Pyroclastic rock

Rocks from the Bishop Tuff, uncompressed with pumice on left; compressed with fiamme on right.

Flight through a μCT-image stack of a lapillus of the volcano Katla in Iceland. Find spot: Beach near Vik at the end of road 215. Acquisition done using "CT Alpha" by "Procon X-Ray GmbH", Garbsen, Germany. Resolution 11,2μm/Voxel, width approx. 24 mm.

3D-Rendering of the above image stack, in parts transparent. Heavy particles in red.

Pyroclastic rocks are clastic rocks composed of rock fragments produced and ejected by explosive volcanic eruptions. The individual rock fragments are known as pyroclasts. Pyroclastic rocks are a type of volcaniclastic deposit, which are deposits made predominantly of volcanic particles.^[1]^[2] 'Phreatic' pyroclastic deposits are a variety of pyroclastic rock that forms from volcanic steam explosions and they are entirely made of accidental clasts. 'Phreatomagmatic' pyroclastic deposits are formed from explosive interaction of magma with groundwater.^[3] The word pyroclastic is derived from the Greek πῦρ, meaning fire; and κλαστός, meaning broken.^{[citation needed]}

Unconsolidated accumulations of pyroclasts are described as tephra. Tephra may become lithified to a pyroclastic rock by cementation or chemical reactions as the result of the passage of hot gases (fumarolic alteration) or groundwater (e.g. hydrothermal alteration and diagenesis) and burial, or, if it is emplaced at temperatures so hot that the soft glassy pyroclasts stick together at point contacts, and deform: this is known as welding.^[4]

One of the most spectacular types of pyroclastic deposit is an ignimbrite, which is the deposit of a ground-hugging pumiceous pyroclastic density current (a rapidly flowing hot suspension of pyroclasts in gas). Ignimbrites may be loose deposits or solid rock, and they can bury entire landscapes. An individual ignimbrite can exceed 1000 km³ in volume, can cover 20,000 km² of land, and may exceed 1 km in thickness, for example where it is ponded within a volcanic caldera.

Classification

Pyroclasts include juvenile pyroclasts derived from chilled magma, mixed with accidental pyroclasts, which are fragments of country rock. Pyroclasts of different sizes are classified (from smallest to largest) as volcanic ash, lapilli, or volcanic blocks (or, if they exhibit evidence of having been hot and molten during emplacement, volcanic bombs). All are considered to be pyroclastic because they were formed (fragmented) by volcanic explosivity, for example during explosive decompression, shear, thermal decrepitation, or by attrition and abrasion in a volcanic conduit, volcanic jet, or pyroclastic density current.^[5]

Clast size	Pyroclast	Mainly unconsolidated (tephra)	Mainly consolidated: pyroclastic rock
> 64 mm	block (angular) bomb (if fluidal-shaped)	blocks; agglomerate	pyroclastic breccia; agglomerate
< 64 mm	lapillus	lapilli	lapillistone (lapilli-tuff is where lapilli are supported within a matrix of tuff)
< 2 mm	coarse ash	coarse ash	coarse tuff
< 0.063 mm	fine ash	fine ash	fine tuff

Pyroclasts are transported in two main ways: in atmospheric eruption plumes, from which pyroclasts settle to form topography-draping pyroclastic fall layers, and by pyroclastic density currents (PDCs) (including pyroclastic flows and pyroclastic surges),^[6] from which pyroclasts are deposited as pyroclastic density current deposits, which tend to thicken and coarsen in valleys, and thin and fine over topographic highs.

During Plinian eruptions, pumice and ash are formed when foaming silicic magma is fragmented in the volcanic conduit, because of rapid shear driven by decompression and the growth of microscopic bubbles. The pyroclasts are then entrained with hot gases to form a supersonic jet that exits the volcano, admixes and heats cold atmospheric air to form a vigorously buoyant eruption column that rises several kilometers into the stratosphere and cause aviation hazards.^[7] Particles fall from atmospheric eruption plumes and accumulate as layers on the ground, which are described as fallout deposits.^[8]

Pyroclastic density currents arise when the mixture of hot pyroclasts and gases is denser than the atmosphere and so, instead of rising buoyantly, it spreads out across the landscape. They are one of the greatest hazards at a volcano, and may be either 'fully dilute' (dilute, turbulent ash clouds, right down to their lower levels) or 'granular fluid based' (the lower levels of which comprise a concentrated dispersion of interacting pyroclasts and partly trapped gas).^[9] The former type are sometimes called pyroclastic surges (even though they may be sustained rather than "surging") and lower parts of the latter are sometimes termed pyroclastic flows (these, also, can be sustained and quasi steady or surging). As they travel, pyroclastic density currents deposit particles on the ground, and they entrain cold atmospheric air, which is then heated and thermally expands.^[10] Where the density current becomes sufficiently dilute to loft, it rises into the atmosphere as a 'phoenix plume'^[11] (or 'co-PDC plume').^[12] These phoenix plumes typically deposit thin ashfall layers that may contain little pellets of aggregated fine ash.^[13]

Hawaiian eruptions such as those at Kīlauea produce an upward-directed jet of hot droplets and clots of magma suspended in gas; this is called a lava fountain^[14] or 'fire-fountain'.^[15] If sufficiently hot and liquid when they land, the hot droplets and clots of magma may agglutinate to form 'spatter' ('agglutinate'), or fully coalesce to form a clastogenic lava flow.^[14]^[15]

References

^ Fisher, Richard V. (1961). "Proposed classification of volcaniclastic sediments and rocks". Geological Society of America Bulletin. 72 (9): 1409. Bibcode:1961GSAB...72.1409F. doi:10.1130/0016-7606(1961)72[1409:PCOVSA]2.0.CO;2.
^ Fisher, Richard V.; Schmincke, H.-U. (1984). Pyroclastic rocks. Berlin: Springer-Verlag. ISBN 3540127569.
^ Fisher 1961, p. 1409.
^ Schmincke, Hans-Ulrich (2003). Volcanism. Berlin: Springer. p. 138. ISBN 9783540436508.
^ Heiken, G. and Wohletz, K., 1985 Volcanic Ash, University of California Press;, pp. 246.
^ Philpotts, Anthony R.; Ague, Jay J. (2009). Principles of igneous and metamorphic petrology (2nd ed.). Cambridge, UK: Cambridge University Press. p. 73. ISBN 9780521880060.
^ Schmincke 2003, pp. 155–176.
^ Fisher & Schmincke 1984, p. 8.
^ Breard, Eric C.P.; Lube, Gert (January 2017). "Inside pyroclastic density currents – uncovering the enigmatic flow structure and transport behaviour in large-scale experiments". Earth and Planetary Science Letters. 458: 22–36. Bibcode:2017E&PSL.458...22B. doi:10.1016/j.epsl.2016.10.016.
^ Schmincke 2003, pp. 177–208.
^ Sulpizio, Roberto; Dellino, Pierfrancesco (2008). "Chapter 2 Sedimentology, Depositional Mechanisms and Pulsating Behaviour of Pyroclastic Density Currents". Developments in Volcanology. 10: 57–96. doi:10.1016/S1871-644X(07)00002-2. ISBN 9780444531650.
^ Engwell, S.; Eychenne, J. (2016). "Contribution of Fine Ash to the Atmosphere From Plumes Associated With Pyroclastic Density Currents" (PDF). Volcanic Ash: 67–85. doi:10.1016/B978-0-08-100405-0.00007-0. ISBN 9780081004050.
^ Colombier, Mathieu; Mueller, Sebastian B.; Kueppers, Ulrich; Scheu, Bettina; Delmelle, Pierre; Cimarelli, Corrado; Cronin, Shane J.; Brown, Richard J.; Tost, Manuela; Dingwell, Donald B. (July 2019). "Diversity of soluble salt concentrations on volcanic ash aggregates from a variety of eruption types and deposits" (PDF). Bulletin of Volcanology. 81 (7): 39. Bibcode:2019BVol...81...39C. doi:10.1007/s00445-019-1302-0. S2CID 195240304.
^ ^a ^b Macdonald, Gordon A.; Abbott, Agatin T.; Peterson, Frank L. (1983). Volcanoes in the sea : the geology of Hawaii (2nd ed.). Honolulu: University of Hawaii Press. pp. 6, 9, 96–97. ISBN 0824808320.
^ ^a ^b Allaby, Michael, ed. (2013). "Fire-fountain". A dictionary of geology and earth sciences (Fourth ed.). Oxford University Press. ISBN 9780199653065.

Pyroclastic rock

Classification

See also

References

Other reading