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Breadcrust Bombs As Indicators of Vulcanian Eruption Dynamics at Guagua Pichincha Volcano, Ecuador

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Breadcrust Bombs As Indicators of Vulcanian Eruption Dynamics at Guagua Pichincha Volcano, Ecuador Bull Volcanol (2007) 69: 281–300 DOI 10.1007/s00445-006-0073-6 RESEARCH ARTICLE Heather M. N. Wright . Katharine V. Cashman . Mauro Rosi . Raffaello Cioni Breadcrust bombs as indicators of Vulcanian eruption dynamics at Guagua Pichincha volcano, Ecuador Received: 2 May 2005 / Accepted: 24 March 2006 / Published online: 7 July 2006 # Springer-Verlag 2006 Abstract Vulcanian eruptions are common at many resultant bombs are dense. At pre-fragmentation melt volcanoes around the world. Vulcanian activity occurs as H2O contents of >~0.9 wt%, only glassy rinds are dense either isolated sequences of eruptions or as precursors to and bomb interiors vesiculate after fragmentation. For sustained explosive events and is interpreted as clearing of matrix glass H2O contents of ≥1.4 wt%, rinds are thin and shallow plugs from volcanic conduits. Breadcrust bombs vesicular instead of thick and non-vesicular. A maximum characteristic of Vulcanian eruptions represent samples of measured H2O content of 3.1 wt% establishes the maxi- different parts of these plugs and preserve information that mum pressure (63 MPa) and depth (2.5 km) of magma that can be used to infer parameters of pre-eruption magma may have been tapped during a single eruptive event. More ascent. The morphology and preserved volatile contents of common H2O contents of ≤1.5 wt% suggest that most breadcrust bombs erupted in 1999 from Guagua Pichincha eruptions involved evacuation of ≤1.5 km of the conduit. volcano, Ecuador, thus allow us to constrain the physical As we expect that substantial overpressures existed in the processes responsible for Vulcanian eruption sequences of conduit prior to eruption, these depth estimates based on this volcano. Morphologically, breadcrust bombs differ in magmastatic pressure are maxima. Moreover, the presence the thickness of glassy surface rinds and in the orientation of measurable CO2 (≤17 ppm) in quenched glass of highly and density of crack networks. Thick rinds fracture to degassed magma is inconsistent with simple models of create deep, widely spaced cracks that form large either open- or closed-system degassing, and leads us rectangular domains of surface crust. In contrast, thin instead to suggest re-equilibration of the melt with gas rinds form polygonal networks of closely spaced shallow derived from a deeper magmatic source. Together, these cracks. Rind thickness, in turn, is inversely correlated with observations suggest a model for the repeated Vulcanian matrix glass water content in the rind. Assuming that all eruptions that includes (1) evacuation of the shallow rinds cooled at the same rate, this correlation suggests conduit during an individual eruption, (2) depressurization increasing bubble nucleation delay times with decreasing of magma remaining in the conduit accompanied by open- pre-fragmentation water content of the melt. A critical system degassing through permeable bubble networks, (3) bubble nucleation threshold of 0.4–0.9 wt% water exists, rapid conduit re-filling, and (4) dome formation prior to the below which bubble nucleation does not occur and subsequent explosion. An important part of this process is densification of upper conduit magma to allow repressur- Editorial responsibility: J. White ization between explosions. At a critical overpressure, trapped pressurized gas fragments the nascent impermeable . H. M. N. Wright (*) K. V. Cashman cap to repeat the process. Department of Geological Sciences, University of Oregon, Eugene, OR 97403-1272, USA . e-mail: [email protected] Keywords Breadcrust bomb Vulcanian Water content Tel.: +1-541-3465987 Degassing . Permeability Fax: +1-541-3464692 M. Rosi Dipartimento Scienze della Terra, University Pisa, Introduction Via S. Maria 53, I-56126 Pisa, Italy Vulcanian eruptions are short (seconds to minutes), violent outbursts that eject relatively small volumes of magma R. Cioni 3 Dipartimento Scienze della Terra, University Cagliari, (<1 km ; Morrissey and Mastin 2000). These eruptions Via Trentino 51, may occur either as a series of discrete events or as I-09124 Cagliari, Italy precursors to sustained subplinian or Plinian eruptions 282 (e.g., Nairn and Self 1978; Druitt et al. 2002). High glassy rinds to suggest that breadcrust bombs produced by pyroclast ejection velocities during individual events disruption of the cryptodome at Mount St. Helens, WA, (≤400 m/s; Morrissey and Mastin 2000) reflect high mass 1980, resulted from pre-eruptive magma degassing that eruption rates that result from gas pressurization within the produced a sufficient delay in syn-eruptive bubble conduit (Chouet et al. 1994; Cruz and Chouet 1997; nucleation to allow rind formation. In a different volcanic Arciniega-Ceballos et al. 1999). Resultant volcanic plumes setting, Polacci et al. (2001) proposed that breadcrusting of can reach up to several km in height for a single eruption or pumiceous clasts produced during the June 15 climactic up to 20 km for repeated eruptions and produce moderately eruption of Pinatubo volcano, 1991, was promoted by dispersed deposits (Morrissey and Mastin 2000). Vulca- locally high temperatures and lower volatile content. nian eruptions may generate pyroclastic avalanches, Additionally, Yamagishi and Feebrey (1994) hypothesized pyroclastic flows, block and ash flows, distal, thin ash that unusual breadcrust bombs with vesicular outer rinds falls, and proximal, often breadcrusted ballistic blocks and dense interiors from Tokachidake volcano, Japan, (e.g., Vougioukalakis 1995). Of these, breadcrusted clasts reflect pre-eruptive magma degassing along cracks beneath are particularly characteristic of Vulcanian eruptive styles. an impermeable cap. Although different in specifics, all A long-standing question about Vulcanian eruptions is three recent models for vulcanian breadcrust-bomb forma- whether the overpressures required to drive these explo- tion require some amount of pre-eruptive volatile loss. sions result solely from the accumulation of magmatic What conditions promote the pre-eruptive degassing and volatiles beneath an impermeable cap (e.g., Turcotte et al. pressurization apparently required to produce Vulcanian 1990; Fagents and Wilson 1993; Clarke et al. 2002)or explosions? Despite the frequency of Vulcanian eruptions whether they require interaction of magma with external at volcanoes with actively growing lava domes of water (e.g., Schmincke et al. 1990; Capra et al. 1998). Early intermediate to silicic compositions, and the real hazard estimates of ballistic block ejection velocities of ≤600 m/s they pose, the physical processes responsible for this type (Fudali and Melson 1972; Self et al. 1979) were too high to of activity are poorly understood. In particular, there are be produced by magmatic gases alone, thus involvement of few constraints on processes that modulate the observed external water was invoked to explain particularly violent cyclic behavior (an exception being the well-documented events (Melson and Saenz 1974; Self et al. 1979; Fisher events at Soufrière Hills Volcano, Montserrat, e.g., Druitt et and Schmincke 1984; Francis 1993; Woods 1995). How- al. 2002; Edmonds et al. 2003; Formenti et al. 2003). Here ever, new models of ballistic behavior reduce these velocity we use abundant and variably breadcrusted bombs estimates by half, although gas velocity itself may be produced during activity at Guagua Pichincha volcano, higher than ballistic ejection velocity (Fagents and Wilson Ecuador, in late 1999 to examine processes responsible for 1993; Morrissey and Mastin 2000). These models require Vulcanian activity of this system. Furthermore, the char- overpressures of only ~10–20 MPa, overpressures achiev- acteristic association of breadcrust bombs with Vulcanian able by a combination of decompression-induced degas- eruptions (e.g., Morrissey and Mastin 2000) suggests that a sing, groundmass crystallization, and permeable gas study of bomb formation should provide important insight migration beneath an impermeable barrier (Nakada et al. into the general nature of Vulcanian explosive activity. 1995; Sparks 1997; Stix et al. 1997; Barmin et al. 2002; Melnik and Sparks 2002; Edmonds et al. 2003). Like the explosions that produce them, breadcrust The 1999 eruptions of Guagua Pichincha volcano bombs have been variably interpreted to reflect either quenching of magma by external water (e.g., Fisher and Guagua Pichincha is a dacitic stratovolcano located 12 km Schmincke 1984; Francis 1993) or delayed vesiculation of west of Quito, Ecuador (Fig. 1), in the Central Volcanic partially degassed magma (e.g., Turcotte et al. 1990; Zone of the South American Andes. It has been active for Hoblitt and Harmon 1993; Yamagishi and Feebrey 1994). the past 50,000 years, evolving into its current eruptive Studies that invoke a magmatic origin for this bomb type phase almost 12,000 years ago. Early phases were vary in explanations of the mechanism by which dominated by effusive eruptions that formed the lava breadcrusting occurs. Exterior cracking (and resultant cone, slope failure and formation of a breached amphithe- crack patterns) may occur (1) as a result of interior ater, and subsequent effusive and explosive eruptions from expansion of a bomb with a quenched exterior rind, (2) in the central vent in the amphitheater (Barberi et al. 1992). response to thermal contraction of the outer surface, or (3) Holocene eruption styles at Guagua Pichincha volcano from stresses applied during impact. In his original study of have been dominantly explosive
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