Archaeoseismology and Palaeoseismology in the Alpine ... - Tierra

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The observed surficial fault breaks show vertical offset of 0.5‐1.0m, with normal slip. According to magnitude vs displacement relationships it comes out to be a threshold magnitude of 6.5 for primary faulting like at Caporio site. Figure 5: Flow Chart showing the major categories developed for the earthquake size estimation procedure SEISMIC HAZARD ESTIMATIONS Estimating earthquake size is not simple and many methods are in use. Understanding the type of earthquake size estimate made (e.g. local magnitude, surface‐wave magnitude, or seismic moment), and being consistent throughout the analysis is very important. Different approaches and techniques are in practice, for the estimation of earthquake size for seismic hazard. Estimating Earthquake Sizes An estimation procedure has been divided into five parts in order to understand the individual components making up the procedure. These divisions are: the type of seismic hazard estimate approaches, scaling parameters, techniques, and data (Fig. 5). Types of Seismic Hazard Estimates The type of seismic hazard estimate needed, guides the development of seismic hazard analysis. The way the uncertainties in data are considered or weighed in the analysis depends on the type of seismic hazard estimate. (A few types of commonly used earthquake estimates are as follows.) Characteristic Earthquake Maximum Earthquake Maximum Credible Earthquake (MCE) Floating Earthquakes Approaches Historical earthquake approach Paleoseismic Approach Source Characterization Approach. Regional Approach Relative‐Comparison Approach Scaling Parameters Historical Seismicity Fault Rupture Length Fault Rupture Area Fault Displacement Seismic Moment Strain Rate Techniques Historical Seismicity Technique: 1 st INQUA‐IGCP‐567 International Workshop on Earthquake Archaeology and Palaeoseismology 154 Earthquake Size‐Fault Parameter Correlations: These relations can be applied by estimating fault rupture length, area and displacement. Fig. 6: Data and regression for surface‐wave magnitude vs. length of surface rupture (from Bonilla and others, 1984). Fault Rupture Length: A relationship developed (Fig. 6) from all historical earthquake events studies. Correlation is used to convert the length parameter into earthquake size parameter by Bonilla and others (1984), is Ms = 6.04 + 0.704 (log L), where L is the surface rupture length in kilometers and the relation is valid over the range of Ms = 5.5 – 8. Wesnousky (1986) has used seismic moment rather than magnitude in length correlations (Fig. 7). Fault‐rupture‐length relations are widely used in interplate regions to determine an average or expected earthquake size. These values can be used directly for characteristic and maximum earthquake estimates. Fig. 7: Seismic moment vs. earthquake rupture length; data from faults with slip rates above and below 1 cm/yr are distinguished as well as the sense of displacement. Equations for lines are log M0 = A + B log L, the right regression line is for slip rates greater than 1cm/yr (solid circles); the left line is for slip rates less than 1 cm/yr (from Wesnousky, 1986) ‐ Fault‐rupture Area: Once the fault rupture area is estimated, empirical relations such as by Wyss (1979) can be used (Fig. 8). This relation is M= log A +4.5 for M>5.6 where M is magnitude and A is fault area in square kilometers. Fault area method is especially useful in areas with an unusually deep seismogenic zone that could accommodate large potential earthquakes. Fault area relations can also be used in cases where a fault is blind or buried, such as blind thrust under an actively deforming anticline. ‐ Fault Displacement: Empirical earthquake size‐fault displacement relationship is developed by Slemmons (1982a) and Bonila and others (1984) by correlating surface wave magnitude with maximum displacement. An example of one of these relationships using all earthquakes is shown in Fig. 9. Seismic Moment (Fig. 10) Strain Rate Technique
Fig. 8: Data and regression for magnitude vs. fault‐rupture area (from Wyss, 1979). Data Data include the information collected as various input values used for the size estimation Fig. 9: Data and regression for surface‐wave magnitude vs. maximum surface displacement (from Bonilla and others, 1984) Fig. 10: Log fault length vs. log moment for large interplate and intraplate earthquakes (Scholz et al, 1986) Acknowledgements: Thanks to Dr. Leonello Serva for his invaluable contribution towards supervision, guidance and all the way help for successful completion of this work at ANPA, Italy. This work was carried out during a 6 month fellowship award by International Atomic Energy Agency (IAEA) to the author.Eutizio Vittori, A. M. Michetti and Luca Ferreli provided all the logistic . 1 st INQUA‐IGCP‐567 International Workshop on Earthquake Archaeology and Palaeoseismology 155 help alongwith some very stimulating discussions on paleoseismology and capable faults. References Allen C.R. (1986). Seismological and Paleoseismological Tehniques of Research in Active Tectonics. Active Tectonics, National Academy Press, Washington D.C, PP. 148 – 153. Brunamonte F., Michetti A. M., Serva L. and Vittori E. (1993). Seismic Hazard Evaluation in Central Italy: Preliminary results of the Rieti Basin Project. Annali Di Geofisica, vol.xxxvi, (1), April, PP. 253‐262, Depolo C.M. and Slemmons DB. (1990). Estimation of Earthquake size for Seismic Hazards. Reviews in Engineering Geology, Vol. viii, Geological Society of America, Inc. 3300 Penrose Place, P.O Box 9140, Boulder, Colorado 80301, 1‐28. Keller E. A. “Investigation of Active Tectonics: Use of Surficial Earth Processes”. In: Active Tectonics, National Academy Press, Washington D.C, PP. 136‐147, 1986. Mayer L. (1986). Tectonics Geomorphology of Escarpments and Mountain Fronts., In Active Tectonics, National Academy Press, Washington D.C, 125‐135. Michetti A. M., Brunamonte F., Serva L., Whitney R.A. (1995) Seismic Hazard Assessment From Paleoseismic Evidence in the Rieti Region, Central Italy. Proceedings of International Congress on perspective in Paleoseismology, 63‐82. Michetti A.M. (1993). Coseismic Surface Displacemet Vs Magmitude: Relationship from Paleoseismological Analysis in the central Apeninnes (Italy). Proceedings of the CRCM, 93, Kobe, December 6‐11, 375‐380. Ramelli A.R. (1990). Implications of the Meers Fault on Seismic Potential in the Central United States. Reviews in Engineering Geology, Vol. viii, Geological Society of America, Inc. 3300, 59‐ 75. Reiter L. (1990). Earthquake Hazard Analysis. Columbia University Press, New York, 97p. Schumm S.A. (1986). Alluvial River Response to Active Tectonics”. In: Active Tectonics, National Academy Press, Washington D.C, PP. 80‐94. Schwartz D.P. and Coppersmith K.J. (1986). Seismic Hazard: New Trends in Analysis using Geologic Data. In: Active Tectonics, National Academy Press, Washinton D.C, PP.215‐230. Serva L. (1993). An Analysis of the World Major Regulatory Guides for Nuclear Power Plant Seismic Design. Engianucleare/ANNO. 10/N.2/May‐SEPTEMBER, PP. 77‐96. Slemmons D. B. and Depolo C.M. (1986). Evaluation of Active Faulting and Associated Hazards. In: Active Tectonics, National Academy Press, Washington D.C, PP. 45‐61. Vittori E. Sylos Labini S. and Serva L. (1991). Paleoseismology: Review of the state of the art. Investigation of Historical Earthquakes in Europe, Tectonophysics, 193, 9‐32. Yeats R.S. (1986). Active Faults Related to Folding, In: Active Tectonics, National Academy Press, Washington D.C, PP. 63‐79
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Abstracts Volume Archaeoseismology
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Edita e imprime: Sección de Public
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1 st INQUA‐IGCP‐567 Internation
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the importance of performing absolu
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indicative of strike‐slip faultin
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DISCUSSION Based on detailed field
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Table 1: Source parameters used in
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elations. However, the attenuation
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mostly concentrated on the DST in I
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continuous support. N. Shalev, G. G
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The tumulus initial morphology show
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our understanding and prediction of
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spans, with a threefold increase fr
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Nevertheless the lack of research,
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earthquake. In uncertain cases, as
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The site reconnaissance successfull
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Table 1: Surface faulting extent re
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The graben has a markedly asymmetri
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are a valuable addition to the rout
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to 400 m) the calculated values for
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RISK ANALYSIS The created hazard ma
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290 m water depth the basin accumul
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CONCLUSIONS From the palaeostress a
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Fig. 2: Geological map of the study
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however, the massive 1995 earthquak
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mapped on the slopes above Qiryat
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interpreted as either an expression
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The Shepran Cave is located on the
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properties. The mean value of speci
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excavated a deep trench, thus provi
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Fig. 8: Seismic ground shaking may
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elevant qualitative criteria are po
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CONCLUDING REMARKS The exposed exam
Page 105 and 106: produced by significantly different
Page 107 and 108: It is possible that a portion of th
Page 109 and 110: In addition, the Database of histor
Page 111 and 112: were published by IGME (1983) and E
Page 113 and 114: 1 st INQUA‐IGCP‐567 Internation
Page 115 and 116: The city collapsed and it was aband
Page 119 and 120: Fig. 4: Slipped lintel in a window
Page 121 and 122: to overcome shear resistance and in
Page 123 and 124: Newmark, N.M. (1965). Effects of ea
Page 125 and 126: associated with various tsunamis (<
Page 129 and 130: this method, the magnitude of the e
Page 133 and 134: etween pieces. Fragments have not f
Page 137 and 138: on the exact date of the earthquake
Page 139 and 140: THE ARCHAEOLOGICAL ZONE COLOGNE Aft
Page 143 and 144: affecting the Alcázar was about 50
Page 147 and 148: archaeoseismology could instead bec
Page 149 and 150: In the area later occupied by Vilni
Page 155: Fig. 2: Assemblage of landforms ass
Page 159 and 160: Fig. 3: Relationships among magnitu
Page 161 and 162: CONCLUSIONS 1. Spatial distribution
Page 163 and 164: The stratigraphic sequence (Fig. 4)
Page 165 and 166: especially in the zones of hanging
Page 169 and 170: interpretations are based on relati
Page 173 and 174: Fig. 5: Gray‐scale value laser im
Page 177 and 178: (~40 cm), F‐ rotated building str
Page 179 and 180: Index 1 st INQUA‐IGCP‐567 Inter
Page 181: 1 st INQUA‐IGCP‐567 Internation
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