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Flank Collapse and Large-Scale Landsliding in the Cape Verde Islands, Off West Africa

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Flank Collapse and Large-Scale Landsliding in the Cape Verde Islands, Off West Africa Article Geochemistry 3 Volume 9, Number 7 Geophysics 19 July 2008 Q07015, doi:10.1029/2008GC001983 GeosystemsG G ISSN: 1525-2027 AN ELECTRONIC JOURNAL OF THE EARTH SCIENCES Published by AGU and the Geochemical Society Click Here for Full Article Flank collapse and large-scale landsliding in the Cape Verde Islands, off West Africa D. G. Masson and T. P. Le Bas National Oceanography Centre, University of Southampton, European Way, Southampton SO14 3ZH, UK ([email protected]) I. Grevemeyer and W. Weinrebe IFM-GEOMAR, Wischhofstrasse 1-3, D-24148 Kiel, Germany [1] Large-scale landslides occur on the flanks of many volcanic oceanic islands worldwide. None have taken place in historical time, but their geohazard potential, especially their ability to generate tsunamis, is large. The Cape Verde Islands are a group of 10 large and several smaller volcanic islands off the coast of West Africa between 15 and 17°N. A single flank landslide has previously been described from the island of Fogo, but systematic analysis of the Cape Verde group has until now been lacking. This paper describes and interprets a multibeam bathymetry data set covering the slopes of the western Cape Verde Islands, including those of the islands with the most recent volcanic activity, Fogo in the southwest, and Santo Antao in the northwest. All of the larger islands show evidence of large flank landslides, although only Fogo and the southwest part of Santo Antao have failed in the last 400 ka. Tope de Coroa, the volcano at the southwest end of Santo Antao, has been inactive for the past 170 ka and is judged to have a low landslide potential unless volcanic activity resumes. In contrast, there would seem to be a high probability of a future east directed landslide on Fogo, from the area of the highly active Pico do Fogo volcano, although it is impossible to predict a timescale for such an event. A tsunami generated by such a landslide could have a catastrophic effect on the adjacent island of Santiago and possibly even farther afield on the West African coast. Components: 6206 words, 11 figures, 1 table. Keywords: Cape Verde; landslide; swath bathymetry. Index Terms: 3045 Marine Geology and Geophysics: Seafloor morphology, geology, and geophysics; 3070 Marine Geology and Geophysics: Submarine landslides; 8488 Volcanology: Volcanic hazards and risks. Received 11 February 2008; Revised 6 June 2008; Accepted 11 June 2008; Published 19 July 2008. Masson, D. G., T. P. Le Bas, I. Grevemeyer, and W. Weinrebe (2008), Flank collapse and large-scale landsliding in the Cape Verde Islands, off West Africa, Geochem. Geophys. Geosyst., 9, Q07015, doi:10.1029/2008GC001983. 1. Introduction Masson et al., 2002; Watts and Masson, 1995], Hawaii [Moore et al., 1989, 1994], Reunion [2] Evidence for flank collapse and large-scale [Labazuy, 1996; Ollier et al., 1998], Cape Verde landsliding (hereafter referred to as landslide or Islands [Day et al., 1999]). Large landslides incor- 3 landsliding) is preserved on many volcanic ocean porating tens of km of rock are, however, rare islands worldwide (Canary Islands [Masson, 1996; events even on geological timescales, and no Copyright 2008 by the American Geophysical Union 1 of 16 Geochemistry 3 masson et al.: large-scale landsliding, cape verde islands Geophysics 10.1029/2008GC001983 Geosystems G Figure 1. Map showing the regional setting of the Cape Verde Islands. Magenta shaded area shows area of multibeam bathymetry coverage. Inset shows location off West Africa at 15° to 17°N. events larger than about 5 km3 are known to have the near stationary nature of the African plate is occurred in historical time [Ward and Day, 2003]. with respect to the underlying mantle [Holm et al., The geohazard potential of a large volcanic island 2006]. Many of the islands show overlapping landslide is thus poorly constrained by observation, periods of active volcanism, although Sal and Maio although all authors agree that, in addition to local in the east have the oldest dated volcanic rocks (12 destruction on the island, such an event is likely to and 16 Ma, respectively) and only Fogo and Santo have considerable tsunamigenic potential [Mader, Antao, at the western ends of the northern and 2001; Masson et al., 2006; McMurtry et al., 2004; southern arms of the ‘‘horseshoe,’’ respectively, have Ward and Day, 2001]. It is thus important that all experienced significant volcanism in the last 500 ka oceanic islands likely to be affected by landslides [Holm et al., 2006; Plesner et al., 2002]. Fogo is are subjected to geohazard assessment. Here we entirely covered in young volcanic rocks and ‘‘may evaluate the geomorphology of the submarine be entirely Quaternary in age’’ [Holm et al., 2006]. slopes of the Cape Verde Islands and assess which areas have been affected by landslides in the [4] Prior to the work carried out in this study, geological past. A brief assessment of future geo- landslides had only been reported from Fogo hazard potential is also included. [Day et al., 1999; Le Bas et al., 2007]. Here, a single landslide is seen on the eastern flank of the island (Figure 2a). It is partially filled by volcanic 2. Location and Geological Setting products from the Pico do Fogo volcano, a highly active volcanic center that has erupted, on average, [3] The Cape Verde Islands are a horseshoe-shaped every 20 years since the islands were discovered by group of volcanic islands located 550–800 km off European explorers some 500 years ago [Fonseca the West African coast between 15° and 17°N et al., 2003; Torres et al., 1998]. (Figure 1). They are the culmination of the Cape Verde Rise, an area of elevated seafloor over 1000 km across, interpreted as the topographic 3. New Data expression of an underlying mantle plume [Holm et al., 2006; McNutt, 1988]. The islands show only [5] The data described in this paper consist of a weak age progression from east to west, reflecting multibeam bathymetry and acoustic backscatter 2of16 Geochemistry 3 masson et al.: large-scale landsliding, cape verde islands Geophysics 10.1029/2008GC001983 Geosystems G Figure 2. Photographs of (a) Pico do Fogo from the east with the Monte Amarelo landslide scar in the background. The semicircular landslide scarp on Fogo is about 9 km in diameter and up to 1 km high. (b) the Monte Amarelo landslide scar viewed from inside the landslide scar (partially filled with young volcanic rocks). (c) Santo Antao from the southwest. The inner landslide scarp (its top denoted by dashed line) surrounding the Tope de Coroa volcano on Santo Antao is about 6 km across. images. Multibeam bathymetry and backscatter east to Santo Antao in the west (Figure 3). For the data were collected using an Atlas Hydrosweep southern island chain, the western flank of system on R/V Meteor cruise 62/3 and a Simrad Santiago and the area around Fogo and Brava were EM 12 system on RRS Charles Darwin cruise 168. surveyed. No data were collected around the east- Multibeam coverage extends along both flanks of ern islands of Sal, Boavista and Maio. Marine data the northern island chain from Sao Nicolau in the were combined with NASA Shuttle Radar Topog- 3of16 Geochemistry 3 masson et al.: large-scale landsliding, cape verde islands Geophysics 10.1029/2008GC001983 Geosystems G Figure 3. Summary of multibeam data from the western Cape Verde Islands. Contour interval 200 m. Boxes show locations of later plan view figures. Arrows show view direction of 3-D figures. NS, Nola Seamount; SA, Santo Antao; SV, Sao Vicente; SL, Santa Luzia; SN, Sao Nicolau; ST, Santiago; F, Fogo; and B, Brava. raphy Mission (SRTM) data from the islands, allow- (Figures 2a, 2b, and 4). This volcano is located to ing correlation of onshore and offshore structures. the east of a semicircular escarpment, the Bordiera escarpment, open to the east and rising, in places, 4. Bathymetry and Backscatter up to 1000 m above the floor of the ‘‘caldera’’ it encloses. The escarpment has been interpreted as Interpretation the scar of an ancient landslide, the Monte Amarelo landslide [Day et al., 1999]. A minimum age of 4.1. Fogo, Brava, and the Western Flank of 80 ka has been suggested for the landslide, but this Santiago age estimate is poorly constrained [Fonseca et al., [6] The island of Fogo is dominated by the Pico do 2003]. Since that time, volcanic activity has been Fogo volcano, rising over 2800 m above sea level almost entirely contained within the landslide scar, 4of16 Geochemistry 3 masson et al.: large-scale landsliding, cape verde islands Geophysics 10.1029/2008GC001983 Geosystems G Figure 4. (a) Oblique 3-D image of Fogo and Brava, viewed from the southeast, based on swath bathymetry offshore and SRTM data onshore. The relationship between the interpreted landslide scar on the island and the landslide debris offshore is clearly seen. (b) Plan (map) view of Fogo and the surrounding seafloor showing the relative extent of the landslide scar and debris field and the position of the Pico do Fogo volcano within the landslide scar. Contours are at 200 m intervals with thousand meter contours in bold (orange, 1000 m; green, 2000 m; blue, 3000 m). The volcanic cones on the right of the image are on the lower slope of Santiago island. For location, see Figure 3. giving rise to the present-day Pico do Fogo volca- [7] The small island of Brava has not been volca- no. Prior to 1785, frequent eruptions from the nically active in historical time, although it exhibits summit of the volcano were recorded; since that higher levels of seismicity than Fogo [Fonseca et time, eruptions have occurred from fissures near its al., 2003].
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