Tsunami hazard assessment of Guadeloupe Island (F.W.I.) related to a megathrust rupture on the Lesser Antilles subduction interface

Roger, Jean; Dudon, Bernard; Zahibo, Narcisse

doi:10.5194/nhess-13-1169-2013

Cited by 17 publications

(14 citation statements)

References 51 publications

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“…The fault in this area is the inferred source of a large earthquake in 1946 that may have been accompanied by a few tens of centimeters of tectonic subsidence (Weil-Accardo et al, 2016). It is also the inferred source of a larger earthquake in 1843 (Feuillet et al, 2011;Roger et al, 2013), but accounts of the 1843 earthquake provide few hints of an attending tsunami and no evidence for tsunami damage (Bernard and Lambert, 1988;Shepherd, 1992;Bernard and Lambert, 1992).…”

Section: Hypothetical Hazards From the Puerto Rico Trenchmentioning

confidence: 99%

Extreme waves in the British Virgin Islands during the last centuries before 1500 CE

et al. 2017

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Extraordinary marine inundation scattered clasts southward on the island of Anegada, 120 km south of the Puerto Rico Trench, sometime between 1200 and 1480 calibrated years (cal yr) CE. Many of these clasts were likely derived from a fringing reef and from the sandy flat that separates the reef from the island's north shore. The scattered clasts include no fewer than 200 coral boulders, mapped herein for the first time and mainly found hundreds of meters inland. Many of these are complete colonies of the brain coral Diploria strigosa. Other coral species represented include Orbicella (formerly Montastraea) annu laris, Porites astreoides, and Acropora palmata. Associated bioclastic carbonate sand locally contains articulated cobble-size valves of the lucine Codakia orbicularis and entire conch shells of Strombus gigas, mollusks that still inhabit the sandy shallows between the island's north shore and a fringing reef beyond. Imbricated limestone slabs are clustered near some of the coral boulders. In addition, fields of scattered limestone boulders and cobbles near sea level extend mainly southward from limestone sources as much as 1 km inland. Radiocarbon ages have been obtained from 27 coral clasts, 8 lucine valves, and 3 conch shells. All these additional ages predate 1500 cal yr CE, all but 2 are in the range 1000-1500 cal yr CE, and 16 of 22 brain coral ages cluster in the range 1200-1480 cal yr CE. The event marked by these coral and mollusk clasts likely occurred in the last centuries before Columbus (before 1492 CE). The pre-Columbian deposits surpass Anegada's previously reported evidence for extreme waves in post-Columbian time. The coarsest of the modern storm deposits consist of coral rubble that lines the north shore and sandy fans on the south shore; neither of these storm deposits extends more than 50 m inland. More extensive overwash, perhaps by the 1755 Lisbon tsunami, is marked primarily by a sheet of sand and shells found mainly below sea level beneath the floors of modern salt ponds. This sheet extends more than 1 km southward from the north shore and dates to the interval 1650-1800 cal yr CE. Unlike the pre-Columbian deposits, it lacks coarse clasts from the reef or reef flat; its shell assemblage is instead dominated by cerithid gastropods that were merely stirred up from a marine pond in the island's interior. In their inland extent and clustered pre-Columbian ages, the coral clasts and associated deposits suggest extreme waves unrivaled in recent millennia at Anegada. Bioclastic sand coats limestone 4 m above sea level in areas 0.7 and 1.3 km from the north shore. A coral boulder of nearly 1 m 3 is 3 km from the north shore by way of an unvegetated path near sea level. As currently understood, the extreme flooding evidenced by these and other clasts represents either an extraordinary storm or a tsunami of nearby origin. The storm would need to have produced tsunami-like bores similar to those of 2013 Typhoon Haiyan in the Philippines. Normal faults and a thrust fault provide nearby tsunami ...

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Section: Hypothetical Hazards From the Puerto Rico Trenchmentioning

confidence: 99%

Extreme waves in the British Virgin Islands during the last centuries before 1500 CE

et al. 2017

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“…The absolute horizontal accuracy of SRTM data is 20 m (circular error at 90 % confidence) and the absolute as well as relative vertical accuracy is less than 16 m (linear error at 90 % confidence) and 10 m, respectively (USGS, 2006;Kellndorfer et al, 2004). Previous studies on SRTM (Zielinski and Chimel, 2007;Karwel and Ewiak, 2008;Hanson et al, 2011;Roger et al, 2013;Løvholt et al, 2012;Taubenböck et al, 2008) report that these data sets perform better than their standard specification and hence can be used for a variety of applications, such as coastal vulnerability or inundation mapping. In our analysis, the aim of using DEM is to evaluate and separate the lowest area from other higher areas along the coasts for which the SRTM data proves sufficient with its specifications.…”

Section: Regional Elevationmentioning

confidence: 93%

Coastal vulnerability assessment of Puducherry coast, India, using the analytical hierarchical process

Murali

Ankita

Amrita

et al. 2013

Nat. Hazards Earth Syst. Sci.

180

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Abstract. As a consequence of change in global climate, an increased frequency of natural hazards such as storm surges, tsunamis and cyclones, is predicted to have dramatic affects on the coastal communities and ecosystems by virtue of the devastation they cause during and after their occurrence. The tsunami of December 2004 and the Thane cyclone of 2011 caused extensive human and economic losses along the coastline of Puducherry and Tamil Nadu. The devastation caused by these events highlighted the need for vulnerability assessment to ensure better understanding of the elements causing different hazards and to consequently minimize the after-effects of the future events. This paper demonstrates an analytical hierarchical process (AHP)-based approach to coastal vulnerability studies as an improvement to the existing methodologies for vulnerability assessment. The paper also encourages the inclusion of socio-economic parameters along with the physical parameters to calculate the coastal vulnerability index using AHP-derived weights. Seven physical-geological parameters (slope, geomorphology, elevation, shoreline change, sea level rise, significant wave height and tidal range) and four socio-economic factors (population, land use/land cover (LU/LC), roads and location of tourist areas) are considered to measure the physical vulnerability index (PVI) as well as the socio-economic vulnerability index (SVI) of the Puducherry coast. Based on the weights and scores derived using AHP, vulnerability maps are prepared to demarcate areas with very low, medium and high vulnerability. A combination of PVI and SVI values are further utilized to compute the coastal vulnerability index (CVI). Finally, the various coastal segments are grouped into the 3 vulnerability classes to obtain the coastal vulnerability map. The entire coastal extent between Muthiapet and Kirumampakkam as well as the northern part of Kalapet is designated as the high vulnerability zone, which constitutes 50 % of the coastline. The region between the southern coastal extent of Kalapet and Lawspet is the medium vulnerability zone and the remaining 25 % is the low vulnerability zone. The results obtained enable the identification and prioritization of the more vulnerable areas of the region in order to further assist the government and the residing coastal communities in better coastal management and conservation.

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“…On the other hand passive zones like the Northeastern American margin experienced intraplate earthquakes and margin destabilizations leading to landslides triggering tsunamis (Driscoll et al, 2000;Twichell et al, 2009;Tappin, 2010). As an example, the 1929 Grand Banks M w ∼ 7.2 earthquake was followed by a transoceanic tsunami recorded further at Portuguese coastal tide gages (Fine et al, 2005;Ruffman and Hann, 2006), related afterward to a submarine landslide triggered by the seismic shaking. In the passive zones are also included oceanic hot spots highlighted…”

Section: Generalitiesmentioning

confidence: 99%

“…But, as the seismic knowledge of the Caribbean region is relatively new in comparison to other active zones of the world like the Japanese trench or the Mediterranean Sea for example, the lack of big earthquakes reported during the last 500 years is probably the main reason leading to hasty conclusions about the non-capacity of the Antilles subduction zone to produce megathrust earthquakes of M w = 7.0 and more (see Murty et al, 2005, for example). In fact the last earthquakes (that have been recently named megathrust events by Feuillet et al, 2011a) exhibited go back to 11 January 1839 (M w ∼ 7.3) and 8 February 1843 (M w ∼ 8.0/8.5) and these events are not historically known to have been followed by destructive tsunamis (Feuillet et al, 2011a;Roger et al, 2013). Notice that this subduction zone is also the theater of nonthrust events like the 1974 M S = 7.6 (McCann et al, 1982) or more recently the 18 February 2014 M w ∼ 6.5 normalfault earthquakes.…”

Section: The Antilles Subduction Zonementioning

confidence: 99%

“…This magnitude value, set within the range of the estimated maximum of 8.0 < M Wmax < 8.5, and the corresponding fault plane parameters have been chosen following the recent studies of Feuillet et al (2011a), Roger et al (2013), and Hayes et al (2013) about the 8 February 1843 Lesser Antilles earthquake, and in agreement with used dataset and empirical relations obtained by Strasser et al (2010), Blaser et al (2010), and Murotani et al (2013). For information, a M w ∼ 8.4 earthquake corresponds approximately to a moment magnitude (M 0 ) of 6 × 10 21 N m according to the relation M w = 2 3 Log (M 0 ) − 6.0 (Hanks and Kanamori, 1979) leading to a maximum rupture area of ∼ 4 × 10 4 km 2 and a maximum rupture slip of 5 m conforming to these relations.…”

Section: Tsunami Generation Scenariosmentioning

confidence: 99%

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Impact of a tsunami generated at the Lesser Antilles subduction zone on the Northern Atlantic Ocean coastlines

Roger

Frère²,

Hébert

2014

Adv. Geosci.

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Abstract. On 11 March 2011, a M w ∼ 9.0 megathrust earthquake occurred off the coast of Tohoku, triggering a catastrophic tsunami reaching heights of 10 m and more in some places and resulting in lots of casualties and destructions. It is one of a handful of catastrophic tsunamis having occurred during the last decade, following the 2004 Indonesian tsunami, and leading to the preparation of tsunami warning systems and evacuation plans all around the world. In the Atlantic Ocean, which has been struck by two certified transoceanic tsunamis over the past centuries (the 1755 "Lisbon" and 1929 Grand Banks events), a warning system is also under discussion, especially for what concerns potential tsunamigenic sources off Iberian Peninsula. In addition, the Lesser Antilles subduction zone is also potentially able to generate powerful megathrust ruptures as the 8 February 1843 M w ∼ 8.0/8.5 earthquake, that could trigger devastating tsunamis propagating across the Northern Atlantic Ocean. The question is in which conditions these tsunamis could be able to reach the Oceanic Islands as well as the eastern shores of the Atlantic Ocean, and what could be the estimated times to react and wave heights to expect? This paper attempts to answer those questions through the use of numerical modelings and recent research results about the Lesser Antilles ability to produce megathrust earthquakes.

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Tsunami hazard assessment of Guadeloupe Island (F.W.I.) related to a megathrust rupture on the Lesser Antilles subduction interface

Cited by 17 publications

References 51 publications

Extreme waves in the British Virgin Islands during the last centuries before 1500 CE

Extreme waves in the British Virgin Islands during the last centuries before 1500 CE

Coastal vulnerability assessment of Puducherry coast, India, using the analytical hierarchical process

Impact of a tsunami generated at the Lesser Antilles subduction zone on the Northern Atlantic Ocean coastlines

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