Propagation, linkage, and interaction of caldera ring-faults: comparison between analogue experiments and caldera collapse at Miyakejima, Japan, in 2000
- 1.1k Downloads
The formation of ring faults yields important implications for understanding the structural and dynamic evolution of collapse calderas and potentially associated ash-flow eruptions. Caldera collapse occurred in 2000 at Miyakejima Island (Japan) in response to a lateral intrusion. Based on geophysical data it is inferred that a set of caldera ring faults was propagating upward. To understand the kinematics of ring-fault propagation, linkage, and interaction, we describe new laboratory sand-box experiments that were analyzed through Digital Image Correlation (DIC) and post-processed using 2D strain analysis. The results help us gain a better understanding of the processes occurring during caldera subsidence at Miyakejima. We show that magma chamber evacuation induces strain localization at the lateral chamber margin in the form of a set of reverse faults that sequentially develops and propagates upwards. Then a set of normal faults initiates from tension fractures at the surface, propagating downwards to link with the reverse faults at depth. With increasing amounts of subsidence, interaction between the reverse- and normal-fault segments results in a deactivation of the reverse faults, while displacement becomes focused on the outer normal faults. Modeling results show that the area of faulting and collapse migrates successively outward, as peak displacement transfers from the inner ring faults to later developed outer ring faults. The final structural architecture of the faults bounding the subsiding piston-like block is hence a consequence of the amount of subsidence, in agreement with other caldera structures observed in nature. The experimental simulations provide an analogy to the observations and seismic records of caldera collapse at Miyakejima volcano, but are also applicable to caldera collapse in general.
KeywordsCollapse calderas Ring faults Analogue modeling Fault kinematics Digital image correlation
Collapse calderas are kilometer-scale volcanic depressions bordered by ring faults that form during the evacuation of crustal magma chambers (Williams 1941). Evacuation may be due to lateral intrusion into the host rock or due to upward eruption along conduits or faults, initiating subsidence of the magma-chamber roof and caldera floor (Smith and Bailey 1968). Understanding the link between eruption dynamics and caldera subsidence requires knowledge of the structural progression, including the development and changing location of the active near-surface and underground faults.
Caldera volcanoes exist in nearly all tectonic settings (Newhall and Dzurisin 1988), and may be associated with the largest explosive eruptions known on Earth (Druitt and Sparks 1984). During the last 100 years, however, explosive eruptions at calderas have been of moderate size; fewer than 5% have reached a VEI>4 eruption (Newhall and Dzurisin 1988). Calderas at basaltic volcanoes experience collapse, which is not necessarily associated with major eruption volumes (e.g. Mauna Loa, Fernandina, Piton de la Fournaise, and Miyakejima). However, the structural inventory, such as the configuration of associated ring faults and dikes, is similar for silicic and basaltic volcanoes including near-vertical or variously dipping faults.
Geological and geophysical studies of caldera volcanoes suggest contrasting details of caldera fault architectures (e.g. Smith and Bailey 1968, Lipman 1984, 1997). Experimental studies generally produce several sets of outward-dipping reverse faults and steeply inward-dipping, peripheral normal faults during a single collapse event (e.g. Roche et al. 2000; see section “Digital image processing results” and Supplementary Material S1) demonstrating that the different structures found in the field can coexist. In contrast, most numerical simulations fail to predict reverse faults (e.g. Folch and Marti 2004; Gray and Monaghan 2004; see Supplementary Material S1).
The caldera collapse associated with the 2000 Miyakejima lateral dike intrusion and magma chamber deflation is probably the best instrumentally recorded caldera forming event. Deformation and seismicity records, as well as observations of eyewitnesses, allow a detailed investigation into the chronology of events, showing sequentially upward propagating faults and depression widening near the surface (Geshi et al. 2002; Nakada et al. 2005). In this paper, we first examine the progression of caldera formation at Miyakejima. Then we compare it with the results of laboratory simulations analyzed with a digital image correlation technique. The experiments give sub-millimeter deformation time-series, providing new insights into the variable propagation and linkage of ring faults and revealing the structural complexity of calderas.
The Miyakejima caldera collapse sequence
Miyakejima Island is a 9 km wide, 815 m high inhabited island located to the southeast of Honshu, Japan. Volcanic activity on Miyakejima has been observed frequently in 1874, 1940, 1962, and 1983 (Tsukui et al. 2001). The island’s morphology has been shaped by repeated explosive eruptions, some associated with caldera collapse (e.g. 2,500 years ago), others with effusive fissure eruptions on the flanks (GVP). In summer 2000 a new, 1.7 km wide caldera developed at the summit of Miyakejima, the floor of which subsided to a depth of 250 m above sea level, giving a cumulative subsidence of 1.6 to 2.1 km (Geshi et al. 2002).
Structural architecture and kinematics of ring-faults
In spite of these detailed observations on Miyakejima Island, the geometric evolution and kinematics of ring faults, including fault propagation and interaction, are still incompletely understood. Despite years of vigorous debate, there is not yet a consensus on whether caldera faults at Miyakejima and elsewhere are inward- or outward-dipping (e.g., Gudmundsson and Nilsen 2006; Acocella 2007) since there is field evidence for both structures. New eruptions may initiate from faulting of magma chamber roofs, such as hypothesized for Miyakejima. Thus, the propagation direction of ring faults, as well as their interaction, are of major importance for understanding syn-collapse eruption locations and vent dynamics (e.g. Geshi and Oikawa 2008; Holohan et al. 2008), syn-collapse magma-chamber dynamics (Kennedy et al. 2008), conduit widening, sites for post-collapse volcanism (e.g. Saunders 2001), geothermal activity (e.g. Goff et al. 2000), and mineralization (e.g. Stix et al. 2003).
Laboratory experiments on caldera formation above a deflating magma-chamber analogue (see recent reviews by Cole et al. 2005; Acocella 2007, 2008; Marti et al. 2008; and references therein) suggest that caldera collapse generates two sets of ring structures, an inner set of outward-dipping reverse ring faults enclosed by a second set of inward-dipping normal faults (cf. Appendix S1). Field and geophysical data, however, suggest various expressions of those ring fault architectures; outward- and inward-dipping ring faults are evident at Rabaul, Papua New Guinea (Mori and McKee 1987), whereas caldera collapse at Fernandina, Galapagos in 1968 apparently occurred along inward-dipping ring faults (Simkin and Howard 1970), a configuration also known from eroded calderas in the Western USA (Lipman 1984). While inward-dipping ring faults may cause a “space problem” during subsidence to prohibit major conduit opening (Branney 1995), outward-dipping faults are rarely observed at the surface due to landslide processes (Lipman 1984). In some caldera systems, contemporaneous sub-parallel ring faults appear to provide magma pathways, e.g., Deception and Rabaul (Newhall and Dzurisin 1988), implying that the faults develop progressively and that at times more complex configurations of ring faults may be active.
In order to better understand the structural and temporal evolution of caldera subsidence at Miyakejima and other basaltic (and silicic) volcanoes, as well as to clarify the link between surface expression and deep structural framework of calderas, we present new experimental results analyzed with the aid of a high-resolution digital recording technique. Our results show the dynamic evolution of ring-fault formation, propagation and interaction, and also demonstrate the ability to quantify the kinematics of these processes, as detailed in the next section.
Experimental setup and scaling
The experiments were performed in a sand box, and cross-sectional development could be investigated through two glass panes set up at a distance of 10 cm (Fig. 4). To simulate reservoir deflation, we used a retractable piston with an area of 10 × 10 cm2 emplaced within a cut-out of the same size in the basal plate. At the beginning of the experiment, the piston was located at the level of the basal plate, which was overlain by the analogue crustal material. Using a computer-controlled motor, we set piston retraction at a subsidence rate of 0.015 cm s-1 for 120 s, to a total subsidence of 1.8 cm. In systematic experimental tests, we varied the chamber depth to evaluate the influence of the roof aspect ratio (AR), which ranged from 0.41 to 3.01 in eleven individual experiments. This AR range also covers the geometric configuration of the Miyakejima caldera system, to which the results are compared in section “Comparison of experimental structures to Miyakejima chronology”.
The experiments were geometrically and partially dynamically scaled (cf. Hubbert 1937; Sanford 1959) to fit the configuration of natural calderas regarding roof aspect ratio and subsidence. The geometric scaling factor was 2.5 × 10-5, so that 1 cm in the experiments corresponds to approximately 400 m in nature. As a crustal analogue material, we used a 1:5 mixture of wheat starch (cf. Donnadieu and Merle 1998) and dry quartz sand (Cobbold and Castro 1999). We determined the coefficient of internal friction μF for the starch-sand mixture with the ring shear test; the angle of internal friction φF is ~28° and thus comparable to natural systems. The natural cohesion of crustal materials is in the range of 105 to 107 Pa (e.g. Hoshino et al. 1972), while the cohesion of the analogue material is 70 Pa. Considering a scaling factor of 2.5 × 10-5, cohesion in our experiments is thus properly scaled. A comparison of experiments with pure sand and the mixed sand-starch material showed similarly oriented structures, although the structural resolution obtained in the sand-starch mixture is considerably higher and provides additional details. Particulars of ring-shear granular material tests and the scaling procedure are provided in the Electronic Supplementary Material.
Time-dependent viscosities of the magma analogue were not considered in these experiments, since we focused our investigation on brittle fracturing only. Other limitations of our experiments include the simplified geometry, rheology, and sidewall effects. The subsiding magma chamber roof is simulated by a retracting undeformable piston that induced stresses at the base of the overlying roof. In nature, the pressure within the magma chamber should be different from lithostatic, so that the distribution and relative intensity of stresses within the roof could be different from those in the experiment. We note however, that the chamber geometry is in agreement with plutons that are often nearly flat-roofed (e.g. Pitcher 1993, Zak and Paterson 2006). Furthermore, subsidence occurred along panes of glass that might influence experimental results by friction. However, the structures produced during the experiments were the same in the vicinity and away from the glass panes. In addition, our results broadly mimic those of other studies, yielding geometric similarity even though different materials and apparatus were used (cf. Acocella 2008).
Digital image processing results
For AR < 1, shear zones first appear at depth. A first set of outward-dipping reverse faults initiates underground at the sides of the retracting piston (Fig. 5a). These reverse faults propagate in tandem upwards and reach the surface at outward-dips of ~50° near the surface and 80° at depth. When they reach the surface after ~0.2 cm (~80 m in nature) of subsidence, a second, steeper reverse-fault set forms and propagates upward, while the first set of faults becomes inactive. Then, in the caldera periphery, extensional fractures commence to propagate downwards and develop into inward-dipping normal faults (Fig. 5h, i). After subsidence of ~0.6 to 0.7 cm (~250 m in nature) these peripheral normal faults join with the reverse faults at depth (Fig. 5j). This fault linkage affects the activity of the former dominant reverse faults; they become inactive for most of the ensuing experiment duration. Occasionally near-surface segments of the reverse ring-fault reactivate. Overall, however, subsidence exceeding 0.7 cm is accommodated almost entirely by displacement along faults that are inward-dipping near the surface and subvertical to steeply outward-dipping at depth (Fig. 5l).
For roof aspect ratios >1, faulting is initially asymmetric, with laterally alternating propagation and activity of individual faults which develop at larger numbers and different scales compared to low-AR calderas (Fig. 6). The period of downsag observed at the surface lasts up to ~0.26 cm of subsidence, during which a sequence of faulting occurs beneath the surface. First, reverse faults develop near the magma chamber margin at about 0.1 cm of subsidence in a symmetric fashion (similar as in AR = 0.6 experiment; Fig. 6a, b). Then a second, steeper reverse fault develops on one side of the chamber roof (here to the right of the chamber; Fig. 6b) propagating upwards to the center of the magma chamber roof. When another fault on the opposite side of the chamber (here to the left) develops, displacement transfers from the second to the newly formed fault (Fig. 6d). This is the first fault that reaches the surface with a dip of about 30°, increasing to 45° in the upper part of the chamber roof and then steepening to 70° for most of the fault length down to its base at the chamber side. Further sets of faults may develop in alternating patterns, broadening the structural caldera diameter at the surface. In general, the simultaneous activity of two successive reverse-fault pairs on each side of the magma chamber is short-lived, so that displacement is generally focused on one reverse-fault pair. With about 1.2 cm of subsidence (Fig. 6f), the first inward-dipping reverse faults develop at the caldera periphery. A clear propagation direction, however, is not always recognizable; thus, the periphery faults appear to localize contemporaneously over their entire length. Immediately after interlinkage of the normal and reverse ring-fault segments, the upper parts of the outward-dipping faults become inactive (Fig. 6i, j). However, at greater subsidence, they can sporadically become reactivated allowing faulting in the upper part of the subsiding roof.
High-AR caldera formation includes a series of reverse ring faults that lead to a continued disintegration of the subsiding piston. Consequently, collapse of high-AR calderas tends to occur in a segmented (piecemeal) fashion, whereas low-AR calderas are characterized by the subsidence of a more or less coherent piston.
Thus, our experiments reveal complexly propagating and interacting ring faults that develop sequentially, which may help explain the chronologic and geometric patterns observed at Miyakejima during the 2000 caldera collapse.
Comparison of experimental structures to Miyakejima chronology
The 2000 Miyakejima collapse is probably the best instrumentally recorded caldera-forming event, since it was observed in detail at the surface and monitored with many geophysical methods. Seismic activity below the summit was distributed in a 2 km wide, columnar swarm, the top of which migrated to shallower depths (Fig. 3; Propagation Phase), while the summit of Miyakejima was initially deflating before caldera collapse occurred at the surface on 8 July. Based on the collected data, Geshi et al. (2002) developed a conceptual model for the structural evolution of the collapse caldera including upward propagation of reverse ring faults. Our experimental results bear a striking resemblance to the model by Geshi et al. (2002). With detailed information about the kinematics of ring fault evolution, the experiments contribute to an understanding of events prior to and during collapse in July and August 2000, especially to the Propagation Phase indicated in Fig. 3.
Our experimental results also provide a possible explanation for vent migration and the location of geothermal activity during caldera collapse. According to Geshi and Oikawa (2008), the first phreatomagmatic eruptions at the beginning of collapse occurred near the caldera centre, whereas subsequent eruptions took place at the marginal areas of the caldera. In addition, geothermal activity in the post-caldera stage was concentrated along the rim of the caldera floor. Displacement transfer from inner reverse ring faults that first reach the surface near the centre of the caldera to outer ring faults accompanied by the inactivation of the earlier ring faults, as observed during the experiments, offers a possible explanation for these observations.
The main aim of our experimental study was, with the help of the DIC technique, to analyze and quantify the kinematics of ring faulting during magma chamber deflation. The structural configuration of our experiments reproduced structures observed during earlier experimental studies (e.g. Roche et al. 2000). However, in addition to earlier studies, the DIC results of our models show that the outward-dipping faults initiate at the margins of the magma chamber and propagate in tandem (for low AR), or in alternating sequence (high AR), upwards. In later stages, the inward-dipping ring faults are initiated from surface extension fractures that transform into shear fractures, propagating downwards. Displacement transfer and inactivation of fault segments, as well as linkage, occur between the normal faults and the earlier reverse ring fault; this is considered to be the final structural stage along which most of the successive subsidence occurs.
These findings are, in principal, consistent with earlier conceptual models of caldera collapse (e.g. Branney 1995). However, our experimental results have the advantage that kinematics and timing of individual ring faults can be quantified and that these results can thus be compared to natural examples, such as Miyakejima volcano. Our findings can be applied to other caldera collapse events, such as the 2007 collapse on Reunion Island. Piton de la Fournaise, a basaltic island volcano, similarly showed deflation of a shallow magma chamber, followed six days later by caldera floor subsidence and successive morphologic caldera widening (Michon et al. 2008). Reactivation of existing structural weaknesses may have contributed to the spatiotemporal evolution of the faults.
In general, our observation that caldera ring faults develop in a continuous sequence that explains the multifaceted expression of caldera faults in natural caldera systems, implies that the propagation of the initial ring faults in subsiding calderas can stop, while eruptions may take place along newly-forming sets of peripheral ring faults. This could account for the large widths of many ring-dike complexes, which have previously been explained by stoping (e.g. MacDonald 1972) but are in fact constructed during several magma chamber deflation events with successive ring-dike systems.
Magma transport within upward-propagating ring faults is possible from the initial stages of subsidence. However, the downward-propagating peripheral ring faults can only act as magma feeders if they link to the reverse faults at depth, as our experiments have shown they do. The experiments also suggest that magma transport along the initial ring faults may become inhibited due to their closure. Therefore, the temporal variability of the ring faults during subsidence implies that the location of conduits is also temporally variable, tending to propagate outwards, which in turn could explain local stratigraphic discontinuities and inconsistencies. Vent migration, and in some cases vent multiplication during caldera eruptions has been observed, e.g., in Valles, Long Valley, and Santorini (Druitt 1986; Hildreth and Mahood 1986; Self et al. 1986; Holohan et al. 2008). These observations can be interpreted as a consequence of the reconfiguration of the conduit system due to sealing and establishment of magma pathways along a dynamically developing ring fault system.
In a broader sense, an enhanced understanding of the kinematics of ring fault propagation that can be gained from our experimental results may also contribute to better comprehension of caldera-collapse mechanisms, eruption and hazard potential of unrest periods at caldera volcanoes (Scandone and Acocella 2007), magma-chamber dynamics, and interpretation of geophysical monitoring data of calderas, as has been demonstrated for the 2000 caldera collapse at Miyakejima (section “Comparison of experimental structures to Miyakejima chronology”). In addition, ring-fault evolution as a function of subsidence has significance for the location of post-collapse volcanism (e.g. Sierra Negra, Galapagos, Ecuador (Geist et al. 2008)) and geothermal fields (e.g. Goff et al. 2000; Geshi and Oikawa 2008), which are located preferentially along the traces of ring faults at the surface (cf. Scandone and Acocella 2007).
During flexure, the first outward-dipping faults develop near the magma chamber margins and propagate upwards in the subsurface.
For small aspect ratios (shallow and large chambers), reverse ring faults propagate simultaneously, while for high aspect ratios (deep or small chambers) reverse ring faults propagate sequentially.
During continuous subsidence, new, steeper-dipping reverse faults form outside the earlier-formed faults, and displacement is transferred to the new faults before the earlier ones become inactive. Hence the structural diameter of the caldera widens.
Normal faults develop from extensional fractures in the zone of maximum extension at the caldera periphery and propagate downwards.
At depth, the downward-propagating normal faults interact and link with the lower segments of the reverse faults. Consequently, the activity of the upper segments of the reverse faults diminishes.
The final structural expression of a caldera may be bound by inward- or outward- dipping faults, depending on the amount of subsidence and interaction and linkage of both fault types (cf. Acocella 2007).
Our experimental results provide detailed insights into the kinematics and timing of ring fault evolution that help explain field observations and monitoring data of natural caldera volcanoes. The described sequence of ring fault evolution is useful to the understanding of caldera collapse at Miyakejima volcano in 2000 and other collapse events such as at Piton de la Fournaise in 2007.
The authors thank Nina Kukowski and Onno Oncken for support and permission to work in the Geodynamic modeling lab, and Matthias Rosenau, Thomas Ziegenhagen, Günther Tauscher, Frank Neumann, Babtiste Scholly, and Nicolas Le Corvec for assistance. St. B. is grateful for financial support from Axel Vollbrecht, and T.R.W. acknowledges financial support by the DFG (WA 1642/1-4). Additionally, the authors thank Nobuo Geshi, Takao Ohminato, and Bogdan Ernescu for organizing and providing seismic data for Miyakejima. Finally, Olivier Roche, Nobuo Geshi, Joan Martí, and an anonymous reviewer are acknowledged for helpful reviews and John Stix for editorial work.
This article is distributed under the terms of the Creative Commons Attribution Noncommercial License which permits any noncommercial use, distribution, and reproduction in any medium, provided the original author(s) and source are credited.
Movie of the results of experiment No. 2D_15-118 with a roof aspect ratio of 1.54. Colors display rotational strain around the z-axis (perpendicular to screen; see scale on the right hand side) calculated. Red color represents counter-clockwise rotation of the particles, whereas blue color represents clockwise rotation of the particles. The duration of the experiment is 120 s, during which a subsidence of 1.8 cm was achieved. The spatial resolution of the data processing is around 0.2 mm. Movie is in AVI format, runs in IrfanView and many other free players. (DOC 186 kb) (AVI 28467 kb)
- Acocella V (2008) Structural development of calderas: a synthesis from analogue experiments. In: Gottsmann J, Marti J (eds) Caldera volcanism. analysis, modelling and response. Elsevier, Amsterdam, pp 285–312Google Scholar
- Adam J, Urai JL, Wieneke B, Oncken O, Pfeiffer K, Kukowski N, Lohrmann J, Hoth S, van der Zee W, Schmatz J (2005) Shear localisation and strain distribution during tectonic faulting—new insights from granular-flow experiments and high-resolution optical image correlation techniques. J Struct Geol 27:283–301CrossRefGoogle Scholar
- Branney MJ (1995) Downsag and extension at calderas: new perspectives on collapse geometries from ice-melt, mining, and volcanic subsidence. Bull Volcanol 57:303–318Google Scholar
- Druitt TH (1986) Vent evolution and lag breccia formation during the Cape Riva eruption of Santorini. Greece J Geol 93:439–454Google Scholar
- Furuya M, Okubo S, Tanaka Y, Sun W, Watanabe H, Oikawa J, Maekawa T (2001) Caldera formation process at the 2000 Miyakejima volcano detected by spatio-temporal gravity change. J Geogr 110:217–225 (in Japanese with English abstract)Google Scholar
- Gudmundsson A, Nilsen K (2006) Ring faults in composite volcanoes: structures, models and stress fields associated with their formation. In: Troise C, De Natale G, Kilburn CRJ (eds) Mechanisms of activity and unrest at large calderas. Geol Soc London Spec Pub 269:83-108Google Scholar
- Hoshino K, Koide H, Inami K, Iwamura S, Mitsui S (1972) Mechanical properties of Japanese Tertiary sedimentary rocks under high confining pressures. Bull Geol Survey Japan 244:1–200Google Scholar
- Hubbert MK (1937) Theory of scale models as applied to the study of geologic structures. Geol Soc Am Bull 48:1459–1520Google Scholar
- MacDonald GA (1972) Volcanoes. Prentice-Hall, New JerseyGoogle Scholar
- Marti J, Geyer A, Folch A, Gottsmann J (2008) A review on collapse caldera modeling. In: Gottsmann J, Marti J (eds) Caldera volcanism — Analysis, modelling and response. Elsevier, Amsterdam, pp 233–284Google Scholar
- Nakada S, Nagai M, Yasuda A, Shimamoto T, Geshi N, Ohno M, Akimasa T, Kaneko T, Fujii T (2001) Chronology of the Miyakejima 2000 eruption: characteristics of summit collapsed crater and eruption products. J Geogr 110:168–180 (In Japanese with English abstract)Google Scholar
- Newhall CG, Dzurisin D (1988) Historical unrest at large calderas of the world. US Geol Survey Bull 1855:1–1108Google Scholar
- Pitcher WS (1993) The nature and origin of granite. Chapman and Hall, LondonGoogle Scholar
- Sakai S, Yamada T, Ide S, Mochizuki M, Shiobara H, Urabe T, Hirata N, Shinohara M, Kanazawa T, Nishizawa A, Fujie G, Mikada H (2001) Magma migration from the point of view of seismic activity in the volcanism of Miyake-jima Island in 2000. J Geogr 110:145–155 (In Japanese with English abstract)Google Scholar
- Smith RL, Bailey RA (1968) Resurgent cauldrons. Geol Soc Am Mem 116:613–662Google Scholar
- Tsukui M, Niihori K, Kawanabe Y, Suzuki Y (2001) Stratigraphy and formation of Miyakejima Volcano. J Geogr 156:156–167 (In Japanese with English abstract)Google Scholar
- Williams H (1941) Calderas and their origin. Bull Dept Geol Sci Univ California 25:239–346Google Scholar
- White DJ, Take WA, Bolton MD (2001) Measuring soil deformation in geotechnical models using digital images and PIV analysis. In: 10th International Conference on Computer Methods and Advances in Geomechanics, Tucson, ArizonaGoogle Scholar