Ash

Explosive volcanic eruptions typically eject hot mixtures of fragmented rock (tephra or ash) and volcanic gases into the atmosphere to form a volcanic plume. The most common forms of magma can be divided into three broad types, based on their chemical composition:

1. Basaltic magma (SiO₂ 45-55 wt%; high in Fe, Mg, Ca; low in K, Na)

2. Andesitic magma (SiO₂ 55-65 wt%; intermediate in Fe, Mg, Ca, Na, K)

3. Rhyolitic magma (SiO₂ 65-75%; low in Fe, Mg, Ca; high in K, Na)

Changes in style of activity are common during eruptions, with explosive eruptions being particularly favoured by high (magmatic) gas content, and high melt viscosity (andesitic to rhyolitic magmas), or by the presence of external water (e.g. Sheridan and Wohletz, 1983; Scandone et al., 2007). Volcanic plumes formed by explosive eruptions are mixtures of gas, quenched and fragmented silicate material (tephra) and other aerosol particles derived from both the magmatic emissions and background air (e.g. Durant et al., 2010; Ilyinskaya et al., 2010; Oppenheimer et al 2010). The smaller solid particles (radii < 2 mm) are referred to as volcanic ash. Component and morphological analyses of the erupted ash, and comparison of these data with those from other monitoring techniques, demonstrates a clear relationship between ash features and styles of explosive activity (e.g. Heiken and Wohletz, 1985; Martin et al., 2008; Rust and Cashman, 2011, Taddeucci et al. 2004).

The effects of airborne ash include:

Climate: Injection of volcanic ash into the stratosphere and troposphere influences the Earth’s radiation balance by interacting with both solar and thermal radiation as a function of the ash’s optical properties (IPCC 2007). In the troposphere volcanic aerosols indirectly modify climate by acting as cloud condensation nuclei. This happens over the range of volcanic activity from quiescent degassing (Yuan et al., 2011) to large volcanic eruption plumes.

Aviation: Before March 2010 the Civil Aviation Authority did not permit civil aircraft to fly in the presence of volcanic ash. Following the 2010 Eyjafjallajökull eruption, this zero-tolerance approach was changed to permit flights within ash concentrations less than 2 x 10^-3 g cm^-3 (CAA, 2010).

Human Health: High levels of respirable ash (particle radius less than 5 μm) in the air are not yet known to result in serious injury or disease from inhalation. However acute respiratory symptoms are commonly reported by people during and after ash falls (Blong, 1984)

Heavy ash fall may result in the collapse of roofs under the weight of ash and this can be deadly for people within buildings. The deposition of volcanic ash can increase trace metal (iron) concentrations in the local environment (ocean), especially following explosive eruptions (Martin et al., 2009), and this can increase the productivity of phytoplankton in areas with limited nutrients (Jones and Gislason, 2008; Gabrielli et al., 2008).

Quantifying the effects of ash requires knowledge of ash loading, composition, morphology and size, as well as the physical dimensions and location of the ash plume. In addition, tephra from explosive volcanic eruptions holds information about magma dynamics in the critical zone where fragmentation occurs and eruption style is decided.

The infrared (IR) transmission or emission spectra of volcanic plumes shows a rapid variation with wavelength due to absorption lines from atmospheric and volcanic gases as well as broad scale features principally due to particulate absorption. While the gas lines have provided important insights into volcanic processes (Burton et al., 2001, 2003; Oppenheimer et al., 2006; Edmonds, 2003, Sawyer et al 2008) the ash features have not been analysed to the same extent. The ash signature depends on the composition and size distribution of ash particles.

Figure 1. Extinction coefficients obtained for ice, volcanic ash (Peters, 2012), pumice, andesite, H2SO4, quartz, chlorite, obsidian.

Figure 1 shows an example of different extinction coefficients computed using the same size-distribution (with an effective radius of 2 μm) and different refractive indexes.

The published infrared spectral refractive index of volcano-related ash and rock shows a large variability, presumably because the ash composition is changing. This is reflected in the variability of IR spectra measured from satellites for different volcanoes and eruptions (Clarisse, 2010; Gangale, 2010).

Satellite data

Different instruments (and platform) can be used for ash analysis:

Polar Orbiting Satellites (LEO)

Instrument	Platform	Agency	Service Start	Service End
Imagers
AVHRR	TIROS-N; NOAA-6 to 19; MetOp-A	NOAA / ESA	1978	Present
ATSR-2	ERS-2	ESA	1995	Present
ASTER	EOS-Terra	NASA	2000	Present
AATSR	ENVISAT	ESA	2002	03/2012
MERIS	ENVISAT	ESA	2002	03/2012
MODIS	EOS-Terra EOS-Aqua	NASA	2000 2002	Present Present
Lidar
CALIPO	CALIPSO	NASA	2006	Present
IR Spectrometers
AIRS	EOS-Aqua	NASA	2002	Present
TES	EOS-Aura	NASA	2004	Present
IASI	MetOp-A MetOp-B	ESA	2006 2012	Present Present
Limb/Occultation Instruments
SAGE
SAGE-2			1984
MIPAS	ENVISAT	ESA	2002	03/2012
HIRDLS	EOS-Aura	NASA	2004	Present
UV/VIS spectrometers
GOME	ERS-2	ESA	1995
SCIAMACHY	ENVISAT	ESA	2002	03/2012
OMI	EOS-Aura	NASA	2004	Present
GOME-2	MetOp-A	ESA	2006	Present

Satellite data

Different instruments (and platform) can be used for ash analysis:

Geostationary satellites (GEO)

Instrument	Platform	Agency	Service Start	Service End
Imagers
SEVIRI	MSG-8 MSG-9 MSG-10	ESA	08/2002 12/2005 07/2012	~2019 ~2021 ~2022
Sounder/Imager	GOES	NOAA	1983	Present
MTSAT-1R MTSAT-2		JAXA	2005 2010	2010 Present
Limb/Occultation Instruments
SAGE
SAGE-2			1984

See Also

Near real time SEVIRI RGB Composites Ash
Volcanic Ash Spectroscopy
ARIA refractive index database