Littérature scientifique sur le sujet « Magma chamber dynamics »
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Articles de revues sur le sujet "Magma chamber dynamics"
1
Segall, Paul. « Magma chambers : what we can, and cannot, learn from volcano geodesy ». Philosophical Transactions of the Royal Society A : Mathematical, Physical and Engineering Sciences 377, no 2139 (7 janvier 2019) : 20180158. http://dx.doi.org/10.1098/rsta.2018.0158.
Texte intégralRésumé :
Geodetic observations on volcanoes can reveal important aspects of crustal magma chambers. The rate of decay of deformation with distance reflects the centroid depth of the chamber. The amplitude of the deformation is proportional to the product of the pressure change and volume of the reservoir. The ratio of horizontal to vertical displacement is sensitive to chamber shape: sills are efficient at generating vertical displacement, while stocks produce more horizontal deformation. Geodesy alone cannot constrain important parameters such as chamber volume or pressure; furthermore, kinematic models have no predictive power. Elastic response combined with influx proportional to pressure gradient predicts an exponentially decaying flux, leading to saw-tooth inflation cycles observed at some volcanoes. Yet many magmatic systems exhibit more complex temporal behaviour. Wall rock adjacent to magma reservoirs cannot behave fully elastically. Modern conceptual models of magma chambers also include cumulate and/or mush zones, with potentially multi-level melt lenses. A viscoelastic shell surrounding a spherical magma chamber significantly modifies the predicted time-dependent response; post-eruptive inflation can occur without recharge if the magma is sufficiently incompressible relative to the surrounding crust (Segall P. 2016 J. Geophys. Res. Solid Earth , 121 , 8501–8522). Numerical calculations confirm this behaviour for both oblate and prolate ellipsoidal chambers surrounded by viscoelastic aureoles. Interestingly, the response to a nearly instantaneous pressure drop during an explosive eruption can be non-monotonic as the rock around the chamber relaxes at different rates. Pressure-dependent recharge of a non-Newtonian magma in an elastic crust leads to an initially high rate of inflation which slows over time; behaviour that has been observed in some magmatic systems. I close by discussing future challenges in volcano geodesy. This article is part of the Theo Murphy meeting issue ‘Magma reservoir architecture and dynamics’.
2
Townsend, Meredith, et Christian Huber. « A critical magma chamber size for volcanic eruptions ». Geology 48, no 5 (6 février 2020) : 431–35. http://dx.doi.org/10.1130/g47045.1.
Texte intégralRésumé :
Abstract We present a model for a coupled magma chamber–dike system to investigate the conditions required to initiate volcanic eruptions and to determine what controls the size of eruptions. The model combines the mechanics of dike propagation with internal chamber dynamics including crystallization, volatile exsolution, and the elastic response of the magma and surrounding crust to pressure changes within the chamber. We find three regimes for dike growth and eruptions: (1) below a critical magma chamber size, eruptions are suppressed because chamber pressure drops to lithostatic before a dike reaches the surface; (2) at an intermediate chamber size, the erupted volume is less than the dike volume (“dike-limited” eruption regime); and (3) above a certain chamber size, dikes can easily reach the surface and the erupted volume follows a classic scaling law, which depends on the attributes of the magma chamber (“chamber-limited” eruption regime). The critical chamber volume for an eruption ranges from ∼0.01 km3 to 10 km3 depending on the water content in the magma, depth of the chamber, and initial overpressure. This implies that the first eruptions at a volcano likely are preceded by a protracted history of magma chamber growth at depth, and that the crust above the magma chamber may have trapped several intrusions or “failed eruptions.” Model results can be combined with field observations of erupted volume, pressure, and crystal and volatile content to provide tighter constraints on parameters such as the eruptible chamber size.
3
Huppert, Herbert E., et Andrew W. Woods. « The role of volatiles in magma chamber dynamics ». Nature 420, no 6915 (décembre 2002) : 493–95. http://dx.doi.org/10.1038/nature01211.
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Carrigan, Charles R., et Randall T. Cygan. « Implications of magma chamber dynamics for Soret-related fractionation ». Journal of Geophysical Research 91, B11 (1986) : 11451. http://dx.doi.org/10.1029/jb091ib11p11451.
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Asmerom, Yemane, S. Andrew DuFrane, Samuel B. Mukasa, Hai Cheng et R. Lawrence Edwards. « Time scale of magma differentiation in arcs from protactinium-radium isotopic data ». Geology 33, no 8 (1 août 2005) : 633–36. http://dx.doi.org/10.1130/g21638ar.1.
Texte intégralRésumé :
Abstract Absolute chronology of magma differentiation processes has been a long-desired goal, given its importance in understanding magma chamber dynamics and its connection to a fundamental understanding of the style and frequency of volcanic eruptions. Broad estimates of the duration of magma differentiation and overall crustal residence times have been made based on a variety of indirect approaches, such as physical models of magma chamber cooling, rates of crystal growth and settling, and long-lived radiogenic isotopes. In contrast, combined 231Pa-235U data may provide a robust measure of the time scale of magma differentiation. Based on 231Pa-235U, 230Th-238U and 226Ra-230Th data from Taal volcano, Luzon Arc, Philippine Archipelago, we show that 231Pa-235U data may provide a robust direct measure of the time scale of magma differentiation. A closed-system magma fractionation model gives a 231Pa-235U differentiation time scale in the range of 30 k.y., while the 226Ra-230Th time scale is considerably younger. The time scales are reconciled if we consider either fluid-mixing or magma-mixing models. The fluid-mixing model gives a time scale of differentiation similar to the 231Pa-235U closed-system time scale and is supported by the 230Th-238U data. The magma-mixing model gives a considerably longer time, in the range of 55 k.y. The combined observations support the robustness of the 231Pa-235U chronology, indicating a differentiation time scale in the range of 30 k.y., although this time scale for other volcanoes may vary depending on size and thermal state of the magma chamber. The 226Ra-230Th closed-system model ages, which yield much younger estimates for magma differentiation, are not likely to reflect time scales of magma differentiation.
6
Sigmarsson, O., I. Vlastelic, R. Andreasen, I. Bindeman, J. L. Devidal, S. Moune, J. K. Keiding, G. Larsen, A. Höskuldsson et Th Thordarson. « Remobilization of silicic intrusion by mafic magmas during the 2010 Eyjafjallajökull eruption ». Solid Earth 2, no 2 (2 décembre 2011) : 271–81. http://dx.doi.org/10.5194/se-2-271-2011.
Texte intégralRésumé :
Abstract. Injection of basaltic magmas into silicic crustal holding chambers and subsequent magma mingling or mixing is a process that has been recognised since the late seventies as resulting in explosive eruptions. Detailed reconstruction and assessment of the mixing process caused by such intrusion is now possible because of the exceptional time-sequence sample suite available from the tephra fallout of the 2010 summit eruption at Eyjafjallajökull volcano in South Iceland. Fallout from 14 to 19 April contains three glass types of basaltic, intermediate, and silicic compositions recording rapid magma mingling without homogenisation, involving evolved FeTi-basalt and silicic melt with composition identical to that produced by the 1821–1823 AD Eyjafjallajökull summit eruption. The time-dependent change in the magma composition suggests a binary mixing process with changing end-member compositions and proportions. Beginning of May, a new injection of primitive basalt was recorded by deep seismicity, appearance of Mg-rich olivine phenocrysts together with high sulphur dioxide output and presence of sulphide crystals. Thus, the composition of the basaltic injection became more magnesian and hotter with time provoking changes in the silicic mixing end-member from pre-existing melt to the solid carapace of the magma chamber. Finally, decreasing proportions of the mafic end-member with time in the erupted mixed-magma demonstrate that injections of Mg-rich basalt was the motor of the 2010 Eyjafjallajökull explosive eruption, and that its decreasing inflow terminated the eruption. Significant quantity of silicic magma is thus still present in the interior of the volcano. Our results show that detailed sampling during the entire eruption was essential for deciphering the complex magmatic processes at play, i.e. the dynamics of the magma mingling and mixing. Finally, the rapid compositional changes in the eruptive products suggest that magma mingling occurs on a timescale of a few hours to days whereas the interval between the first detected magma injection and eruption was several months.
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Vestergaard, Rikke, Gro Birkefeldt Møller Pedersen et Christian Tegner. « The 1845–46 and 1766–68 eruptions at Hekla volcano : new lava volume estimates, historical accounts and emplacement dynamics ». JOKULL 70 (8 avril 2021) : 35–56. http://dx.doi.org/10.33799/jokull2020.70.035.
Texte intégralRésumé :
We use new remote sensing data, historical reports, petrology and estimates of viscosity based on geochemical data to illuminate the lava emplacement flow-lines and vent structure changes of the summit ridge of Hekla during the large eruptions of 1845–46 and 1766–68. Based on the planimetric method we estimate the bulk volumes of these eruptions close to 0.4 km3 and 0.7 km3, respectively. However, comparison with volume estimates from the well-recorded 1947–48 eruption, indicates that the planimetric method appears to underestimate the lava bulk volumes by 40–60%. Hence, the true bulk volumes are more likely 0.5–0.6 km3 and 1.0–1.2 km3, respectively. Estimated melt viscosity averages for the 1766–68 eruption amount to 2.5 x10**2 Pa s (pre-eruptive) and 2.5x10**3 Pa s (degassed), and for the 1845–46 eruption 2.2x10**2 Pa s (pre-eruptive) and 1.9x10**3 Pa s (degassed). Pre-eruptive magmas are about one order of magnitude more fluid than degassed magmas. In the 1845–46 and 1947–48 eruptions, SiO2 decreased from 58–57 to 55–54 wt% agreeing with a conventional model that Hekla erupts from a large, layered magma chamber with the most evolved (silica-rich) magmas at the top. In contrast, the lava-flows from 1766–68 reveal a more complicated SiO2 trend. The lava fields emplaced in 1766 to the south have SiO2 values 54.9–56.5%, while the Hringlandahraun lava-flow that erupted from younger vents on the NE end of the Hekla ridge in March 1767 has higher SiO2 of 57.8%. This shows that the layered magma chamber model is not suitable for all lava-flows emplaced during Hekla eruptions.
8
Utkin, I. S., O. E. Mel’nik, A. A. Afanas’ev et Yu D. Tsvetkova. « Effect of Quartz Deposition on the Dynamics of Magma Chamber Degassing ». Moscow University Mechanics Bulletin 73, no 6 (novembre 2018) : 129–34. http://dx.doi.org/10.3103/s0027133018060018.
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Mollo, Silvio, Flavio Di Stefano et Francesca Forni. « Editorial for the Special Issue “Mineral Textural and Compositional Variations as a Tool for Understanding Magmatic Processes” ». Minerals 11, no 2 (21 janvier 2021) : 102. http://dx.doi.org/10.3390/min11020102.
Texte intégralRésumé :
This Special Issue of Minerals collects seven different scientific contributions highlighting how magma chamber processes and eruption dynamics studied either in the laboratory or in nature may ultimately control the evolutionary histories and geochemical complexities of igneous rocks [...]
10
Marsh, Bruce D. « Solidification fronts and magmatic evolution ». Mineralogical Magazine 60, no 398 (février 1996) : 5–40. http://dx.doi.org/10.1180/minmag.1996.060.398.03.
Texte intégralRésumé :
AbstractFrom G. F. Becker's and L. V. Pirsson's early enunciations linking the dynamics of magma chambers to the rock records of sills and plutons to this day, two features stand at the centre of nearly every magmatic process: solidification fronts and phenocrysts. The structure and behaviour of the envisioned solidification front, however, has been mostly that akin to non-silicate, non-multiply-saturated systems, which has led to confusion in appreciating its role in magmatic evolution. The common habit of intruding magmas to carry significant amounts of phenocrysts, which can lead to efficient fractionation, layering, and interstitial melt flow within extensive mush piles, when coupled with solidification fronts, allows a broad understanding of the processes leading to the rock records of sills and lava lakes. These same processes are fundamental to understanding all magmas.The spatial manifestation of the liquidus and solidus is the Solidification Front (SF); all magmas, stationary or in transit, are encased by SFs. In the ideal case of an initially crystal-free, cooling magma, crystallinity increases from nucleation on the leading liquidus edge to a holocrystalline rock at the trailing solidus. The package of SF isotherms advances inward, thickening with time and, depending on location — roof, floor, or walls — and the initial crystallinity of the magma, is instrumental in controlling magmatic evolution. Bimodal volcanism as well as much of the structure of the oceanic crust may arise from the behaviour of SFs.In mafic magmas, somewhere near a crystallinity (N) of 55% (vol), depending on the phase assemblage, the SF changes from a viscous fluid (suspension (0<N<25) and mush (25<N<55%)) to an elastic crystalline network (rigid crust (55<N<100%)) of some strength containing interstitial residual melt. With thickening of the roofward SF of some mafic magmas, the weight of the leading, viscous portion repeatedly tears the crust near N ∼ 55–60%, efficiently segregating the local residual melt into zones of interdigitating silicic lenses. This is SF instability (SFI), a process of possible importance in continental crust initiation and evolution, in producing silicic segregations in oceanic crust, and in recording the inability of the viscous part of the upper SF ever to detach wholly in typical (<∼ 1 km) sheet-like magmas. These granophyric and pegmatitic segregations, individually reaching 1–2 m in thickness and 30–50 m in length, form thick (∼ 50–75 m) zones that can be misconstrued as sandwich horizons where the last liquids might have accumulated. In effectively splitting the magma chemically and spatially, SFI is, in essence, a form of chaos (i.e. silicic chaos).Differentiation of initially crystal-free, stationary magmas is limited to processes occurring within SFs, which operate in competition with the rate of inward advancement of solidification. Local processes operating on characteristic time scales longer than the time for the SF to advance a distance equal to its own thickness are suppressed. Enormous increases in viscosity outward within the viscous, leading portion of the SF efficiently partition the distribution of melt accessible to eruption. Eruptible melts lie essentially inward of the SF and are thus severely restricted in silica enrichment. The silica-enriched SFI melts are thus generally inaccessible to collection and eviction unless the host SF is reprocessed or “burned back” through, respectively, later regional magmatism or massive, late-stage re-injection. And because of large viscosity contrasts between SFI melts and host basalts, once freed, SFI melts are literally impossible to homogenize back into the system and may collect and compact against the roof to form large silicic masses. Unusually voluminous, bulbous masses of silicic granophyre present along, and sometimes warping, the roofs of large diabase sills may reflect collections of remobilized blobs of SFI melts. These bulbous masses may be later added to the continental crust through solid state creep.In sheets made of phenocryst-rich, singly saturated magma, most phenocrysts are able through settling or floating to avoid capture by the advancing SFs. Significant differentiation is possible through extensive settling of initial phenocrysts and upward leakage of interstitial residual melt from the associated cumulate pile, which over-thickens the lower SF, greatly tipping the competitive edge against suppression of melt leakage by advancing solidification. Dense interstitial melts may similarly drain from roofward cumulates of light phenocrysts. The variation in crystal size and modal abundance in these cumulate piles are intimate records of prior crystallization, transport, and filling.Magmas in transit erode SFs and thoroughly charge the magma with crystals, facilitating fractionation and differentiation, especially if the body occasionally comes to rest. The key to protracted differentiation through fractional crystallization is not crystallization in stationary, closed chambers, but the repeated transport and chambering of magma or the periodic resupply to chambers of phenocryst-rich magma. This is punctuated differentiation, which may be the general case. Close corollaries are that thick, closed sheets of initially crystal-free, multiply-saturated magma undergo precious little overall differentiation, and that deciphering the sequence and crystallinity, including in transit phenocryst entrainment, growth, and sorting, of the filling events is central to unravelling intrusive history.Variations in temperature, whether on phase diagrams or in actual magmas, are intrinsically linked to commensurate variations in space and time in magmatic systems. The spectrum of all physical and chemical processes associated with magma is accordingly strongly partitioned in space and time.The idea of a magma chamber as a vat of low crystallinity melt crystallizing everywhere within and differentiating through crystal settling is unrealistic. A magma chamber formed of any number of crystal-laden inputs, encased by inward-propagating, dynamic solidification fronts, and where significant differentiation is tied to the dynamics of late-stage, interstitial melt within extensive mush piles is more in accord with the rock record.
Thèses sur le sujet "Magma chamber dynamics"
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Mann, Crystal. « Magma chamber dynamics at Soufrière Hills volcano, Montserrat ». Thesis, McGill University, 2010. http://digitool.Library.McGill.CA:80/R/?func=dbin-jump-full&object_id=94980.
Texte intégralRésumé :
Implicit in active, steady-state magmatic systems is their persistent activity and unchanging behavior in terms of composition and eruptive styles. The ongoing eruption (July 1995 April 2010) of the Soufrière Hills volcano (SHV), Montserrat, provides an ideal setting for understanding this steady-state behavior. Mafic enclaves are ubiquitous in andesitic magma erupted from SHV. The mafic enclaves are basalt to basaltic andesite (49 56 wt. % SiO2) in composition. Based on their chemistry, mineralogy and petrology, they are divided into three types. Prior to intrusion, basaltic magma underwent significant differentiation of amphibole at deep crustal levels. Type 1 (T1) and Type 2 (T2) enclaves represent hybrid magmas which are a mixture of differentiated basaltic magma and the host andesite, while Type 3 (T3) enclaves represent basaltic magma which ponded prior to intrusion and underwent significant additional fractionation of plagioclase. The T1 enclaves sample a vesiculated upper portion of the mixing horizon, while the T2 enclaves sample a less vesiculated, deeper, and slightly more rigid portion of this horizon. The T3 enclaves were near the temperatures of the andesite reservoir at the time of their intrusion; they demonstrate mixing on a physical mixing only, i.e., crystal transfer. The T1 enclaves formed when they reached buoyancy due to vesiculation and detached from the mixing horizon to rise upward in the andesite, whereas T2 enclaves formed during subsequent intrusions, during mafic overturn. The SHV demonstrates periodic and regular explosive activity, for which we can quantify changes in volatile content over time. Volatile analyses from phenocryst-hosted melt inclusions sampled from andesitic pumice cluster at 2.8 5.4 wt. % H2O, with ~ 3000 ppm Cl and negligible CO2. We interpret these volatile contents to mirror conditions in the lower conduit and upper magma reservoir beneath the volcano. Our model of the SHV magmatic system suggests thatUne caractéristique des systèmes magmatiques à l'équilibre est leur activité persistante et leur comportement c onstant en termes de compositions et styles d'éruption. L'éruption en cours (Juillet 1995 Avril 2010) du volcan de Soufrière Hills (SHV), Montserrat, représente une configuration idéale pour comprendre cet état d'équilibre éruptif. Les enclaves mafiques sont omniprésentes dans les magmas andésitiques émis à SHV. La composition de ces enclaves varie de basaltes à andésites basaltiques (49 56 % SiO2). Elles se répartissent en trois types selon leur chimie, minéralogie et pétrologie. Avant intrusion dans le magma andésitique, les magmas basaltiques ont fractionné une quantité importante d'amphibole dans la croûte profonde. Les enclaves de type 1 (T1) et type 2 (T2) représentent des magmas hybrides, soit un mélange de basalte différencié et d'andésite hôte, tandis que les enclaves de type 3 (T3) représentent un magma basaltique qui a stagné avant intrusion et a subi un fractionnement additionnel de plagioclase. Les enclaves T1 proviennent de portions vésiculaires de la partie supérieure du front de mélange, tandis que les T2 proviennent d'un niveau moins vésiculaire, plus profond et légèrement plus rigide ce cet horizon. Les enclaves T3 étaient proches de la température du réservoir andésitique au moment de leur intrusion et ne montrent du mélange que d'une manière physique, soit des transferts de cristaux. Les enclaves se sont formées lorsqu'elles sont devenues moins denses à cause de la vésiculation et se sont détachées de l'horizon de mélange pour monter dans le magma andésitique, tandis que les T2 se sont formées durant des intrusions successives, causant de la convection mafique. Le SHV connaît une activité explosive et régulière, pour laquelle il est possible de quantifier des changements en volatiles au cours du temps. Des analyses des volatiles dans les inclusions vitreuses des phénocr
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Hunt, Emma J. « Magma chamber dynamics in the peralkaline magmas of the Kakortokite Series, South Greenland ». Thesis, University of St Andrews, 2015. http://hdl.handle.net/10023/6900.
Texte intégralRésumé :
Understanding crystallisation in magma chambers is a key challenge for igneous petrology. It is particularly important to understand the origins of layering in peralkaline rocks, e.g. the kakortokite (nepheline syenite), Ilímaussaq Complex, S. Greenland, as these are commonly associated with high value multi-element economic deposits. The kakortokite is a spectacular example of macrorhythmic (>5 m) layering. Each unit consists of three layers comprising arfvedsonite-rich (sodic-amphibole) black kakortokite at the base, grading into eudialyte-rich (sodic-zirconosilicate) red kakortokite, then alkali feldspar- and nepheline-rich white kakortokite. Each unit is numbered -19 to +17 relative to a characteristic well-developed horizon (Unit 0), however there is little consensus on their development. This project applies a multidisciplinary approach through field observations combined with petrography, crystal size distributions (CSDs), mineral and whole rock chemistries on Units 0, -8 to -11 and a phonolite/micro-nephelinolite (“hybrid”) sequence that crosscuts the layered kakortokite. Textures and compositions are laterally consistent across outcrop and indicators of current activity are rare. CSDs indicate in situ crystallisation with gravitational settling as a minor process. Chemical discontinuities occur across unit boundaries. The layering developed through large-scale processes under exceptionally quiescent conditions. The discontinuities reflect open-system behaviour; units were formed by an influx of volatile-rich magma that initiated crystallisation in a bottom layer. Nucleation was initially suppressed by high volatile element concentrations, which decreased to allow for crystallisation of arfvedsonite, followed by eudialyte, then alkali feldspar and nepheline to form each tripartite unit. The chemistry of the hybrid indicates mixing between a primitive (sub-alkaline) magma and kakortokite. Thus injections of magmas of varying compositions occurred, indicating a complex plumbing system below current exposure. The lessons learned at Ilímaussaq, which is extremely well exposed and preserved, are relevant to understanding magma chamber dynamics in the more common instances of pervasively altered peralkaline rocks.
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Bain, Amelia Anne. « Quantitative field constraints on the dynamics of silicic magma chamber rejuvenation and overturn ». Thesis, University of British Columbia, 2010. http://hdl.handle.net/2429/27430.
Texte intégralRésumé :
A number of recent papers by Bachmann and co-authors investigate a hypothesis that the catastrophic eruption of large-volume, crystal-rich silicic magmas is a consequence of reheating (so-called rejuvenation) and overturn of partially molten, buoyant silicic material by repeated injection of dense, hot mafic magma. In support of this model, we analyse an extensive suite of kinematic indicators for the buoyant overturn of silicic crystal mush layers of the Coastal Maine Magmatic Province, apparently in response to the injection and cooling of hot, dense mafic magmas. We use spectral analysis, microtextural analysis and scaling theory to identify, characterise and understand the length-scales of deformation along sharp interfaces separating mafic and silicic intrusive layers, from the scale of individual crystals (~1 cm) to in excess of the mafic layer thickness (>100 m). Deformations at the largest scale lengths are comparable to the silicic layer thickness, consistent with Rayleigh-Taylor theory, and support a conjecture that mafic recharge can cause large-scale overturning of silicic magma chambers. By contrast, deformations at the scale of crystals probably record buoyancy effects related to melt percolation and intermediate scales are explained by compaction. The evolution of rejuvenation is investigated and a condition for large-scale overturn of the chamber is proposed. This work provides the first field-based confirmation of the rejuvenation-overturn hypothesis. Additional laboratory experiments addressing the overturn of a particle-rich buoyant fluid layer overlain by a denser fluid layer are outlined in Appendix C.
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Matthews, Naomi Elizabeth. « Magma chamber assembly and dynamics of a supervolcano : Whakamaru, Taupo Volcanic Zone, New Zealand ». Thesis, University of Oxford, 2011. http://ora.ox.ac.uk/objects/uuid:71fedeaf-7153-4a7d-9113-9f32071ec721.
Texte intégralRésumé :
This thesis employs crystal-specific techniques, combined with field observations, petrology, geochemistry and numerical modelling to reconstruct the magmatic system associated with the ~ 340 ka Whakamaru supereruption, New Zealand. Comparisons are drawn with the ~ 74 ka Youngest Toba Tuff (YTT) supereruption. Whakamaru Group Ignimbrites contain five pumice types, characterised by different mineralogies and crystal contents. Pumice petrography and geochemistry indicate that basaltic magma mixing occurred, possibly triggering eruption. Geothermobarometers suggest an eruption temperature of ~ 770°C and magma storage at ~ 5 km depth. High-resolution thermal records from Ti-in-quartz analysis indicate a thermal pulse of ~ 100°C prior to eruption. Diffusion timescales show multiple recharge events with the most significant event occurring ~ 35 y prior to eruption. Zircon U-Pb data show that most crystallisation occurred at ~ 400 ka, with antecrysts and xenocrysts incorporated. Zircon trace-element data suggest multiple recharge events and complex mixing over ~ 100 ky, consistent with an incrementally growing reservoir. Oxygen-isotope data illustrate that zircon, quartz and feldspar crystallised together in equilibrium, with isotopically homogenous magma sources feeding the reservoir over time. Whakamaru and YTT tephra thickness and grain-size data were used in ash dispersal modelling. Results indicate the YTT eruption had a ~ 35 km column height and erupted volumes of 1500 – 1900 km³, with deposition from a co-ignimbrite phase; whereas Whakamaru had a Plinian column ~ 45 km high with SE dispersal and a minimum volume of ~ 400 km³. The widespread dispersal of large volumes of fine ash from both eruptions would have had global environmental consequences. The data are integrated to reconstruct a new Whakamaru magma reservoir model. The complex crystal records indicate the system was characterised by long periods of incremental assembly, mixing, recycling of material, and reactivation during multiple recharge episodes which perturbed the system and primed the magma for eruption.
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Vassalli, Melissa <1977>. « Numerical simulations of magma chamber dynamics at Campi Flegrei, and associated seismicity, deformation and gravity changes ». Doctoral thesis, Alma Mater Studiorum - Università di Bologna, 2008. http://amsdottorato.unibo.it/986/1/Tesi_Vassalli_Melissa.pdf.
Texte intégralRésumé :
Understanding the complex relationships between quantities measured
by volcanic monitoring network and shallow magma processes is a crucial
headway for the comprehension of volcanic processes and a more realistic
evaluation of the associated hazard. This question is very relevant at Campi
Flegrei, a volcanic quiescent caldera immediately north-west of Napoli (Italy).
The system activity shows a high fumarole release and periodic ground slow
movement (bradyseism) with high seismicity. This activity, with the high
people density and the presence of military and industrial buildings, makes
Campi Flegrei one of the areas with higher volcanic hazard in the world.
In such a context my thesis has been focused on magma dynamics due
to the refilling of shallow magma chambers, and on the geophysical signals
detectable by seismic, deformative and gravimetric monitoring networks that
are associated with this phenomenologies. Indeed, the refilling of magma
chambers is a process frequently occurring just before a volcanic eruption;
therefore, the faculty of identifying this dynamics by means of recorded signal
analysis is important to evaluate the short term volcanic hazard.
The space-time evolution of dynamics due to injection of new magma
in the magma chamber has been studied performing numerical simulations
with, and implementing additional features in, the code GALES (Longo et al.,
2006), recently developed and still on the upgrade at the Istituto Nazionale di
Geofisica e Vulcanologia in Pisa (Italy). GALES is a finite element code based
on a physico-mathematical two dimensional, transient model able to treat
fluids as multiphase homogeneous mixtures, compressible to incompressible.
The fundamental equations of mass, momentum and energy balance
are discretised both in time and space using the Galerkin Least-Squares and
discontinuity-capturing stabilisation technique. The physical properties of
the mixture are computed as a function of local conditions of magma composition,
pressure and temperature.The model features enable to study a broad
range of phenomenologies characterizing pre and sin-eruptive magma dynamics
in a wide domain from the volcanic crater to deep magma feeding
zones.
The study of displacement field associated with the simulated fluid dynamics
has been carried out with a numerical code developed by the Geophysical
group at the University College Dublin (O’Brien and Bean, 2004b),
with whom we started a very profitable collaboration. In this code, the seismic
wave propagation in heterogeneous media with free surface (e.g. the
Earth’s surface) is simulated using a discrete elastic lattice where particle interactions
are controlled by the Hooke’s law. This method allows to consider
medium heterogeneities and complex topography.
The initial and boundary conditions for the simulations have been defined
within a coordinate project (INGV-DPC 2004-06 V3_2 “Research on active
volcanoes, precursors, scenarios, hazard and risk - Campi Flegrei”), to which
this thesis contributes, and many researchers experienced on Campi Flegrei
in volcanological, seismic, petrological, geochemical fields, etc. collaborate.
Numerical simulations of magma and rock dynamis have been coupled as
described in the thesis.
The first part of the thesis consists of a parametric study aimed at understanding
the eect of the presence in magma of carbon dioxide in magma in
the convection dynamics. Indeed, the presence of this volatile was relevant
in many Campi Flegrei eruptions, including some eruptions commonly considered
as reference for a future activity of this volcano. A set of simulations
considering an elliptical magma chamber, compositionally uniform, refilled
from below by a magma with volatile content equal or dierent from that
of the resident magma has been performed. To do this, a multicomponent
non-ideal magma saturation model (Papale et al., 2006) that considers the
simultaneous presence of CO2 and H2O, has been implemented in GALES.
Results show that the presence of CO2 in the incoming magma increases its
buoyancy force promoting convection ad mixing. The simulated dynamics
produce pressure transients with frequency and amplitude in the sensitivity
range of modern geophysical monitoring networks such as the one installed
at Campi Flegrei .
In the second part, simulations more related with the Campi Flegrei volcanic
system have been performed. The simulated system has been defined
on the basis of conditions consistent with the bulk of knowledge of Campi
Flegrei and in particular of the Agnano-Monte Spina eruption (4100 B.P.),
commonly considered as reference for a future high intensity eruption in this
area. The magmatic system has been modelled as a long dyke refilling a small shallow magma chamber; magmas with trachytic and phonolitic composition
and variable volatile content of H2O and CO2 have been considered. The
simulations have been carried out changing the condition of magma injection,
the system configuration (magma chamber geometry, dyke size) and the resident
and refilling magma composition and volatile content, in order to study
the influence of these factors on the simulated dynamics. Simulation results
allow to follow each step of the gas-rich magma ascent in the denser magma,
highlighting the details of magma convection and mixing. In particular, the
presence of more CO2 in the deep magma results in more ecient and faster
dynamics. Through this simulations the variation of the gravimetric field has
been determined.
Afterward, the space-time distribution of stress resulting from numerical
simulations have been used as boundary conditions for the simulations of
the displacement field imposed by the magmatic dynamics on rocks. The
properties of the simulated domain (rock density, P and S wave velocities)
have been based on data from literature on active and passive tomographic
experiments, obtained through a collaboration with A. Zollo at the Dept. of
Physics of the Federici II Univeristy in Napoli. The elasto-dynamics simulations
allow to determine the variations of the space-time distribution of
deformation and the seismic signal associated with the studied magmatic dynamics.
In particular, results show that these dynamics induce deformations
similar to those measured at Campi Flegrei and seismic signals with energies
concentrated on the typical frequency bands observed in volcanic areas.
The present work shows that an approach based on the solution of equations
describing the physics of processes within a magmatic fluid and the
surrounding rock system is able to recognise and describe the relationships
between geophysical signals detectable on the surface and deep magma dynamics.
Therefore, the results suggest that the combined study of geophysical
data and informations from numerical simulations can allow in a near future
a more ecient evaluation of the short term volcanic hazard.
6
Vassalli, Melissa <1977>. « Numerical simulations of magma chamber dynamics at Campi Flegrei, and associated seismicity, deformation and gravity changes ». Doctoral thesis, Alma Mater Studiorum - Università di Bologna, 2008. http://amsdottorato.unibo.it/986/.
Texte intégralRésumé :
Understanding the complex relationships between quantities measured
by volcanic monitoring network and shallow magma processes is a crucial
headway for the comprehension of volcanic processes and a more realistic
evaluation of the associated hazard. This question is very relevant at Campi
Flegrei, a volcanic quiescent caldera immediately north-west of Napoli (Italy).
The system activity shows a high fumarole release and periodic ground slow
movement (bradyseism) with high seismicity. This activity, with the high
people density and the presence of military and industrial buildings, makes
Campi Flegrei one of the areas with higher volcanic hazard in the world.
In such a context my thesis has been focused on magma dynamics due
to the refilling of shallow magma chambers, and on the geophysical signals
detectable by seismic, deformative and gravimetric monitoring networks that
are associated with this phenomenologies. Indeed, the refilling of magma
chambers is a process frequently occurring just before a volcanic eruption;
therefore, the faculty of identifying this dynamics by means of recorded signal
analysis is important to evaluate the short term volcanic hazard.
The space-time evolution of dynamics due to injection of new magma
in the magma chamber has been studied performing numerical simulations
with, and implementing additional features in, the code GALES (Longo et al.,
2006), recently developed and still on the upgrade at the Istituto Nazionale di
Geofisica e Vulcanologia in Pisa (Italy). GALES is a finite element code based
on a physico-mathematical two dimensional, transient model able to treat
fluids as multiphase homogeneous mixtures, compressible to incompressible.
The fundamental equations of mass, momentum and energy balance
are discretised both in time and space using the Galerkin Least-Squares and
discontinuity-capturing stabilisation technique. The physical properties of
the mixture are computed as a function of local conditions of magma composition,
pressure and temperature.The model features enable to study a broad
range of phenomenologies characterizing pre and sin-eruptive magma dynamics
in a wide domain from the volcanic crater to deep magma feeding
zones.
The study of displacement field associated with the simulated fluid dynamics
has been carried out with a numerical code developed by the Geophysical
group at the University College Dublin (O’Brien and Bean, 2004b),
with whom we started a very profitable collaboration. In this code, the seismic
wave propagation in heterogeneous media with free surface (e.g. the
Earth’s surface) is simulated using a discrete elastic lattice where particle interactions
are controlled by the Hooke’s law. This method allows to consider
medium heterogeneities and complex topography.
The initial and boundary conditions for the simulations have been defined
within a coordinate project (INGV-DPC 2004-06 V3_2 “Research on active
volcanoes, precursors, scenarios, hazard and risk - Campi Flegrei”), to which
this thesis contributes, and many researchers experienced on Campi Flegrei
in volcanological, seismic, petrological, geochemical fields, etc. collaborate.
Numerical simulations of magma and rock dynamis have been coupled as
described in the thesis.
The first part of the thesis consists of a parametric study aimed at understanding
the eect of the presence in magma of carbon dioxide in magma in
the convection dynamics. Indeed, the presence of this volatile was relevant
in many Campi Flegrei eruptions, including some eruptions commonly considered
as reference for a future activity of this volcano. A set of simulations
considering an elliptical magma chamber, compositionally uniform, refilled
from below by a magma with volatile content equal or dierent from that
of the resident magma has been performed. To do this, a multicomponent
non-ideal magma saturation model (Papale et al., 2006) that considers the
simultaneous presence of CO2 and H2O, has been implemented in GALES.
Results show that the presence of CO2 in the incoming magma increases its
buoyancy force promoting convection ad mixing. The simulated dynamics
produce pressure transients with frequency and amplitude in the sensitivity
range of modern geophysical monitoring networks such as the one installed
at Campi Flegrei .
In the second part, simulations more related with the Campi Flegrei volcanic
system have been performed. The simulated system has been defined
on the basis of conditions consistent with the bulk of knowledge of Campi
Flegrei and in particular of the Agnano-Monte Spina eruption (4100 B.P.),
commonly considered as reference for a future high intensity eruption in this
area. The magmatic system has been modelled as a long dyke refilling a small shallow magma chamber; magmas with trachytic and phonolitic composition
and variable volatile content of H2O and CO2 have been considered. The
simulations have been carried out changing the condition of magma injection,
the system configuration (magma chamber geometry, dyke size) and the resident
and refilling magma composition and volatile content, in order to study
the influence of these factors on the simulated dynamics. Simulation results
allow to follow each step of the gas-rich magma ascent in the denser magma,
highlighting the details of magma convection and mixing. In particular, the
presence of more CO2 in the deep magma results in more ecient and faster
dynamics. Through this simulations the variation of the gravimetric field has
been determined.
Afterward, the space-time distribution of stress resulting from numerical
simulations have been used as boundary conditions for the simulations of
the displacement field imposed by the magmatic dynamics on rocks. The
properties of the simulated domain (rock density, P and S wave velocities)
have been based on data from literature on active and passive tomographic
experiments, obtained through a collaboration with A. Zollo at the Dept. of
Physics of the Federici II Univeristy in Napoli. The elasto-dynamics simulations
allow to determine the variations of the space-time distribution of
deformation and the seismic signal associated with the studied magmatic dynamics.
In particular, results show that these dynamics induce deformations
similar to those measured at Campi Flegrei and seismic signals with energies
concentrated on the typical frequency bands observed in volcanic areas.
The present work shows that an approach based on the solution of equations
describing the physics of processes within a magmatic fluid and the
surrounding rock system is able to recognise and describe the relationships
between geophysical signals detectable on the surface and deep magma dynamics.
Therefore, the results suggest that the combined study of geophysical
data and informations from numerical simulations can allow in a near future
a more ecient evaluation of the short term volcanic hazard.
7
Shortland, Robert Andrew. « Physical and chemical interactions between coexisting acid and basic magmas at Elizabeth Castle, Jersey, Channel Islands ». Thesis, University of Derby, 2000. http://hdl.handle.net/10545/230934.
Texte intégralRésumé :
Elizabeth Castle forms part of the South-East Granite Complex of Jersey, Channel Islands and is one of several multi-magma complexes in the region. The rocks have calc-alkaline signatures indicative of a subduction zone setting. In the western half of the Elizabeth Castle complex, the outcrops are wholly granophyre, while to the east, granophyre and minor monzogranite are intimately associated with diorite. The dioritic rocks form part of a layered series which is preserved at several localities. The layered diorites were initially intruded by multiple sub-horizontal granitic sheets. All contacts between the diorite and the granitic sheets are crenulate, indicating that the two were present as coexisting magmas. Fine-grained, dark margins in the diorites contain quench textures such as spherulitic plagioclase and acicular apatite, and are interpreted as chilled margins. At many contacts a narrow tonalitic marginal zone, with acicular amphiboles, is present. Field relationships suggest that this is a hybrid produced by interaction between coexisting dioritic and granitic magmas and this is confirmed by modelling based on geochemical data. It is proposed that within the marginal zones the presence of volatile-rich fluids, increased temperatures and a decrease in viscosity promoted chemical diffusion across the dioritegranite interface. The transfer of elements, together with the presence of volatiles, promoted the growth of hydrous mafic phases and suppressed crystallization of alkali feldspar. At the same time, fluid infiltration modified the composition of the dioritic magma. Field evidence indicates that these processes took place in a narrow time frame prior to further granitic intrusion. Parts of the sheeted complex were extensively disrupted by the later granitic intrusions, producing large areas rich in dioritic enclaves. Within these disrupted areas a grey inhomogeneous rock is encountered. Field and petrographic evidence suggest that this is a hybrid rock produced by the physical mixing of dioritic and granitic magmas. Linear chemical trends confirm this interpretation. Minor intrusions comprising red granite dykes, basic dykes, composite dykes and aplite sheets cut the complex.
8
Konstantinou, Konstantinos I. « Seismological studies of magma injection processes : volcano monitoring and imaging of magma chambers ». Thesis, Durham University, 2001. http://etheses.dur.ac.uk/3847/.
Texte intégralRésumé :
The processes associated with magma injection at shallow depths within the crust have been the topic of many geophysical studies, some investigating the seismicity that accompanies volcanic activity and others attempting to map the subsurface extent and geometry of the resulting magma bodies. The aim of this study is to obtain a better understanding of these processes by investigating the nature of seismic signals that accompany volcanic eruptions and by seismically imaging a magma body beneath a mid-ocean ridge, both located on, or adjacent to Iceland. The seismic phenomena associated with the 1996 Vatnajӧkull subglacial eruption in central Iceland, have been studied using data recorded by both temporary (HOTSPOT) and permanent (SIL) seismic networks. These networks comprise 60 broadband and short-period three-component seismographs and cover most parts of the country. Two very active volcanic systems, Bárdarbunga and Grimsvӧtn, are situated underneath the Vatnajokull ice cap. The volcanoseismic signals recorded there were categorised according to their waveform shape and frequency content, into three groups: (a) low-frequency events (1-2 Hz); (b) mixed-frequency events (1-4 Hz); and (c) volcanic tremor. The eruption was preceded by intense seismic activity which began with a = 5.6 earthquake located at the Bárdarbunga volcanic system. The epicentres of the earthquake swarm that followed the M(_w), = 5.6 event initially delineated the Bárdarbunga caldera rim and then migrated towards Grimsvӧtn, to a place where a fissure was later observed. Pre-eruptive tremor started at least two days before the eruption as a harmonic signal around five narrow frequency bands (0.5-0.7, 1.6, 2.2, 2.8 and 3.2 Hz). Co-eruptive tremor started as a broadband, continuous signal which evolved into low-amplitude background tremor interrupted by high-amplitude, cigar-shaped bursts. Further analysis revealed that continuous tremor and the cigar-shaped bursts had all the characteristics of low- dimensional chaotic signals. Geophysical and geochemical evidence suggest that a lateral migration of magma from Bárdarbunga facilitated the rupture of the roof of a magma chamber, situated at the fissure area, which subsequently erupted as tephra on the glacier. The second phase of the RAMESSES (Reykjanes Ridge Axial Melt Experiment: Structural Synthesis from Electromagnetic and Seismics) experiment involved the acquisition of multichannel seismic reflection data from 39 along- and across-axis lines shot over the magmatically active 57º 45'N axial volcanic ridge. The data from one along-axis line were processed using a variety of techniques that mainly aimed at reducing the large amount of coherent noise present, a result of scattered energy at the rough seabed. The final processed section revealed a number of reflection events that could be interpreted as intra-crustal reflections, originating from the interface between pillow lavas and sheeted dykes, and from the top part of a thin melt lens.
9
El-Rassi, Dorota. « Fluid dynamics in magma chambers with application to sulphide settling ». Thesis, National Library of Canada = Bibliothèque nationale du Canada, 2000. http://www.collectionscanada.ca/obj/s4/f2/dsk1/tape4/PQDD_0024/MQ50400.pdf.
Texte intégral
10
Gilbert, Andrew. « Crystal mobilisation in convecting magma chambers : an analogue experimental approach ». Thesis, University of Cambridge, 2017. https://www.repository.cam.ac.uk/handle/1810/267176.
Texte intégralRésumé :
Solidified igneous intrusions from originally liquid magma chambers display a large number of different sedimentary features. These features include the gravitational collapse of sidewalls producing slumps and the layering produced by gravitational settling of crystals. In the chamber fluid-dynamic processes such as convection are expected to occur due to cooling at the roof producing dense gravitationally unstable liquid, and the crystallisation of interstitial liquid changing the composition of the remaining liquid possibly reducing the density causing the liquid to rise up. The crystals which form in basaltic magma chambers have a high propensity to be mobilised due to convection and other fluid-dynamic processes including replenishment by a secondary intrusion. Convective mobilisation of plagioclase grains in vertical, tabular intrusions is seen from flat profiles of apparent aspect ratio as a function of dyke width. These flat profiles were formed due to scouring of gravitationally unstable sidewall mushes, and these crystals then become entrained in the convecting liquid. Convection only ceases once the volume of crystals in suspension reaches a critical volume fraction leading to an increase in viscosity, which dampens the vigour of convection. The majority of this study is performing and analysing a number of different experiments to look at the behaviour of different styles of analogue particle piles. Particle piles that are formed of inert, plastic particles are subjected to convection in the particle layer and in the bulk overlying fluid, and different styles of mobilisation depending on the heat flux driving convection and the density profile of the pile are observed. The mobilisation style goes from rolling of particles on the surface, to puffs of particles from the surface being lofted into the interior, followed by large particle fountains and then the entire particle pile being completely disaggregated and lofted into the interior of the chamber as the force driving convection is increased. The initiation of mobilisation can be explained by the fluidisation of a particle pile, whilst the high degrees of mobilisation seen in some high Rayleigh number regimes can be explaining by resuspending particles. In experiments where particle piles have a positive density profile (dense particles overlying low density particles) the underlying low density particles can break through the overlying layer in particle fountains and can be explained by a modified fluidisation parameter. These experiments lack the reactivity and cohesion that realistic crystal piles would have. To try and quantify this, I have also performed a series of experiments looking at the rheology of an ice-sucrose suspension, where ice crystals can sinter and aggregate together. Under sheared conditions the forces required to disaggregate ice aggregates can be calculated, with the viscosity of an ice-sucrose suspension being described by a power-law relationship of shear rate and crystal radius. The particle pile experiments show that mobilisation of equivalent crystal piles in magma chambers should be readily observed. As it is not observed, except in replenished magmatic systems, this suggests that the additional forces coming from cohesion and aggregation in crystal piles prevent mobilisation of magmatic crystals. The replenishment by secondary intrusions can lead to forces which overcome the strength of the pile.
Livres sur le sujet "Magma chamber dynamics"
1
Hooft, Emilie Ernestine Ebba. The influence of magma supply and eruptive processes on axial morphology, crustal construction and magma chambers. Woods Hole, Mass : Massachusetts Institute of Technology, Woods Hole Oceanographic Institution, Joint Program in Oceanography/Applied Ocean Science and Engineering, 1997.
Trouver le texte intégral
2
El-Rassi, Dorota. Fluid dynamics in magma chambers with application to sulphide settling. 2000.
Trouver le texte intégralChapitres de livres sur le sujet "Magma chamber dynamics"
1
Montagna, Chiara P., Paolo Papale et Antonella Longo. « Magma Chamber Dynamics at the Campi Flegrei Caldera, Italy ». Dans Active Volcanoes of the World, 201–17. Berlin, Heidelberg : Springer Berlin Heidelberg, 2022. http://dx.doi.org/10.1007/978-3-642-37060-1_7.
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2
Pearce, T. H., M. P. Griffin et A. M. Kolisnik. « Magmatic Crystal Stratigraphy and Constraints on Magma Chamber Dynamics : Laser Interference Results on Individual Phenocrysts ». Dans Collected Reprint Series, 13745–52. Washington, DC : American Geophysical Union, 2014. http://dx.doi.org/10.1002/9781118782064.ch31.
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3
Bachmann, Olivier, et George W. Bergantz. « 17. Deciphering Magma Chamber Dynamics from Styles of Compositional Zoning in Large Silicic Ash Flow Sheets ». Dans Minerals, Inclusions And Volcanic Processes, sous la direction de Keith D. Putirka et Frank J. Tepley III, 651–74. Berlin, Boston : De Gruyter, 2008. http://dx.doi.org/10.1515/9781501508486-018.
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4
Rice, Alan. « Dynamics of Magma Chambers ». Dans Flow and Creep in the Solar System : Observations, Modeling and Theory, 287–305. Dordrecht : Springer Netherlands, 1993. http://dx.doi.org/10.1007/978-94-015-8206-3_18.
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5
Tait, S. R., et C. Jaupart. « Convection and Macrosegregation in Magma Chambers ». Dans Interactive Dynamics of Convection and Solidification, 241–60. Dordrecht : Springer Netherlands, 1992. http://dx.doi.org/10.1007/978-94-011-2809-4_40.
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Yanagi, Takeru. « Configuration and Dynamics of Magma Chambers Beneath Arc Volcanoes ». Dans Arc Volcano of Japan, 59–76. Tokyo : Springer Tokyo, 2011. http://dx.doi.org/10.1007/978-4-431-53996-4_6.
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7
Campbell, I. H. « Fluid Dynamic Processes in Basaltic Magma Chambers ». Dans Developments in Petrology, 45–76. Elsevier, 1996. http://dx.doi.org/10.1016/s0167-2894(96)80004-2.
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« Formation and Dynamics of Magma Chambers and Reservoirs ». Dans Volcanotectonics, 272–324. Cambridge University Press, 2020. http://dx.doi.org/10.1017/9781139176217.007.
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Harper, Brian E., Calvin F. Miller, G. Christopher Koteas, Nicole L. Gates, Robert A. Wiebe, Daniel S. Lazzareschi et J. Warner Cribb. « Granites, dynamic magma chamber processes and pluton construction : the Aztec Wash pluton, Eldorado Mountains, Nevada, USA ». Dans The Fifth Hutton Symposium on the Origin of Granites and Related Rocks. Geological Society of America, 2004. http://dx.doi.org/10.1130/0-8137-2389-2.277.
Texte intégralActes de conférences sur le sujet "Magma chamber dynamics"
1
Rosen, Jeremy S., Brian G. Rusk, Michael A. Clynne et Susan M. DeBari. « MAGMA CHAMBER DYNAMICS AND ERUPTIVE MECHANISMS IN THE CASCADE ARC : INSIGHTS FROM MELT INCLUSIONS AND TITANIUM-IN-QUARTZ THERMOBAROMETRY ». Dans GSA Annual Meeting in Seattle, Washington, USA - 2017. Geological Society of America, 2017. http://dx.doi.org/10.1130/abs/2017am-308453.
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2
Holness, Marian. « Mush or magma chamber ? : the microstructural record of magma fluid dynamical regime and the growth of solidification fronts ». Dans Goldschmidt2021. France : European Association of Geochemistry, 2021. http://dx.doi.org/10.7185/gold2021.3228.
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