A volcanic hazard refers to any potentially dangerous volcanic process that puts human life, livelihoods and/or infrastructure at risk of harm. Several hazards may affect the area around the volcano, such as lava flows, pyroclastic flows, lahars and debris avalanches. Volcanic activity also produces hazards that can affect areas far from the volcano, such as release of gases, ash fall and tsunami. Such hazards can impact areas 100s to 1000s of kilometres from the volcano, with the potential for significant health and economic impacts. ()
Even though volcanoes can be dangerous there are lots of reasons why people live alongside them. There can be emotional, societal and economic benefits. For those living alongside volcanoes, knowing about volcanic hazards is just one way that people can reduce their risk.
Types of volcanic hazard
The following section explains a range of volcanic hazards and the potential impact on people and the environment.
• tephra/ash fall
• lava flows and lava domes
• pyroclastic flows
• landslides and debris avalanches
• lahars (mudflows)
During volcanic eruptions, ash, which is made up of small, sharp, angular fragments of glass and other volcanic rock, may be sent up high into the air, sometimes reaching the stratosphere. Volcanic products are typically named according to clast size which can range from metres down to microns in size. Tephra is used as the capture term to describe all erupted clasts, regardless of size, while the term ash describes particles of less than 2 mm in size.
During an eruption, most tephra will fall to the ground around the volcano. This tephra can load building roofs, and obscure road markings making travel difficult. The loading of tephra of leaves, can lead to the burial of plants, or the stripping of branches from trees, and can therefore have a significant impact on agriculture. The fine-grained nature of volcanic ash means it is easily transported by winds to distance of 100
’s to 1000 ’s km away from the volcano. Due to its abrasive nature, volcanic ash can cause damage to aircraft.
One explanation for the ‘blood red’ clouds at sunset depicted by Edvard Munch in the painting ‘The Scream’ is the volcanic eruption of Krakatau in 1883. The eruption emitted large amounts of gas and ash that changed the colour of the sky worldwide.
Various gases can be emitted by active volcanoes before, during or after an eruptive event and can cause various health hazards locally, but have the potential to affect the climate globally. The five main gases that pose a threat to health are:
- carbon dioxide
- hydrogen chloride, hydrogen fluoride and hydrogen sulphide
- sulphur dioxide
People can be exposed to harmful volcanic gases by breathing them in or through contact with the skin and eyes. The health effects range from mild to serious with occasional deadly exposures. After exposure people may report difficulty breathing and itchy skin.
Volcanic gases are particularly hazardous as they cannot be seen, and because they are denser than ambient air, can pond in depressions around an active volcano. High concentrations of volcanic gas may also be a health hazard inside planes. Sulphur gases convert to sulphate aerosols (mainly sulphuric acid) which, if they reach the stratosphere, may remain there for years causing short-term climate changes.
Lava flows and lava domes
Lavas are flows of magma extruded onto the surface of a volcano. In general it is rare for lavas to cause the direct loss of life, because they usually flow slowly, allowing sufficient time for people to be evacuated. They do however destroy everything in their paths by a combination of burial, crushing and heat, and such eruptions are also associated with emission of volcanic gases and aerosols.
The viscosity, the ease at which a fluid can flow, of lava flows generally increases with silica content and decreases with a rise in temperature and water content. Low-viscosity basalts are the most fluid of the common lava types and are typically erupted at temperatures of 1100°−1200°C. High-viscosity andesites are much less fluid than basalt and are erupted at temperatures of around 700°−900°C.
Or put another way, the iron/magnesium-rich basaltic magmas are the most runny (low viscosity) at one end of the scale and silicon-rich are the least runny (highly viscous) at the other end.
Basaltic magmas can flow relatively long distances. In
contrast, high viscosity lavas (andesites) are typically erupted at low rates
and form short, thick flows or steep-sided domes of that don’t travel far from
The rate of movement of lavas typically ranges from a few metres per hour for high-silica lavas (andesites) to several kilometres per hour for fluid basalts. Lava domes form when high viscous lava is slowly erupted from a volcano. Because of the high viscosity of the lava, it can not travel far from the vent, and a dome of lava builds up. These lava domes are particularly hazardous as the tend to be unstable, and can collapse causing pyroclastic density currents.
Flood basalts are an exceptional form or lava flow. These eruptions are rare, and our understanding of these events is based on study of past eruptions at places like the Deccan Traps, in India, or the Siberian Traps. Such eruptions impact large, up to continental sized (over one million square kilometres) areas, can have thickness of a kilometre, and release large amounts of gas and can cause air pollution and even have an impact on the climate.
We can learn a lot from flood basalts that happen in Iceland. In 2014, the Holuhraun fissure eruption reached the flood basalt size. It is now the largest flood basalt in Iceland since the Laki eruption in 1783-84, which caused the deaths of about 20% of the Icelandic population by environmental pollution and famine and most likely increased levels of mortality, elsewhere in Europe, through air pollution by sulphur-bearing gas and aerosols. Thankfully, flood basalt eruptions are very rare!
Pyroclastic flows are hot ‘density currents’ consisting of mixtures of rock debris and gas, which flow along the ground at high speed. Travelling under gravity, they tend to flow down hillsides, along valleys and towards lower ground; although extremely powerful, or energetic, pyroclastic flows have been known to defy gravity and move uphill. Temperatures of pyroclastic flows can range between 100 °C to 600 °C. They typically travel at 70 mph or faster down the sides of the volcano.
Fountain collapse pyroclastic flows
Pyroclastic flows form by a couple of mechanisms, either by collapse of a lava dome, or during explosive eruptive activity, whereby the mixture of gas and ash that is emitted from the volcano is too dense to rise buoyantly into the atmosphere, and instead collapses around the volcano.
Dome collapse pyroclastic flows
Volcanoes that erupt very viscous, or sticky, lavas to form domes can also produce pyroclastic flows when the dome becomes unstable. Pyroclastic flows are produced when large portions of the dome collapse and disintegrate.
Pyroclastic flows are also called ‘nuées ardentes’, meaning glowing clouds in French
Pyroclastic flows produce deposits of hot ash and rocks around the flanks of the volcano. Temperatures may exceed 400 degrees centigrade in material several months old. These pictures show typical deposits from dome collapse and fountain collapse pyroclastic flows.
Landslides and debris avalanches
Debris avalanches and landslides are common, but are not necessarily caused by an actual volcanic eruption or volcanic activity. They can be triggered as the result of a volcanic explosion or dome collapse, particularly in environments where heavy rainfall is common. Debris avalanches tend to become channelled into valleys and can travel large distances well beyond their source areas. It is difficult to reduce the impact of debris avalanches because they can occur without warning, even on dormant volcanoes, and can devastate large areas. Once initiated, it is impossible to evacuate areas in the paths of debris avalanches because of the great speed with which they travel.
A lahar is a type of volcanic mudflow, which is made up of volcanic debris and water (hot or cold). Lahars move very rapidly at speeds that range from less than 10 km per hour up to a few tens of kilometres per hour. They can occur as a result of eruptions involving ice or snow. This can generate large amounts of meltwater. As these debris-laden flows move down river valleys they can gather more loose material. Lahars can also be triggered, or mobilised, by heavy rainfall.
Viscous mudflows may contain more than 60% sediments (40% water) and have the consistency of wet concrete. Less viscous mudflows, with a higher water content, resemble torrential floods.
Lahars have been a major cause of fatalities in historic times. For example, in 1985 23 000 people died as a result of the Nevado del Ruiz lahar in Colombia. Fatalities and injuries from lahars can be avoided if communities are evacuated quickly to high ground.
Jökulhlaup is an Icelandic word that is used to describe a glacial outburst flood, which is a sudden release of water from a lake that lies under or close to a glacier. One of the triggers of a jökulhlaup could be an eruption of a volcano situated beneath a glacier that melts overlying ice or weakens a dam made of glacial moraine sediments. The sudden removal of the lake dam releases a huge volume of water to produce a ‘megaflood’ that can wash away roads and bridges.
Tsunamis can form in relation to a wide range of geological activity, from earthquakes to landslides. Although less common, volcanoes can also cause tsunamis. In fact, tsunamis have caused the most fatalities associated with volcanic eruptions in historical times. Tsunamis form when water, whether in a lake of the sea, is displaced. On volcanoes, this can occur by a number of mechanisms, for example a submarine eruption, collapse of part of a volcanic edifice or entrance of lahars or pyroclastic density currents into surrounding water. While submarine eruptions may only produce local tsunamis, large devastating tsunamis affecting entire continents can be formed during large explosive pyroclastic density forming eruptions.
An example of such an event is the 1883 eruption of Krakatau, Indonesia. While there is still some discussion as to the exact source of the tsunamis, the eruption produced large pyroclastic flows and led to collapse of the volcano. Numerous tsunamis were produced, with the most devastating resulting in more than 36 000 deaths. More recently, in 2018, another tsunami formed in relation to activity at the same volcanic complex. Anak Krakatau, translating to the ‘child of Anak’, is the volcano which over the past 100 years has built up on the edge of the 1883 Krakatau caldera. In Dec 2018, approximately ~ % of the volcano collapsed into the surrounding seas, forming a tsunami that affected much of the coast along the Sunda Straits, and resulting in the deaths of more than 400 people.
British Geological Survey. 2012. Geohazard note: Volcanic hazards. British Geological Survey.
Dunkley, P N, and Young, S R. 2000. Volcanic hazard mapping for development planning. British Geological Survey, WC/00/20 (Keyworth, Nottingham).
You may also be interested in:
1. BGS 2012
BRITISH GEOLOGICAL SURVEY. 2012. Geohazard note: Volcanic hazards. BRITISH GEOLOGICAL SURVEY.