Structure of volcano plumbing systems: A review of multi-parametric effects

Tibaldi, Alessandro

doi:10.1016/j.jvolgeores.2015.03.023

Cited by 141 publications

(96 citation statements)

References 425 publications

(266 reference statements)

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“…Multiple factors combining to generate such composite fields have been advocated and analyzed: loading due to the edifice (e.g., Dahm, 2000;Pinel and Jaupart, 2000;Maccaferri et al, 2011) and unloading (e.g., Maccaferri et al, 2014), the effects of volcano morphology (e.g., Tibaldi et al, 2014;Corbi et al, 2015), the generation of magma reservoirs and calderas (e.g., Tibaldi, 2015) and the anisotropy of host rocks (Gudmundsson, 2011a). Many dykes do not propagate all the way to the surface, but may be arrested by layers with variable associated stress (Gudmundsson and Philipp, 2006).…”

Section: Factors That Could Affect Stress and Strain In The Earsmentioning

confidence: 99%

Historical Volcanism and the State of Stress in the East African Rift System

et al. 2016

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Crustal extension at the East African Rift System (EARS) should, as a tectonic ideal, involve a stress field in which the direction of minimum horizontal stress is perpendicular to the rift. A volcano in such a setting should produce dykes and fissures parallel to the rift. How closely do the volcanoes of the EARS follow this? We answer this question by studying the 21 volcanoes that have erupted historically (since about 1800) and find that 7 match the (approximate) geometrical ideal. At the other 14 volcanoes the orientation of the eruptive fissures/dykes and/or the axes of the host rift segments are oblique to the ideal values. To explain the eruptions at these volcanoes we invoke local (non-plate tectonic) variations of the stress field caused by: crustal heterogeneities and anisotropies (dominated by NW structures in the Protoerozoic basement), transfer zone tectonics at the ends of offset rift segments, gravitational loading by the volcanic edifice (typically those with 1-2 km relief) and magmatic pressure in central reservoirs. We find that the more oblique volcanoes tend to have large edifices, large eruptive volumes, and evolved and mixed magmas capable of explosive behavior. Nine of the volcanoes have calderas of varying ellipticity, 6 of which are large, reservoir-collapse types mainly elongated across rift (e.g., Kone) and 3 are smaller, elongated parallel to the rift and contain active lava lakes (e.g., Erta Ale), suggesting different mechanisms of formation and stress fields. Nyamuragira is the only EARS volcano with enough sufficiently well-documented eruptions to infer its long-term dynamic behavior. Eruptions within 7 km of the volcano are of relatively short duration (<100 days), but eruptions with more distal fissures tend to have lesser obliquity and longer durations, indicating a changing stress field away from the volcano. There were major changes in long-term magma extrusion rates in 1977 (and perhaps in 2002) due to major along-rift dyking events that effectively changed the Nyamuragira stress field and the intrusion/extrusion ratios of eruptions.

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Section: Factors That Could Affect Stress and Strain In The Earsmentioning

confidence: 99%

Historical Volcanism and the State of Stress in the East African Rift System

et al. 2016

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“…An overpressured dyke exerts tensile stresses along its tip line, which are capable of producing an advancing fracture; once the fracture has formed, the magma intrudes along it and the dyke propagates (review in Tibaldi (2015), and reference therein). If a fracture already exists and has a suitable orientation with respect to the horizontal regional least principal stress (σ 3 ), dyke intrusion is facilitated.…”

Section: Role Of Magma Intrusionsmentioning

confidence: 99%

Interaction between Transform Faults and Rift Systems: A Combined Field and Experimental Approach

2016

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We present a detailed field structural survey of the area of interaction between the active NW-striking transform Husavik-Flatey Fault (HFF) and the N-S Theystareykir Fissure Swarm (TFS), in North Iceland, integrated by analog scaled models. Field data contribute to a better understanding of how transform faults work, at a much higher detail than classical marine geophysical studies. Analog experiments are conducted to analyse the fracture patterns resulting from different possible cases where transform faulting accompanies or postpones the rift motions. Different tectonic block configurations are also considered and results are compared with field data in order to study as thoroughly as possible the interaction between the HFF and the TFS as well as the possible prolongation of the HFF into the TFS. West of the intersection between the transform fault (HFF) and the rift zone (TFS), the former splays with a gradual bending giving rise to a leading extensional imbricate fan. The westernmost structure of the rift, the N-S Gudfinnugja Fault (GF), is divided into two segments: the southern segment makes a junction with the HFF and is part of the imbricate fan; north of the junction instead, the northern GF appears right-laterally offset by about 20 m. Southeast of the junction, along the possible prolongation of the HFF across the TFS, the strike of the rift faults rotates in an anticlockwise direction, attaining a NNW-SSE orientation. Moreover, the TFS faults north of the HFF prolongation are fewer and have smaller offsets than those located to the south. Through the comparison between the structural data collected in the field at the HFF-TFS connection zone and a set of scaled experiments, we confirm a prolongation of the HFF through the rift, although here the transform fault has a much lower slip-rate than west of the junction. Our data suggest that transform fault terminations may be more complex than previously known, and propagate across a rift through a modification of the rift pattern.

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“…Delineating plumbing system structure can therefore provide important insights into: (1) continental rifting (e.g., Ebinger and Casey, 2001;Kendall et al, 2005;White et al, 2008;Ebinger et al, 2010); (2) total melt volume estimates, which can be used to assess the thermomechanical state of the mantle (White et al, 2008;Ferguson et al, 2010); (3) the physiochemical evolution of magma (e.g., Holness and Humphreys, 2003;Cashman and Sparks, 2013); (4) host-rock deformation induced by magma intrusion, which may be expressed at the Earth's surface (e.g., Wright et al, 2006;Biggs et al, 2009;Pagli et al, 2012;Jackson et al, 2013;Magee et al, 2013a;Tibaldi, 2015); and (5) volcanic eruption locations and styles (e.g., Abebe et al, 2007;Gaffney et al, 2007;Mazzarini, 2007;Tibaldi, 2015;Muirhead et al 2016). However, the inaccessibility of active plumbing systems and limitations in exposure at the Earth's surface makes reconstructing the geometry and connectivity of regionally extensive intrusion networks from field outcrops challenging.…”

Section: Introductionmentioning

confidence: 99%

“…In order to delimit plumbing systems, it is therefore important to integrate field observations with data and imaging techniques that probe magma pathways and storage in the subsurface (Tibaldi, 2015). Indirect analytical approaches commonly involve: (1) the examination of ground deformation patterns (e.g., using InSAR, interferometric synthetic aperture radar) inferred to relate to the emplacement of magma (e.g., Pedersen, 2004;Wright et al, 2006;Pagli et al, 2012;Sparks et al, 2012); (2) scrutiny of petrological and geochemical data to assess magma contamination, residence times, crystallization histories, and melt source conditions (Cashman and Sparks, 2013, and references therein); and/or (3) mapping the location and crude geometry of crystallized intrusions or present-day zones of melt using geophysical techniques such as potential field, magnetotellurics, and seismicity (e.g., Cornwell et al, 2006;Whaler and Hautot, 2006;Desissa et al, 2013).…”

Section: Introductionmentioning

confidence: 99%

“…While numerous studies document vertical magma transport in dike-dominated volcanic plumbing systems (e.g., Kendall et al, 2005;Keir et al, 2006;Wright et al, 2006;Corti, 2009;Bastow et al, 2010;Cashman and Sparks, 2013;Muirhead et al, 2015;Tibaldi, 2015), it is also widely accepted that lateral magma flow can occur either within individual plumbing systems where volcanoes may be laterally offset by as much as ~20 km from their magma reservoir (e.g., Fig. 1A; e.g., Curtis, 1968;Cartwright and Hansen, 2006;Gudmundsson, 2006;Aoki et al, 2013;Aizawa et al, 2014;Muirhead et al, 2014;Tibaldi, 2015) or giant radiating dike swarms, which can facilitate lateral magma flow over hundreds to thousands of kilometers (e.g., Ernst and Baragar, 1992;Ernst et al, 1995;Macdonald et al, 2010).…”

Section: Introductionmentioning

confidence: 99%

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Lateral Magma Flow in Mafic Sill‐complexes

Magee

Muirhead

Karvelas

et al. 2016

Acta Geologica Sinica (Eng)

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The structure of upper crustal magma plumbing systems controls the distribution of volcanism and influences tectonic processes. However, delineating the structure and volume of plumbing systems is difficult because (1) active intrusion networks cannot be directly accessed; (2) field outcrops are commonly limited; and (3) geophysical data imaging the subsurface are restricted in areal extent and resolution. This has led to models involving the vertical transfer of magma via dikes, extending from a melt source to overlying reservoirs and eruption sites, being favored in the volcanic literature. However, while there is a wealth of evidence to support the occurrence of dike-dominated systems, we synthesize field-and seismic reflection-based observations and highlight that extensive lateral magma transport (as much as 4100 km) may occur within mafic sill complexes. Most of these mafic sill complexes occur in sedimentary basins (e.g., the Karoo Basin, South Africa), although some intrude crystalline continental crust (e.g., the Yilgarn craton, Australia), and consist of interconnected sills and inclined sheets. Sill complex emplacement is largely controlled by host-rock lithology and structure and the state of stress. We argue that plumbing systems need not be dominated by dikes and that magma can be transported within widespread sill complexes, promoting the development of volcanoes that do not overlie the melt source. However, the extent to which active volcanic systems and rifted margins are underlain by sill complexes remains poorly constrained, despite important implications for elucidating magmatic processes, melt volumes, and melt sources.

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Structure of volcano plumbing systems: A review of multi-parametric effects

Cited by 141 publications

References 425 publications

Historical Volcanism and the State of Stress in the East African Rift System

Historical Volcanism and the State of Stress in the East African Rift System

Interaction between Transform Faults and Rift Systems: A Combined Field and Experimental Approach

Lateral Magma Flow in Mafic Sill‐complexes

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