OF CONTENTS

Page

Abstract-------------------------------------------------------- 1

Introduction---------------------------------------------------- 2

Seismi~ instrumentation----------------------------------------- 6

Hypocenter determination---------------------------------------- 10

Earthquake magnitudes------------------------------------------- 15

Temporal and spatial variation in seismicity-------------------- 16

Summary--------------------------------------------------------- 40

Acknowledgments--------------------------------------------·----- 42

References cited--------~-------------------·-------------------- 43

Appendix-------------------------------------------------------- 46

11

ILLUSTRATIONS

Page

Figure 1. Map showing the location of the Nevada Test Site

and the Southern Nevada Seismic Net-------------- 3

2. Map showing the locations of announced nuclear

tests in the Pahute Mesa and Rainier Mesa

areas-------------------------------------------- 5

3. Graph showing number of events per log versus time

and the time of occurrence of each of the

announced nuclear events------------------------- 17

4a. Graph showing frequency of occurrence for all

data--------------------------------------------- 21

4b. Graph showing the frequency of occurrence during

the 1968-70 nuclear testing program-------------- 23

5-13. Maps showing:

5. Locations of earthquake aftershocks during

the 23 days after event Kasseri----·-------- 25

6. Location of earthquake aftershocks during the

44 days after event Inlet------------------ 26

7. Location of earthquake aftershocks during the

40 days after event Muenster--------------- 27

8. Location of earthquake aftershocks during the

2 days after event Fontina-------------~--- 28

9.' Location of earthquake aftershocks during the

24 days after event Cheshire--------------- 29

Page·

Figures 5-13. Maps showing: (Continued)

10. Location of earthquake aftershocks duri.ng the

5 days after event Estuary----------------- 30

11. Location of earthquake aftershocks during the

3 days after event Colby------------------- 31

12. Location of earthquake aftershocks during the

105 days after event Pool------------------ 32

I 13. Epicenters of all earthquakes located during I

the monitoring period---------------------- 33

14. Graphs showing the distribution of epicentral dis-

tance for sets of aftershocks following events

(a) Kasseri, (o) Inlet, (c) Muenster, (d) Fontina,

(e) Cheshire, (f) Estuary, (g) Colby, (h) Pool--- 36 15. Graphs showing the distribution of focal depth for

sets of aftershocks following events (a) Kasseri,

(b) Inlet, (c) Muenster, (d) Fontina, (e)

Cheshire, (f) Estuary, (g) Colby, (h) Pool, (i)

all aftershocks---------------------------------- 38

16. Vertic~! orthogonal cross sections through the

epicentral regior.. covering the areas shown in

figure 13--------------------------------------- 16

iv

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TABLES

Page

Table 1. Seismograph station data and corrections------------- 7

2. Velocity model used in locating seismic events------- Il

3. Event name, number of aftershocks, days counted, and

event magnitude----------------------------------~- 19

v

ABSTRACT

A total of 1,075 earthquakes occurred in the Pahute Mesa area with

2.5SML~4.9 during the period October 28, 1975, to June 28, 1976. The

majority of these earthquakes are aftershocks of the nuclear events,

Kasseri, Inlet, Muenster, Fontina, Cheshire, Estuary, Colby, and Pool

(5.8~ML~6.3). Smaller nuclear events <ML~5.5) on Rainier Mesa and Yucca

Flat detonated in the same time period did not trigger aftershock

sequences. The aftershock series were displaced laterally from ground

zero and occurred deeper (at 4-6 km) than the nuclear event depth of

burial (-1 km). The aftershocks appear to occur on vertical faults with

approximately north-south strike.

The number of aftershocks following each nuclear event generally

declined as the testing program progressed (for instance, Kasseri trig-

gered twice as many events as Colby). Comparison of this series with

the 1968-70 nuclear test series shows that Benham triggered about nine

times the number of aftershocks associated with Kasseri. Aftershock b-

values were lower during this series than the 1968-70 series. The range

of b-values in the earlier period was 1.7~b~2.0 while during this period

b ranged between 0.9sb~l.4.

1

INTRODUCTION

The principal goal of this program was to locate aftershocks

related to high-yield nuclear tests conducted by the Department of

Energy {formerly Energy Research and Development Administration) at the

Nevada Test Site (NTS) and to document the temporal variation in seis­

micity. The intent of this data report is to make available the basic

seismological observations concerning the nuclear event induced se~s­

micity at NTS during the 1975-76 testing program (Accelerated High Yield

Testing Program). Subsequent reports will present detailed analyses of

these data in relation to the geologic structure, nuclear e~ !nt induced

faulting, and tectonics of the region.

Earthquake activity has been previously observed to follow large

nuclear explosions ou the Pahute Mesa (Boucher and others, 1969; Ryall

and Savage, 1969). In an earlier study by the U.S. Geological Survey

(Hamilton and Healy, 1969; Hamilton and others, 1971; Hamilton and

others, 1972), a dense network of seismic stations was used to monitor

aftershocks from the 1,100-kt Benham test on December 19, 1968, and five

other tests. Two of the tests, Jorum in 1969 and Handley in 1970, were

also in the 1,000-kt yield range. The Almendro event in 1973 was also

monitored for aftershocks (Bayer, 1974) using the USGS Southern Nevada

network with two supplemental stations.

2

w

118° 116°

o CITY OR TOWN 0102030408060

a SEISMIC STATION KILOMETERS

113°

./---+------ARIZONA

\ t T

36°

NEVADA TEST SITE ll' /,, . I '. .

---.. ..

113°

Figure 1.--Hap showing the location of the Nevada Test Site and the Southern tlevada Seismic Net.

The current seismic monitoring program was initiated October 8,

1975, prior to event Kasseri, the second of six large tests in an accel­

erated nuclear testing program in 1975 and early 1976. New seismic

stations were installed in the northern and central part of the NTS

(BMT, NPM, NRM, EPN, TMN, GLR, and SSP). These stations and the ten

stations which were already recording are shown in figure 1. The older

stations include LSM, CPX, and MCV on NTS, Angels Peak (APK), Las Vegas

(LVw), South Pahroc Range {PRN), and four which belong to Sandia Laboratories

including Darwin, Calif. (DAC), Nelson, Nev. (NEL), Tonopah, Nev. {TPH),

and Leeds, Ut~h (LEE). All the stations operated to the end of June

1976 except for a few temporary outages due to power or telephone line

difficulties.

During this report period, there were five nuclear events in the

yield range 200-1,000 kt (kilotons), three events in the 200-500-kt

rang•~, and two events with yields less than 20 kt in the Pahute Mesa and

Rainier Mesa regions of the Nevada Test Site. The location of these

events is shown in figure 2.

During the same period, there were five announced nuclear events on

Yucca Flat (east-central NTS). The yield ranges for these events are:

one in the 200-500-kt range, three in the 20-200-kt range, and one less

than 20 kt. These events are listed in the appendix, but are not shown

in figure 2 or succeeding maps, because they are not believed to be

associated with seismic activity.

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/ " _ __/ '" \ ..,A.,!STUARY l

ltu \ *COLBY-'- )...{*MUENSTER

l £ '\ )ii( KASSERJ FONT INA

+ .,.A._ JVt £ *POOL +

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* 200-1000 KT * 200-500 KT e <20 KT

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F:isure 2.--Hap showing the locations of announced nuclear tests in the Pahute l4esa and Rainier Uesa areas.

SEISMIC INSTRUMENTATION

Station locations, travel time delays, magnitude corrections,

magnification, and equipment types are shown ih table 1. Equipment at

the USGS stations is powered by commercial power whenever possible, but

where commercial power is not available, batteries or gas-driven thermal

electric generator is used. A frequency-modulated tone is carried by

wire or radio to a central point where it is combined with tones from

other stations, and the multiplexed signal is then transmitted by tele­

phone circuits to the USGS office in Las Vegas. There, the signal is

demodulated by discriminators and recorded on 16-mm film.

6

....

Table !.--Seismograph station data and correctior.~

Station Latitude N. Longitude W.

BMT 37°17.01' 116°32.02'

NRH 37°16.73' 116°12.25'

:!:PN 37°12.83' 116°19.42'.

NPM 37°23.04' 116°19.38'

SSP 36°55.52' 116°13.11'

TMN 37° 5.02' 116°26-.53'

GLR 37°11.97' 116° 1.05'

CPX 36°55.89' 116° 3.40'

LSM 36°44.32' 116°16.68~

MCV 36°38.01' 115°59.99'

PRN 37°26.50' 115° 4.00'

DAC 36°16.61' 117°35.62'

TPH 38° 4.49' 117°13.35'

NEL 35°42. 7iJ I 114°50.61'

Travel time delay no. 11

.05 sec.

.18 sec

.01 sec

-.06 sec

.02 sec

.01 sec

-.13 sec

-.16 sec

.02 sec

.03 sec

.57 sec

.39 sec

.24 sec

--

Magnitude l1agnificat!nn correct:f.on2 Seismometet' VCO/amp @ 1 Hz

.19 L-4C 6242 209 K

.33 L-4C 6242 12Z K

-.18 S-13 6202 90 K

.35 L-4C 6242 122 K

.15 NGC-21 6242 188 K

.46 NGC-21 6242 55 K

.02 NGC-21 6242 218 K

.20 NGC-21 6207/L-5 112 K

-.08 S-13 6202 257 K

.34 NGC-21 6207/L-5 217 K

-.40 NGC-21 6202 111 K

-- Benioff

-- Benioff

-- Benioff

01)

Table !·.--Seismograph station data and corrections--Continued

Magnification Station Latitude N. Longitude W. Travel time delay no. 11

Magnitude correc tion2 Seismometer VCO/amp @ 1 Hz

LEE 37°14.59' 113°22.60' .72 sec Benioff

LVW 36°10.20' 115°11.25 1 .60 NGC-21 6207/L-5 22 K

APK 36°19.14' 115°34.44' .25 uec .68 S-13 6242 60 K

lsubtracted from seismic wave arrival times for events in Pahute Hesa and Yucca Flat areas.

2Added to magnitude calculation.

-~·

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The various manufacturer~1of the seismic equipment used in this

investigation are:

Seismometers:

Mark Products (L-4C)

National Geophysical Company (NGC-21)

Geotech Division, Teledyne Industries (S-13)

Develco (L-7D)

Voltage control oscillators:

Develco (Models 6202, 6207, and 6242)

Amplifier:

National Geophysical Company (L-5)

Discriminators:

Develco (Model 6203)

EMTEL (Model 6243)

Film recorder:

Geotech Division, Teledyne Industries

Film viewer:

Geotech Division, Teledyne Industries

l/The use of brand names in this report is for descriptive purposes only

and in no way constitutes endorsement by U.S. Geological Sur-~rey.

9

HYPOCENTER DETER}l!NATION

Hypocenters are computed from arrival times of P waves using the

program HYP071 (Lee and Lahr, 1975). The model of seismic velocities

used in thP. earthquake location program is the same one used by Hamilton

and others (1971) and is shown in table 2.

Earthquake locations were first attempted using only the stations

on NTS. The quality of the final solution of many of the aftershocks

was improved by using selected arrival-time data from stations, PRN,

DAC, TPH, LEE, or APK, if the event was not within the close-in network;

if missing data created a large azimuthal gap between adjacent staLions;

and if impulsive first arrivals were recorded at those stations.

Travel-time station corrections were used in the final location of

all the events. These corrections are intended to be mean compensations

for differences in the structure beneath each station. The corrections

were derived using the following procedure. All the events were located

using data from the NTS stations. Pahute Mesa was divided into a grid

about 4 km on a side and an attempt was made to select an equal number

of the best locations from each square. Fifty-one such events were

chosen, and the mean station residual was calculated for each station

using these events. The earthquakes were relocated using the mean

station residuals as station corrections, and the mean residuals from

this run were added to the previous station corrections to obtain the

final corrections. Corrections for the distant stations were obtained

during this procedure even though t .. ~y were not used in the location

procedure at this point. All the earthquakes were relocated using the

derived st~tion·corrections and all the stations. At several point~

poor individual station readings were culled from the data. The final

locations are listed in the appendix.

10

Table 2.--Velocity model used in locating seismic events

Depth to layer Layer velocity krn krn/sec

o.o 2.7

0.96 3.4

1.33 3.8

2.14 4.4

2.50 5.1

5.00 6.1

25.00 7.0

35.00 8.0

L

11

Only earthquakes greater than or equal to magnitude 2.5 were

located in this study. The appendix also includes events of this magni­

tude or greater which were not lo~atable because of station difficulties

or overlap of events. Whenever possible, an attempt was made to'deter­

mine the approximate duration magnitude of these events. Events in the

appendix with no location or magnitude are bel~eved to be greater than

magnitude 2.5, and the time listed is the P-wave arrival time at the

nearest station. The list of events undoubtedly contains a combination

oi naturally occurring earthquakes, triggered events, and events related

to cavity collapse. Some events, probably related to the cavity col­

lapse, demonstrated emergent P-wave onsets, and good quality locations

for these events were often difficult to obtain.

12

..

L

Another location scheme was also tried and rejected. Station cor-

rections were derived using the nuclear tests themselves by running

HYP071 with the known origin times and locations. These station resi-

duals were then used to locate the aftershocks. Comparing these loca-

tions (B) with the locations found using the previous scheme (A), we

find that scheme A yields SO-percent A- and B-quality solutions, while

scheme B yields 35-percent A- and B-quality solutions. Comparison of

the standard errors in the hypocenters shows that scheme A has consist-

ently smaller standard errors than scheme B. On the other hand, scheme

B locates the nuclear explosions closer to their actual location than

does scheme A. This paradox can apparently be explained by examining

the A- and B-ray paths. The scheme-A first-arrival ray paths (after-

shocks) are predominantly direct arrivals because the depth of the

aftershocks is typically greater than 2 km. For the location model

used, it was found that direct arrivals were first arrivals for events

greater than 2-5 km deep and stations less than 17 km from the epi-

center, or for events greater than 5 km deep and stations less than 130

km distant. These conditions include the preponderance of first arri-

vals for scheme-A determined residuals. For the case of a direct

arrival, the ray leaves the source at an angle (take-off angle, it)

greater than 90°. For scheme A, it is predominantly greater than 90°

and always greater than 40°. For scheme B, the nuclear explosion depth

of burial (all l~ss than 1.5 km) and station distances are such to

always produce refracted first-arrival paths resulting in itS50°. Thus,

nuclear-event ray paths traverse th~ upper layers twice, while the

earthquake ray paths traversa once. The point is that station correc-

tions derived from nuclear events are not likely to be optimal for

locating earthquakes and vice-versa. 13

;--

Another aspect of scheme B is that it produced all negative station

residuals. That is

Residual=T 0 -Tt<O, p p

where T 0 =observed travel time, and p

Tt=theoretical travel time. p

Thi~ observation indicates that the crustal model near-surface layers

have velocities which are too low. Plotting of the average residual

versus the average epicentral distance for each station shows that the

residual is increasing negative out to epicentral distances of about 60

km after which it becomes approximately constant and small negative.

This behavior indicates that the shallow refracted paths are too slow

while the deeper refracted paths are approximately correct. If it were

possible to correct the crustal model, the effect on scheme-A locations

would probably be to reduce the focal depths of the aftershocks some-

what •

.. '

14

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EARTHQUAKE MAGNITUDES

Magnitudes were determined using the duration of the seismic

signal. A formula for calculating du-:ation magnitude (FMAG)(Lee and

others, 1972) is incorporated in the HYP071 program.

FMAG=-0.87+2 log(T)+0.0035D, where FMAG is the local

magnitude, approximating ML· T is the time in seconds from the initial

P-wave motion until the signal amplitude decreases to 1 em

and remains less than 1 em on a 20X Geotech film

viewer, and D is the epicentral distance in km.

Magnitude station corrections were determined for this array by

comparing FMAG determinations to amplitude magnitudes (ML) determined

using a L-7D velocity seismograph at station CPX. Five earthquakes in

the magnitude range 2.4-3.6 were recorded on the L-7D, and equivalent

local Richter magnitudes were determined. A graph of FMAG and ML versus the logarithm of coda length was constructed for each station.

The magnitude increment observed between two straight lines with a slope

of 2 fit to these two data sets was accepted as the magnitude correc-

tion. These corrections are shown in table 1.

For 13 evenLs, it was possible to compare Berkeley or Pasadena

magnitudes with those in this study. The mean difference between the

magnitudes was -0.09, and the standard deviation of the differences was

0.34. The largest difference observed was 0.5 magnitude units. Thus,

the magnitudes ~isted in the appendix are believed to be equivalent to

the Richter magnitude.

15

TEMPORAL AND SPATIAL VARIATION IN SEISMICITY

The number of events occurring per day versus time is plotted in

figure 3. These data show a pattern of aftershock activity that peaks

in essociation with the largest nuclear tests. Eight episodes of in­

creased activity can be noted in association with the events Kasseri,

Inlet, Muenster, Fontina, Cheshire, Estuary, Colby, and Pool. All of

these nuclear events are magnitude ~~5.8 and occur on Pahute Mesa. It

should be noted that between October 8, and October 28, 1975, prior to

event Kasseri, only one earthquake occurred on Pahute Mesa. This event,

on October 25, was in the vicinity of nuclear event Tybo ("ot shown)

detonated May 14, 1975. On November 8, 1975, an earthquake occurred on

Yucca Flat, apparently unrelated to the nuclear testing program. No

other earthquakes were noted on Yucca Flat or Rainier Mesa during the

monitoring period. However, the magnitude of nuclear tests in these

areas were lower <Mt~S.6) than the Pahute Mesa nuclear events. Other

earthquake activity that took place in the area included: an event a

few kilometers southwest of station LSM on January 29, 1976; an event a

few kilometers northeast of station MCV on January 30, 1976; an event 15

km west of NTS on April 24, 1976; and 18 earthquakes (4.2~~~2.5) a few

kilometers south of NTS in June 1976.

The increase in activity at the time of events Keelson and Esrom

(fig. 3) represents earthquakes occurring near event Muenster and is

probably not related to these two Yucca Flat events. Note that a

similar increase in activity occurs in the interval between Muenster and

the Yucca Flat t.:Vents.

16

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Table 3 compares the estimated number of aftershocks associated

with each event for two different time intervals, 23 days and 10 days.

For intervals that overlap one or more nuclear events, the count is

based primarily on earthquake location, but the percentage of unlocated

earthquakes assigned to an event is equal to the percentage of located

earthquakes related to the event. Table 3 shows that the amount of

aftershock activity generally decreased with subsequent shots, although

the magnitude of the nuclear events did not decrease with time. For

instance, Kasseri (M=6.2) triggered about twice as many events as Colby

(M=6.2). Comparing events Kasseri, Muenster, and Colby in figure 3, it

appears that aftershock activity falls off more rapidly following the

last two events than after Kasseri.

In the period from April 1, to June 28, 1976, following completion

of the Accelerated High Yield Testing Program, a mean of 2.7 events/week

was observed in the Pahute Mesa region. This rate can be compared with

0.8 events/week that occurred between January 1971, and March 1973, in

the same region. The magnitude of the events detected during the

earlier interval was comparable with that in this study (Bayer, 1972a,

b, 1973a, b, c, d; Bayer and King, 1972a, b; Bayer and others, 1972);

although it is unknown if events above ML~2.5 were completely reported.

During the earlier period, ~here were 19 announced nuclear events at

NTS. All events were less than magnitude 5.4 and occurred off Pahute

Mesa. Based on these data, an upper-bound estimate of about three is

obtained for the ratio of activity at the end of the current monitoring

period compared with the earlier period.

18

Table 3.--Event name 2 number of after hocks,

days counted, and event magnitude

Nuclear Number of Number of event

Event events days Events/day magnitude

Kasseri 206 23 9.0 6.2

Inlet 36 23 1.6 5.9

~.l:Ut:!nSter 179 23 7.8 6.3

Font ina 108 23 4.7 6.3 ' ! '-

Cheshire 41 23 1.8 5.8

i Estuary 65 23 2.8 5.9 ' ~·

Colby 96 23 4.2 6.3

Pool 87 23 3.8 5.9

Kasseri 197 10 19.7 6.2

Inlet 27 10 2.7 5.9

Muenster 144 10 14.4 6.3

Font ina 80 10 8.0 6.3

Cheshire 59 10 5.9 5.8

Estuary 46 10 4.6 5.9

L Colby 98 10 9.8 6.3

Pool 102 10 10.2 5.9

The frequency of occurrence data and maximum likelihood least

squares (Page~ 1968) fits to L'iic data are shown in [j_gure 4a for five

different time intervals. The equations and corresponding intervals

are:

y2 ......._

Total Logl 0N1=5.47-1.08M 12.8

Kasseri Log 10N1=5.93-1.42M 5.0

Muenster Logl 0N1=4.48-0.95M 6.8

Fontina

Colby

Logl 0N1=4.75-l.09M 6.5

Log N1=4.98-1.15M 1.5 10

where N~=interval frequency l.

df

7

3

4

3

3

M=magnitude midpoint~2.8

M =maximum magnitude 5.0 max

x2=chi-squared values

df=degrees of freedom.

Examination of these data indicates they are complete for magnitude

.2:.2.7.

20

l

1 100 .. _

z

I.

10

COLBY-FONTINA

1 2 3 6

. . . Figure 4a.--Graph showing frequency of occurrence for all data (o)(253

days), 13 days f9llowing event Kasseri (x), 39 days following event Muenster <b,.), 24 days following event Fontina 0, and 14 days follow­ing event Colby (A). The lines are maximum likelihood least squares

to the data.

'j

Figure 4b shows the recurrence data for the 1968-70 testing period

for comparison. These data have been corrected for the difference in

duration magnitude formulas used by adding DM to magnitudes determined

by Hamilton and others (1971) where

DM=0.096M+0.266

The maximum likelihood least squares fit to these data is given by:

Total

Benham

Jorum

Handley

~ d. f.

Log1 0N1=8.03-1.74M 14.3 8

LogloN1=7.91-1.74M 8.8 7

Log 10N1=8.20-2.01M 8.0 4

Log1 0N1=7.89-2.03M 2.2 2

where ~3.39 for total and Benham

M~3.28 for Jorum and Handley

M =5.0 max

Below magnitude 3.39, the data appear to be incomplete for the first two

data sets. While this problem may affect the second two data sets,

incompleteness is not apparent from examination of the data. Tests of

x2 goodness of fit (Walpole and Myers, 1972) for all nine of these

recurrence relations indicate that the hypothesis that the earthquakes

occur according to these relations cannot be rejected at the 5-percent

significance level.

22

• • •

I I· 100

• /TOTAL

. \ BENHAM TO PURSEl

z I L ..

10

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. \ \\ HANDLEY~\\

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6

Figure 4b.--Graph showing the frequency of occurrence during the 1968-70 nuclear testing program 0>; for the Benham-to-Purse period (o) (439 days); for t' Torum-to-Hundley pc.!riocl (4) (191 clays); and for Handley to the end of • •e recording period ~)(280 clays).

Comparison of these data shows that the 1968-70 series of nuclear

tests triggered a larger total number of aftershocks than during the

more recent testing series, in spite of the fact that the 1968-70 series

included only three magnitude-6 or greater nuclear events. On the basis

of the fitted frequency curves for magnitude ~3, Benham <ML=6.3) trig­

gered about nine times as many earthquakes as Kasseri <ML=6.2). It also

appears that b-value has declined with time. During the 1968-70 period,

b-values varied between 1.7 and 2.0, while during the 1975-76 period

values ranged between 0.9 and 1.4.

Figures 5-13 show the aftershock locations as a function of time.

The majority of seismicity associated with event Kasseri occurs west of

a north-south line through gz (ground zero). An event of magnitude

Mt=4.0 was the largest located aftershock which occurred northweRt of

gz. An unlocated magnitude-4.9 aftershock occurred about 5 days after

Kasseri.

Inlet aftershock series is shown in figure 6. These events are

predominantly east of gz. Three magnitude 4.0 or larger unlocated

aftershocks occurred during this period.

The majority of aftershock epicenters shown in figure 7 following

Muenster are north of the shot point. A north-northeast-striking

epicenter lineament north of gz is apparent in this aftershock series

and includes a magnitude-4.0 event. Two other magnitude!-4 aftershocks

were triggered by this event. One of these was locatable and occurred

about 3 km northeast of gz.

24

37°30'...------------.--------------:r-----,

~~·L-------------~~--~----------------~~----~ 116°30 116°15'

'

.5.--Hap showing the locations of earthquake aftershocks during 23 days after event Kasseri (K). Star symbol indicates the

of event Kasseri.

l ~ l

\

37°30'--------.,------------.-----,

,r-----~

/ '

" /

_/ ' \- --- 'I \

\ +

QK \

\+ + ~~ \ I+

\

\ \

EPICENTER Ml \ X > 4.0 I

I X 3.5-4.0

+ 3.0-3.5

+ < 3.0 .10 km I

37000'L.-------~11~6o~30:---L_---------;1;-;-:16~0 ;;157' __ ____.

Figure 6.--Hap showing the location of earthquake aftershocks during the 44 days after event Inlet (I). Star symbol indicates the location of

Circle indicates the location of Kasseri (K).

I

i I l--

! L

! I

I.

I I-

37°30'----------,.-1-------------,.,------,

/ \ ___ _/

\

' 4++ '1 I

oK \~+t I + M + I

x- + L

o, \

\ \ EPICENT~R Ml

I X > 4.0

I X 3.5-4.0

I + 3.0-3.5

I + < 3.0

Scale I

~~·L--------------L-·--~IL---·------------~'L-----~ 116°30 116°15'

Figure 7.--Hap showing the location of earthquake aftershocks during the 40 days after event Muenster (M). Star symbol indicates the location of event Huenster. Circles indicate the locations of Kasseri (K) and

(I). 27

'

37°30'.------------,-------------r------,

--- --""""' . . / '

""' /

_/ ' ,- --\ ~ \ + + 0 \

~ OK M

+ +\

\ 0 I

I

I

\

\ \

EPICENTER

I ML

X > 4.0

X 3.5-4.0

+ 3.0·3.5

+ < 3.0 0 10 km

Scale

37000'(._ _______ _,_ __ .__ _________ -'--:------1

116°30 116°15'

Figure 8.--Hap show:i.ng the location of earthquake aftershocks during the 2 days after e~rent: Fontina (F). Star symbol indicates the location of event Fontina. Circles indicate the locations of Kasseri (K), Inlet (I), and 11uenster (11).

J

. I L

L f

...

~~·~--------------~-----------------------.-------,

0 I

,------"""" / '

/ " \ ___ __/

\ +

+\ +

+ + OK l()M \

\ "- OF + .X ~CH + \ 01

Scale

10 km I

\

\ \

1 EPICENTER ML

X > 4.0

X 3.5-4.0

+ 3.0-3.5

+ < 3.0

'

"' I I

~~·~--------------_.----~------------------~------~ 116°30 116°15'

i. Figure 9 .--Hap showing the location of earthquake aftershocks during the '· · · 24 days after event Cheshire (CH). Star symbol indicates the location

of event: Cheshire. Circles indicate the locations of Kasseri (K), ter (H), and .Font:ina (F). 29

.!

I

37°~'r------------------,----------------------------.---------,

,~----"'""

,/ X '"-. __/ + '

+ +x '-.... ~{~ l

E OM I QK

QCH + \

\ \

EPICENTER

I Ml

X > 4.0

X 3.5-4.0

+ 3.0-3.5

+ < 3.0 0 10 km

Scale

37000''----------'---.1----------""----....J 116°~ 116°15'

Figure 10.--Hap sho\V'ing the location of earthquake aftershocks durins the 5 .days after event Estuary (E). Star symbol indicates the location of event Estuary. Circles indicate the locations of I<asseri (K), Inlet (I), UuenstP-r (M), Fontina (F), and Cheshire (CH).

30

l i l ..

! ..

L

l i

37"30'.------------,-------------.-------,

OK

OCH

\

\ \

1 0 10 km

Scale

Eo +oM

o,

EPICENTER

X X + +

+

Ml

> 4.0

3.5-4.0

3.0-3.5

< 3.0

37000'.._ ________ .__ _ __._ ___________ -'--------1

. 116°30 116°15'

Figure 11.--H:ap showing the location of earthquake aftershocks during the 3 days after event Colby (C). Star symbol indicates the location of event;, Colby. Circ!'es indicate the locations of Kasseri (K), Inlet (I), Muenster (M), Fontina (F), Cheshire (CH), and Estuary (E).

31

37°30'.----------~,-------------,,-------,

+

/-- --""""""' / '

"" /

-+-__/ ' ,- + '1 + \

EQ +

\ oc I +++ '4t + OK +~fJ+ +

\¥-+oF + M + I

\-1:- p~ + L OCH +

~ \ 01 +

\

\ \

\ EPICENTER ML I X > 4.0

I X 3.5-4.0

+ 3.0-3.5 I

I + < 3.0

? 1? km

Scale I

37000' I I I 116°30 116°15'

Figure 12.--Hap showing the location of earthquake aftershocks during the 105 days after event Pool (P). Star symbol indicates t!1e location of event Pool. Circles indicate the locations of Knsseri (K), Inlet (I), Huenster (11:), Fontina (F), Cheshire (CH), Estuary.(E), and Colby (C).

l L

I l

' . -\-

\

+\A + +

\

+

0 5

Scale

10 KM

/

+-_/

X

\

\ \

I

+ /-----~

/ X ' c'~,

'I

+ c

EPICENTER ML

X > 4.0

X 3.5-4.0

+ 3.0-3.5

+ < 3.0

, Figure 13.--Nap showing the epicenters of all earthquakes located during the monitoring period. Brackets indicate the areas used for the vertical sections shown in figure 16.

_l

Eventc associated with Fontina appear in figures 8, 9, 10, 11, 12,

and 13. The activity associated with Fontina is largely west and south

of gz although the largest aftershock (~=4.2) occurred about 2 km

northeast of the shot point.

The Cheshire aftershocks are shown in figure 9 and occur south-

southwest of gz. Ten days after Cheshire, activity was renewed in the

Muenster vicinity on what appears to be a north-striking lineament 1 km

west of gz. The activity south of Fontina gz begins 2 days after Cheshire

as a diffuse group of events farther from gz than during the previous

period.

Aftershocks associated with event Estuary are shown in figure 10.

These earthquakes form a particularly diffuse pattern. The largest

aftershock (~=4.3) near the northern border of NTS is not well loc9ted

because of emergent first motions. This event may be a poorly located

collapse. The magnitude-4.1 event south of the first is a better

located aftershock and is probably a tectonic event that occured 7 hrs

after Estuary.

Figure 11 shows the Colby aftershock series which is also rela-

tively diffuse. The largest located aftershock (~=4.9) is poorly

located and lit "ly to be a collapse event. An unlocated magnitude-4.6

aftershock was also observed.

The Pool aftershock series is shown in figure 12. The events form

an apparent sublineation striking north-northwest on the southeast side

of gz.

Figure 13 shows epicenters of all earthquakes located during the

monitoring period. The brackets indicate the areas used for the verti-

cal sections shown in figure 16.

34

Figure 14 shows the epicentral distribution of aftershocks for each

of the nuclear events. All epicenters ~20 km from the nuclear event ar~

shown at 20 km. Each bar graph covers the time period from the deton-

ation of the current event up to the time of detonation of the next

event. Aftershocks associated with a previous event are included in the . I I_ plot for the current event iri those cases where there is overlap in the

aftershock series. Examination of the epicenter plots together with

these graphs permits some separation of earthquakes into groups asso-

ciated with particular nuclear events. In each case, the aftershocks

which can be clearly related to a given nuclear event appear to be

concentrated within 6 km of gz. The percentage of aftershocks within 6

km of gz for Kasseri, Inlet, Muenster, Fontina, Cheshire (neglecting

those aftershocks near Fontina and Muenster), and Colby varies from 93-

100 percent. The number for Estuary is 88 percent assuming earthquakes

out to 10 km are related to this event. The Pool percentage varies from

52·-100 percent depending on the assumed outer radius for Pool-induced

events. Comparing these percentages with those of Hamilton and others

(1971)(95 percent of aftershocks within 14 km) indicat~ that these

events occur in tighter clusters about gz. The epicentral distance mode

value is in the 1-3 km range except for events Pool and Estuary. In

every case, the aftershock activity is displaced away from gz.

35

w 0'

00 r;:;;l ~ < :;:J Cl --E-4 ez::: < r;:;;l

r... 0

~ r;:;;l ~ :a :;:J z

(a)

KASSERI

%1.-!2 4 6 8 10 12 14 16 18 20

(d)

FONT INA

2 4 6 8 10 12 14

(g)

COLBY

.

1o1 8rn (b) ~t I INLET

101 8t-6~

i 4

2 4 6 8 10 12

(e)

2 L

en 2 4 6 8 10 12 14 16

lOr (h)

8~~~00L M-4

2

19 t

14 12 10 8 6 4

2

(c)

MUENSTER

0o 2 4 6 8 10 12 14 16 18 20

10 l (f)

6r ESTUARY

~fC11Jo.nn D.n, 0 2 4 6 8 10 12 14 16 18 20

1 I I I

0o 2 4 6 8 10 12 14 16 18 20

EPICENTRAL DISTANCE (KM)

Figure 14.--Graphs showing the distribution of epicentral distance for sets of aftershocks following events (a) Kasseri, (b) Inlet, (c) Muenster, (d) Fontina, (e) Cheshire, (f) Estuary, (g) Colby, (h) Pool. Events beyond 20 km are grouped at that distance.

Figure 15 shows the distribution of focal depth for each aftershock

series using only A- and B-quality solutions. For clarity in these

1

graphs, an attempt has been made to show only those earthquakes asso-

L ciated with a given nuclear event. Figure 15d, the Fontina series,

includes earthquakes in that vicinity through event Pool. Figure 15e,

the Cheshire series, does not include aftershocks near Fontina or I

j l"

Muenster. The mode of aftershock focal depths varies between 4 and 6

km, and the average depth varies _from-4 to 9 km depending on the after-.; ' ..

shock series. Few aftershocks occur at depths characteristic of the

nuclear events depth of burial (0.8-1.4 km). This result \vas also

observed during the 1968-70 series (Hamilton and others, 1971). The

smaller nuclear events, magnitude 5.8-5.9, produce shallower events and

a smaller range of focal depth distribution than do the larger events.

With the exception of Inlet, which is the shallowest of all the after-

shock series, there is also a trend to shallower depths with time. The

greater focal depths associated with this series compared to the 1969-70

series is probably completely attributable to the location scheme.

Using location scheme B (referred to above) with these data yields a

mean focal depth of 3.3 km (standard deviation of 2.40 km). Hamilton

and others (1971) found a 3-4 km mean focal depth with 95 percent of the

events in the upper 5 km. The greater dispersion in depths for the

1975-76 series may be attributable to lower station density in the

epicentral region.

'1".-10 sets of orthogonal cross sections are shotm in figure 16.

Comparing these plots with f:f.gure 13 shows that the earthquake hypo-

centers form nearly vertical bands striking approximately north-south.

In most cases, these bands are displaced laterally and 1-2 km below gz

indicating that the earthquakes are occurring on vertical faults that do

not intersect gz. 37

t 4r

0o 2

en 121 1-z 101 w

~ 8

- u. 6

~ 0 I DOB

ffi 41 ~ iCCl

(a)

KASSERI d=8.7

4 6 8 10 12 14 16 21

t

(d)

d=6.4

:E ::::> z 0o 2 4 6 8 10 12 14

t (g)

~B r.A~LBV l d=6.2

! I '-.J 0 2 4 6 8 10 12

f<'

(b) INLET

r~ o. 0o 2 4 6 8 10

(e)

CHESHIRE OrB d=6.7

2

[ ~n Do 0o 2 4 6 8 10

8

61 (h) POOL d=4.2

2 4 6 8

DEPTH (KM)

15 (c)

t I MUENSTER

DOB

! 0o 2 4 6 8 10 12 14 16

6

~ (f) 4 DOB ESTUARY

1 r.-r·3 :~· I I 1 n, 0 2 4 6 8 10 12

401

30~ I

20

10

2 4 6 8 10 12 14 16

Figure 15·.--Graphs showing the distribution of focal depth for sets of aftershocks following events (a) Kasseri, (b) Inlet, (c) Muenster, (d) Fontina, (e) Cheshire, (f) Estuary, (g) Colby, (h) Pool, (i) all aftershocks. dis the mean focal depth for each set. DOB is depth of burial. Events deeper than 15 km are grouped at 15-16 km. Only A and B quality locations are included.

~

.x

X

DIST (KM) 6.37 12.74

DIST (KM) DIST (KM). 6.37 12.74 19.11 B' Ao 0.00 19.11 A'

8 rl- + X Cs:> o.oo 6.37 C'

8 . >s. Bs:> o.oo

8 ~

+ E• -t· t +

•• p•

v. 8

C• K•

.?< ...... ,

+~ X • t

+

X

+

+

. +

+ +-i; . + -fh

X +

+.

+ + +

+ ~; X

•• + X +• -l

: -t +

+ .·:;t -t·

+ +)< +-++

+ +x +

•+t* ++1 • + '\+ + +,.4,

+

X

1-

'X +

X: +

Xx +

>x X

+ .: -+

>l . 1 v. --tX + 8 . -t

X _. X

X

-t v. +

8 +

+ +

~ x: 8 + [:i. '

.. X

X

Figure 16.--Vertical orthogonal cross sections through the epicentral region covering the areas shown in figure 13. ·M' and C'C" include events Kasseri, Muenster, Estuary, and·Colby, BB' and CC' include Pool, 'Inlet, Cheshire and Fontina.

39

+_~

t+. +

X

SUNHARY

1. A total of 1,075 aftershocks <ML~2.5) were detected during the

monitoring period. The rate of earthquake occurrence during this

period is 3.8 events/day compared with 1 event in the 20 days prior

to Kasseri. The magnitude of nu~lear events triggering aftershock

sequences was ML~5.8.

2. Nuclear events with magnitudes ML~5.5 did not trigger aftershock

sequences during the Accelerated High Yield Testing Program, although

smaller nuclear events in the past may have triggered aftershocks.

These events, however, were on Rainier Hesa or Yucca Flat.

3. The number of aftershocks triggered generally increases with the

magnitude of the nuclear event.

4. The number of aftershocks triggered appears to decrease with time

from event to event for a fixed nuclear event magnitude.

5. During the last 3 months of the monitoring period, the rate of

aftershock occurrence was about three times as high as background

level determined during the 1971-73 monitoring period.

6. Comparison of the aftershocks during the 1968-70 testing program

with this program shows that the earlier series produced a larger I ..

proportion of small-to-large earthquakes and a larger number of

aftershocks.

7. Aftershock epicenters were not concentrated at gz, but were dis-

placed laterally 1-2 km. 1'he direction of displacement varies with

each nuclear event.

40

l

8. The focal depth of the majority of aftershocks is in the range 4-6

km. A few events also occur shallower than the shot point, but

very few occur at depths characteristic of the depth of burial.

9. Many aftershocks appear to be occurring on vertical faults with

approximately north-south orientation.

41

ACKNot.JLEGHENTS

The installation and maintenance of the array and associated equip­

ment was performed by John C. West and Eugene D. Sembera under the

general supervision of Kenneth W. King, USGS, Las Vegas, Nevada. Data

were also recorded from stations operated by Sandia Laboratories, NTS.

The authors express grateful acknowledgment to Dr. William H. K.

Lee, USGS, Menlo Park, Calif., for his helpful advice regarding the

location scheme; to Dorris Tendall, Sandia Laboratories, Albuquerque,

N.M., for pLoviding readings of first-arrival-time motion from nuclear

events on Pahute Nesa at stations operated by Sandia; and to Roy D.

Miller, University of California, Berkeley, Calif., for providing mag­

nitudes of nuclear events.

42

l I . .

I .....

' I I .

I.

I

REFERENCES CITED

Bayer, Kenneth C., 1972a, A preliminary seismicity study of the southern

Nevada region for the month of July 1972: U.S. Atomic Energy Comm.

Rept. NV0-746-4, 9 P•

----~1972b, A preliminary seismicity study of the southern Nevada

region for the month of July 1972: U.S. Atomic Energy Comm. Rept.

NVQ-746-8, 9 p.

_____ 1973a, Seismic data report southern Nevada region December 22,

1971-Deccmber 31, 1972: U.S. Dept. Commerce, NOAA, Rept. ERL ESL-

24, 7 p •

----~1973b, A preliminary seismicity study of the southern Nevada

region quarterly report January-March 1973: U.S. Dept. Commerce,

NOAA, Rept. TM ERL ESL-26, 17 p.

1973c, A preliminary seismicity study of the southern Nevada ----~

region for the month of November 1972: U.S. Atomic Energy Comm.

Rept. NV0-746-9, 9 p.

----~1973d, A preliminary seismicity study.of the southern Nevada

region for the month of December 1972: U.S. Atomic Energy Comm.

Rept. NV0-746-6, 9 p.

----~1974, A preliminary seismic study of the southern Nevada region:

u.s. Atomic Energy Comm. Quart. Rept., April-June 1973, NV0-474-1,

89 P•

Bayer, K. c., and King, K. W., 1972a, A preliminary seismicity study of

the southern Nevada region for the month of August 1972: u.s.

Atomic Energy Comm. Rept. NV0-746-5, 9 p.

43

----~1972b, A preliminary seismicity study of the southern Nevada

region for the month of September 1972: lJ.S. Atomic Energy Comm.

Rept. NV0-746-7, 10 p.

Bayer, K. C., Mallis, R. R., and King, K. W., 1972, Earthquakes recorded

by a seismograph network located in the southern Nevada region

January 1 to December 22, 1971: U.S. Atomic Energy Comm. Rept.

NV0-746-TM-3, 13 p.

Boucher, Gary, Ryall, Alan, and Jones A. E., 1969, Earthquakes asso­

ciated with underground nuclear explosions: Jour. Geophys. Research,

v. 74, p. 3808-3820.

Hamilton, R. M., and Healy, J. H., 1969, Aftershocks of the Benham

nuclear explosion: Seismol. Soc. America Bull., v. 59, p. 2271-

2281.

Hamilton, R. M., Smith, B. E., Fischer, F. G., Papanek, P. J., 1971,

Seismicity of the Pahute Mesa area, Nevada Test Sites December 8,

1968-June 30, 1969: U.S. Geol. Survey Open-File Rept. USGS-474-

138, 170 p.

----~1972, Earthquakes caused by underground nuclear explosions on

Pahute Mesa, Nevada Test Site: Seismol. Soc. America Bull., v. 62,

p. 1319-1341.

Lee, w. H. K., Bennett, R. E., and Meagher, K. L., 1972, A method of

estimating magnitude of local earthquakes from signal duration:

U.S. Geol. Survey Open-File Rept., 28 p.

Lee, W. H. K., and Lahr, J. C., 1975, HYP071 (revised)-A computer pro­

gram for determining hypocenter, magnitude, and first motion

pattern of local earthquakes: U.S. Geol. Survey Open-File Rept.

USGS-75-311, 113 P•

44

' I

L

Page, R. A., 1968, Aftershocks and microaftershocks of the great Alaska

earthquake of 1964: Seismol. Soc. America Bull., v. 58, p. 1131-

1168.

Ryall, Alan, and Savage, W. V., 1969, A comparison of seismological

effects for the Nevada underground test Boxcar with natural earth-

quakes in the Nevada region: Jour. Geophys. Research, v. 74, p.

4281-4289.

Walpole, Ronald E., and Myers, Raymond H., 1972, Probability and sta-

tis tics for engineers and scientists: Nel-.T York, l1acmillan Pub.

Co., 506 p.

45

APPENDIX

A chronological listing of the seismic events is contained in this

appendix. For each event the following data are given:

DATE

ORIGIN

LAT

LONG

DEPTH

MAG

NO

GAP

Dl1

RMS

ERH

Date of earthquake: Year, month, and day.

Origin time: hour, minute, and second (Greenwich civil time).

Latitude of epicenter in degrees and minutes.

Longitude of epicenter in degrees and minutes.

Focal depth in km.

Magnitude of the earthquake~·

Number of station readings used in locating the earthquake.

Largest azimuthal separation in degrees between stations.

Epicentral distance in km to the nearest station.

Root mean square error of time residuals in sec.

RMS=l~R. 2/NO, where R. is the time residual for the ith 1 1

station.

Standard error of the epicenter in km. 1

ERH=lsnx2+SDY2, where SDX and SDY are the standard errors

in latitude and longitude, respectively of the epicenter.

ERZ Standard error of the focal depth in km. 1

1Statistical interpretation of standard errors involves assumpt:f.ons

which may not be met in earthquake locations. Therefore, the standard

errors may not represent actual error limits.

46

l_

Q

Q is

Solution quality of the hypocenter. This measure is

intended to indicate the general reliability of the

solution:

_g_ Epicenter Focal depth

A excellent good

B good fair

c fair poor

D poor poor

taken as the average of QS and qn (defined below). For

example, an A and a C yield a B, and two B's yield a B. When QS

and QD are only one level apart, the lower one is used, i.e., an A

and a B yield a B.

QS and QD rating. QS is rated by the statistical measure of the

solution as follows:

g§_ RMS(sec) ERH(km) ERZ(km)

A <0.15 ~1.0 s.2.0

B <0.30 s.2.5 ~5.0

c <0.50 ~5.0

D Others

QD is rated according to the station distribution as follows:

M NO GAP DMN

A ~6 s.90° s.Depth or 5 km

B ~6 .Sl35° :i2x depth or 10 km

c ~6 :sl80° :S50 km

D Others

47

•97'> HH MN St:C f,4T N LONG W OEPTM "AG NO GAP V"IN R"'S f.llH n•z ll

ICT' "t<ASSt ... t• 1'4111.1Tt: MfSj\ YIU.n: 200•1000 I'T 211 14 jO o.tb 37•11.40 111••24. b9 1.27 b.lo

21! 14 o;o 211 14 51 2k 14 'JQ

2~ ,.., 01

;.!R I'> OJ 211 , .. 04 21< ,., D 711 1'> 14 2H ,., 1f. ~H.n; H•I7.4Q 111••74.114 12.17 3.60 10 134 13.1 .tJ9 .7 .II " 211 I'> 74 :>.s -;~ IS 2R 2~ ,., :;>Q 2.5 ;IH , ... 32 1H 1'> i4 21! 15 ~.,

21< 1'> 31'> 211 1!1 H :l~ I'> 3R 2~ ,., 40 ;>II I!> 41 .i'>. i7 J1•1 <1. 11 llb•lt-.41 t~.OQ 4.0'> 9 171 <1.2 .u7 1. 1 1.1> c ;>R 15 H :IH 1"> 41> n I'> 4H 211 1"> '>7 211 15 .,~

2H l'i 'iJ 2H 1'> '>H

"" I'> '>II 211 '" 4 '>1.47 n-17.:.1'> llf>•2'>.PH 4.7 .. 3.1)1> H Ill 10.3 .o7 ·" <12.'> c 711 It> Q 11.:.11 ~7-11-1 ....... 11o•74.50 '> • I I 7.711 12 Rl It. I • I 1 .1 ~.u c , .. ,., on 21! ,., 01 ;Ill It> 112 ;.If< In OJ j!H If> to 111.02 37•1t>.71< llb•74.t>k 7.HR 3. JO Jf) 122 10.7 .I J .H 1.4 M 21< ,., 21 211 lh 3'1 211 11> jH ;>R 1b 41 2.7 ,. .. If> 42 , .. ,, 4'1 2.9 211 lh .,., 3.1 2H 11> 0,7 ) • j

2~ lh '>7 ..... ~ .. n-tt•-"4 Jlt>•24.t\l .24 J.IH 10 '11 t().tt .~q 2.1 17.1 c ")I> 11 07 2ob 2H 17 {I) 3.4 2R 11 ltJ 2h 1'1 ,., 2.5 2~ 11 2b 2.6 21! II )0

211 17 41 '-,',. 4. n-t". n tlb•2J.52 I O.'> l 3.111 ~ 9b "·' .l4 2.2 )..3 H 2H 17 47 ;>H 17 ..... 2.b :i'll 1 ~ 11f> 2.b 7A , .. f)U

:lR p; ,., 1.1l 211 I H ;>) 2.H 21i Ill 27 74.71 i7•11>.4h llb•24.'~b '>.07 J.OII 11 11 'I 10.5 .14 oil ... 4 c ;!jj Ill ~q

2" lq 3h 2~ Ill Jll 2.7 211 II' 44 2ob 211 '" 4'1

"~ 11:1 '>1 4!.7 211 IH '>H 2.8 7ij I 'I Ill 2.'1 2>1 ~~ II 211 I 'I I~>

211 I 'I 21 2.1> 211 I 'I J(l 1.4 2~ '" J2 7.7 711 I 'I 41> 4 ... 14 H•lh 0 Hh 11n•2~>.22 s.1 • lo I I> ll ij(l Hob • u7 •• 1.2 " 211 I 'I )II 2.'> 1H I<J .,2 2.1> 211 ;It) 114 •• (I ;,til 711 II 4 3. •ll 11•11>.7'1 111•-'"·1 0 "· 2. ... '14 12 llh 111.2 ·"" .!i I. I " 211 ;>IJ I 'I 2.ij 711 211 ,., 211 211 .t'l '·"

48

I'll!> 1111 "'l SEC' LAT >I I.IJIIG W OEPTH lUG ,.n CAP IJMI-. ""'s t:tltt t.K?. II

cr ;,>R :Ill 411 ?II ?<I 41< 1:1,411 ]7•11>,'>'> llt>•l'>ol A 10,91 J,09 II 911 10.1 .18 I o I "·' H 211 2•1 '>4 2.8 211 ,, '>II J.l ?.II 11 lo 211 21 n ),) 2" :II 47

'" 'Jt.s 4 211 11 ';{?'--':II 47-1 ... 112 11n•2S,A7 3,'>4 J,)O R 120 43.7 .of:l ·" J,il c 2h n Ot>

21l ~· "). fl'.l J.n 21' 4·:1 11 2K n 1•1 2.7 2~ n 7>1 "·" '" 21 4b J.o 211 2:1 4ol 'j1,7t> 17-11.42 111>•21,71 4,11:1 1,14 12 17 10.8 .oq .s oil II

I 211 n .,,, li,'J'> )1-17.1'> 116•24. 79 ,&7 3.32 12 75 10,7 .27 1.2 10.2 c 21! 27 0,4 :Ill n 0,!]

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