Archaeoseismology and Palaeoseismology in the Alpine ... - Tierra

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Table 1: Rockfall triggering candidate events and evidence type* Age Cluster Candidate Triggering Event 0.9 ±0.05 ka 1202 AD earthquake (his) 1.5 ±0.05 ka 551 AD earthquake (his) 2.2 ±0.05 ka 199 BC earthquake (his) 2.7 ±0.05 ka** 759 BC earthquake (ps; his: book of Amos) 4.0 ±0.7 ka ~2050 BC (ps); no historic data; † 6.0 ±1.0 ka No ps data; † * Evidence types are: known historic earthquakes (his), paleoseismic evidence (ps) ** Dashed line separates known historic earthquakes from unreported in history and prehistoric earthquakes † Other evidence correlated to large (Mw 7 or more) earthquakes (Kagan et al., 2005; Yagoda‐Biran, 2008) Candidate earthquakes were selected from historical earthquake catalogs (Amiran et al., 1994; Guidoboni and Comastri, 2005; Guidoboni et al., 1994). Fig. 4: OSL ages and suggested rockfall triggers. OSL age results for the past 8000 years in black circles with error bars; ages of earthquakes determined by Yagoda (2008) in gray diamonds and by Kagan et al. (2005) in gray triangle; corresponding dates of earthquakes suggested as rockfall triggers in gray lines and labeled at top axis. Earthquakes selected from historical earthquake catalogs (Amiran et al., 1994; Guidoboni and Comastri, 2005; Guidoboni et al., 1994). SUMMARY We estimate rockfall hazard for the town of Qiryat‐ Shemona, Dead Sea Transform, N. Israel. It is concluded that particular parts at SW of town are subject to rockfall hazard. Predicted block velocities and kinetic energy are 10–15 m/s and 18,000–45,000 kJ, respectively (for block volumes of ca. 125 m 3 ). According to preliminary OSL age determination it is apparent that the rockfall events 1 st INQUA‐IGCP‐567 International Workshop on Earthquake Archaeology and Palaeoseismology 72 coincide with selected M>6.5 earthquakes. Recurrence interval for the events is 850 years, while the last rockfall probably triggered by the 1202 AD earthquake. For further reading about the rockfall hazard estimation and OSL age determination discussed above, see Kanari (2008). References Amiran, D.H.K., Arieh, E. and Turcotte, T. (1994). Earthquakes in Israel and Adjacent Areas ‐ Macroseismic Observations since 100 Bce. Israel Exploration Journal, 44(3‐4): 260‐305. Begin, Z.B. (2005). Destructive earthquakes in the Jordan Valley and the Dead Sea — their reoccurrence interval and the probability of their occurrence, Geol. Surv. Israel, Report GSI/12/2005. Dussauge‐Peisser, C. et al. (2002). Probabilistic approach to rock fall hazard assessment: potential of historical data analysis. Nat. Hazards Earth Syst. Sci., 2: 15‐26. Dussauge, C., Grasso, J.R. and Helmstetter, A.S. (2003). Statistical analysis of rockfall volume distributions: Implications for rockfall dynamics. Journal of Geophysical Research‐Solid Earth, 108(B6). Freund, R. et al. (1970). Shear Along Dead‐Sea Rift. Philosophical Transactions of the Royal Society of London Series a‐ Mathematical and Physical Sciences, 267(1181): 107‐130. Garfunkel, Z. (1981). Internal structure of the dead‐sea leaky transform (rift) in relation to plate kinematics. Tectonophysics, 80(1‐4): 81‐108. Guidoboni, E. and Comastri, A. (2005). Catalogue of earthquakes and tsunamis in the Mediterranean area from the 11th to the 15th century. Istituto Nazionale di Geofisica e Vulcanologia, Rome, 1037 pp. Guidoboni, E., Comastri, A. and Traina, G. (1994). Catalogues of Ancient Earthquakes in the Mediterranean Area up to the 10th Century. Instituto Nazionale di Geofisica, Roma, 504 pp. Guzzetti, F., Reichenbach, P. and Wieczorek, G.F. (2003). Rockfall hazard and risk assessment in the Yosemite Valley, California, USA. Nat. Hazards Earth Syst. Sci., 3: 491‐503. Jones, C.L., Higgins, J.D. and Andrew, R.D. (2000). Colorado Rockfall Simulation Program Version 4.0 Manual. CDOT‐SYMB‐ CGS‐99‐1, Colorado Department of Transportation, Denver, CO 80222. Kagan, E.J., Agnon, A., Bar‐Matthews, M. and Ayalon, A. (2005). Dating large infrequent earthquakes by damaged cave deposits. Geology, 33(4): 261‐264. Kanari, M. (2008). Evaluation of rockfall hazard to Qiryat‐ Shemona ‐ possible correlation to earthquakes. GSI/24/2008, Geol. Surv. Isr., Jerusalem. Keefer, D.K. (1984). Landslides caused by earthquakes. Geol Soc Am Bull, 95(4): 406‐421. Malamud, B.D., Turcotte, D.L., Guzzetti, F. and Reichenbach, P. (2004). Landslide inventories and their statistical properties. Earth Surface Processes and Landforms, 29(6): 687‐711. Yagoda‐Biran, G. (20080. Seismic hazard estimation along eastern margins of Sea of Galilee by back analysis of seismically induced natural and structural failures. (In Hebrew). GSI/02/08, Geol. Surv. Isr., Jerusalem.
1 st INQUA‐IGCP‐567 International Workshop on Earthquake Archaeology and Palaeoseismology TSUNAMIGENIC DEPOSITS ALONG THE SOUTHERN GULF OF CÁDIZ (SOUTHWESTERN SPAIN) CAUSED BY TSUNAMI IN 1755? B. Koster (1), D. Vonberg (1) and K. Reicherter (1) (1) RWTH Aachen University, Neotectonics and Natural Hazards, Lochnerstr. 4‐20, D‐52056 Aachen, GERMANY. Benjamin.Koster@rwth‐aachen.de, David.Vonberg@rwth‐aachen.de Abstract: Shallow drilling in coastal areas proved sedimentary evidence for palaeo‐tsunamis along a 50 km long segment of the Atlantic coast of southern Spain. The study area was the coast between Barbate and Zahara de los Atunes, both on top of rocky cliffs as well as in lagunas and along sedimentary beaches. In our studies we focused on drill cores, on which we did sedimentary analysis (sieve curves), as well as magnetic susceptibility and foraminifera identification. They give us clues to one or more tsunami events in this region. Different characteristics have been detected and evaluated, such as “fining‐up” sequences with coarse shell debris and rising magnetic susceptibility as well as outcropped “backwash” sediments at Barbate beach. Geomorphologic clues by former publications can be validated like the bridge at Los Lances Bay which acted like a huge flute mark. Key words: 1755 Lisbon tsunami, tsunamites, back flow sediments, Gulf of Cádiz TSUNAMIGENIC DEPOSITS ALONG THE COAST BETWEEN BARBATE AND TARIFA Outcrop evidence and shallow percussion drilling in coastal areas proved sedimentary evidence for palaeotsunamis along a 50 km long segment of the Atlantic coast of southern Spain. We studied the coast between Barbate and Tarifa (Fig. 1 and Fig. 2), situated on top of rocky cliffs as well as in lagunas and along sedimentary beaches (Marismas de Barbate and Zahara de los Atunes, Los Lances N of Tarifa). Also, we focused on bays (Bolonia, Valdevaqueros), which are most probably sheltered from direct tsunami wave action. However, reflections of the waves may occur and may hit these bays. In these bays, the Roman villages of Baelo Claudia and Mellaria, respectively, have been situated (e.g. Silva et al., 2006, 2009). Fig. 1: Map of the study area between Barbate and Tarifa; every dot indicate a location of shallow drilling to detect tsunamite layers. Following, we will describe the different situations at several locations in the study area. 73 Marismas de Barbate The marshlands of Barbate have only little elevation of about 0 to 1.0 m above mean sea level and are flooded permanently by the tide. This ideal tsunamite reservoir was probed with percussion coring with an open window sampler. We reached depths of about 5.0 meters. After core description the same site was drilled with a sampler with PVC liners for lab analyses. Cores provided evidence for tsunamigenic layers. Laboratory analyses validated the clues of the field‐work. We found "fining‐up" sequences, typical for tsunamites (Bryant, 2007), with coarse grain size at the bottom up to fine clays at the top of these layers, as well as shell debris. The sequences include foraminifera, such as sponge spiculae sp., elphidium crispum and globigerina sp. They are indicator for tsunamigenic deposits, in fact their habitat lies in deep water regions. Deep water foraminifera can only deposit at landside by an event, which affects the whole water head (e.g. Nott, 2006; Bryant, 2007). Fig. 2: Map of theBarbate and Zahara de los Atunes area with possible tsunami action (green arrows); box at the beach shows place of outcrop evidence near to Barbate.
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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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Page 31 and 32: Nevertheless the lack of research,
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Page 43 and 44: Table 1: Surface faulting extent re
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Page 55 and 56: to 400 m) the calculated values for
Page 57 and 58: RISK ANALYSIS The created hazard ma
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Page 61 and 62: CONCLUSIONS From the palaeostress a
Page 63 and 64: Fig. 2: Geological map of the study
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Page 103 and 104: CONCLUDING REMARKS The exposed exam
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associated with various tsunamis (<
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this method, the magnitude of the e
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etween pieces. Fragments have not f
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on the exact date of the earthquake
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THE ARCHAEOLOGICAL ZONE COLOGNE Aft
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affecting the Alcázar was about 50
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archaeoseismology could instead bec
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In the area later occupied by Vilni
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Fig. 2: Assemblage of landforms ass
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Fig. 8: Data and regression for mag
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Fig. 3: Relationships among magnitu
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CONCLUSIONS 1. Spatial distribution
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The stratigraphic sequence (Fig. 4)
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especially in the zones of hanging
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interpretations are based on relati
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Fig. 5: Gray‐scale value laser im
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(~40 cm), F‐ rotated building str
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Index 1 st INQUA‐IGCP‐567 Inter
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