Archaeoseismology and Palaeoseismology in the Alpine ... - Tierra

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OUTLOOK In the next step, the main focus of attention is on the intensity analysis and the calculation of the roughness in 3D‐space. Different approaches have been given in the literature, within these the roughness‐length method and the root mean square method are promising, which we are going to test. Acknowledgements: We would like to thank C. Grützner and N. Hoffmann for constructive criticism, T. Fernandez‐Steeger for fruitful discussions and helpful suggestions and J. Beier for various support during the field work. References Benedetti, L., Finkel, R., Papanastassiou, D., King, G., Armijo, R., Ryerson, F., Farber, D., Flerit, F., 2002. Postglacial slip history of the Sparta Fault (Greece) determined by 36 Cl cosmogenic dating: evidence for non‐periodic earthquakes. Geophys. Res. Lett., 29, 87‐1–87‐4. Benedetti, L., Finkel, R., King, G., Armijo, R., Papanastassiou, D., Ryerson, F., Flerit, F., Farber, D., Stavrakakis, G., 2003. Motion on the Kaparelli fault (Greece) prior to the 1981 earthquake sequence determined from 36 Cl cosmogenic dating. Terra Nova, 15. 118‐124. Fardin, N., Stephansson, O., Jing, J., 2001. The scale dependence of rock joint surface roughness. International Journal of Rock Mechanics & Mining Science, 38, 659‐669. Fardin, N., Feng, Q., Stephansson, O., 2004. Application of a new in situ 3D laser scanner to study the scale effect on the rock joint surface roughness. International Journal of Rock Mechanics & Mining Science, 41, 329‐335. Ganas, A., Bosy, J., Petro, L., Drakatos, G., Kontny, B., Stercz, M., Melis, N. S., Cacon, S., Kiratzi, A., 2007. Monitoring active structures in eastern Corinth Gulf (Greece): The Kaparelli fault. Acta Geodyn. Geomater., Vol.4, No.1 (145), 1‐9. Hubert, A., King, G., Armijo, R., Meyer, B., Papnastasiou, D., 1996. Fault re‐activation, stress interaction and rupture propagation of 1981 Corinth earthquake sequence. Earth and Planetary Science Letters, 142, 573‐ 585. Kokkalas, S., Jones, R.R., McVaffrey, K.J.W., Clegg, P., 2007a. Quantitative fault analysis at Arkitsa, central Greece, using 1 st INQUA‐IGCP‐567 International Workshop on Earthquake Archaeology and Palaeoseismology 172 terrestrial laser‐scanning (LiDAR). Bull. Geol. Soc. Greece, vol. XXXX,1959‐1972. Kokkalas, S., Pavlides, S., Koukouvelas, I., Ganas, A., Stamatopoulos, L., 2007b. Paleoseismicity of the Kaparelli fault (eastern Corinth Gulf): evidence for earthquake recurrence and fault behavior. Boll. Soc. Geol. It. (Ital.J.Geosci.), Vol. 126, No. 2, 387‐395. Kulatilake, P.H.S.W., Um, J., 1999. Requirements for accurate quantification of self‐affine roughness using the roughness‐ length method. Int. J. Rock Mech. Min. Sci. & Geomech. 36, 5‐ 18. Kuhn, D., Prüfer, S., 2007. Anwendung des Terrestrischen Laserscanners im Landslide Monitoring.‐ In: Otto, F. (Hrsg.): Berichte von der 16. Tagung für Ingenieurgeologie. 7.‐10. März 2007, Bochum. Rabatel, A., Deline, P., Jaillet, S., Ravanel, L., 2008. Rock falls in high‐alpine rock walls quantified by terrestrial lidar measurements: A case study in the Mont Blanc area, Geophys. Res. Lett., 35, L10502, doi:10.1029/2008GL033424. Rahman, Z., Slob, S., Hack, R., 2006. Deriving roughness characteristics of rock mass discontinuities from terrestrial laser scan data. Proceedings of the 10th IAEG Congress, Engineering geology for tomorrow's cities, Nottingham, United Kingdom, 6‐10 September 2006. Engineering geology for tomorrow's cities. Sagy, A., Brodsky, E.E., Axen, G.J., 2007. Evolution of fault‐surface roughness with slip. Geology, 35: 283‐286. Slob, S., Hack, H.R.G.K., Feng, Q., Röshoff, K., Turner, A.K., 2007. Fracture mapping using 3D laser scanning techniques.‐ In: Sousa et. al.: 11th congress of the ISRM, 9‐13 July, 2007, Lisbon, Portugal, 299‐302. Stewart, I., 1996. A rough guide to limestone fault scarps. Journal of Structural Geology, Vol. 18, No. 10., 1259‐1264. Travelletti, J., Oppikofer, T., Delacourt, C., Malet, J.‐P., Jaboyedoff, M., 2008. Monitoring landslide displacements during a controlled rain experiment using a long‐range terrestrial laser scanning (TLS). The International Archives of the Photogrammetry, Remote Sensing and Spatial Information Sciences. Vol. XXXVII. Part B5. Beijing 2008, 485‐490. Tse, R., Cruden, D.M., 1979. Estimating joint roughness coefficients. Int. J. Rock Mech. Min. Sci. & Geomech. 16, 303‐ 307
1 st INQUA‐IGCP‐567 International Workshop on Earthquake Archaeology and Palaeoseismology TESTING THE HYPOTHESIS OF EARTHQUAKE‐RELATED DAMAGE IN STRUCTURES IN THE LYCIAN ANCIENT CITY OF PINARA, SW TURKEY B. Yerli (1) ,S. Schreiber (2), K.G. Hinzen (2), J.H. ten Veen (3) and M. and M. Sintubin (4) (1) Institute for Geology, Mineralogy and Geophysics, Ruhr University, Universitätsstrasse 150, D‐44801, Bochum, GERMANY. baris.yerli@rub.de (2) Earthquake Geology Group, Cologne University, Vinzenz‐Pallotti‐Str. 26, 51429 Bergisch Gladbach. GERMANY (3) TNO Built Environment and Geosciences, P.O. Box 80015, 3508 TA, THE NETHERLANDS (4) Geodynamics & Geofluids Research Group, K.U. Leuven, Celestijnenlaan 200E, 3001 Leuven, BELGIUM Abstract: Earthquake‐related damage in archaeological structures can provide important clues to increase our knowledge of the timing and magnitude of historical earthquakes. However, anthropogenic and other natural influences make the investigation more complex. The quantitative methods (e.g. laser scanning) have been used in Pınara Ancient City to distinguish the manmade damage from seismic‐related damage. The geological investigations and archaeoseismological observations indicate that the city of Pınara has been affected by earthquakes but the relicts have been also despoiled. The Sarcophagus of Arttumpara in Pınara is deformed and the upper two massive limestone decks have been rotated ca. 5° in clockwise direction and traces of an explosion have been observed on the second ceiling. These features make the sarcophagus a reliable and an interesting example for testing the origin of the cause of damage. Key words: archaeoseismology, laser scanning, damage modelling INTRODUCTION Archaeoseismological studies usually attempt to investigate a possible connection between damage to the archaeological structures and historical or instrumental earthquakes. The important challenge lies in separating earthquake‐related damage from anthropogenic and other natural causes (Ambraseys et al., 2004; Guidoboni, 2002). Recent seismological engineering models can be used to test the hypothesis that observed building damage is of seismogenic nature (e.g. Hinzen, 2005) by seeking a systematic relation between building response and the seismic source or ground motion. Fig. 1: Plate tectonic map of the eastern Mediterranean (modified after ten Veen, 2004). FBFZ = Fethiye Burdur Fault Zone, MM = Menderes Massive, PT = Pliny Trench, ST = Strabo Trench In the following, the geological and seismological setting of Pınara and surroundings will be described, followed by a sketch of the archaeoseismological results. 173 Subsequently, measurements and in‐situ observations are examined with respect to being suitable traces for earthquake‐related damage. We conclude that the main task will be to differentiate between earthquake‐related damage and anthropogenic damage. We propose to employ methods based on laser scanning and discrete element modelling for examining causes of the damage on the structures. THE ESEN BASIN The tectonic evolution of southwestern Turkey (Fig. 1) is characterized by a multi‐stage deformation, which is initially related to the Cretaceous – Middle Miocene Neothetys closure and subsequently to the collision of African and Eurasian plates in Late Miocene to Recent times. This tectonic process was followed by the initiation of the north and south Anatolian transform fault systems (NAF and EAF). These transform fault systems accommodate the westward extrusion of the Anatolian platelet (e.g. Barka and Kadinsky‐Cade, 1988; Westaway, 1994; Armijo et al., 1999; ten Veen et al., 2008). In southwestern Turkey the neotectonic activity is represented by the so‐called Fethiye‐Burdur Fault Zone (Barka and Reilinger, 1997; FBFZ); a domain with many sub‐parallel NE‐SW trending fault segments and basins in the area between Fethiye and Burdur. The Eşen Basin together with many similar fluvio‐lacustrine extensional basins are located in the tectonically complex FBFZ and are likely foundered in response to gravitational collapse of the Lycian Orogen that formed during several thrusting phases in the Cretaceous – Middle Miocene period (e.g. Collins and Robertson, 1999; Alçiçek et al., 2006, Alçiçek, 2007).
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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
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produced by significantly different
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It is possible that a portion of th
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In addition, the Database of histor
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were published by IGME (1983) and E
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The city collapsed and it was aband
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Fig. 4: Slipped lintel in a window
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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 (<
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Page 133 and 134: etween pieces. Fragments have not f
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Page 139 and 140: THE ARCHAEOLOGICAL ZONE COLOGNE Aft
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Page 149 and 150: In the area later occupied by Vilni
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Page 157 and 158: Fig. 8: Data and regression for mag
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Page 161 and 162: CONCLUSIONS 1. Spatial distribution
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Page 173: Fig. 5: Gray‐scale value laser im
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