751.00 sq km
Eastern Caribbean (UTC-4)
74,584 (2021 est.)
Full Country Name
Commonwealth of Dominica
Dominica is the largest and most northerly of the Windward Islands. The lowest point in the country is at sea level along the coast and the highest is Morne Diablotins (1,447 m). The island has a tropical rainforest climate with characteristically warm temperatures and heavy rainfall with the humidity tempered by the northeast trade winds. Dominica is especially vulnerable to hurricanes as the island is located in the hurricane belt.
The island is sparsely populated with ~74,584 people inhabiting its 751 square kilometres. A significant portion of the population lives in and around the capital city of Roseau. Approximately 2,200 Kalinago people inhabit this enclave now known as the Kalinago/Carib Territory. English is the official language but a large portion of the population speaks Creole and a few northern villages speak Kokoy.
In the event of a volcanic eruption, earthquake or tsunami the Office of Disaster Management is the official authority in Dominica.
Office of Disaster Management
c/o Ministry of National Security, Immigration and Labour
Dominica has nine potentially active volcanic centres making the island primarily composed of volcanic rocks and their weathering products. The only exception is a minor discontinuous formation of uplifted Pleistocene to Holocene conglomerates and corals along the west coast. Based on 43 K-Ar and 50 radiocarbon dates, the volcanic stratigraphy of the island can be subdivided into four units: 1) Miocene, 2) Pliocene, 3) ‘Older Pleistocene’ and 4) ‘Younger Pleistocene’ – Recent. The four units are separated by three unconformities which are not all island-wide, as volcanism continued at some centres while weathering and erosion took place at others which had become extinct. The west coast of Dominica, along the entire outcrop length of the Pliocene volcanoes, is remarkably linear. Along much of this coastline are Pleistocene outcrops of water-worked block and ash flow deposits now present as pebble and conglomerate beds which locally contain raised coral reef limestone (Martin-Kaye 1960; Sigurdsson and Carey 1991). This strongly suggests that this linear coastline marks a normal fault where the island is being uplifted.
The oldest rocks lie along the east or Atlantic coast. They are deeply dissected and weathered low-K basaltic terranes yielding radiometric ages between 6.92 and 5.22 Ma (Monjaret 1985, Bellon 1988). These older rocks are cut by numerous younger andesitic dikes yielding Pliocene ages (3.35 to 2.76 Ma) (Bellon 1988).
From about 3.7 Ma, volcanism appears to have been almost continuous, forming a number of now largely extinct centres that are so deeply dissected that only outlines of their characteristic morphology can be seen. The most widespread deposits of these Pliocene volcanoes appear to comprise remnants of large basaltic to andesitic stratovolcanoes.
Pleistocene to recent activity has been dominated by Pelean-style dome-forming eruptions. In the early Pleistocene (1.7 – 2 Ma), volcanism was constrained to the northern half of Dominica and led to the development of Morne Diablotins, a large stratovolcano, and Morne aux Diables, a smaller Pelean dome complex (Smith et al. 2013). About 1 Ma ago a major change occurred in the focus of volcanism, with activity switching from the northern to the southern half of the island. In the north, volcanism continued in a reduced manner at Diablotins and Aux Diables. During the late Pleistocene (0 – 1.1 Ma) at least six more volcanic centres developed: Morne Anglais, Morne Trois Piton, Micotrin, Morne Watt, Grand Soufrière Hills, and the Plat Pays Volcanic Complex.
In addition to dome-forming eruptions, ignimbrite deposits also crop out across the island representing what would have been explosive pyroclastic density current activity. The Roseau Sequence located in the south-central part of the island consists of a series of six to seven ignimbrite forming eruptions that occurred between ca. 20 and 70 ka (Howe et al. 2014). Deposits from these eruptions outcrop throughout the Roseau Valley and along the southern coast of Dominica outside the Soufrière Depression. The Layou Ignimbrite outcrops within the confines of the Layou valley and is thought to be sourced from Trois Piton (Smith et al., 2013). The northern ignimbrites, found at Grand Savanne and Londonderry are thought to be sourced from Diablotins (Sparks, Sigurdsson, and Carey 1980, Smith et al. 2013).
The seismicity plots of earthquakes in the Dominica area reveal a high level of background activity, with more than 12,000 events displayed in the plot of all events from 1955. East of Dominica shallow and intermediate depth events occur. The biggest events in this area for the instrumental period have been close to magnitude 7, with the most recent on 1969/12/25. Dominica also suffered serious damage from the 1843/02/08 magnitude 8.0 earthquake which was located north-east of Guadeloupe. Shaking in Roseau and in the southern part of the island was at MMI VIII where the walls of most masonry buildings were cracked, some severely. Several old walls and chimneys were thrown down. In the northern part of the island at Londonderry and Melville Hall the sugar works and other stone buildings were destroyed. At Melville Hall the river bed sank by a few inches and the river was diverted twenty feet to the south. Damage to sugar works in the north was estimated at £4,500. One person was killed. Here, the MMI was at MMI IX.
The 2007/11/29 major north of Martinique event was also strongly felt in Dominica. It was described as a rather lengthy strong tremor; reports, from a team of our staff that was in the field at the time, indicate that the strongest shaking effects produced small rock slides off hillsides; trees and flowers; at one guesthouse, guests were visibly shaken and all guests ran outside. Pots, pans and crockery in cupboards were also heard to be shaking.
Dominica has also experienced strong shaking from the significant magnitude events that have occurred along the arc. Seismic activity north of Dominica maintained a relatively low level for most of the instrumental era, which for the database of the Seismic Research Centre (SRC) begins in 1955. The first earthquake located in the area was on 1957/04/18 and was of magnitude 3.6. From that time until 2004/11/20, there were about 130 events located in the area. Then on 2004/11/21, an earthquake of duration magnitude 6.0 occurred in the area north of Dominica at shallow depth. There was significant damage in northern Dominica, associated with MMI VII. The dense elongated cluster of earthquakes north of Dominica seen in the epicentral plot is as a result of the more than 8,000 aftershocks associated with that event in the years following, with the largest, at duration magnitude 5.8, occurring on 2005/02/14. By 2011, activity in the area had subsided to a new normal background level, with an annual count of about 20 events.
In 2012, the number of events located in the area returned to and exceeded the 2007 level and continued for a few years and now manifests periods of lower level interspersed by bursts of elevated numbers. This pattern of activity is somewhat unusual and it continues to be closely watched.
In addition to the earthquakes that arise from tectonic processes, there may also be volcanic earthquakes associated with the nine known volcanic centres in Dominica. Along with the background level of seismicity that is generally associated with volcanoes that is not indicative of volcanic unrest, there have been significant episodes of volcanic unrest, with elevated levels of seismicity that are part of the normal pattern associated with these centres. The clusters of events seen in northern and southern Dominica arise from this both background and periods of elevated activity. It is anticipated that elevated, shallow volcanic seismicity would be associated with the volcanic centres, precursory to any future volcanic activity.
Dominica can attribute its rugged beauty to having one of the highest concentrations of potentially active volcanoes in the world. It is the only island in the Eastern Caribbean with more than one ‘live’ (likely to erupt again) volcano. In fact, it has NINE ‘live’ volcanoes; seven of which are located in southern Dominica within 10 km of the capital, Roseau.
Past Volcanic Activity
Dominica’s volcanoes have erupted many times and in different ways in the past. Some of the eruptions from the larger volcanoes and calderas have been very explosive, generating large pyroclastic flows and ash, and then forming the large volcanic domes of Morne Diablotins, Morne Trois Pitons and Morne Plat Pays. The white cliffs in the Roseau valley and at Grand Bay beach were produced by such explosive eruptions. Smaller and younger lava domes such as Morne Micotrin, Canot, Crabier and Morne Patates produced smaller eruptions in the past, similar to the Soufrière Hills Volcano in Montserrat. The last eruption of this type occurred about 500 years ago from Morne Patates. More recently, small phreatic/steam eruptions have occurred in the Valley of Desolation.
|Volcano||Last Known Eruption|
|Foundland||>50,000 years ago|
|Morne Diablotins||<40,000 years ago|
|Morne aux Diables||<40,000 years ago|
|Grande Soufriere Hills||~11,000 years ago|
|Morne Anglais||<10,000 Years ago|
|Morne Trois Pitons/Microtrin||~1,100 years ago|
|Morne Plat Pays/ Patates||~500 years ago|
|Valley of Desolation/Morne Watt||Phreatic/Steam eruptions 1880, 1997|
Future Volcanic Activity
Predictions of future activity in Dominica can be made based on:
- analysis of past volcanic activity at the volcanoes
- the pattern of shallow earthquakes
- A comparison of behaviour at other similar volcanoes that are better understood (e.g. Montserrat).
Geological studies of past volcanic activity tell us that the centres in the south of Dominica are the youngest, and that lava dome eruptions have been very common. Dominica’s next eruption is therefore likely to be a lava dome-forming eruption in southern Dominica where there have been at least 9 intense volcanic earthquake swarms (series of earthquakes) during the last 100 years. A major earthquake swarm occurred between 1998 and early 2000, and was associated with the Morne Plat Pays and Morne Anglais volcanic centres. From 2009-2010, there were intense earthquake swarms associated with the Morne aux Diables volcano in the north. The location of the1998-2000 earthquake swarm epicenters indicates that the next magmatic eruption is likely to occur in La Falaise/ Canot area of the Plat Pays Volcanic Centre
When will the next eruption occur?
Past eruptions large enough to leave a geological record have occurred in this area on average every ~500-1000 years, and it has been about 500 years since the last one (Patates). Furthermore, intense earthquake swarms in Southern Dominica indicate that magma may be moving towards the surface. Scientists believe there is a greater than 50% chance that an eruption will occur in this area within the next 100 years.
The Boiling Lake
The Boiling Lake is a volcano-hydrothermal feature located in an area next to the Valley of Desolation in southern Dominica. The lake is roughly 60m in diameter and approximately 15m deep. The Boiling Lake is the second largest feature of its kind in the world with the largest being Frying Pan Lake in New Zealand.
In its normal state of activity the lake is boiling but occasionally there have been fluctuations in water levels and temperatures. Since 1876 there have been at least eight (8) recorded instances of changes in the water levels of the Boiling Lake. The more recent changes in lake water levels was noticed between November 2016 and January 2017 and November 2021 to May 2022. During this period water levels rose and fell several times.
The Valley of Desolation and the Boiling Lake itself are considered sites of interest for locals and visitors to Dominica. They have been part of the Morne Trois Pitons National Park, a UNESCO World Heritage Site since 1987.
There are nine potentially active centres in Dominica, each of which are discussed below.
Valley of Desolation
- 15.31°N, 61.3°W
- Elevation – 826m
- Last eruption – 1997 (phreatic)
Past eruptive activity
Demange et al. (1985) provide three dates related to prehistoric phreatic activity of the Valley of Desolation. One of these dates (4,050 years B.P.) is of a lahar deposit exposed in the River Blanc near Casso, thought to have originated from the Valley of Desolation. The other two (3,750 and 2,900 years B.P.) are from lithic ash deposits within two small explosion craters in the Valley itself. These dates suggest that explosive activity has occurred from vents within the Valley of Desolation for at least 4,000 years. Historical eruptions The Valley of Desolation has been the source of two historic phreatic eruptions, on January 4th, 1880 and on July 9th, 1997. Neither explosion was directly witnessed. Future eruptions The most likely type of volcanic activity to occur from the Valley of Desolation is a phreatic eruption from the Boiling Lake or one of the other explosion craters in the area. Phreatic eruptions are steam-driven eruptions that eject fragments of old rock and ash into the air and are very common in geothermal areas. They are not true volcanic eruptions in that they do not erupt fresh magma, although they can emit dangerous gases. Individual phreatic explosions may last up to an hour or more, and a series of blasts may continue intermittently for several months or even years. They may be accompanied by volcanic earthquakes. In some instances, particularly if they occur in a sequence, phreatic eruptions may represent precursory activity to an actual magmatic eruption. In the event of a phreatic eruption from the Valley of Desolation the direct effects will probably only be felt over a small area of up to a few 100s of metres from the vent, although ballistic projectiles may be throw up to 1-2 km and ashfall may affect areas a considerable distance downwind of the vent. The ash cloud generated during the 1880 phreatic eruption from the Valley of Desolation was carried westward by the wind, and ash fell over an elongated area downwind of the source about 3 km wide. The sky darkened over Roseau, and up to 6 mm of ash and accretionary lapilli fell over the town. In general, however, such an eruption will only be dangerous to humans if they are near the vent at the time; and major effects are likely to be constrained within a two km radius of the vent. However, the water, ash and steam ejected during a phreatic eruption are likely to be acidic, and would contaminate nearby streams. Phreatic eruptions may also eject enough water to generate small floods or lahars in nearby streams, and lahars were generated in the Roseau and Pointe Mulatre rivers in this way during the 1880 phreatic eruption. Despite these possible effects, the area affected by a phreatic eruption will be very small compared with that affected by a magmatic eruption.
Plat Pays Volcanic Complex
- 15.27°N, 61.35°W
- Elevation – 960m
- Last eruption – ~500 years ago
Morne Plat Pays is a stratovolcano with a central complex of eroded summit domes that rises to an elevation of 960 m. The volcano is truncated on its southwestern side exposing a ~ 900 m high collapse scarp beneath Morne Plat Pays which forms the northeastern margin of the adjacent Soufrière depression. At least 16 small lava domes occur in this complex, some within and some outside the depression.
Past eruptive activity
No dates are available for the early activity directly associated with the Plat Pays stratovolcano. Exposures near the summit are dominantly of thick andesitic lava, indicating effusive activity. Minor exposures of block and ash flow and other volcaniclastic deposits are present in heavily vegetated areas below the summit area, indicating periods of dome growth and collapse. A poorly-exposed, surficial pyroclastic deposit containing semi-vesicular andesitic clasts crops out on the eastern edge of the Soufrière depression and to the north and east of Morne Plat Pays. This deposit, which probably formed by Asama-style activity, has been dated at 6.6 to 6.8 ka and may represent the most recent activity from this volcano (Lindsay et al. 2003).
There have been no reports of volcanic eruptions from the Plat Pays volcanic complex in historic time. However, radiocarbon ages of pyroclastic flow deposits from Morne Patates indicate that this dome may have been active as recently as 450 years ago, which roughly coincides with the period of earliest European arrival in the area. In 1994 spontaneous combustion and subsequent melting of native sulphur in the lower Sulphur Springs area led to a “sulphur fire” over an area of approximately 1 km2. This slow-flowing, molten sulphur resulted in false rumours of an eruption of lava.
1. Effusive dome-forming eruption from Morne Canot or Morne Patates The last 25,000 years of volcanic activity at the Plat Pays volcanic complex have been dominated by effusive dome-forming activity, and this is considered the most likely style of activity for the next magmatic eruption from this volcano. Based on the location and pattern of seismicity in recent decades, in particular the 1998-2000 swarm, a future dome-forming eruption is more likely than not to occur within the next 100 years, and is likely to occur in the vicinity of Morne Canot. Such an eruption could, however, occur from anywhere within the complex, and until precursory signs (such as an escalation of the earthquake swarm and/or onset of phreatic activity) appear which will provide a more accurate estimate of vent location, it is difficult to say with certainty where activity will occur. Morne Patates is, in fact, the site of the most recent magmatic eruptions in Dominica. The scenario of a dome-forming eruption from Morne Canot is considered the most likely for a future magmatic eruption in Dominica.
2. Explosive eruption from Morne Plat Pays The 6.8 ka old andesitic pyroclastic flow deposit (Asama style activity) exposed on the flanks of Morne Plat Pays indicates that explosive magmatic eruptions have occurred from this center in the recent past, and may occur here again in the future. A similar eruption in the future may produce a low eruption column, collapsing a few hundreds of meters above the vent. Collapse of such a low column may generate pyroclastic flows and surges radially around the volcano, but would not produce significant ash fall. Ballistic projectiles would be a hazard within ~5 km of the vent, and lahars and volcanic earthquakes could also occur. Such an eruption would affect an area radially around Morne Plat Pays and could potentially impact a greater area than a dome-forming eruption.
- 15.28°N, 61.33°W
- Elevation – 1123m
- Last eruption – < less than 10,000 years ago
Morne Anglais is a prominent peak located just to the east of Roseau. It is a stratovolcano with a prominent summit dome. Morne John, a single Pelean dome with its own apron of block and ash flows, lies on its northeastern flank.
Past eruptive activity
Demange et al. (1985) describe three stages of past activity at Morne Anglais. Stage 1 involved a period of dome growth and collapse, resulting in a series of block and ash flow deposits. A period of St. Vincent style activity occurred during Stage 2, producing a sequence of basaltic-andesite scoria and ash flow, scoriaceous surge and scoriaceous fall deposits, some of which contain evidence of magma co-mingling. These deposits are exposed intermittently along the west coast and in roadcuts to the west and southwest of the volcano. A sequence of scoriaceous deposits exposed within the Soufrière depression and dated at 28,450 (Wadge 1985) and 26,400 (Demange et al. 1985) years B.P. may possibly be correlated with these deposits. The most recent major phase of activity, stage 3, was again characterised by dome growth and collapse, and resulted in the present morphology of a central Pelean dome complex surrounded by aprons of block and ash flow deposits. A block from one of the Anglais block and ash flow deposits gave a K-Ar age of 0.43 Ma, which, based on morphological criteria and the possible presence of excess argon, is thought to be too old (Demange et al. 1985). The western and southern flanks of Morne Anglais contain outcrops of an undated andesitic pumice and ash-rich pyroclastic flow deposit <2 m thick that represent a period of explosive activity and are thought to be the youngest deposits from Anglais (Lindsay et al. 2003). Very little is known about the age and nature of Morne John.
There have been no reports of historical eruptions from Morne Anglais or Morne John. Future eruptions The proximity of Morne Anglais to the recent volcanic earthquake swarm, and in particular the cluster of earthquakes directly beneath its summit, indicate that eruptions are likely to occur from here in the future. The most recent activity at Morne Anglais has been explosive in nature (Lindsay et al. 2003) and St. Vincent style explosive activity occurred extensively during Stage 2. The most likely future activity at this centre is therefore considered to be an explosive andesitic or basaltic magmatic eruption, possibly preceded by a period of phreatic activity. The vent would probably be located at or near the summit, as in past eruptions. Such an eruption would generate a buoyant eruption cloud of ash and larger rock fragments, which may subsequently collapse to generate pumiceous pyroclastic flows and surges in all directions around the vent, particularly down all major nearby valleys including the Roseau and Geneva rivers and their tributories (brown area on the hazard map). Less frequent but more energetic pyroclastic flows and surges would be less restricted by topography and would have the potential to cover greater areas and may even reach as far south as Soufrière and as far north as Massacre to the west and Boetica to the east (yellow area on the hazard map). In the absence of ash fall data specific to Morne Anglais, the pattern of ash fall thickness and distribution exhibited during the 1902 eruption of the Soufrière in St. Vincent (Robertson 1992) has been used to define a possible ash fall pattern. Ballistic projectiles would be common, and would mainly affect an area within 5 km of the vent. Lighter fragments (such as pumice or scoria) may be kept buoyant in the eruption plume for much greater distances before falling back to Earth. The explosive phase of the eruption may be followed by rapid extrusion of a lava dome. Lahars and volcanic earthquakes would also occur, and may continue long after the eruption itself has ended. Such an explosive eruption may last for years but could also be short-lived (weeks to months). Whatever the duration, areas affected by the eruption will remain uninhabitable for many years. There have been several periods of dome growth and collapse at Morne Anglais in the past, and this type of activity may also occur in the future. A scenario involving a dome-forming eruption from Anglais would not significantly alter the hazard map, although the area affected by pyroclastic flows and surges would be smaller and more concentrated on the west of the volcano, due to the presence of channeling river valleys to the west and topographic highs to the east.
- 15.34°N, 61.32°W
- Elevation – 1165m
- Last eruption – ~1100 years ago
This centre comprises the Wotten Waven caldera (the southernmost caldera within the Central Graben) together with the twin Pelean domes and associated craters of Micotrin. The caldera is elongated SW-NE, parallel to the chain of Pelean volcanoes that bound the southern margin of the Central Graben. It is approximately 7 km long and 4.5 km wide, and parts of the margin are fault controlled. Subsidence volume has been estimated at 5-7.7 km3 (Demange et al. 1985). The two coalesced domes of Micotrin, located in the caldera near its northeastern margin, lie within a number of craters, the largest of which has a diameter of 3.5 km. Between the crater rim and the domes is a “moat” which is now filled in places by lakes (e.g. the Boeri and Freshwater lakes).
Past eruptive activity
This centre has exhibited a variety of past eruptive activity. Activity between 40 and 20 ka was characterised by large explosive Plinian eruptions generating ignimbrites; more recent activity has taken the form of Pelean dome-forming eruptions producing block and ash flows and smaller pumiceous pyroclastic flows.
The Roseau Tuff
The Roseau Tuff is a thick sequence of ignimbrites (partly welded), pumiceous surges and pumice lapilli fall deposits (Sigurdsson 1972) that crops out in the area between the Micotrin dome and the west coast at Roseau. The source for the Roseau Tuff is not well known. Sigurdsson (1972) proposed vents under the Micotrin/Trois Pitons domes, whereas Demange et al. (1985) proposed that much of the ignimbrite originated from within the Wotten Waven caldera. The Plinian eruptions that produced the Roseau Tuff are thought to have occurred over a >20,000 year period (from >46,000 to ~25,000 years B.P.)
Other large ignimbrite-producing eruptions
Within southern Dominica there are other ignimbrite sequences with similar ages to the Roseau Tuff, suggesting that they may also be associated with these Plinian eruptions. These include thick ignimbrite sequences on the east coast at Grand Fond and Rosalie, and on the south coast at Grand Bay. If these ignimbrites indeed had a similar source area to the Roseau Tuff, then the former may have overtopped ridges north of Watt Mountain (now covered by the domes of Trois Pitons and Micotrin), whereas the latter, termed the Grand Bay Ignimbrite by Lindsay et al. (2003) and thought by them to have originated from the Plat Pays volcanic centre, may have flowed over a low divide between Watt Mountain and Morne John and down the Perdu Temps river valley to reach the present coast at Grand Bay. A submarine fan extending at least 7 km offshore is thought to represent an offshore extension of the Grand Bay ignimbrite (Lindsay et al. 2003). Lateral equivalents of the Grand Bay ignimbrite have been recognised along the south coast from west of Morne Fous to Petit Savane in the east (Lindsay et al. 2003). Another Plinian sequence composed of ignimbrites, pumiceous surges and one fall layer of similar age to the Roseau ignimbrites (38,610 to 30,270 years B.P.), has been described from the Wall House quarry on the western flanks of Morne Anglais. Whether these deposits represent distal facies of the ‘Wotten Waven’ ignimbrites or the products of a contemporaneous eruption from Morne Anglais is not known. If the Wotten Waven/Micotrin centre is the source area for all major ignimbrites in southern Dominica, then the 17 available radiocarbon dates from the Roseau, Grand Fond-Rosalie and Grand Bay tongues, together with field relations, suggest that this major Plinian eruptive sequence can, in fact, be subdivided into 6 possible phases of activity: ~25,000; ~29,000; ~35,000; ~38,000; ~46,000 and >46,000 years B.P.
After the emplacement of the Roseau Tuff and associated ignimbrites, activity continued from the Wotten Waven/Micotrin area as indicated by an ignimbrite at En Bas Petit Fond (Ma Robert) on the east coast dated at 19,500 years B.P, and the occurrence south of Micotrin of deposits from small Plinian and Pelean eruptions that occurred approximately 1,000 years ago. The latter represents the most recent activity associated with the Wotten Waven caldera, and may have originated from the Micotrin domes or other unrecognised vents associated with the caldera margin. Historical eruptions There have been no reports of historical eruptions from the Wotten Waven/Micotrin centre.
1. Dome-forming eruption from Morne Micotrin The recognition of relatively recent (~1 ka) Pelean and Plinian activity associated with Micotrin, together with the proximity to historic seismicity, indicates that the Wotten Waven/Micotrin centre could be the site of future eruptions. The most recent activity from this centre has occurred from the Micotrin dome complex, and this is considered the most likely vent area for future eruptions. Recent past behaviour at this volcano indicates that future activity is most likely to be dome forming. The type and duration of hazardous phenomena associated with such an eruption would be similar to that described for a dome-forming eruption from the Plat Pays volcanic complex. The phase of effusive dome-forming activity is likely to be preceded by a series of phreatic eruptions, and possibly even by a period of ‘vent-clearing’ explosive magmatic activity. Dome collapse pyroclastic flows and surges could occur down major valleys on both sides of the volcano, and reach the sea at Roseau and Canefield to the west and Rosalie on the east (brown area on the hazard map). The town of Roseau is, in fact, built on top of a pyroclastic flow fan which was produced during past eruptions at the Wotten Waven/Micotrin centre. More energetic pyroclastic flows and surges would not be so constrained by topography and may reach as far as Mahaut, Loubiere and La Plaine (yellow area on hazard map). Ballistic projectiles would be a hazard within ~5 km of the vent, and lahars and volcanic earthquakes could also occur. The pattern of accumulated ash fall thickness and distribution exhibited between 1995 and 2001 by the ongoing eruption of the Soufrière Hills volcano in Montserrat (Norton et al. 2001) has been used to define the probable ash fall pattern on the hazard map for this scenario. Ash would fall in copious amounts downwind from the volcano.
2. Explosive Plinian eruption from the Wotten Waven caldera Although the last Plinian eruptions from the Wotten Waven caldera probably occurred >19 ka ago, the vigorous geothermal activity at Wotten Waven, together with shallow seismicity beneath the caldera and the possibility that the Plinian eruptions around 1 ka were from vents on the caldera boundary faults, indicates that the possibility of a future Plinian eruption from this centre must be considered. The Wotten Waven caldera is a volcano-tectonic depression that in all likelihood has boundary faults extending to depth. Such a depression may hydrostatically attract any rising head of magma, with the boundary faults providing easy access to the surface. A reactivation of the Wotten Waven caldera could produce a major explosive eruption which would affect most of Dominica. Plinian activity is the most explosive type and results from gas-rich felsic magma that has differentiated in a high-level magma chamber. Such an eruption must be considered the worst-case scenario for a future eruption in Dominica. Plinian eruption columns can reach altitudes of 50 km, although most are lower, generally in the 10-20 km range, so that the material is dispersed by both upper and lower tropospheric winds (Trades and Anti-Trades) as well as by the stratispheric easterlies. The pattern of ash fall thickness and distribution exhibited during the 1902 eruption of the Soufrière in St. Vincent (Robertson 1992) has been used to define a possible ash fall pattern. The collapse of a high Plinian eruption column rich in ash would result not only in ash fall over a wide area, but also extensive valley-fill ignimbrites and associated ash-rich surges (brown area on the hazard map), the latter representing the greatest hazard. Such surges would travel extensively; the pumiceous surges (or ‘ash hurricanes’) produced by prehistoric eruptions of Mt. Pelée extended at least 12 km south of the crater to the very outskirts of the island capital of Fort de France (Smith and Roobol 1990). All major surrounding valleys would be affected, including the Roseau river and its tributaries. Whereas Morne Trois Pitons and Micotrin would provide some morphological barrier to the east of the Wotten Waven caldera, there is no barrier to the west, and ash surges are likely to travel in that direction unimpeded. Energetic surges could also expand to the northeast and devastate the entire central part of the island (yellow area on the hazard map). Morne Diablotins and a ridge of older volcanic rocks to its southeast (see relief map) are likely to form a barrier to the far north; to the south, however, the surges are likely to jump over lower volcanoes and to pass through gaps between them so that most of the island would be devastated. Such an eruption would also produce extensive ballistic projectiles, lahars, volcanic earthquakes and lightning strikes. In such a scenario most of the island south of a line connecting the towns of Salisbury and Marigot would fall in the very high and high integrated hazard zones.
Morne Diablotins and Morne aux Diables
- 15.5°N, 61.42°W
- Elevation – 1447m
- Last eruption – <40,000 years ago
Morne aux Diables
- 15.61°N, 61.43°W
- Elevation – 861m
- Last eruption – <40,000 years ago
Both Morne Diablotins and Morne aux Diables comprise eroded Pelean domes and deeply gullied pyroclastic aprons. Morne Diablotins is the largest and highest volcanic center on Dominica, and is the second highest mountain in the Eastern Caribbean (La Soufrière in Guadeloupe is the highest). Measuring 22 km x 18 km at its base and rising to a height of 1,421 m, it dominates the northern part of the island. Morne aux Diables, forming a peninsula at the extreme north of the island, comprises a central complex of eroded Pelean domes and craters surrounded by flanks of dominantly lithified block and ash flow deposits.
Past eruptive activity
Morne Diablotins is a composite structure comprising several superimposed stratigraphic units. The ‘Older Pleistocene’ volcano, believed to have been very similar to Morne Trois Pitons and Micotrin in form, underwent extensive Pelean activity producing block and ash flows and andesite lava flows (Martin-Kaye 1960; Wadge 1989). A single age of 1.77 Ma (Bellon 1988) from an andesite lava flow has been obtained from these extensive deposits. Pelean-style eruptions also characterise the ‘Younger Pleistocene’ to Recent activity of Morne Diablotins, with block and ash flows reaching the southwest, northwest and northeast coasts. Available ages for these deposits range from 0.72 Ma (Monjaret 1985) to >46,620 years B.P. (Smith and Roobol unpublished data). This Pelean activity was followed by explosive Plinian activity that produced pumiceous fall deposits and ignimbrites dated from >22,200 to >40,000 years B.P. (Sparks et al. 1980a,b; Wadge 1989). The ignimbrite deposits form five radial tongues around the volcano, and have been referred to as the Grand Savanne ignimbrite (Sparks et al. 1980a). The ignimbrites on the wetter Atlantic coast are weathered yellow and lithified while those on the drier Caribbean coast remain white and unlithified, although at Grand Savanne they show welding (Sparks et al. 1980a). These pumiceous deposits are overlain by unconsolidated block and ash flow deposits, which are well exposed in two valley infills on the west coast near Pointe Crabier and Coulibistri.
Morne aux Diables
Morne aux Diables is a stratovolcano measuring 7 km by 7 km and rising to a height of 856 m. Its northern boundary is a steep, 3.8 km-long linear cliff oriented E-W suggesting a fault scarp. This volcano is composed of a central complex of eroded faceted Pelean domes from which dominantly lithified block and ash flow deposits radiate out in all directions to form the flanks. There are five parasitic domes that form an east-west belt across the southern flanks. One of these at West Cabrit is now linked to the island by beach deposits and a swamp. Although the stratigraphy exposed in the sea cliffs is dominated by block and ash flow deposits, a section measured near Douglas Point shows lithified ignimbrites, pumiceous surge deposits and lapilli fall beds that are overlain by lithified semi-vesicular block and ash flow and surge deposits. These indicate that, in addition to the dominant Pelean activity, this center has also undergone Plinian- and Asama-style activity.
Three K-Ar ages of 1.68, 1.72 and 2.01 Ma (Monjaret 1985; Bellon 1988) show Morne aux Diables to be essentially of ‘Older Pleistocene’ age. Despite this, there is considerable evidence for rejuvenation during the Late Pleistocene to Holocene. Three tongues of unconsolidated block and ash flow deposits extend to the northwest coast and two to the northeast coast; such unconsolidated pyroclastic deposits in the Lesser Antilles are believed to be younger than about 70,000 years (Smith and Roobol 1990). One of these tongues exposed in a new road section on the east coast near the hamlet of Enbas (north of Vieille Case) contains pieces of non-charred wood up to 30 cm long, which have yielded a radiocarbon age of >46,740 years B.P. Unconsolidated block and ash flow deposits associated with the East Cabrit dome on the west coast also indicate a young age. The presence of these unconsolidated pyroclastic deposits suggests that the Morne aux Diables volcano has been rejuvenated during the Late Pleistocene to Holocene, resulting in the formation of young Pelean domes near the current summit and on the western flank.
There have been no reports of historical eruptions from either Morne Diablotins or Morne aux Diables.
Effusive dome-forming eruption form Morne aux Diables Although lithified deposits around Douglas Point indicate that Plinian and Asama style explosive activity has occurred during the ‘Older Pleistocene’ stage of Morne aux Diables, the resurgent Holocene activity at this center has been restricted to Pelean-type eruptions and a dome-forming eruption is therefore considered the most likely scenario for future activity at this center. Past activity at Morne aux Diables indicates that a future dome could develop from either central or flank parasitic vents; for the purpose of this scenario a central vent is assumed.
The type and duration of hazardous phenomena associated with such an eruption would be similar to that described for dome-forming eruptions from the Plat Pays volcanic complex and Micotrin. The phase of effusive dome-forming activity is likely to be preceded by a series of phreatic eruptions, and possibly even by a period of ‘vent-clearing’ explosive magmatic activity. Dome collapse pyroclastic flows and surges could occur down major valleys on all sides of the volcano, and reach the sea at Portsmouth, Savane Paille and Clifton to the west, and Penville, Vieille Case and Hiroula Bay to the east (brown area on the hazard map). More energetic pyroclastic flows and surges would not be so constrained by topography and may reach Glanvillia in the southwest and affect areas in and around Thibaud to the east and Dos D’ane and La Source to the southeast (yellow area on hazard map). If the vent occurs on the western flank of the volcano, for example near The Cabrits or Portsmouth, towns to the east of the volcano such as Vieille Casse and Pennville are unlikely to be affected by pyroclastic flow and surge activity. Ballistic projectiles would be a hazard within ~5 km of the vent, and lahars and volcanic earthquakes could also occur. Ash would fall in copious amounts downwind from the volcano.
- 15.307°N, 61.305°W
- Elevation – 1224m
- Last eruption – ~1300 years ago
Past eruptive activity
Demange et al. (1985) describe the western foundations of the volcano as comprising massive andesite lavas now exposed in the River Claire on Curbin Estate and in a little ravine west of Robinson Estate. An age of 0.46 Ma was obtained on a block from a breccia exposed on the northeastern flanks of the volcano. The smooth outer eastern flanks of Watt Mountain, in association with the description of ignimbrites in the upper Jack River which have been dated at 10,290 years B.P. (Seismic Research Unit 2000), suggest that this center may also have undergone a period of Plinian eruptions. The most recent activity from this center is thought to have occurred around 1,300 years ago when an andesite cryptodome was intruded into the lower western flanks of the volcano in the vicinity of Du Mas Estate. Collapse of the uplifted flanks generated debris flows which were converted into lahars when they entered the adjoining rivers. Exposure of the cryptodome generated a series of vulcanian explosions producing a sequence of andesitic lapilli fall deposits exposed at Morne Prosper, and block and ash flows from the gravitational collapse of the dome. Where exposed together the latter overlie or pass into the lahars. Wood collected from laharic deposits that interfinger with the block and ash flows associated with this eruption give dates of 1,350 and 1,270 years B.P (Demange et al. 1985). As a result of these eruptions a conical-shaped crater, partly filled by coarse block and ash flow deposits, was formed between Robinson and Du Mas estate. Like the Micotrin dome and the Babillard Estate crater, this crater lies on or near the margin of the Wotten Waven caldera, and extrusion of the cryptodome may in fact have been more closely related to the most recent activity of the Wotten Waven caldera than to Watt Mountain itself.
There have been no reports of historical eruptions from Watt Mountain.
Although two phases of young explosive activity (1.3 and 10 ka) may have been sourced from this volcano, there is no concrete evidence that it has been active in the recent past. However, the proximity of recent seismicity together with the vigour of the adjacent Valley of Desolation hydrothermal field does suggest that an eruption may occur from this centre in the future. Past activity from Watt Mountain appears to have been largely effusive, resulting in lava flows and domes, with associated block and ash flows. This is considered the most likely style of activity for a future eruption.
Morne Trois Pitons
- 15.37°N, 61.33°W
- Elevation – 1387m
- Last eruption – ~1100 years ago
Morne Trois Pitons is a large volcanic structure located within the Central Graben. Its summit is now occupied by three coalesced Pelean domes with a volume of approximately 1.5 km3 (Wills 1974).
Past eruptive activity
Demange et al. (1985) divide the eruptive history of Morne Trois Pitons into three phases. Rocks of the undated oldest phase are exposed on the west coast north of Roseau and on the northern side of the Boeri River, where they lie on top of andesitic lava flows of Pliocene age. Characteristic of this phase are thick, coarse-grained block and ash flow deposits which are inter-bedded with conglomerates that represent their reworked equivalents. The conglomerates are well exposed near Canefield on the west coast. Locally these deposits are overlain by young reef limestones. Deposits of phase 2 are pumiceous in character and reflect a shift from Pelean to Plinian-style activity. Ignimbrites from these eruptions cover an area of 62 km2 and are mainly exposed in two tongues, one extending northeast towards the valley of the Pagua River and the other northwest to reach the west coast at Layou, where at least three flow deposits are exposed. One of these deposits has been dated at >40,000 years B.P. (Wadge 1989). Further inland, the ignimbrites are much thicker, reaching thicknesses of >180 m in the upper reaches of the Layou river (Wills 1974). The eruption that led to these pumiceous deposits is thought to have produced a caldera of diameter of about 6 km within the northern part of the Central Graben (Demange et al. 1985; Roobol and Smith unpublished data). During the third phase, the current complex of Pelean domes was extruded into a large 3.5 km diameter crater with a rim preserved to the east. Another crater rim to the southwest of the domes possibly represents the margins of a younger and smaller crater associated with the Pelean activity. Eruptions associated with these domes produced an extensive apron of block and ash flow deposits. These deposits have yielded radiocarbon ages of 17,240 (Wadge 1989) and 25,310 (Roobol et al. 1983) years B.P.
There have been no reports of historical eruptions from the Trois Pitons centre.
There is no evidence for recent activity at the Trois Pitons centre, but occasional shallow seismicity beneath the volcano together with its youthful appearance indicates it may erupt again. Future eruptions could be either dome-forming or explosive, and are likely to originate from the summit region. Until more detailed work has been done on this centre it is impossible to determine the likelihood of a future eruption.
Grand Soufrière Hills
- 15.31°N, 61.27°W
- Elevation – 1447m
- Last eruption – ~11,000 years ago
The Grand Soufrière Hills is a poorly-studied, major volcanic center situated on the southeast coast. It is deeply dissected, but has a distinct circular crater 1.9 km in diameter that opens to the east. A Pelean dome occupies the centre of the circular crater, and pyroclastic deposits mantle the southeastern flank of the volcano. Lava flows and dikes forming headlands protruding into the Atlantic Ocean on its southeastern flanks may be exposed remnants of the underlying Miocene basement.
Past eruptive activity
Sigurdsson and Carey (1991) describe a pyroclastic fan extending southeast from the breached crater, and outcrops at Corossol reveal a sequence of block and ash flow deposits, a thin blast deposit, a mudflow deposit and pumiceous pyroclastic flow deposits (ignimbrite), indicating a range of past-activity at this centre. To the southeast of the Grand Soufrière Hills centre on the coast there are a number of unconsolidated valley-fill block and ash flow deposits suggestive of relatively recent activity. A megabreccia of large (up to 3 m) flow-banded andesite clasts set in a semi-lithified medium-grained ash matrix exposed at Pointe Mulatre is also thought to have been derived from the Grand Soufrière Hills (Sigurdsson and Carey 1991). Two dates have been obtained from samples from block and ash flow deposits from this center, a K-Ar age of 0.8±0.4 Ma (Wadge 1989) and a radiocarbon age of 10,320 years B.P. (Smith and Roobol unpublished data). A further radiocarbon date of 11,000 years B.P. was obtained from the blast deposit at Corossol (Sigurdsson and Carey 1991). The 0.8 Ma age is thought to reflect 40Ar contamination from magmatic gases and thus may be too old (Wadge 1989).
There have been no reports of historical eruptions from the Grand Soufrière Hills centre.
Very little is known about the Grand Soufrière Hills centre, and until more detailed work has been done it is impossible to determine the likelihood of a future eruption. Currently there is no evidence of a voluminous magma reservoir beneath this centre and the probability of a large-scale magmatic eruption is considered remote. However, two 10 – 11 ka ages indicate there has been some activity here in the not so distant past, and we believe it should be regarded as potentially active until new information becomes available to clarify its eruptive history.
Valley of Desolation
Along the length of Dominica are a number of crater-like features, usually in the rain forest and not easily studied, that may be phreatic/phreatomagmatic explosion craters. The best known concentration of these craters is the Valley of Desolation/Boiling Lake area, referred to in the past as the “Grand Soufrière” (e.g. Sapper 1903; Robson and Wilmore 1955), where several small explosion craters are associated with vigorous hydrothermal activity. Since the name “Grand Soufrière” is no longer commonly used in Dominica, we refer to this area (extending from the actual Valley of Desolation to the Boiling Lake) as the “Valley of Desolation”. This region is characterised by numerous hot springs, bubbling pools and fumaroles over an area of approximately 0.5 km2. Over the last 100 years, temperatures of fumaroles have generally ranged between 91° and 99°C, and those of hot springs and bubbling mud pools between 40°and 96°C (Sapper 1903; Robson and Willmore 1955; Brown 2002).
The Boiling Lake itself has an area of approximately 85 x 75 m and its usual depth has been estimated at about 10-15 m. Over the last 100 years, temperatures taken at the edge of the Boiling Lake have generally ranged between 80° and 90°C (Sapper 1903; Robson and Willmore 1955; Brown 2002). However, the water level and temperature of the lake have both been known to drop considerably in the past, for example in 1876, 1900, 1901, 1971, 1972 and in 1988 (Ober 1880; James 1988). A small explosion in 1901 from an “empty” lake released harmful gases (probably mainly CO2) into the atmosphere and killed two people who were at the water’s edge at the time (Elliot 1938; Bell 1946). In 1972, locals reportedly bathed in the Boiling Lake, whose levels and temperatures had dropped. In 1988 the normal water level had dropped by about 30 ft., and the temperature at the waters edge was <30°C (James 1988).
Plat Pays volcanic complex
Three main areas of geothermal activity are associated with the Plat Pays volcanic complex. The largest area is located on the margin of the Soufrière depression in the Sulphur Springs National Park region, and was termed the Terre Elm fumaroles by Wadge (1985) but is now more commonly known as Sulphur Springs. Another smaller area of geothermal activity is located in a cliff adjacent to Galion, a village between the Patates and Crabier domes. The Sulphur Springs and Galion fields are characterised by areas of steaming, altered ground with numerous sulphur-coated fumaroles and minor hot springs. The few temperature measurements taken over the last 100 years reveal fumarole temperatures of between 90° and 100°C (Sapper 1903; van Soest et al. 1998; Brown 2002). The fumaroles of Galion and Sulphur Springs have high concentrations of H2O, CO2 and H2S and generally low concentrations of SO2, HCl and CO (Brown 2002). These concentrations, together with the low temperatures of the fumaroles, are consistent with a meteoric-fluid dominated hydrothermal system. The third area of fumarolic activity is found at Champagne, a zone of gas emission 200 m north of Pte. Guignard on the beach and extending to at least 20 m offshore. The underwater fumaroles here are manifested by bubble trains rising towards the surface, and appear to be aligned along roughly east-west trending fractures in lava which can be correlated with similarly-trending fractures in adjacent lava onshore. Minor thermal activity is also present at the foreshore near Soufrière village, where diffuse gas discharge occurs in shallow water. Some minor fumaroles in the crater of Morne Patates were described by Wills (1974), but are no longer present (Lindsay et al. 2003). In recent years the geothermal activity in the Soufrière valley region has been monitored at roughly yearly intervals. Other than minor changes in gas flux and sulphate content, no significant changes have been observed in their character, temperature or chemistry (J-C. Komorowski, pers. comm. 2000; Brown et al. 2002; P. Joseph pers. comm. 2004).
Several fumaroles and hot springs are located within the Wotten Waven caldera. The largest area of activity is located near the village of Wotten Waven, in and adjacent to the River Blanc, a tributary of the Roseau river. Within the river valley itself there are numerous bubbling pools and fumaroles with temperatures of up to 99°C. A 2 m wide cave approximately 6 m above the river bed on the northern side of the river is the site of a milky-white pool of water (80°-93°C) whose level rises and falls every 10 seconds. Loud bubbling sounds issue from within the depths of the cave. About 40 m north of the cave, above the River Blanc, several other vigorously bubbling pools are present. The largest of these, Yellow Pool, is ca. 2 m x 1.5 m in size, and is milky white or clear, depending on whether it is the dry or wet season, respectively. Its temperature also varies according to season: 71°-74°C in the wet season; and 87°-93°C in the dry season (Joseph and Lindsay 2002). Several other smaller pools in and adjacent to a small stream that passes through the area range in temperature from 50°to 99°C. A fumarole in a nearby field had a temperature of 100°C in May 2000. An old report by Drumm (1849) on the Wotten Waven geothermal area suggests it was just as active, if not more active, 150 years ago. Minor warm spring activity is also present at the Trafalgar Falls, in Papillote and a temperature of 39.2°C was recorded by van Soest et al. (1998). A landslide in September 1995 buried the pools and hot spring at the base of the ‘father falls’ (James 1997) impeding access to this once-popular tourist destination.
Although there are no major areas of geothermal activity associated with Micotrin, some of the streams adjacent to the southern dome have banks with patches of orange-stained rocks indicating that there may be some as yet unidentified warm springs higher up the dome.
Morne aux Diables
Numerous hot springs and patches of hot ground are present in the vicinity of Glanvillia south of Portsmouth. They form an area of thermal activity 2.5 km by 1.5 km in size, roughly half of which is immersed in the shallow waters of Prince Rupert Bay at depths of 20 to 70 ft. Onshore temperatures of up to 102°C were recently (February 2004) recorded from an area of hot ground near the mouth of the Picard River in Glanvillia. The submarine springs occur as both large isolated springs and as areas of more diffuse degassing via many smaller springs. The largest and deepest solitary spring is located in 70 ft of water to the south of the thermal area. Vigorous venting of hot discolored water from this feature has led to the formation of a depression in the sea bed 110 ft in diameter. Bubbles from this spring reach the water surface despite the 70 ft water depth (compared to a maximum depth of origin of only 15 ft at Champagne Pool in the south). Divers visiting the area in February 2004 reported the sea bed too hot to push their hands into the sand and the boat anchor, when raised, was still warm to the touch.
Minor fumarolic activity has also been reported on the northwestern slopes of Morne Diablotins (Robson and Tomblin 1966), to the west of Morne aux Diables on the coast at Toucari village (in a roadside excavation now infilled) and on Morne Turner (A. James pers. comm. 2003). An area of cold spring activity, known as the ‘Penville Cold Soufrière’, is located in the northwestern, younger crater of Morne aux Diables (Robson and Tomblin 1966), in the upper part of the Lamothe River. The springs are located to the north of the main summit area, and cover an area of about 25 m2. The activity is manifested as milky to clear vigorously bubbling pools and cold “frying pan” features with temperatures of 23°-29°C and an acidic pH (1-2) (Joseph and Lindsay 2002; Joseph and Robertson 2003). A strong H2S odour is present and vegetation is dead or absent in the immediate area. Several bubbling springs also occur in a nearby stream, and are surrounded by large patches of white filamentous algae. In 2013, the Government of Dominica, with Multi-Lateral Development Bank assistance, sponsored the drilling of three slim exploration holes in the Wotton Waven area. Temperatures above 235°C were recorded in these wells and in 2014, the first of three planned production wells was drilled with similar temperatures encountered at a depth of just over 1,500 metres. This well is currently shut in for a three month heat build-up period after which the well will be tested in accordance with international standards. Plans are reportedly to build a 10-15 MW power plant initially, which is the current power demand of the island (extracted from Huttrer and LaFleur, 2015).
Dominica is one of the countries within the Eastern Caribbean that aspires to harness geothermal energy. Earlier exploration activities on the island suggested that the Wotten Waven area and Soufriere Galion appear to have the best prospects for geothermal development. In 2008, a European Union funded exploratory programme found that the Roseau Valley was an ideal area for geothermal development and the geothermal resources in the Wotten Waven area could possibly generate 130 MW. Successive to this, three slim hole well, WW-1, WW-2 and WW-3, were drilled from 2011-2012 by the Iceland Drilling Company and a field potential of 65 MW was confirmed in the Wotten Waven area. The production phase followed which included the drilling of production (WW-P1) and reinjection (WW-R1) wells and a flow test conducted on WW-P1 in June 2014 confirmed an electric power generation potential of 10MW. In August 2016, the Government of Dominica announced the construction of a 7 MW geothermal plant in two stages of 3.5 MW each. The government plans to establish a company to construct the plant and is working towards the Geothermal Development Bill inclined to establish the legal framework for the development of geothermal energy in Dominica.
Andreieff P, Bellon H, Westercamp D (1976) Chronometrie et stratigraphie compare des edifices volcaniques et formations sedimentaires de la Martinique (Antilles Français) Transactions VIIth Caribbean Geological Conference (Guadeloupe 1974) p. 345-356.
Arculus RJ, Wills KJA (1980) The petrology of plutonic blocks and inclusions from the Lesser Antilles: Journal of Petrology 21:743-799. Atwood T (1791) The history of the island of Dominica, London.
Baker PE, Westercamp D, Bouysse Ph. (1990) Geology of the Lesser Antilles (The Northern Volcanic Caribbees): in Dengo G, Case JE eds., The Geology of North America H – The Caribbean Region: Geological Society of America 156-160.
Bell H (1946) Glimpses of a Governor’s Life – Dominica.
Bellon H, Pelletier B, Westercamp D (1974) Donnes geochronometriques relatives au volcanisme martiniquais: Comptes Rendus de l’ Academie Sciences, Paris 279:457-460.
Bellon H (1988) Reconnaissance chronologique des deux premieres phases d’activite volcanique en Dominique (Petites Antilles): C.R. Acad. Sci Paris 306:1487-1492.
Bert L (1880) Eruption et chute de poussieres volcaniques, le 4 janvier 1880, a la Dominique (Antilles anglaises): Comptes Rendus de l’ Academie Sciences, Paris 90:622-624.
Briden JC, Rex DC, Faller AM, Tomblin JF (1979) K-Ar geochronology and paleomagnetism of volcanic rocks in the Lesser Antilles island arc: Philosophical Transactions Royal Society London, series A 291:485-528.
Brown GM, Holland JG, Sigurdsson H, Tomblin JF, Arculus RJ (1977) Geochemistry of the Lesser Antilles volcanic island arc: Geochimica et Cosmochimica Acta 41:785-801.
Brown LK (2002) Gas Geochemistry of the Volcanic Hydrothermal Systems of Dominica and St. Lucia, Lesser Antilles: Implications for Volcanic Monitoring. Unpublished Senior Honors Thesis, Department of Earth and Planetary Sciences, University of New Mexico. 31pp.
Carey SN, Sigurdsson H (1980) The Roseau ash: Deep-sea tephra deposits from a major eruption on Dominica, Lesser Antilles arc. Journal of Volcanology and Geothermal Research 7: 67-86.
Cas RAF, Wright JV (1987) Volcanic successions, modern and ancient.
Chapman and Hall. pp 528. Daubrée M (1880a) Examen d es poussières volcaniques tombées le 4 janvier 1880 à la Dominique et de l’eau qui les accompagnait. Comptes Rendus de l’ Academie Sciences, Paris 90:624-626 (repeated in Bull. Soc. Geog. 20:72-75).
Daubrée M (1880b) Produits solides et liquides qui continuaient à sortir, en avril 1880, d’un cratère de la Dominique (Antilles anglaises). Comptes Rendus de l’ Academie Sciences, Paris 91:949-950.
Date, A.W.2015. The Eastern Caribbean Energy Interconnection Grid Feasibility study, Proceedings World Geothermal Congress 2015, Melbourne Australia
Davidson JP (1984) Petrogenesis of Lesser Antilles island arc magmas: Isotope and geochemical constraints [Ph.D. thesis] University of Leeds, 258p.
Demange J, Leborne H, Traineau H, Westercamp D (1985) Histoire volcano-structurale de la Region sud de la Dominique: Bureau de Recherches Geologiques et Minieres, Institut Mixte de Recherches Geothermiques, Rapport 85 SGN 068 IRG-GTH, 114p.
Deplus C, Le Friant A, Boudon G, Komorowski J-C, Villemant B, Harford C, Ségoufin J, Cheminée J-L (2001) Submarine evidence for large-scale debris avalanches in the Lesser Antilles Arc. Earth and Planetary Science Letters 192:145-157.
Donnely TW, Rogers JJW, Pushkar P, Armstrong RL (1971) Chemical evolution of the igneous rocks of the eastern West Indies; an investigation of thorium, uranium and potassium distribution, and lead and strontium isotope ratios. in: Donelly TW (ed): Caribbean geophysical, tectonic and petrologic studies: Geological Society of America Memoir 130:181-224.
Drumm WM (1849) Earthquakes in Dominica. The Dominica Colonists, Saturday April 21 1849.
Earle KW (1928) Geological notes on the island of Dominica. B.W.I. Geol. Magazine 65:169-187. Elliot EC (1938) Boiling Lake – The 1900 Story. In: Broken Atoms. Elliot WR (1893) Letter to Nature, Nature 1224, vol. 47; April 13th 1893.
Eldridge (1880) Recent volcanic eruption at the grand Souffriere, in the island of Dominica. Procedings of the Royal Geographical Society 2:363-366. Endlich FM (1880) The Island of Dominica. The American Naturalist 14 (11):761-772.
Hawkesworth CJ and Powell M (1980) Magma genesis in the Lesser Antilles island arc: Earth and Planetary Science Letters 45:297-308. Hovey EO (1904) Boiling Lake of Dominica: Geological Society of America Bulletin 16:570-571.
Howe, T M, J Lindsay, P Shane, A K Schmitt, and D Stockli. 2014. “Re-evaluation of the Roseau Tuff eruptive sequence and other ignimbrites in Dominica, Lesser Antilles.” Journal of Quaternary Science 29 (6):531-546.
Huttrer. G.W. 2000. Geothermal Activity Status in the Volcanic Caribbean Islands, Proceedings World Geothermal Congress 2000, Kyushu- Tohoku, Japan.
Huttrer. G.W, La Fleur. J, 2015. The Eastern Caribbean Energy Interconnection Grid Feasibility study, Proceedings World Geothermal Congress 2015, Melbourne Australia
Isaacs MC, Shepherd JB (1986) Seismic Research Unit Internal Report.
Iundt F (1982) Geochemical study of Dominica island. BRGM report 85SGN102GTH 36pp.
James A (1997) And they came tumbling down……The Mega-Slides of 1995. The New Forester (Dominica) Vol. X (1997). James A (1988) A Cool Boiling Lake? The New Chronicle (Dominica) (June 1988).
Joseph E, Lindsay J (2002) Sampling of geothermal features in Saint Lucia and Dominica 14th – 20th November 2002. Seismic Research Unit Internal Report.
Joseph E, Robertson R (2003) Sampling of geothermal features in St. Lucia and Dominica, 3rd – 9th November 2003. Seismic Research Unit Internal Report.
Komorowski J-C, Hammouya G (1998) Analytical results and report on the current activity of the Soufrière area as of December 8-9 1998. Unpublished report presented to the Government of Dominica.
Le Friant A, Boudon G, Komorowski J-C, Deplus C (2002) L’île de la Dominique, á l’origine des avalanches de débris les plus volumineuses de l’arc des Petites Antilles. C.R. Geoscience 334:235-243.
Lindsay, J M, A L Smith, M J Roobol, and M V Stasiuk. 2005. “Dominica.” In Volcanic Hazard Atlas of the Lesser Antilles, edited by J M Lindsay, R E A Robertson, J B Shepherd and S Ali, 1-48. Trinidad and Tobago, W.I.: Seismic Research Unit, The University of the West Indies.
Lindsay JM, Stasiuk MV, Shepherd JB (2003) Geological history and potential hazards of the late-Pleistocene to Recent Plat Pays volcanic complex, Dominica, Lesser Antilles: Bulletin of Volcanology 65: 201-220.
Martin-Kaye PHA (1960) Preliminary notes on the geological map of Dominica. Unpublished progress reports of the Government Geologist. nos. 1-12 Geological Survey, Windward Islands.
Martin-Kaye PHA (1969) A summary of the geology of the Lesser Antilles: Overseas Geology and Mineral Resources 10:172-206.
Mattioli GS, Jansma PE, Jaramillo L, Smith A (1995) Sector collapse in island arc volcanoes: a digital topographic and bathymetric investigation of the Qualibou Depression, St. Lucia, Lesser Antilles. Caribbean Journal of Science 31(3-4):163-173.
Monjaret M-C (1985) Contribution a l’etude de l’arc des Petites Antilles. Le Volcanisme de la Dominique. Donnees chronologiques, mineralogiques et geochimiques. Unpublished thesis, Universite de Bretagne Occidentale, pp77.
Newhall C, Dzurisin D (1988) Historical Unrest at Large Calderas of the World. US Geological Survey Bulletin 1855(2): p 924. Nicholls HAA (1880a) The volcanic eruption in Dominica: Nature 21:372-373
Nicholls HAA (1880b) Visit to the scene of the late volcanic eruption. The Dominican, January 17 1880 Norton G, Harford C, Young S (2001) Volcanic Geology of Montserrat, West Indies. Field Guide.
Ober FA (1880) Camps in the Caribbees: The adventures of a Naturalist in the Lesser Antilles. Boston, US: Lee and Shepherd; Edinburgh: Douglas. (Reviewed in Nature July 8 1880 p215).
Prestoe (1876) On the discovery of a Boiling Lake in Dominica. Procedings of the Royal Geographical Society 20 (III):230-232.
Pushkar P (1968) Strontium Isotope Ratios in Volcanic Rocks of Three Island Arc Areas: Journal of Geophysical Research 73:2701-2714. Robertson REA (1992) Volcanic Hazard and Risk Assessment of the Soufrière Volcano, St. Vincent, West Indies. MPhil, Earth Sciences, The University of Leeds, Leeds.
Robson GR (1964) An earthquake catalogue for the Eastern Caribbean 1530 – 1960. Bulletin of the Seismological Society of America 54(2):785-832.
Robson GR, Barr ICG (1960) Unidentified Earth Tremors in Dominica, West Indies. Nature 188 (4747):366.
Robson GR, Barr ICG (1967) Report of the investigation into the Dominica tremors of 1959 and 1960. University of the West Indies, Seismic Research Unit Special Publication 9.
Robson GR, Tomblin JF (1966) Catalogue of the active volcanoes of the world including solfatara fields, part 20, the West Indies. International Association of Volcanologists, pp. 1-56.
Robson GR, Willmore PL (1955) Some heat measurements in West Indian Soufrières: Bulletin Volcanologique 17:13-39.
Roobol MJ, Smith AL (1976) Mt. Pelée Martinique: a pattern of alternating eruptive styles. Geology 4:521-524.
Roobol MJ, Smith AL (2004) Volcanology of Saba and St. Eustatius islands, Northern Lesser Antilles: Memoir Netherlands Royal Academy of Arts and Science.
Roobol MJ, Wright JV, Smith AL (1983) Calderas or gravity-slide structures in the Lesser Antilles island arc? Journal of Volcanology and Geothermal Research 19:121-134.
Roobol MJ, Smith AL, Wright JV (1985) Dispersal and chartacteristics of pyroclastic fall deposits from Mt. Misery volcano, West Indies: Geologische Rundschau 74(2):321-325.
Sapper K (1903) Ein Besuch von Dominica. Centralblatt für Mineralogie, Geologie, Paleontologie: 305-314.
Seismic Research Unit (2000) Volcano Hazard Report for Southern Dominica: Interpretation of 1998-2000 Earthquakes and Hazard Mapping Results. Unpublished report submitted to the Government of Dominica.
Seismic Research Unit (2001) Volcano Hazard Report for Southern Dominica: Update to March 15 2001: Unpublished Report, Seismic Research Unit, University of the West Indies 11p.
Shepherd JB (1986) Earthquake series in Dominica, March 9-10 1986. Caribbean Disaster Preparedness Newsletter 5:5-6.
Shepherd JB, Lynch L, Stasiuk M, Latchman J, Lindsay J, Devine J, Hoblitt C, Miller D (2000) Shallow Magma Intrusion Generates Volcanic Earthquake Swarm Beneath Dominica, West Indies, September 1998 to July 2000. Conference Abstracts, IAVCEI General Assembly, Bali.
Shepherd JB, Lindsay JM, Stasiuk M (2003) Volcanic Hazards in Dominica. in: Beyond Walls: Multi-disciplinary Perspectives, Volume II: Dominica. School of Continuing studies, University of the West Indies.
Sigurdsson H (1972) Partly-welded pyroclast flow deposits in Dominica, Lesser Antilles. Bulletin of Volcanology 36:148-163.
Sigurdsson H, Carey SN (1991) Caribbean Volcanoes: A Field Guide to Martinique, Dominica and St. Vincent. Geological Association of Canada, Toronto 1991 field trip guidebooks, pp. 1-101.
Smith AL, Roobol MJ, Gunn B (1980) The Lesser Antilles: A discussion of Island Arc Volcanism: Bulletin Volcanologique 43: 287-302.
Smith AL, Roobol MJ (1990) Mt. Pelée, Martinique: A study of an active island arc volcano: Geological Society of America Memoir 175: 105p.
Smith, A L, M J Roobol, G S Mattioli, J E Fryxell, G E Daly, and L A Fernandez. 2013. “The volcanic geology of the mid-arc island of Dominica, Lesser Antilles: the surface expression of an island-arc batholith.” Geological Society of America Special Paper 496.
Sparks RSJ, Sigurdsson H, Carey SN (1980a) The entrance of pyroclastic flows into the sea, I. Oceanographic and geologic evidence from Dominica, Lesser Antilles. Journal of Volcanology and Geothermal Research 7:87-96.
Sparks RSJ, Sigurdsson H, Carey SN (1980b) The entrance of pyroclastic flows into the sea, II. Theoretical considerations on subaqueous emplacement and welding. Journal of Volcanology and Geothermal Research 7:97-105.
Stasiuk MV, Shepherd JB, Latchman J, Lindsay JM (2002) Intrusion-induced caldera fault slip imaged by shallow seismicity on Dominica, West Indies, 1998-2000. Seismological Research Letters 73:242.
Tomblin JF (1972) Seismicity and plate tectonics of the eastern Caribbean: Transactions VI Caribbean Geological Conference (Margarita 1971) 277-282.
Tomblin J, Aspinall W, Almorales HJ, Shepherd JB (1974) Dominica local earthquakes, 1974. Reports 1 – 7; Seismic Research Unit.
van Soest MC, Hilton DR, Kreulen R (1998) Tracing crustal and slab contributions to arc magmatism in the Lesser Antilles island arc using helium and carbon relationships in geothermal fluids. Geochim. Cosmochim. Acta 62:3323-3335.
Wadge G (1985) Morne Patates volcano, Southern Dominica, Lesser Antilles. Geological Magazine 122(3):253-260.
Wadge G (1989) A preliminary analysis of volcanic hazards in Dominica: Unpublished report, Seismic Research Unit, University of the West Indies, Trinidad, 20p.
Wadsworth ME (1880) The volcanic dust from Dominica. Nature, July 22 1880, p266-267.
Watt E (1880) Recent volcanic eruption in Dominica. Nature May 27 1880 p77. Westercamp D (1976) Petrology of the Volcanic Rocks of Martinique West Indies: Bulletin Volcanologiqe 39:173-200.
Westercamp D, Andreieff P (1989) Carte Geologique de la Martinique au 1:50,000 et notice explicative; France, Serv Geologique Nacional, BRGM
Whitham AG (1985) Transport and deposition of pyroclastic materials in subaqueous environments. Unpublished PhD dissertation, University of Cambridge, 150p.
Whitham AG (1989) The behaviour of subaerially produced pyroclastic flows in a subaqueous environment: Evidence from the Roseau eruption, Dominica, West Indies. Marine Geology 86:27-40.
Wills K (1974) The Geological History of Southern Dominica and Plutonic Nodules from the Lesser Antilles. Unpublished PhD thesis, University of Durham.