Magma‐driven subcritical crack growth and implications for dike initiation from a magma chamber

Chen, Zuan; Jin, Z.-H.

doi:10.1029/2006gl026979

Cited by 13 publications

(8 citation statements)

References 17 publications

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“…The rheology of magma chamber wall rocks will be strongly affected by prolonged heating, and thus critical brittle fracture may not be the dominant mode of initial chamber rupture. Anelastic processes, such as the viscous blunting of dike tips, and viscoelastic relaxation of deviatoric stresses around the chamber have been shown to strongly affect the initiation and propagation of cracks [e.g., Dragoni and Magnanensi , 1989; Jellinek and DePaolo , 2003; Chen and Jin , 2006]. However, these processes are not straightforward to quantify, so other criteria are currently more reliable for estimating maximum chamber overpressures.…”

Section: Magma Chamber Overpressurementioning

confidence: 99%

Organization of volcanic plumbing through magmatic lensing by magma chambers and volcanic loads

2009

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[1] The development of discrete volcanic centers reflects a focusing of magma ascending from the source region to the surface. We suggest that this organization occurs via mechanical interactions between magma chambers, volcanic edifices, and dikes and that the stresses generated by these features may localize crustal magma transport before the first eruption occurs. We develop a model for the focusing or ''lensing'' of rising dikes by magma chambers beneath a free surface, and we show that chambers strongly modulate dike focusing by volcanic edifices. We find that the combined mechanical effects of chambers, edifice loading, and dike propagation are strongly coupled. Chambers deeper than $20 km below the surface with magmatic overpressure in the range of 20-100 MPa should dominate dike focusing, while more shallow systems are affected by both edifice and chamber focusing.

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Section: Magma Chamber Overpressurementioning

confidence: 99%

Organization of volcanic plumbing through magmatic lensing by magma chambers and volcanic loads

2009

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“…1, where a = a ( t ) denotes the crack length and t is time. This 2‐D dyke propagation model has been adopted in a number of studies, for example, Rubin (1995a,b), Roper & Lister (2005) and Chen & Jin (2006).…”

Section: Theoretical Modelsmentioning

confidence: 99%

“…1, where a = a(t) denotes the crack length and t is time. This 2-D dyke propagation model has been adopted in a number of studies, for example, Rubin (1995a,b), Roper & Lister (2005) and Chen & Jin (2006). Dyke propagation is driven by the net pressure on its surfaces due to magma flow, lithostatic stress and tectonic stress.…”

Section: Magma Pressure Along the Dyke Surfacesmentioning

confidence: 99%

“…Rubin (1998) examined subcritical crack growth in partially molten rocks from a surface energy point of view. Chen & Jin (2006) investigated subcritical dyke growth from a crustal magma chamber. Using a viscoelastic energy dissipation approach without considering temperature-dependent viscoelastic properties, they obtained the relationship between the subcritical propagation velocity and dyke length, and found that dykes grow at velocities on the order of 10 −8 -10 −6 m s -1 .…”

Section: Introductionmentioning

confidence: 99%

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Subcritical dyke propagation in a host rock with temperature-dependent viscoelastic properties

Chen

Jin

2011

Geophysical Journal International

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S U M M A R YIn this paper, we examine the effects of temperature-dependent viscoelastic properties of the host rock on the subcritical growth of a dyke from a magma chamber. A theoretical relationship between the velocity of subcritical dyke growth and dyke length is established using a perturbation solution of stress intensity factor at the dyke tip and a viscoelastic crack growth theory in which the temperature-dependent creep properties are taken into account. The temperature field around the dyke is calculated using an analytic solution. The numerical results for a dyke subcritically propagating from a magma chamber indicate that while the general dyke growth characteristics are similar to those with constant creep properties, the subcritical dyke growth velocity is increased by an order of magnitude by considering the temperature dependence of the creep properties. Hence, the subcritical growth duration before the dyke reaches the unstable growth state is significantly shortened.

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“…Others relate dyke propagation rates to the stress intensity factor (e.g. Anderson & Grew 1977; Atkinson 1987; Chen & Jin 2006). Attempts have been made to account for the process zone surrounding the tip of the propagating dyke (e.g.…”

Section: Introductionmentioning

confidence: 99%

The propagation of a dyke driven by gas-saturated magma

Maimon

Lyakhovsky

Melnik

et al. 2012

Geophysical Journal International

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S U M M A R YA new mathematical and numerical model is presented for the propagation of a pressure-and buoyancy-driven dyke filled with volatile-saturated magma and a gas cap at its upper part. The model accounts for coupling between conduit flow of a bubbly magma, gas filtration through the magma, gas accumulation in a gas cap and elastic deformation and fracturing of the host rock. All these processes allow studying different regimes of dyke propagation. The rate of propagation of dykes is controlled by the rate of the fracturing at the tip and by the flow rate of magma inside the dyke. When high energy is needed to fracture the host rock and magma viscosity is low, the rate of propagation is controlled by the rate of fracturing (fracturecontrolled regime). When the energy to fracture the host rock is low, propagation is controlled by the magma flow rate (magma-controlled regime). We study the transition between these regimes for the case of a constant magma vesicularity and constant mass of gas in the cap. Under these conditions, the propagation of the dyke is self-similar. In the fracture-controlled regime the propagation rate only weakly depends on the amount of the gas in the gas cap, whereas at the magma-controlled regime it is significantly enhanced with increase the mass of gas at the cap. The gas pressure in the cap opens the dyke in front of the magma and allows magma flow rates that are significantly higher than predicted by models that ignore the gas cap. The maximum propagation rate is obtained at the transition between the fracture-and magma-controlled regimes. If the gas mass in the gas cap is high enough, a gas pocket can separate from the magma as a distinct unconnected pocket and propagate as a gas-filled crack at a constant velocity. Pressure decreases during ascent leads to higher vesicularity and faster gas filtration through the magma and into a gas cap. Gradual increase of the mass of gas in the cap is important in accelerating the propagation rate of dykes.

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Magma‐driven subcritical crack growth and implications for dike initiation from a magma chamber

Cited by 13 publications

References 17 publications

Organization of volcanic plumbing through magmatic lensing by magma chambers and volcanic loads

Organization of volcanic plumbing through magmatic lensing by magma chambers and volcanic loads

Subcritical dyke propagation in a host rock with temperature-dependent viscoelastic properties

The propagation of a dyke driven by gas-saturated magma

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