Text

Seismic Activity Near VC Summer Nuclear Station for Jul-Sept,1980
	ML19345B627
Person / Time
Site:	Summer
Issue date:	09/30/1980
From:	Talwani P; SOUTH CAROLINA, UNIV. OF, COLUMBIA, SC
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O TECHNICAL REPORT 80-3 SEISMIC ACTIVITY NEAR THE V.C. SUMMER NUCLEAR STATION For the Period July - September 1980 l

l by Pradeep Talwani Principal Investigator Geology Department University of South Carolina Columbia, S.C. 29208 Contract No. N230519 80120209%

Technical Report 80-3 SEISMIC ACTIVITY NEAR THE V. C. SUMMER Hl: CLEAR STATION For the Period July - September 1980 by Pradeep Talwani Principal Investigator Geology Department University of South Carolina Columbia, S. C. 29208 Contract No. N230519

_ _ _ _ _ _, ~.. -

1 INTRODUCTION This report presents the analysis of se'ismic data recorded near the V. C. Summer Nuclear Power Station in South Carolina. During the reporting period (July 1 - September 30,1980) shallow microearthquake activity averaged less than one locatable event per day (= 0.73 event / day).

Four events of magnitude > 2.0 were recorded for this reporting period.

Insrnu:xnTArzcn The data were recorded by a four station seismic network operated by S.C.E. and G.

. Data were also obtained from JSC, a permanent station of the South Carolina seismographic network and a portable digital event detector (station JIM). These seismic stations are shown in Figure 1 and listed in Appendix I.

IZT!!GD Events were located using a computer program HYP071 (Lee and Lahr, 1972) and a velocity model developed for the Monticello Reservoir area (Appendix II). The event magnitudes are calc'ulated from the signal durations at station JSC, where the duration (D) and magnitude (M )

L relation is

-1.83 + 2.04 log D M

=

L The daily energy release was calculated using a simplified magnitude (M ) energy (E) relation (Gutenberg and Richter,1956)

L log 10E 11.8 + 1.5 M

=

L

2 RESULTS In the recording period 67 locatable events were recorded.

These are listed in Appendix III.

Figure 2 shows the cumulative events recorded in July, August and September 1980. The majority of events (44) occurred as a swarm in the last ten days of July and the first few days of August.

The location of the swarm defines no new area of activity with epicenters continuing to plot in the southwest portion of the lake (Ficure 4). With the exception of this swarm the reporting period is marked by a very low level of seismicity (14 events in August and 9 in September).

A cross section, 2.0 km in width from A to B is shown in Figure 3, showing the shallow (< 4.0 km) character of the events. The monthly locations are shown in Figures 4 - 6.

A cumulative (from December 1977 to September 1980) map is shown in Figure 7.

In Figures 2 - 7 only events with an RMS of < 0.1 sec have been plotted.

COMP 11RISON OF SEISHICITY WITH RESERVOIR LEVELS Monticello reservoir is a pumped storage facility and the decrease in reservoir levels associated with power generation is recovered when water is pumped back into the reservoir.

Correspondingly there can be variations up to about 8 feet per day between the maximum and minimum water levels.

Figure 8 shows the comparison of water level to seismicity.

The top two graphs show the water level and also the change of water level per day. The log energy per day and number of events per day are shown on the lower graphs.

During the reporting period there was one seismicity peak, occurring in July. A gap in the data exists in the middle of the swarm (July 25 - 28) es

3 due to an instrument malfunction at JSC.

(Cata from JSC are used to determine the number of events per day and log E per day.)

b-Valucs The b-values were obtained for events occurring in monthly periods.

As the number of events was not largs Utsu's (1971) method was used.

In this method s 1(a e b

=

Ifig - sMs where M $

sum of magnitude of all earthquakes having magnitudes equal

=

to or larger than fis total number of those earti] quakes s =

and 10

=

+ !3 baM/ log e n

1 bart where n

factor for correcting the effort of the length of the

=

magnitude interval aM. baM is given in Table 18, p. 388 (Utsu,1971).

The b-values for monthly periods are shown in Figure 9.

The sharp peak in June is due to the statistical nature of the calculation (only 5 events occurred in June).

CONCLUSION During this reporting period seismicity was at a low level with a relatively large seismicity swarm occurring at the end of July and first of August (Figure 8, Events / day).

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REFERE CES Gutenberg, B. and Richter, C. F. (1956). Magnitude and energy of earthquakes, Ann. Geof. 9. p.1-15.

Lee, W. H. K. and Lahr, J. C. (1972). A computer procran for determining hypocenter, ragnitude and first rotion pattern of local earthquakes, Revisions of HYPO 71, t!.S.G.S. Open-file report, 100 pp.

Utsu, T. (1971).

Aftershocks and Earthquake Statistics (III);

Analysis of the distribution of earthquakes in ragnitude, time, and space with special consideration to clustering characteristics of earthquake occurrence (1): Journal of the Faculty of Science, Hokkaido l'niv. Series VII (Ceophysics), 3, no. 5.

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APPEf' DIX I STATICN LOCATIOM i:0 STN.

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001 34 19.91' 81 17.74' 2

002 34 11.58' 81 13.81' U

3 003 34 21.09' 81 27.41' 0

4 004 34 25.72' 81 12.99' U

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JSC 34 16.80' 81 15.60' U

6 JIM 34 20.21' 81 19.47' 7

DW1 34 20.50' 81 20.42' e

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APPENDIX II f40NTICELLO RESERV0IR VELCCITY f40 DEL Veloci ty -

Depth km/sec km 1.00 0.00 5.40 0.03 5.90 '

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APPEtiDIX III LOCATI0il 0F EVEllTS 9

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.c Cc=puter printout of IIY?O71 showing data for locatica of events.

Cole =n 1 Date.

Colu=n 2 Origin time (t!CT) h.n.sec.

Colt =:13 Latitude (:l) degrees, =in.

Colt n 4 Longitude (ii) degrees, =in.

Coltr n 5 Depth (k=).

Co lt.~t 6 Local duration magnitude.

Colu=n 7

!!o. of station readings used to locate event.

P a.d S arrivals frca saae stations are regarded as 2 readings.

Colt =n 8 Lar;ect aci.uthal separation in degrees beta een stations.

Column 9 Epicentral. distance in !=t to nearest station.

Cole =n 10 Root mean square error of time residuals in sec.

P2S=fR /h0, witere R is the time residual for t

the ith siation.

Colt =n 11 Standard error of the epicenter in k:t Colt =n 12 Standard error of the focal depth in km.

Statistical interpretation of standard errors involves assumptions which cay not be met in earthquake locations.

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If ER!t or ER:' is blank, this means that it cannot be computed, because or insurficient data.

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000801 636:46.29 34-18.60 81-20.37 1.80 1.32 12 151 3.3 0.08 0.3 0.8 n1

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