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A Comparison of Strong and Weak Ground-Motion in Wellington City

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A Comparison of Strong and Weak Ground-Motion in Wellington City S&G 3638 l SITE EFFECTS FROM SEISMIC SHAKING: A COMPARISON OF STRONG AND WEAK GROUND-MOT[ON IN WELLINGTON CITY AND THE HUTr VALLEY J. John'Ihber Institute of Geophysics Victoria University of Wellington S. Sritharan, G. H. McVerry Institute of Geological and Nuclear Sciences J. H. Ansell Institute of Geophysics Victoria University of Wellington A Report to Earthquake and War Damage Commission May 1993 Contents Summary 1 1. Introduction 2 2. Data Collection and Site Specification 4 3. Data Analysis and Results 12 3.1 Fourier Spectral Ratios 14 3.1.1 Lower Hutt Fourier Spectral Ratios 17 3.1.2 Wellington Fourier Spectral Ratios 24 3.2 Response Spectral Ratios 30 3.2.1 Inwer Hutt Response Spectral Ratios 30 3.2.2 Wellington Response Spectral Ratios 35 4. Discussion 35 5 Recommendations for Further Work 42 6 Conclusions 43 7. Acknowledgements 43 8. References 44 Appendix A 46 Summary Weak- and strong-motion records have been compared at six sites in Lower Hutt and ten sites in Wellington cily. The comparisons have been made in terms of Fourier spectral ratios of ground velocity and 5% damped response spectral ratios of ground acceleration. The peak accelerations for the strong-motion data range from 0.5% g to 10% g while the weak-motion range is 0.005% g to 0.4% g. Non-linear behaviour does not appear to be significant over this ground motion range. In general the strong-motion ratios lie within one standard deviation of the weak-motion ratios at most frequencies, though the strong-motion ratios tend to lie below the mean of the weak-motion ratios. Only one site common to the weak- and strong-motion recorders was located on more than 10 m of soft soil. At this site, the lower strong-motion ratios might be due to non-linear behaviour. One site on about 70 m of alluvial gravels also had lower strong-motion ratios. One site on alluvium and thick gravel to a total depth of 275 m in the Hutt Valley had a greater strong- motion response in the longer period range. A site near the edge of the valley on alluvium had its peak at a shorter period in the weak-motion ratios. FO 1. Introduction The importance of localised variations in earthquake ground motions has become widely recognised in the past few years, particularly after the amplifications seen in Mexico city in 1985 and San Francisco in 1989. Many New Zealand cities are built in sediment filled valleys or on recent fill and thus a similar amplification potential exists here. Ideally one would measure strong ground motion directly at a variety of sites to determine the relative levels of shaking, but sufficiently large events are too infrequent to provide enough information. Alternatively, in regions similar to New Zealand where damaging earthquakes are expected, but infrequent, the ground response due to microearthquakes has been successfully used to identify areas which subsequently experienced damaging shaking in a large earthquake (Borcher(it, 1991). Recent microzoning studies in the Wellington region (lkber and Smith, 1992) have shown there is a wide of range of weak-motion amplifications here (Figure 1). The question remains just how well these weak-motion amplifications can be used to predict strong motions, and particularly, how dependent is the non- linearity on the geologic properties of the soil. The purpose of this study is to make a first attempt to compare weak-motion recordings in the Wellington region to the limited strong-motion data. The ultimate goal is to determine the relationship between amplification in weak and strong ground motions, including the level of shaking where non-linear effects become important It is hoped to use the comparisons between weak- and strong-motion amplifications observed in the Wellington region study to extrapolate the results to weak-motion surveys which may be carried out in other parts of New Zealand where there are no strong-motion data. While the data have been interpreted to some extent, the primary results of the project are the presentation of the strong and weak motions processed in the same way on the same plots. The "strong-motion" 91/01/28 12:59 North Component L()8 L24 L11 L15 L14 L()6 L23 L()5 L()4 L22 L21 L20 L 19 L 18 L02 120.0 108.0 108.0 96.0 96.() Time (seconds) 84.0 84.0 72.0 72.0 60.0 60.0 1 1 Figure 1. Seismograms displayed approximately along the length of the Hutt Valley The firm, valley edge sites are L08, L14, and L19. There is a general decrease in amplitude E when going up-valley from Petone (L24) to L02. Note the high amplitude at L18, which is located over a drained and filled swamp in Naenae. The maximum velocity at site L18 is 4.5 mm/s. 4 data collected to date in the Wellington region extends only to about 10% g, so that significant non-linear effects were not expected. However this study does provide the comparison of data ranging from .005% g to 10% g. Almost all of the strong- motion recorders are still operating so when a large earthquake occurs in the future, it will be poesible to compare the weak motions from the current study to larger motions. Up to 30 weak-motion recordings have been collected at each site whereas often only one or two strong-motion records exist The weak-motion recordings show a wide variation of amplifications at the same site for different earthquakes (lhber and Smith, 1992). Therefore the approach in this study has been to show the range and mean of the weak-motion amplifications and to overlay these ranges with the strong-motion data. Effects due to individual earthquakes have not been considered in this report. For a detailed study of the strong-motion records of the 1973, 1977, and 1990 earthquakes, see Sritharan and McVerry (1992). The basic information about these earthquakes is listed in'Ihble 1. 2. Data Collection and Site Specification The data used in this study come from three different sources. The strong- motion data have been produced by the IGNS strong-motion network. We have lim- ited our analysis to the largest earthquakes recorded before 1991. The two largest earthquakes are the events in 1973 and 1977 (Table 1). These two events were rather different in frequency content. The 1973 earthquake had a strong long-period response while the 1977 earthquake was richer in high frequencies (Sritharan and McVerry, 1990). Two smaller earthquakes that occurred in 1990 were included in the analysis because the 1973 and 1977 earthquakes were not recorded at one of the strong-motion sites. 5 'Ihble 1. Earthquakes used in strong-motion analysis. Date Time Lat Lon Depth Mag MM Intensity Epicentral (km) In Wellington Distance from and Lower Hutt Site L14 05/01/77 13:54 39.13S 175.18E 173 7.0 V 235 18/01/77 05:42 41.84S 174.58E 33 6.0 V 73 19/02/90 05:34 40.47S 176.44E 34 5.9 - 154 04/10/90 23:48 41.64S 175.51E 23 4.9 - 67 Thble 2. Earthquakes used in weak-motion analysis (locations from DSIR Seismolog- ical Observatory) Wellington Array Year Month Day Hrmn Sec Lat Lon Depth Mag Distance fivm (km) site COT 1991 OCT 13 1642 17.24 41.80S 174.55E 30.5 2.9 60 1991 OCT 23 1438 45.27 37.00S 177.26E 216.3 5.8 523 1991 OCT 25 2106 5.49 38.02S 176.19E 213.3 5.6 383 1991 OCT 27 1142 16.78 41.37S 174.36E 33.7 2.8 35 1991 OCT 28 0304 28.68 41.51S 174.19E 42.8 3.2 54 1991 OCT 29 2019 21.87 41.43S 175.01E 28.3 3.2 25 1991 OCT 31 1422 10.31 41.82S 173.98E 44.4 4.8 88 1991 NOV 05 2016 41.97 41.42S 174.62E 30.8 2.9 19 1991 NOV 07 1647 51.75 40.60S 173.65E 96.7 3.7 121 1991 NOV 09 1836 50.71 40.47S 173.30E 158.0 4.3 153 1991 NOV 12 1403 8.27 41.04S 174.51E 54.3 3.7 35 1991 NOV 13 0602 37.32 41.24S 172.53E 229.0 4.4 187 1991 NOV 14 1154 58.17 40.22S 173.61E 152.1 4.0 154 1991 NOV 16 0035 39.95 37.11S 176.90E 263.2 6.1 500 1991 NOV 26 0943 39.54 39.71S 174.84E 114.5 4.6 176 1991 NOV 26 1514 29.90 41.06S 174.75E 31.2 2.5 26 1991 NOV 28 1544 8.80 41.43S 173.91E 42.8 3.5 73 1991 NOV 29 1340 56.69 39.94S 175.10E 27.4 3.4 152 1991 DEC 03 0943 7.28 41.08S 174.48E 35.8 3.4 33 1991 DEC 08 0423 29.68 41.25S 175.35E 30.5 4.2 49 1991 DEC 08 0615 37.42 41.24S 175.35E 29.9 3.7 49 1991 DEC 08 1007 24.37 41.25S 175.34E 28.5 3.1 48 1991 DEC 08 1010 42.82 41.24S 175.34E 27.2 2.9 48 1991 DEC 12 1411 57.05 41.23S 175.34E 27.2 3.1 48 1991 DEC 16 0446 28.55 41.27S 173.89E 61.8 3.8 73 1991 DEC 18 0818 10.04 40.68S 175.48E 10.4 3.6 90 1991 DEC 31 0459 28.16 41.25S 174.87E 28.4 2.9 10 6 1991 DEC 31 1028 59.48 41.50S 174.50E 19.8 3.0 32 1992 JAN 02 1445 23.69 41.04S 174.47E 16.3 2.8 37 1992 JAN 05 1004 42.27 41.30S 172.76E 154.2 4.5 168 Lower Hutt Array Year Mon Day Hrmn Sec Lat Lon Depth Mag Distance from (km) site L14 1990 NOV 27 1529 5.18 40.41S 174.46E 7.0 3.6 99 1990 NOV 29 2305 0.60 40.69S 174.66E 58.9 4.5 64 1990 NOV 30 1738 37.08 40.73S 174.95E 16.1 4.0 56 1990 DEC 9 0742 13.34 40.64S 175.39E 40.9 3.2 77 1990 DEC 12 0702 26.81 41.62S 175.37E 25.0 3.5 57 1990 DEC 16 1454 48.78 41.14S 175.16E 33.0 3.2 23 1990 DEC 16 1608 32.24 41.59S 173.64E 58.9 3.7 114 1990 DEC 20 1558 57.86 40.95S 174.65E 65.6 3.5 39 1990 DEC 23 2008 16.30 41.02S 174.59E 42.0 3.6 37 1990 DEC 26 1120 28.66 39.05S 175.26E 139.8 4.7 244 1990 DEC 29 1049 51.16 41.31S 174.11E 48.6 3.7 68 1991 JAN 9 1550 14.91 41.06S 174.73E 59.9 3.6 25 1991 JAN 11 1645 3.28 40.77S 176.32E 25.2 4.1 128 1991 JAN 15 1045 31.46 40.41S 174.47E 13.1 3.3 99 1991 JAN 11 1712 54.52 38.56S 175.62E 193.2 4.6 303 1991 JAN 22 1443 59.72 41.65S 175.40E 23.6 3.1 61 1991 JAN 24 1714 53.04 40.73S 175.38E 33.8 3.4 68 1991 JAN 26 1133 18.11 41.59S 174.48E 10.9 2.8 54 1991 JAN 28 1258 47.50 41.89S 171.61E 8.3 5.7 285 1991 JAN 28 1800 54.52 41.90S 171.73E 17.3 5.8 276 1991 FEB 1 1742 14.24 41.64S 175.49E 23.8 3.2 65 ....................
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