ML20033B246

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Description of Seismometric Data Recorded at Mammoth Lakes, Ca
ML20033B246
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Issue date: 11/30/1981
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NUDOCS 8112010094
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.

o i e T

sg DESCRIPTICN T SEL90EIRIC DMA IE00RDED AT MPMolE IAKES, CALUUNIA l

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SOUm CMOLDR EIECIRIC & GAS ONPANY l

Noverber,1981 l

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I 8112010094 811119 PDR ADOCK 05000395 A

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i DESCRIPTICN T SE:I.90EIRIC DA'IA RECORDED AT MMM7IH IAKES, CEDUNIA Introducticn In early 1979 a sequence of earthquakes began at the eastern front of the c iamic activity reached a Sierra Nevada near Martmoth Lakes, ('alifornia.

e maxinun in late may,1980, with the occurrenm of foar events of local Richter magnitude Mn 2. 6.0.

The sequence provirtv1 an excellent opportunity for recording earthquakes at close range. A large set of data was recorded in the epicentral distance range frun 0 to 25 kilmeters.

'Ibe earthquakes tv-<'svred mainly within the Sierra Nevada batholith, idiately south of Iong Valley caldera. Mechanisms of the earthquakes were svizninantly strike-slip, with east-northeasterly axes of minuman cmpressive stress. Focal depths of the nederate to large magnitude events (magnit,vk" 4 to 6) were generally in the range 5 to 16 kilmeters.

'Ihe purpose of this paper is to describe the characteristics of normal-depth tectonic earthquakes in the magnitude range ML 4 to 5, recorded at very short epicentral distances.

Instrmentation

'Ihe data tv@ned herein were recorded on wideband digital event-recording aai~eydg5 as described by Peppin and Bufe (1980). Iong period (~10 sec) seismsreters were arployed, and the digitization rate was 100 sartples per second. '!he recording bandwidth is 0.1 to 50 Hz, displamt-flat. Figure 1 shows synthetic and observed t-alibration pnlaas, dertonstrating the wide bandwidth of the system. 'Ihe bandwidth permits detennination of such

patau==L?.rs as aaiamic nment, synthetic Richter magnitude (M *), and 3

maxuman amleration, all frm the same revutus. With 12-bit resolution, analog systan noise less than one digital count, and a fra.W,3f-16 aminrs.pi:

step, total signal anplitude variaticm of us to 92 dB can be r+-@N.

Recording Sites Figure 2 show epicenters of scme of the larger events of the sequence, and four sites occupied by wi h hand digital sei= % iaphs: Mannoth Ranger Station, Whitmore Hot Spring, Ibck Creek, and McGee Creek. 'Ibe Mannoth and Whitmore stations lie witlun Img Valley cal &ra, whose southern margin is shown in the figure. Body waves travelling to those stations are affected substantial-ly by seismic absviyLion. 'Ibe same is the case at the Rock Creek site, which is situated on poorly cmso11 dated glacial debris. By cxmtrats, the McGee Creek site is situated cn a thin veneer (a few neters) of glacial debris overlying metauutgesed Ordovician rocks that are draped over the granite batholith. Seismic waves arriving at the McGee Creek site travel'alnest entirely in web:ut rock.

McGee Creek is the site nost centrally located with respect to the earthquake l

epicenters.

Seismic Msnents and Maanih*=

denoted by M *, were cmputed following Synthetic Richter local magnih*=,

L a pivcedure similar to that used by Bakun and Lindh (1977). Synthetic

~

(M *) are plotted against Berkeley magnih*= (M ) in Figure 3.

magnih * =

L L

'Ibe 1.ine of unit slope through the origin shows that M

  • is a fairly tmhia=SA L

estimator of Berkeley M. Figure 4 is a plot of ML* versus the log of t

seismic nment (m) for the entire data set (nore than 1,000 earthquakes).

b

she upper-rightzost datm points are those of Uhrhammer and Ferguson (1980) for three of the four largest events (ML 2. 6.0), which were too large to be recorded cm the wiaahand instruents. She dashed line is the pih14=hed Inment-eagnitude relaticn of Thatcher and Hanks (1973).

Hypocentral' Distances Hypocentral distances given herein are caputed cnly frm observation of the arrival time interval bebeen P and S phases. Figure 5 illustrates the ease with which S-P time can be read frcm the wideband displarwant seismo-grams. The top trace is Radio W W time rraa. The P and S velocities used in caputing hypocentral distance frm S-P are 5.2 and 3.0 kilmeters/sec, respectively. For these velocities, the hypocentral distance is 7.1 kilo-meters per second of S-P time.

A-1%s A-lavograms were cmputed by double differentiating the displae==nt records.

Numerical tests shcw that this procedure is stable because of high, wirWnd signal-to-noise ratio. A lcw-pass filter is applied at 25 Hz. Results of the differentiations for the McGee Creek record of the ML 4.5 earthquake of May 26, 1980, 14:38 UIC are shcun in Figures 6-8.

Events were selected for cmputation of acceleration records so as to include all events of Mc > 4.0, and those events of smaller magnitude with the smallest S-P times. The results of the selection are shown in Figure 9 and Table 1 for the Mannoth Ranger Station site, and in Figure 10 and Table 2 for the McGee Creek site. Figure 9 shows hypocentral distance (cx3tputed frm S @ time) versus matent and magnitude for the Manneth station. Index nm bers are keyed to Table 1.

At McGee Creek (Figure 10), miniman hyEn.whal

1 distances are smaller than at Mamoth Ranger Station, reflecting the situaticn of W Cmek directly above the seisiv3enic zone. At McGee Creek events of magnitude less than 3 occurred as shallev as 3 kilcmeters, while for ML ~ 4.5 the shortest hypoc=hal distance is about 5 kilometers.

Figures 11 and 12 show peak acceleraticn versus mcznent and magnitude for the Manmoth and McGee Creek stations, regectively. Index m =h es are keyed to Tables 1 and 2 as before. Brackets show the peak acceleration measured frcm each horizontal cxmponent of ground moticn (where both ccmpo-nents were available). 'Ihe peak accelerations at McGee Creek exceed those at Marmoth by an amount too large to be attributable scely to the average diffe-rence in hypocu h al distance. It is conclivhi that the effect is due largely to absorption of seismic waves propagating through the e alriara to the Marmoth staticn. Peak accelerations at the Whitnere and Rock Creek stations are also considerably less than at McGee Creek, an effect likewise attribu-table to substantial seismic absorption.

Respanse Spectra of 4 < ML < 5 Earthquakes Recorded at McGee Creek Response spectra were <-alm 1ated for five events of average magnitude 4.5 and average S-P time of 0.85 sec at Mosee Creek (average hypocentral distance 6.0 kilometers). Horizontal w@e_nt response spectra of these events (in$ex nunbers 1, 4, 14, 27, and 48 in Table 2) are shown in Figures 13-22 for 2, 5, and 7 percent of critical damping.

Statistics of the 10 response spectra were <-a_1mlated an the hacia of an assuned logiesul distribution of pseudo-relative respanse velocity at any given frequency. Mean and mean-plus-one-standard deviation response spectra for the ensenble are given in Figures'23, 24 and 25'for 2, 5, and 7 percent of critical danping.

Ctronarison of Marmoth ' Lakes Spectra ~with ' Spectra Derived 'for 'a hypothetical Magnitude 4.'S'RIS~ Event

'Ihere are several important factors to be considered before attatpting to use the results given above to assess response %L.a develooed for design,

or analysis of the Virgil C. Sumer Nuclear Station. Direct emparison is problematical for three reasons. Firstly, it is implausible that a RIS event of local magnitude as high as 4.5 oculd occur near tenticello reservoir.

Secondly, in terms of seismic source parameters, the Marmoth Iakes earthquakes may not resenble, at high frequencies (2. 5 Hz), a hypothetical RIS event of the same local magnitude (i.e. magnitude determined at a frequency of ~1 Hz).

'Ihirdly, a direct camparison of the free-field Marmoth Lakes spectra with spectra developed to analyze the motion of large massive structures requires assmptions that may not be valid.

In Figure 26 are plotted, for 5% danping, mean and mean + o spectra of the McGee Creek recordings for events of average magnitude 4.5, along with a mean + o spectrun developed, by the applicant at the request of the NBC, for a hypotehtical RIS event of the same magnitude (Appendix X, Figure 1, Supplenental Seismologic Investigation, Virgil C. Suntner Nuc: lear Staticn, Decenber 1980). The focal depth specified for the hypothetical magnitude 4.5 RIS event was 2 kilaneters, as opposed to an average hypocentral distance of 6 kilmeters for the ensenble of earthquakes recorded at McGee Creek. In this nMitional respect, the spectra plotted in Figure 26 are not strictly cczn-parable. As plotted, the mean + o spectra for the Marmoth Lakes and hypo-thetical RIS events are similar in tenns of zero-pericd acceleration, maxinun i

f response acceleration and maxinun pseudc>-relative response velocity.

1 I

l

Beferences Archuleta, R.J., Spudich, P., Cranswick,'E. and Mueller, C., 1981 Source piu Ewrs of the 1980 Marmoth Iakes, ralifornia, earthquake sequence, ' Jour.

Geophys. Res., subnitted for pnb1ication.

Bakun, W.H. and Lindh, A., 1977. Teral magniHM, seismic mments, and coda durations for earthquakes near Oroville, califnrnia, Bull. Seism.

Soc. A_m., 67, 615-630.

Savage, J.C., Licowski, M.,

Prescott, W.H.

and King, N.E,, 1981 Strain ammlation near the epicenters of the 1978 Bishop and 1980 Marmoth Lakes, California, ea 6, Bull. Seism. Soc. Am., 71, 465-476.

South Carolina Electric and Gas Cmpany,1980. Supplemental Seismologic Investigation, Virgil C. Sumer Nuclear Station Unit 1.

'Ihatcher, W. and Hanks, T.C.,1973.

Source pa - Wwrs of Southern california u

earthquakes, Jour. Geophys. Res., 3,8547-8576.

Uhrhar:rner, R.A. and Ferguson, R.W.,1980. 'Ibe 1980 Mannoth Lakes sequence,

California Division of Mines and Geology Special Report,150, Marmoth Lakes, California Earticuakes of May 1980. 131-136.

O t

9

TABLE 1 0

SEIS20 GRAPHIC DAL RD00RDE:D AT STATICN MAMME (37.6476 N,118.9609 W)

I.D.#

Date Time S-P Icg Mo Peak Accel.

Magnitude M (sec)

(dyn-on)

(horizcntal Ougnants) (Berke 3ey) L (cVs ec2) 1 1979 12 8 156 1.84 19.93 1.8700 1.1800 2.9*

2 12 9 128 1.36 18.53 0.1980 0.1510 1.6*

3 12 9 235 2.88 18.61 0.1620 0.1440 1.7*

4 12 9 832 3.80 19.91 1.9400 1.5560 3.2 5

12 12 541 1.04 18.64 0.1130 0.0765 1.6*

6 12 12 545 1.04 18.57 0.1980 0.2020 1.7*

7 12 12 1342 1.60 18.94 0.4320 0.4390 2.0*

8 12 14 454 0.93 19.59 1.4900 1.4800 2.7*

9 12 14 455 0.96 18.45 0.1920 0.2900 1.8*

10 12 14 603 0.98 20.39 1.9200 1.9700 3.4 11 12 14 1410 1.55 18.80 0.1540 0.0860 1.8*

12 12 14 1951 1.10 19.15 1.6700 0.8380 2.7*

13 12 14 2231 1.70 18.60 0.2220 0.3460 1.8*

14 12 14 2324 2.00 18.74 0.1090 0.0750 1.7*

15 12 15 833 1.04 18.91 0.7290 0.4250 1.8*

16 12 16 630 1.90 20.10 2.0500 2.0200 3.6 17 12 18 1704 1.23 19.06 1.1300 0.6640 2.4*

18 12 18 2245 1.04 18.55 0.4600 0.5210 1.9*

19 12 19 803 1.00 18.62 0.2070 0.3730 1.9*

20 12 19 1236 1.10 18.44 0.3390 0.2090 1.7*

21 12 19 1300 0.96 18.86 1.7200 1.0300 1.8*

22 12 20 17 1.04 19.47 1.8400 1.8900 2.6*

23 12 21 600 1.00 18.61 0.5300 0.2600 1.9*

24 12 21 2010 0.91 19.07 2.4100 1.5400 2.5*

25 12 31 1329 1.02 19.04 2.1500 1.0400 2.3*

26 1980 11 2020 1.04 19.45 1.8700 1.3000 3.2*

27 1 2 1703 1.06 19.60 2.4900 1.7500 2.8*

28 1 15 1

2.45 20.41 2.3600 1.5200 3.2 29 1 18 842 1.04 19.41 1.6000 1.7500 2.7*

30 1 30 2018 1.12 20.33 2.5000 2.2500 3.0 l

31 2 14 1431 1.28 20.24 6.8800 4.4000 3.1 32 2 22 230 3.90 20.90 2.9500 1.3900 3.9 33 3 15 1531 2.34 20.84

- 4.1200 3.4700 3.8 34 3 20 2215 1.24 20.76 6.9900 3.2600 3.8 35 3 20 2355 1.50 20.38 12.2000 5.1900 3.3 36 3 26 1442 1.70 20.68 7.9900 4.9800 3.5 37 3 26 1643 1.47 20.33 5.2800 2.9300 3.2 38 3 27 226 1.44 21.15 13.8000 9.6100 4.3 39 3 27 230 1.34 20.31 1.7600 1.3000 3.6 40 3 28 322 1.10 19.70 5.4100 7.8900 3.l*

41 3 29 728 1.36 20.40 3.3900 2.5400 3.4 42 5 26 1721 1.10 10.39 4.4000 2.6400 3.1 43 5 26 1739 1.52 10.9,9 3.6100 2.9500 3.8 44 5 26 1856 2.00 20.75 4.7800 3.3200 3.8 45 5 26 1858 2.15 22.74 76.4000 27.6000 5.5 46 5 26 1908 2.15 20.49 2.2500 2.1400 3.3 47 5 26 1911 2.10 20.74 2.1000 2.1100 3.8 l

48 5 26 1925 2.20 21.84 20.400 14.0000 4.7 l

49 5 26 2149 0.93 19.79' 3.5300 2.9700 3.0*

50 5 27 637 2.20 21.32 5.3000 6.2900 4.1 l

Syntbetic ML

i

~

5 51 5 27 645 1.30 21.83 26.7000 26.2000 4.0 52 5 27 1328 2.20 21.61 6.0400 3.9600 4.3 53 5 27 1502 3.12 21.01 3.7700 4.0800 4.0 54 5 27 1542 3.10 20.88 2.1100 1.7200 4.0 55 5 27 1611 1.70 21.13 12.5000 12.3000 4.0 56 5 27 1710 3.10 20.82 2.9700 4.0800 4.3 l

57 5 27 1837 3.80 2'J.95 5.3500 5.2900 4.0 58 5 27 1902 7.70 22.18 13.2000 14.8000 4.8 59 5 27 2007 1.00 20.44 2.4800 2.1200 2.8 60 5 27 2135 3.00 21.24 4.4600 5.2300 4.3 61 5 28 555 1.70 21.23 13.6000 7.1100 4.0 e

e O

l T.-_.-,,--

s TAB [E 2 SEISPOGRAPHIC DMA RB00EUD AT SDdICE MXIEE (37.5497 % 118.0149%)

C Magnitude M I.D.4 Date Time S-P Ing Ib Peak Accal.

(sec)

(dyn-an)

(horizontal my..i u) (Berkeley) L (a:Vsec2) 1 1980 5 26 1305 0.87 21.51 171.0000 80.3000 4.3 2

5 26 1405-0.82 20.97 60.7000 105.0000 4.2*

3 5 26 1417 0.70 20.65 62.1000 94.2000 4.0*

4 5 26 1438 0.83 21.65 109.0000 172.0000 4.5 5

5 26 1605 0.85 20.96 143.0000 126.0000 4.3*

6 5 26 1618 0.86 20.85 44.0000 68.3000 4.0*

7 5 26 1738 0.92 21.09 70.5000 43.2000 3.8 8

5 26 1740 0.92 20.95 43.5000 44.9000 3.3 9

5 26 1806 0.85 20.45 31.8000 17.9000 3.1 10 5 26 1856 0.94 21.05 44.4000 142.0000 3.8 11 5 26 1858 0.86 22.58 167.0000 217.0000 5.5 12 5 26 1908 0.64 20.94 106.0000 139.0000 3.3 13 5 26 1911 0.83 20.68 25.3000 22.4000 3.8 14 5 26 1925 0.86 21.64 69.0000 97.1000 4.7 15 5 26 2004 0.85 21.28 64.4000 105.0000 4.1 16 5 26 2143 0.84 20.86 42.1000 98.8000 3.7 17 5 26 2056 0.58 20.79 84.1000 61.5000 3.3 18 5 26 2159 1.00 20.75 22.7000 25.2000 3.8 19 5 26 2236 1.00 20.54 9.6200 10.3000 3.6 20 5 26 2320 0.82 20.89 48.4000 70.7000 4.0 21 5 27 44 0.93 21.13 71.3000 89.9000 3.6 22 5 27 54 0.84 20.87 55.7000 69.8000 4.l*

23 5 17 115 0.74 20.57 64.3000 100.0000 4.l*

24 5 27 202 0.59 21.29 234.0000 186.0000 3.6 25 5 27 344 0.89 21.23 109.0000 75.6000 3.7 26 5 27 537 0.71 20.51 63.6000 48.2000 3.4 27 5 27 637 0.85 20.83 0.0000 63.0000 4.1 28 5 27 647 1.03 20.73 9.2600 6.5500 4.0 29 5 27 950 1.01 21.23 42.4000 46.3000 4.2*

30 5 27 1028 1.00 20.41 27.8000 21.4000 3.2 31 5 27 1047 0.92 20.74 0.0000 70.0000 3.1 32 5 27 1328 0.81 20.91 37.5000 38.0000 4.3 33 5 29 1417 1.00 21.20 34.0000-41.5000 4.2 34 5 29 459 0.89 20.95

'61.0000 54'.0000 3.9 35 5 29 1337 0.83 20.79 40.4000 58.9000 3.1 36 5 29 1556 0.89 20.91 74.7000 77.3000 4.l*

37 5 29 1721 0.81 21.54 201.0000 160.0000 4.1 38 5 30 1202 0.90 21.37 164.0000 79.1000 3.9 39 5 30 1542 0.85 21.25 65.5000 66.6000 4.0 40 5 30 1549 0.82 20.66 39.1000 48.7000 3.5-41 5 30 1824 0.92 21.36 108.0000 81.3000 4.5*

42 5 31 59 0.96 21.25 165.0000 90.5000 4.5

-43 5 31 806 0.95 21.02 24.3000 44.3000 4.1 44 5 31 1012 0.74 21.53 66.300 136.0000 4.3 45 5 31 1329 0.71 20.46 0.0000 73.0000 4.2*

46 5 31 1344 0.73 20.70 43.8000 89.5000 4.1*

47 5 31 1409 0.83 20.42 14.2000 13.5000 3.2 48 5 31 1517 0.90 22.17 214.0000 250.0000 4.8 49 5 31 1521 0.90 21.33 68.0000 121.0000 4.0 50 5 31 1531 0.82 20.96 73.8000 64.3000 3.8

  • synthetic Mn

51 5 31 2315 1.06 20.88 66.8000 98.0000 3.8 52 6 1 318 0.63 20.84 53.5000 25.1000 3.2 53 6 1 909 0.45 19.95 22.5000 0.0000 3.9*

54 6 1 1728 0.81 21.10 55.9000 73.0000 3.6 4

55 6 2 1535 0.85 21.35 169.0000 109.0000 4.5*

I 56 6 4 24 1.30 20.24 1.6200 1.6900 2.9*

57 6 4 546 0.92 19.74 13.0000 8.5800 3.3 58 6 4 835 1.05 20.34 20.2000 28.5000 3.4 1

59 6 4 1257 0.64 19.51 20.2000 20.4000 3.4*

60 6 4 1700 1.01 19.66 4.3300 3.6900 2.8*

61 6 4 1910 0.85 20.79 26.1000 32.2000 3.8 I

62 6 6 826 0.54 20.15 30.4000 34.9000 3.7*

63 6 6 953 0.62 20.20 27.5000 28.0000 3.7*

G4 6 6 1121 0.57 19.52 13.6000 16.8000 3.3*

65 6 6 1627 0.75 20.38 31.0000 34.9000 3.5 66 6 7 132 1.08 21.01 23.5000 20.0000 3.9 67 6 10 447 0.63 19.33 6.3300 c5.2300 2.9*

68 6 10 1330 0.58 19.34 18.9000 19.1000 3.4*

69 6 11 443 0.90 20.75 26.5000 27.5000 3.9*

70 6 11 951 0.53 19.31 13.5000 15.2000 3.3*

71 6 20 414 0.50 18.70 1.2000 0.0000 2.3*

72 6 20 1136 0.63 19.37 10.8000 0.0000 3.2*

73 6 20 1725 0.87 20.50 18.80000 0.0000 4.0 74 6 21 32 0.50 18.61 1.7700 0.0000 l

75 6 24 2106 0.63 19.34 9.6700 9.0100 3.l*

76 6 24 2145 0.55 20.16 33.5000 37.8000 3.7*

77 6 24 2234 0.57 19.66 22.6000 25.3000 3.4*

i 78 6 24 2235 0.53 18.99 10.7000 7.2100 3.0*

79 6 24 2241 0.53 19.22 0.0000 16.6000 3.3*

80 6 25 2057 0.53 18.93 13.3000 8.9500 '

3.l*

81 6 25 2159 0.57 18.94 5.4900 4.5300 2.7*

82 6 30 1324 0.58 19.26 8.7500 8.0000 83 7 1 2130 0.68 20.43 25.7000 30.9000 3.7*

84 71 1757 0.55 19.24 16.2000 8.9300' 3.l*

85 7 13 1057 1.03 20.08 8.7400 6.7500 3.3 86 7 16 1619 0.94 20.71 21.0000 21.0000 3.4 l

  • Synthetic 4 l

~

t l

Thee. Col Pulse Col Pulse b e.d t

t t

t t

t t

t t i i*

TME (SEC)

FIGURE 1 Systan respcnse of the Digital Event Recorder seim uga;A to stepwise input in acceleration (lower tra

), with theoretical re= rase for camparison (30% critical danping at a free period of 5 sec, top trace). Rizziness of ciserved trace is caused by 40-Hz energy frcrn nearby powerlines. Amplitudes of emputed and observed pulses agree to within a factor of 10%.

(Source: Peppin and Bufe,1980) m e

MAMMOTH LAKES L

g

M R.S.

i aWHITMORE O

O O

O 0e CROWLET G=

b b

e O

e e

GEE b

ROCK CREEK 4

e LC 4

g e

9@O

\\

O Y

0 37.5 N -f-119.0%

118.75%

O e

O e

0 0

O 5

10 KM Map showing epicenters of sme of the l

larger events of the 1979-1980 sequence MAGNITUDE (octagens), and sites occupied by wideband digital seimiwtags (larger at top indic Iang (-30 km) half-ellipoe O

triangles).

=

ates southern boundary of

^~

i 2

3 11 5

NM FIGURE 2

2, x

a= =x Iv

\\

1

\\

s s

v-

=

9 n

3 s

s o

n - :: ~~V : ~i E v : v v :-

x a

I r

5 t

o age j

i A

A AX i

ag

,4*

o e

^e

)

L x

n 4

x J< x Z

e_,

a x

o q-x, L_)

3 2 2 3

L:

5 3

3E94E_E

V

~

FIGURE 3 Synthetic g* versus adjusted 4-station observed 4 at the Berkelef stations ARC, MIN, BRK, and MIC.

LUb l'1 U =

t1.UJ I U. U I J l'iL L1U.Oc 1 U.U4J N=

1018

^

/

+WT

/

/ Y

' ROC

/

c V RS mVCE

/

03

/

m M

/

t e

/

o Nm M

/

  • 0+

5

'r/

~

/^

~

co N

5 6

.z.

=

w

- + +

shn U

xO a

. Em oN 5

FB

=

y#

e I

a 03 d

~

5 0

y_9 -

g e

t_J E

l f

CD A

1

~

2 P%n e

~

l D

e I

l l-I l

~

1 2

3 4

5 6

7-V y

^ '] (\\l

.)

l i

FIGURE 4 Irg of seismic nrment versus M,*; 1018 datun points were used in the regressian, which l

I gives essentially unit slope (the solid lire). Cbmpare with a similar regressian by

'Ihatcher and Hanks (1973), the dashed line.

]

)

52 5

ll s

s n.

1

]

l

~

N O~

F-824.

895.

1606.

I Vn m

i m

  • O u

v FIGURE 5 vertical (Z) and horizontal (R and T) uncorrected displacement seismograms for the 4 4.5 earthquake of 14:38 UIC, May 26, 1980, recorded at McGee Creek. Amplitudes are digital courits. 'Ibe upper trace is MN time code.

g d

e

?

)

4 1-

- }

5 f,

2 b

2= L

>Q 4

!N

~3E t

4

)

Y b

-o

~

w c

wr

. r e

N M

N 1

l Z

CM Z

CM/S Z

GALS 1

l l

0.044 0.73 34.2 j

]

m

/

m m

v o

FIGURE 6 Vertical ccrnpanent instrument-corrected displacement, and velccity and acceleration records obtained frcm differentiation. The event is the same as in Figure 5.

~

p 4

6 g

<)t 3

E*

3I

>d 4

?

s k;

~

m k

i M

f.J Ld a

ce 5

to 8

I ff m

D

~

1 E

CM E

CM/S E

GALS 0.077 2.02 109.4 R

}

m n

/

J J_:

J o

m FIGURE 7' East emponent instrument-corrected displacement, and velocity and acceleration records obtained fran differentiation. The event is the same as in Figure 5.

}..

j' l

l l

a i

i i,'

i i

$,[

I, I

I I

1 N4 g

1 5,

I>

>?

W i

a L1J ~

v>

=-

1.

4

>Q LLJ z

f:

if

._ H 1 -

N CM N

CM/S N

GALS 0.132 3.35 172.1 n

/

n m

l v

L O

FIGURE 8 North cuwent instrument-corrected disph-nt, and velocity and acceleration records obtained frun differentiation. The event is the same as in Figure 5.

o xv.

MS Xso.

X3.

Xsa.

X28.

3 3*

X50. X52.X4s.

Xus.

X14.

Xus g xi,X s Xis.

X3 s.

X951.

X2 d7-gg, xy.

e

'4 x-xy/Si-xsi.

x,,,

x,,,

p->sid;',Y"'.

Ni-cc I-J g

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12".13, 1:3. F. ,i.. a..u r. rV.- i..." - (\\J jlP.L 114. N 2 0,"3 6 25. 4 '7.g7y3, ii; w6, 3 } Pl? % := .R9. Bl: 4 3. D7* NS. -$8 "D O.3Ns.. q7, -[ve.-h.s!' 7,,, 3,, 5 8 b7. 31. ISO. (f") =56. ! U E = 0 Z C O L l 1 O r 2 M 3 4 5 g o = J z l Illi lil li l lil lil I ll11 I lilli C 2^v ~2.. 2L0 2C .. v v LOG MDMENT FIGURE 12 Peak ground acceleration versus magnitude and seismic m2nent at McGee Creek. Brackets denote each of two horizontal ccruponents. hWs are keyed to Table 1.

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F RE'3 U INCY - M Z ioo.e s o.e t.e o.1 QttI t i I t Ittt t t t t t I1 t t e a t t t i 100.0 < +, ', - :*& Qr-p 7 - - A. 78hr-r ;4.- - -- --f- . d -- --,. /-N - - 8 , /. f.c N ? ?*?%. '1 # ~ r ~!* * ~ '. " *4.'.*;~.7 h'.' _ ' ' ' ~ ?,/ / _.,. _ p 2--. 4-t.s. -, f...,,. c t <_4 f ( u s<*.1 N. ._/-c,' y/ . < W- / ... e-4 r -_ ~.. e,., : d.s., d> :: ?.\\. c.,,, /< / t.-/ '. c. _i -t 1 7. .(- /,o 4- . ~..\\ \\ t ?....> o r s-#. "s r *-- < '- ,s '\\\\.\\. l - y,y{ .s. /sa.. A s. z ;,'- ,n.c,q <.7 ' y,.c. 1

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F RE'3 U E NCY - M Z too.o io.o 1.o o. If f I f f I I i ttii i t t t I ittt t t t i e t 100.0 -.-,. b A. y,. 4 -,.- -.1,. L. w.,7t A r. 4 - -..A.-.4...... ,s.s ,- ' l.

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FRIOU E NCY-H Z i o... i... i.. Il i 1 1 1 I f f 11 i l I I I I t 11t iit I I i i 100.0 <,_ =..L n. W, &{ '.r,,s...L

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