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extensional Montserrat-Harvers fault system (MHFS) (Feuillet et al., 2010). The MHFS includes an ESE-trending lineament interpreted as the Belham Valley fault (BVF) (Harford et al., 2002). Figure 6. Montserrat bathymetry and tectonic model. seA cAlIpso mArIne cruIse dAtA The December 2007, SEA-CALIPSO experiment (Seismic Experiment with Airgun-source – Caribbean Andesitic Lava Island Precision Seismo-geodetic Observatory) at Montserrat, Lesser Antilles, was an onshore-offshore seismic study the crust and magmatic system under Montserrat and the Soufriere Hills volcano (SHV) (Paulatto et al., 2010; Shalev et al., 2012; Voight et al., 2010). The experiment included a 48 channel, 600 m streamer, and 2600 in3 airgun seismic reflection survey that explored local submarine deposits and faults and expanded knowledge based on previous seismic and bathymetric studies (Feuillet et al., 2001; Feuillet et al., 2002). GeoloGIcAl And tectonIc settInGs The volcanic island of Montserrat is located in the northeastern Lesser Antilles. The three andesitic volcanic centers of the island that have been active are: Silver Hills (~1- 2Ma), Centre Hills (~0.4-1Ma), and Soufriere Hills-South Soufriere Hills (~0.3Ma to present) as shown in figure 10. Through the process of continuous dome collapsing and building, accumulating piles of pyroclastic and debris flows and deposits the centers are eventually built. These deposits accumulate in large wedges offshore from direct flows and erosion and also as major collapse features; it is estimated that at least 50% of erupted products are transported offshore (Le Friant et al., 2008). Due to its complicated tectonic setting as a result of its upper arc, where oblique subduction causes large scale left lateral shear accommodated by regional extension and arc- 26 perpendicular normal faulting (Feuillet et al., 2001). Feuillet et al., (2001) have shown that on the southern edge of Montserrat of the Havers-Montserrat Fault System (HMFS), part of a series of regional right-stepping en echelon normal fault systems (Kenedi, 2010). Figure 7. Oblique aerial view of Montserrat from the SW. In the figure above the grey land cover is a collection of ash, mud and pyroclastic debris from multiple dome collapse and lahar events since 1995. The dashed black lines are faults (Belham Valley Fault-BVF, Richmond Hill Fault-RHF, St. George’s Hill-SGH, Garibaldi Hill-GH, Richmond Hill-RH). The extensional faulting of southern Montserrat appears to have influenced the location of volcanism, as the volcanic centers of SHV align in a WNW-ESE trend. The faulting has influenced the topography of the region, causing the major uplifts of St. George’s and Garibaldi Hills along the Belham Valey Fault (BVF) (Harford et al., 2002; Kenedi et al., 2010). probAble locAtIon(s) of hydrothermAl systems In montserr At The presence of deep faulting in conjugate sets is supported by both field observation and geophysical evidence such as gravity data indicating a NNW- striking fault through Centre Hills (Hautmann et al., 2008). In the vicinity of St. George’s Hill (SGH), it constitutes transfer zones, where stress is shifted between faults. Both the relay ramp and the region of interacting faults are characterized by increased permeability by the formation of a fracture network (Curewitz and Karson, 1997). In addition, the faulting around SGH is validated also by seismic reflection data of Montserrat as well as earthquake locations, hence a deep enough system to coincide with the hydrothermal system. As seen by Hill (1997) who modeled earthquake swarms as occurring in network mesh, which is consistent with a cloud of seismicity that cannot be resolved into specific faults (Kenedi, 2010). A similar fracture mesh has been documented as enabling fluid circulation in hydrothermal systems (Rowland & Sibson, 2004; Sibson, 1996; Sibson, 2000). GHC BULLETIN, AUGUST 2012PDF Image | Geothermal Prospecting for Nevis and Montserrat
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