The 1900 Mw 7.6 earthquake offshore north–central Venezuela: Is La Tortuga or San Sebastián the source fault?

Colón, Sirel; Audemard, Franck; Beck, Christian; Ávila, Jesús Guadalupe Arreola; Padrón, Carlos; Batist, Marc De; Paolini, M.; Leal, A.F.; Welden, Aurélien van

doi:10.1016/j.marpetgeo.2015.06.005

Cited by 8 publications

(7 citation statements)

References 26 publications

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“…The SSF and LVF have produced intermediate to large magnitude earthquakes (Table S1.1). The SSF ruptured during the September 12, 2009 M w 6.1, the damaging 1967 M 6.5 Caracas (Pérez, 1998a;Suárez & Nábělek, 1990), and the 1900 M 7.6 to M 8.0 earthquakes, where the latter ruptured the eastern SSF segment (Figure 2; Colón et al, 2015;Pacheco & Sykes, 1992). Microseismicity (M ≤ 4) has been detected on the SSF, with a greater number of events on its eastern segment than on its central and western segments (Pérez et al, 1997).…”

Section: San Sebastian and La Victoria Faultsmentioning

confidence: 99%

“…The E‐W trending SSF and the WSW‐ENE trending LVF accommodate ~90% of the CA‐SA motion (i.e., ~19 mm/yr) in the western segment of the plate boundary in north‐central Venezuela (Figure 1) (Pérez et al., 2018; Schubert, 1981). The SSF has a fairly simple 280 km long fault trace (Colón et al., 2015; Escalona et al., 2011; Schubert & Krause, 1984), and connects to the western EPF across the Gulf of Cariaco pull‐apart basin (Escalona et al., 2011; Schubert, 1985). The LVF has a 230 km long trace and terminates in the Gulf of Cariaco (Schubert & Krause, 1984).…”

Section: Active Faults and Geology Of The Ca‐sa Transform Plate Boundarymentioning

confidence: 99%

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Strain Partitioning and Interseismic Fault Behavior Along the Caribbean‐South American Transform Plate Boundary

et al. 2021

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We combine Global Positioning System and Interferometric Synthetic Aperture Radar (InSAR) data to characterize the interseismic behavior (i.e., locked or creeping), and strain partitioning for the faults along the Caribbean‐South American transform plate boundary. Interseismic strain is distributed mainly on three faults, the San Sebastian, El Pilar, and Central Range faults, but partitioning occurs across multiple faults in the west (San Sebastian and La Victoria faults) and east (Sub‐Tobago Terrane, Central Range, and South Coast faults). In northern Venezuela, slip is partitioned on the San Sebastian (16.4 ± 1.7 mm/yr) and La Victoria (4.3 ± 0.9 mm/yr) faults. In north‐eastern Venezuela, the El Pilar fault accommodates slip at a rate of 18.6 ± 1.8 mm/yr. In Trinidad and Tobago, slip is partitioned between the Sub‐Tobago Terrane (3.0 ± 0.1 mm/yr), Central Range (14.5 ± 2.0 mm/yr), and South Coast (3.0 ± 0.1 mm/yr) faults. The La Victoria, San Sebastian, the western El Pilar segment, and Sub‐Tobago Terrane faults are locked to depths of 16.2 ± 4.0 km, 7.7 ± 5.2 km, 6.7 ± 2.8 km, and 8.0 ± 0.2 km, respectively. The eastern segment of the El Pilar, the Central Range, and the South Coast faults all creep. Our new InSAR results indicate that the entire Central Range Fault is creeping. The locked western segment of this transform plate boundary is capable of producing a Mw 8 earthquake, which is a significant finding regarding seismic hazard and risk.

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Section: San Sebastian and La Victoria Faultsmentioning

confidence: 99%

Section: Active Faults and Geology Of The Ca‐sa Transform Plate Boundarymentioning

confidence: 99%

Strain Partitioning and Interseismic Fault Behavior Along the Caribbean‐South American Transform Plate Boundary

et al. 2021

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“…The 1900 AD event is the second largest earthquake (Ms 7.6) [Pacheco and Sykes 1992] in magnitude in the Venezuelan seismic catalog, after the 1766 event (Mw 7.8), whose felt area is twice as large as the surface of the entire country, but the 1900 AD event is the largest earthquake of all times at crustal depth. All five tsunamigenic earthquakes are considered to be crustal events [e.g., Audemard 2007, Colón et al 2015.…”

Section: Tsunamigenic Earthquakesmentioning

confidence: 99%

“…The 1900 AD tsunami waves were reported along most of the Ensenada de Barcelona coast (Barcelona Embayment, W of Cumaná) and Los Roques Archipelago (Figure 3 and inset), being this quake attributed to the SSF segment running offshore Cabo Codera by Colón et al [2015], based on fresh seafloor scarps detected by high resolution shallow reflection seismics in 2007. After Audemard [1999,2007], the 1530 and 1853 earthquakes were produced by the Cariaco Trough segment of the EPF west of Cumaná, within a restricted over-1000-m-deep marine pull-apart basin on the SSF-EPF right-lateral releasing step-over (Figures 2 and 3), whereas the 1929 and 1997 events occurred on the EPF segment east of Cumaná, inside the <100-mdeep Cariaco Gulf (Figure 2).…”

Section: Tsunamigenic Earthquakesmentioning

confidence: 99%

“…By the way, the best descriptions of damage by this earthquake were undoubtedly his. He even estimated the possible epicentral area of this earthquake [see Colón et al 2015 for more details). Based on his observations on water levels and relative river bed heights narrated above, we have estimated that water level has been raised at El Rincón seaport by about 2 m, eventually 3 m, since water was running on the higher and commonly abandoned channel of the Neverí River.…”

Section: The October 29 Th 1900 Tsunamimentioning

confidence: 99%

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Reliability of first-hand accounts on the study of historical tsunamis in northeastern Venezuela (southeastern Caribbean Sea)

Audemard

Guzman

2017

Annals of Geophysics

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The occurrence of tsunami waves on the eastern Caribbean Venezuelan coasts during 5 Venezuelan (local) earthquakes (01-IX-1530, 15-VII-1853, 29-X-1900, 17-I-1929 and 9-VII-1997, have been confirmed through the search and evaluation of written accounts by primary sources (eye witnesses) of tsunami inundation during these events. Among the outcomes of this new assessment are: 1) the run-up heights of several of those tsunamis have been substantially reduced. In fact, maximum run-up heights for the 5 tsunamis are: 5-7 m at Cumaná for the 1530 event, 5 m at Barlovento and 3 m at the Neverí mouth for the 1900 tsunami, 3 m at western Cumaná for the 1853 and 1929 events and about 1 m for the 1997 earthquake. 2) These new estimates on wave heights for local earthquakes restrict the search for tsunamites by trenching and coring to mainly the first 500-m-wide strip from the coastline in low-lying flatlands. The source of these tsunami waves may be complex. Some are the result of coastal-submarine sliding AD, 1997, tectonic slip on active strike-slip (or normal oblique slip) faults (1530 AD, 1900 or combination of tectonic slip and sliding (1853 AD). Appropriate numerical modeling of tsunami wave generation, migration and inundation are urgently in need to understand these tsunami mechanics.

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Tsunami deposits of the Caribbean – Towards an improved coastal hazard assessment

Engel

Oetjen

May

et al. 2016

Earth-Science Reviews

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The 1900 Mw 7.6 earthquake offshore north–central Venezuela: Is La Tortuga or San Sebastián the source fault?

Cited by 8 publications

References 26 publications

Strain Partitioning and Interseismic Fault Behavior Along the Caribbean‐South American Transform Plate Boundary

Strain Partitioning and Interseismic Fault Behavior Along the Caribbean‐South American Transform Plate Boundary

Reliability of first-hand accounts on the study of historical tsunamis in northeastern Venezuela (southeastern Caribbean Sea)

Tsunami deposits of the Caribbean – Towards an improved coastal hazard assessment

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