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all geography including DSDP/ODP Sites and Legs
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Correction: Active transform faults in the Gulf of Guinea: insights from geophysical data and implications for seismic hazard assessment
The Damaging Earthquake of 9 October 859 in Kairouan (Tunisia): Evidence from Historical and Archeoseismological Investigations
Active transform faults in the Gulf of Guinea: insights from geophysical data and implications for seismic hazard assessment
The Tunisian Homogenized Macroseismic Database (Second Century–1981): First Investigations
Stress Change and Fault Interaction from a Two Century‐Long Earthquake Sequence in the Central Tell Atlas, Algeria
Abstract The Upper Rhine Graben (URG) is a seismically active tectonic structure in intraplate Europe. Large and moderate earthquakes have occurred along the URG in the past but no coseismic surface faulting has been reported so far. We investigated active faulting along the western edge of the northern URG and identified the 25 km-long linear Riedseltz–Landau normal fault scarp as a major tectonic structure affecting late Pleistocene and Holocene deposits. The fault zone is exposed in the Riedseltz quarry where it affects Pliocene sand and gravels and overlying late Pleistocene (Wurm) units. These units have not been buried deeper than a few tens of metres and yet the fault zone contains cataclastic deformation textures. Cataclasis is demonstrated by spalling and transgranular fractures in quartz grains concentrated in deformation bands with reduced grain size. The observed microstructures suggest multiple phases of deformation with cataclasis followed by emplacement of a prominent Fe-oxide matrix into deformation bands, and later emplacement of a clay-rick matrix into fractures. Previous geological and geophysical studies along the fault show late Pleistocene (Wurm) loess deposits ( c. 24–10 ka before present) and early Holocene sand–silty deposits with individual or cumulative 1.5 and 0.7 m surface slip, respectively. Field observations and previous results from shallow geophysics provide a minimum 0.15 mm a −1 time-averaged slip rate. The Riedseltz fault parameters integrated in a dislocation model suggest a minimum Mw 6.6 earthquake as a plausible scenario in the northern URG. The observations of cataclasis in shallowly buried sediments coupled with observations of the late Quaternary fault scarp call for palaeoseismic studies that may document the occurrence of a larger earthquake on the western edge of URG. Surface faulting of young, shallowly buried sediments associated with cataclasis provides new evidence for assessing the occurrence of large earthquakes and seismic hazard assessment in the northern URG.
Tectonosedimentary evidence in the Tunisian Atlas, Bou Arada Trough: insights for the geodynamic evolution and Africa–Eurasia plate convergence
Onset of aseismic creep on major strike-slip faults
Erratum to Episodic Behavior of the Jordan Valley Section of the Dead Sea Fault Inferred from a 14-ka-Long Integrated Catalog of Large Earthquakes
Episodic Behavior of the Jordan Valley Section of the Dead Sea Fault Inferred from a 14-ka-Long Integrated Catalog of Large Earthquakes
Rupture characteristics of the A.D. 1912 Mürefte (Ganos) earthquake segment of the North Anatolian fault (western Turkey)
We studied the faulted Al Harif Roman aqueduct, located on the north–trending, ~90-km-long Missyaf segment of the Dead Sea fault, using four archaeological excavations, three paleoseismic trenches, and the analysis of six tufa cores. Damage to the aqueduct wall exhibits successive left-lateral fault offsets that amount to 13.6 ± 0.2 m since the aqueduct construction, which is dated younger than 65 B.C. Radiocarbon dating of sedimentary units in trenches, building cement of the aqueduct wall, and tufa cores constrain the late Holocene aqueduct history. The building stone types, related cement dating, and tufa deposits of the aqueduct indicate two reconstruction-repair episodes in A.D. 340 ± 20 and A.D. 720 ± 20. The combined analysis of trench results; successive building and repair of aqueduct wall; and tufa onsets, growths, and interruptions suggests the occurrence of four faulting events in the last ~3500 yr, with a cluster of three events in A.D. 160–510, A.D. 625–690, and A.D. 1010–1210, the latter being correlated with the 29 June 1170 large earthquake. Our study provides the timing of late Holocene earthquakes and infers a lower and upper bound of 4.9–6.3 mm/yr slip rate along the Missyaf segment of the Dead Sea fault in Syria. The inferred successive faulting events, fault segment length, and related amount of = 7.3–7.5 for individual earthquakes. The identification of the coseismic slip yield M w temporal cluster of large seismic events suggests periods of seismic quiescence reaching 1700 yr along the Missyaf fault segment.
Abstract We conducted palaeoseismic studies along the North Anatolian fault both east and west of the Marmara Sea to evaluate its recent surface rupture history in relation to the well-documented historical record of earthquakes in the region, and to assess the hazard of this major fault to the city of Istanbul, one of the largest cities in the Middle East. Across the 1912 rupture of the Ganos strand of the North Anatolian fault west of the Marmara Sea, we excavated 26 trenches to resolve slip and constrain the earthquake history on a channel–fan complex that crosses the fault at a high angle. A distinctive, well-sorted fine sand channel that served as a marker unit was exposed in 21 trenches totaling over 300 m in length. Isopach mapping shows that the sand is channelized north of the fault, and flowed as an overflow fan complex across a broad fault scarp to the south. Realignment of the feeder channel thalweg to the fan apex required about 9±1 m of reconstruction. Study of the rupture history in several exposures demonstrates that this displacement occurred as two large events. Analysis of radiocarbon dates places the age of the sand channel as post ad 1655, so we attribute the two surface ruptures to the large regional earthquakes of 1766 and 1912. If each was similar in size, then about 4–5 m of slip can be attributed to each event, consistent with that reported for 1912 farther east. We also found evidence for two additional surface ruptures after about ad 900, which probably correspond to the large regional earthquakes of 1063 and 1344 (or 1354). These observations suggest fairly periodic occurrence of large earthquakes (RI= c . 283±113 years) for the past millennium, and a rate of c . 16 mm/a if all events experienced similar slip. We excavated six trenches at two sites along the 1999 Izmit rupture to study the past earthquake history along that segment of the North Anatolian fault. One site, located in the township of Köseköy east of Izmit, revealed evidence for three surface ruptures (including 1999) during the past 400 years. The other trench was sited in an Ottoman canal that was excavated (but never completed) in 1591. There is evidence for three large surface rupturing events in the upper 2 m of alluvial fill within the canal at that site, located only a few kilometres from the Köseköy site. One of the past events is almost certainly the large earthquake of 1719, for which historical descriptions of damage are nearly identical to that of 1999. Other earthquakes that could plausibly be attributed to the other recognized rupture of the Izmit segment are the 1754, 1878 or 1894 events, all of which produced damage in the region and for which the source faults are poorly known. Our palaeoseismic observations suggest that the Izmit segment of the North Anatolia fault ruptures every one and a half centuries or so, consistent with the historical record for the region, although the time between ruptures may be as short as 35 years if 1754 broke the Izmit segment. Release of about 4 m of seismic slip both west and east of the Marmara Sea this past century (1912, 1999) support the contention that Istanbul is at high risk from a pending large earthquake. In that historical records suggest that the last large central Marmara Sea event occurred in 1766, there may be a similar 4 m of accumulated strain across the Marmara basin segment of the North Anatolian fault.