GMPV
Geochemistry, Mineralogy, Petrology & Volcanology

Will Hutchison

Will Hutchison is a postdoctoral researcher at the Department of Earth Sciences (University of St Andrews). He uses a range of geophysical and geochemical techniques to understand the causes and consequences of magmatism and volcanic activity. Will is currently working as part of the HiTech AlkCarb consortium investigating the roof zones of alkaline magmatic systems in Greenland.

Building a lava dome: one block at a time

Building a lava dome: one block at a time

Lava domes form when lava is extruded from a volcanic vent, but is too viscous to flow far away. Think of thick treacle that does not flow as easily as runny honey, and so when it is extruded, it forms a “lava pile” around the vent. Lava domes commonly form within the crater of a larger volcano (e.g. Mt. St. Helens), but can also stand alone or form part of a “dome complex”.

A lava dome can take on a variety of shapes and sizes dependent upon many factors, including lava chemical composition, viscosity and extrusion rate. Some of the different types of lava domes range from “pancake domes”, generally short and wide, to “spiny domes”, where lava cools and breaks into blocks of rock. Volcanologists have observed over time that every lava dome is different, even at the same volcano or during the same eruption. The number of factors that influence the behaviour of a lava dome makes it difficult to understand the processes occurring during lava dome growth. There is still a lot of research necessary before we can think about forecasting behaviour during a dome-building eruption.

Lava dome hazards

There are many hazards associated with dome-building eruptions, and they are often linked to explosive volcanic activity. In the same way that landslides occur in a slope made of soil, lava domes can collapse if they become oversteepened. Lava dome stability can also be affected by intense bouts of rainfall, as the rainwater can be pressurised when it comes into contact with the hot dome (temperatures at eruption are generally in excess of 850˚C), thus turning the rainwater into steam and forcing the solidified lava to fracture apart, causing collapse. Other causes for collapse include a build-up of gas within the dome, or a change in direction of the lava extrusion.

Pyroclastic flows from dome collapse in Montserrat, June 1997. Credit BGS.

A number of things can happen when a lava dome collapses, ranging from small scale rockfalls, to debris avalanches, to pyroclastic density currents (turbulent mixtures of gas and rock that can travel at speeds of over 100 kilometres per hour). Any of these can be devastating to communities surrounding the volcano, as pyroclastic density currents cannot be redirected using the same methods that have been utilised for lava flow diversion.

Hazards for scientists

Despite how dangerous these events can be to populated areas, very little is known about various causes of a collapse. This is mainly because the internal structure of a lava dome is uncertain. We think there is a ductile, frictionless core that is surrounded by a solid, friction-controlled rind (think of a soft caramel encased by hard chocolate). A dome often also includes talus aprons, which are piles of loose rubbly material that accumulate due to rockfalls that occur during dome growth.

Research into lava dome collapse can be split into three main areas: field observations, analogue and laboratory experiments, and numerical modelling. Field observations of real life environments and landscapes are vital for creating conceptual models of a lava dome.

Conceptual diagram of internal structure, and photo of the dome at Mt. Unzen (2016). Credit: Claire Harnett

 

The missing particle of the puzzle

After fieldwork at both Mt. Unzen and Soufrière Hills Volcano, my research has focused on numerical modelling of lava dome collapse. The aim is to build a computer simulation of a lava dome, and then change conditions in the model to create various “model scenarios” for collapse. This allows us, for example, to change the gas pressure (something we know to cause collapse at a real dome) in our synthetic lava dome, and vary the time period over which forces are exerted upon the dome.

To do this, we use discrete element method (DEM) modelling. DEM considers the simulated lava dome as an assembly of individual particles/blocks, which means that the model can evolve dynamically and the particles act according to gravity and their interactions with neighbouring particles. We generate a particle based material that represents lava. We then give the particles a speed and a direction to simulate extrusion, and we control the point at which parts of the material start to behave as a solid (i.e. representing a realistic cooling/solidification process).

Discrete element model of a very simplistic lava dome. Credit: Claire Harnett

Although these models are still in development, we are able to replicate the growth patterns observed at lava domes. For example we see when a lava dome reaches its maximum height (determined by the rock properties), it starts to grow outwards rather than upwards. We aim to create software that can further our understanding of the processes occurring within a dome, with the ultimate goal of use in observatories. Scientists monitoring the volcano could then input what they see occurring during a volcanic eruption, and have a greater chance of predicting what will happen next.

These models are proving to be a really exciting and innovative way to study lava dome growth and collapse, and will reveal some of the mysteries of lava domes and the dangers they pose.

A movie of lava dome emplacement, where red material acts as ductile core, and grey material acts as solid rock. 

Blog post written by Claire Harnett. For more information, keep your eyes peeled for the paper coming soon! Or get in touch with Claire on Twitter.

Living with volcanic gases

Living with volcanic gases

Professor Tamsin Mather, a volcanologist in Oxford’s Department of Earth Sciences reflects on her many fieldwork experiences at Masaya volcano in Nicaragua, and what she has learned about how they effect the lives of the people who live around them. 

Over the years, fieldwork at Masaya volcano in Nicaragua, has revealed many secrets about how volcanic plumes work and impact the environment, both in the here and now and deep into the geological past of our planet.

Working in this environment has also generated many memories and stories for me personally. From watching colleagues descend into the crater, to meeting bandits at dawn, or driving soldiers and their rifles across the country, or losing a remotely controlled miniature airship in Nicaraguan airspace and becoming acquainted with Ron and Victoria (the local beverages), to name but a few.

I first went to Masaya volcano in Nicaragua in 2001. In fact, it was the first volcano that I worked on for my PhD. It is not a spectacular volcano. It does not have the iconic conical shape or indeed size of some of its neighbours in Nicaragua. Mighty Momotombo, just 35 km away, seems to define (well, to me) the capital Managua’s skyline. By comparison, Masaya is a relative footnote on the landscape, reaching just over 600 m in elevation. Nonetheless it is to Masaya that myself and other volcanologists flock to work, as it offers a rare natural laboratory to study volcanic processes. Everyday of the year Masaya pumps great quantities of volcanic gases (a noxious cocktail including acidic gases like sulphur dioxide and hydrogen chloride) from its magma interior into the Nicaraguan atmosphere. Furthermore, with the right permissions and safety equipment, you can drive a car directly into this gas plume easily bringing heavy equipment to make measurements. I have heard it described by colleagues as a ‘drive-through’ volcano and while this is not a term I like, as someone who once lugged heavy equipment up 5500 m high Lascar in Chile, I can certainly vouch for its appeal.

Returning for my fifth visit in December 2017 (six years since my last) was like meeting up with an old friend again. There were many familiar sights and sounds: the view of Mombacho volcano from Masaya’s crater rim, the sound of the parakeets returning to the crater at dusk, the pungent smell of the plume that clings to your clothes for days, my favourite view of Momotombo from the main Managua-Masaya road, Mi Viejo Ranchito restaurant – I could go on.

But, as with old friends, there were many changes too. Although in the past I could often hear the magma roaring as it moved under the surface, down the vents, since late 2015 a combination of rock falls and rising lava levels have created a small lava lake visibly churning inside the volcanic crater. This is spectacular in the daytime, but at night the menacing crater glow is mesmerising and the national park is now open to a stream of tourists visiting after dark. Previously, I would scour the ground around the crater for a few glassy fibres and beads of the fresh lava, forced out as bubbles burst from the lava lake (known as Pele’s hairs and tears after the Hawaiian goddess of the volcano – not the footballer) to bring back to analyse. Now the crater edge downwind of the active vent is carpeted with them, and you leave footprints as if it were snow. New instruments and a viewing platform with a webcam have been put in, in place of the crumbling concrete posts where I used to duct-tape up my equipment.

Footprints in the Pele’s hair. Image credit: Tamsin Mather

This time my mission at Masaya was also rather different. Before I had been accompanied solely by scientists but this time I was part of an interdisciplinary team including medics, anthropologists, historians, hazard experts and visual artists. All aligned in the shared aim of studying the impacts of the volcanic gases on the lives and livelihoods of the downwind communities and working with the local agencies to communicate these hazards. Masaya’s high and persistent gas flux, low altitude and ridges of higher ground, downwind of it, mean that these impacts are felt particularly acutely at this volcano. For example, at El Panama, just 3 km from the volcano, which is often noticeably fumigated by the plume, they cannot use nails to fix the roofs of their houses, as they rust too quickly in the volcanic gases.

The team was drawn from Nicaragua, the UK and also Iceland, sharing knowledge between volcano-affected nations. Other members of the team had been there over the previous 12 months, installing air quality monitoring networks, sampling rain and drinking water, interviewing the local people, making a short film telling the people’s stories and scouring the archives for records of the effects of previous volcanic degassing crises at Masaya. Although my expertise was deployed for several days installing new monitoring equipment (the El Crucero Canal 6 transmitter station became our rather unlikely office for part of the week), the main mission of this week was to discuss our results and future plans with the local officials and the communities affected by the plume.

Some of the team working on Masaya: Left to right Dave Lynch, Evgenia Ilyinskaya, Rachel Whitty, Peter Baxter, Tamsin Mather, Jennifer Le Bond, Gudrun Halla Tulinius and Sara Barsotti. Image credit: Tamsin Mather

Having worked at Masaya numerous times, mainly for more esoteric scientific reasons, spending time presenting the very human implications of our findings to the local agencies, charged with monitoring the Nicaraguan environment and hazards, as well managing disasters was a privilege. With their help we ran an information evening in El Panama. This involved squeezing 150 people into the tiny school class room in flickering electric light, rigging up the largest TV I have ever seen from the back of a pick-up and transporting 150 chicken dinners from the nearest fried chicken place! But it also meant watching the community see the film about their lives for the first time, meeting the local ‘stars’ of this film and presenting our work where we took their accounts of how the plume behaves and affects their lives and used our measurements to bring them the science behind their own knowledge.

Workshop at El Panama. Image credit: Tamsin Mather

Watching the film it was also striking to us that for so many of this community it was the first time they had seen the lava lake whose effects they feel daily. Outside the school house there were Pele’s hair on the ground in the playground and whiffs of volcanic gas as the sun set – the volcano was certainly present.  However, particularly watching the film back now sitting at home in the UK, I feel that with this trip, unlike my others before, it is the people of El Panama that get the last word rather than the volcano.

 

 

Blog written by Tamsin Mather (University of Oxford). You can follow the project on Twitter @UNRESPproject. UNRESP project is funded by GCRF Building Resilience programme. 

A little fracture can go a long way: How experiments illuminate our understanding of volcanic eruptions

A little fracture can go a long way: How experiments illuminate our understanding of volcanic eruptions

What controls how violently a volcano erupts?

Stratovolcanoes like Mount St Helens (USA), Gunung Merapi (Indonesia), or Volcán de Colima (Mexico) tend to erupt in two distinct ways: effusively and/or explosively. Effusive eruptions are eruptions where lava is extruded without any major explosions. Although effusive eruptions can be dangerous, at stratovolcanoes they tend to be restricted to volcanic craters and loss of life and property is relatively limited. On the other hand, explosive eruptions tend to be more catastrophic and can devastate local populations and land. What’s peculiar is that stratovolcanoes often switch their eruptive behaviour between effusive and explosive (sometimes during the same eruption!) and volcanologists aren’t totally sure why.

Stratovolcanoes can erupt both explosively and effusively. Mount Sinabung in Indonesia (L) erupting explosively in 2015. Mount St. Helens in the USA (R) in 2006 during a period of effusive eruption. Sinaburg photo credit: SUTANTA ADITYA/AFP. Mount St. Helens photo credit: Willie Scott, USGS.

A lot of processes can affect eruption style, but one that volcanologists spend a lot of time thinking about is how gases build up in and are released from the volcanic system.

Experimental volcanologists, like me, try to address this problem by conducting scalable lab experiments that help reveal the pathways that gases take to the surface. We try to understand how the permeability of the volcanic system – the ease with which the volcanic system allows gas to move within it – changes over time.

Fear the shear

As rising magma travels up through the conduit on its way to the surface, the rigid conduit walls try to slow it down: magma tends to rise more slowly at the conduit’s edges than at its center. A knock-on effect of this is that the stresses acting on the magma – in this case, shear stresses – are largest at the conduit margins. These stresses tend to stretch the magma, sometimes resulting in fracture development and, because of this, a lot of volcanic outgassing (gas release from the system as a whole) is observed at conduit rims. One spectacular example of this type of outgassing event is at Santiaguito volcano in Guatemala where you can sometimes see volcanic gases escaping in an annulus around the conduit:

Shear fractures pose a conundrum: they’re not optimally oriented to direct gases accumulating in the centres of volcanic conduits up towards the surface. To understand how magma deformation can produce escape pathways for gas similar to those seen at Santiaguito volcano, we ran a series of laboratory experiments in which we sheared magma at temperature and pressure conditions relevant to volcanic systems. Using a deformation apparatus, we could shear cylindrical samples of a two-phase magma – containing bubbles and melt – by twisting them.

Our goal was to see if we could make the samples permeable simply by deforming them in shear.

Schematics of our samples before deformation (L) and after deformation (R). The black circles in the starting material are argon bubbles; the white space is the melt. After deformation, the bubbles are stretched in the direction of deformation (as indicated by the red line). The picture shows a sample after deformation; the entire sample surface is covered by an iron jacket that isolates the pore fluid (inside of the sample) from the confining pressure (outside the sample). Image credit: Alex Kushnir.

 

Experiments with a twist

To keep things simple we used a synthetic glass with a composition comparable to natural volcanic products. We also used argon to create bubbles instead of water (since dissolved water can change the melt viscosity and we wanted to keep this parameter constant!). Most importantly of all: we checked that all our samples were impermeable before deformation. In practice, this meant that no gas could travel from the top of the sample to the bottom of the sample.

We found that for samples deformed at low shear strain rates (i.e. low twist rates), the bubbles became very stretched in the direction of shear but never coalesced and, so, the samples never became permeable.

For samples deformed quickly (i.e. high twist rates), bubbles became stretched and again did not coalesce. However, at these high twist rates fractures developed perpendicular to the overall foliation!  Thus the samples deformed at the high twist rates became permeable.

These fractures are well known to structural geologists: Mode I (or extension) fractures. They open in response to a tensile force, which acts to pull the magma apart in the direction of shear. In our study, only samples that were sheared quickly contained these Mode I fractures and became permeable.

Scanning Electron Microscope images of the magma deformed at low twist rates (L) and at high twist rates (R). The arrows show the sense of direction (the top of the photos is being moved to the right) and the dotted red line shows the foliation in the samples. The fracture in (R) is oriented at approximately 90° to the overall sample foliation. Photo credit: Alex Kushnir.

 

Big picture from a tiny sample

We confirmed something that volcanologists have known for a long time: when you deform magma slowly, it tends to relax and flow in response to the applied stress.  But if you deform that same magma quickly, it tends to break.

What’s novel about our study is how the magma broke. If you superimpose a shear zone onto conduit margins, things start to look a bit like this:

Idealized (and definitely not to scale!) schematic of shear-induced fractures near conduit margins. Given the general sense of shear at conduit margins when magma rises, Mode II (or shear) fractures are typically oriented approximately parallel to the conduit margins and directed slightly into the conduit. Mode I (or extension) fractures, on the other hand, are oriented such that they can potentially direct gases from near the centre of conduits upwards and outwards to the surface. Image credit: Alex Kushnir.

In general, the shear fractures run parallel to the conduit margins, which is great for getting gas out of the system, but not so great for grabbing the gas from the centre of the magma column, where it’s expanding and accumulating. That’s where these handy Mode I fractures might come into play. They’re oriented in an optimal direction for sampling the gas in the interior of the magma column and directing the gas upward and outward toward the conduit margins, where they can join a high permeability highway to the surface.

Of course, our samples are tiny compared to a volcano and we aren’t yet able to say how prevalent this process may be. However, our experimental approach shows that you can start to learn a lot about a big problem from a centimeter-scale sample!

Blog written by Alex Kushnir. For more information check out the recent paper. Or get in touch with Alex on twitter.

Update on the Agung volcanic eruption in Indonesia

Update on the Agung volcanic eruption in Indonesia

Since our last blog, Agung has had two months to reflect and has recently begun a strong ash venting process, with incandescence visible at night in the summit. Updates from Magma Indonesia, the official communications hub for natural hazards in Indonesia, have highlighted an elevated level of volcanic tremor and an evacuation zone to 12 km radius around the volcano is being enforced. You can follow Magma Indonesia on twitter, and see regular updates on Agung. To the frustration of anyone wishing to fly in or out of Bali, the ash emissions are heading southwest, towards Bali airport, and so the Indonesian authorities have closed the airport as a preventative measure.On 29th November this restriction was lifted as the prevailing wind was no longer transporting ash towards the airport.

The ash plume is rising to only to 3 km above Agung, which is 6 km above sea level. This is the height where jet aircraft are climbing to cruising altitude with a full fuel load, and so are particularly vulnerable to engine failure due to ash ingestion. There is a possibility to take a ferry to Lombok and fly from there. Rinjani volcano on Lombok erupted last year, resulting in a closure to airspace, but fortunately Rinjani seems to be quiet now. There have been reports of people refusing to leave the evacuated area around Agung. It is always best to follow the instructions of the local authorities during an eruption. The Indonesian volcano evacuations have been very successful in recent years with many thousands saved in a series of timely evacuations from Merapi during its eruption in 2010.

Ash from the Agung eruption is collected by the Indonesian volcano monitoring authorities. Image from Magma Indonesia.

The pattern of activity we have seen to date allows for a direct comparison with that observed during the first days of the 1963 eruption, as reported by Self and Rampino [2012]. Then, there were two days of felt seismic activity followed by explosive activity, associated with a lava emission which eventually produced a 7.5 km long lava flow (after 26 days). The explosive activity produced ash and incandescent material that was ejected to 6 km above the craters. Pyroclastic flows, generated either from the collapsing front of the lava flows or the explosive activity, were visible running down canyons on the north and south flanks. After nearly a month of this activity the eruption ramped up to a significant explosion, generating a plume to  19-26 km altitude above sea level. A further tall eruption column was formed during an explosion ~2 months later, and then mild explosions and lahars continued for several months, before the eruption ended.

Comparing with the current activity, it appears that the 1963 eruption was a lot more energetic in its onset. The incandescent ash venting for some days now has not yet led to a more explosive phase and there is no sign yet of a lava flow. However, the transition could be such that pyroclastic flows appear with little to no warning, hence we must stress the importance of adhering to the evacuation procedures. However, this could change quickly, and the transition could be such that pyroclastic flows appear with insufficient time to escape for anyone within the evacuation zone. How the eruption will develop from here is hard to judge. The most likely evolution would be towards a lava effusion as in 1963, but there could be a sudden transition to explosive activity or, whilst lower probability, cessation of activity.

While the activity is very disruptive for local populations and the economy of Bali due to the impact on tourism of airspace closures, this does afford volcanologists with the opportunity to use the new modern techniques to track the eruption and hopefully gain a better insight into the processes which drive the activity. In this way we will progress towards a better understanding of the relationship between the signals that the volcano produces and the imminent activity, allowing better eruption forecasts. We will update this blog as the eruption evolves.

Novel plume monitoring techniques are being employed by Magma Indonesia.

Blog written by Mike Burton, GMPV President (gmpv@egu.eu), and the GMPV science officer team.