- Izu-Bonin-Mariana Arc
The Izu-Bonin-Mariana (IBM) arc system is an outstanding example of a
plate tectonic convergent boundary. IBM extends over 2800 km south from near Tokyo, Japan, to beyond Guam, and includes the Izu Islands. Bonin Islands, and Mariana Islands; much more of the IBM arc system is submerged below sealevel. The IBM arc system lies along the eastern margin of the Philippine Sea Platein the Western Pacific Ocean. It is most famous for being the site of the deepest gash in Earth's solid surface, the Challenger Deepin the Mariana Trench.
The IBM arc system formed as a result of
subductionof the western Pacific plate. The IBM arc system now subducts mid-Jurassic to Early Cretaceous lithosphere, with younger lithosphere in the north and older lithosphere in the south, including the oldest (~170 million years old, or Ma) oceanic crust. Subduction rates vary from ~2cm (1 inch) per year in the south to 6cm (~2.5 inches) in the north.The IBM arc system is an excellent example of an intra-oceanic convergent margin (IOCM). IOCMs are built on oceanic crustand contrast fundamentally with island arc built on continental crust, such as Japan or the Andes. Because IOCM crust is thinner, denser, and more refractory than that beneath Andean-type margins, study of IOCM melts and fluids allows more confident assessment of mantle-to-crust fluxes and processes than is possible for Andean-type convergent margins. Because IOCMs are far removed from continents they are not affected by the large volume of alluvial and glacial sediments. The consequent thin sedimentary cover makes it much easier to study arc infrastructure and determine the mass and composition of subducted sediments. Active hydrothermal systems found on the submarine parts of IOCMs give us a chance to study how many of earth's important ore deposits formed.
Historical importance of IBM arc system
Guam in the southern IBM arc system is where Magellan first landed after his epic crossing of the Pacific Ocean in 1521.The
Bonin Islandswere a significant stop for water and supplies for New Englandwhaling during the early 19th century. At that time they were known as the Peel Islands.Terrible battles were fought on the islands of Saipan and Iwo Jima in 1944 and 1945; many young Japanese and American soldiers died in these battles. George H. W. Bushwas shot down in 1945 near Chichijimain the Bonin Islands.Twelve Japanese seaman were stranded in June 1944 on volcanic Anatahanfor seven years, along with the overseer of the abandoned plantation and an attractive young Japanese woman. Novel and 1963 movie Anatahan is based on these events.The B-29 bomber Enola Gayflew from Tinianto drop the first atomic bomb on Hiroshimain 1945.Sergant Shoichi Yokoihid out in the wilds of Guam for 28 years before coming out of hiding in 1972.The Brown tree snakewas accidentally introduced during World War IIand has since devastated native birds on Guam.
Boundaries of IBM Arc system
lithosphereproduced by the IBM arc system during its ~50 Ma history are found today as far west as the Kyushu-Palau Ridge, up to 1,000 km from the present IBM trench. The IBM arc system is the surficial expression of the operation of a subduction zoneand this defines its vertical extent. The northern boundary of the IBM arc system follows the Nankai Troughnortheastward and onto southern Honshu, joining up with a complex system of thrusts that continue offshore eastward to the Japan Trench. The intersection of the IBM, Japan, and Sagami trenches is the only trench-trench-trench triple junction on Earth. The IBM arc system is bounded on the east by a very deep trench, which ranges from almost 11km deep in the Challenger Deepto less than 3 km where the Ogasawara Plateauenters the trench. The southern boundary is found where the IBM Trench meets the Kyushu-Palau Ridge near Belau. hus defined, the IBM arc system spans over 25° of latitude, from 11°N to 35°20’N
The IBM arc system is part of the
Philippine Sea Plate, at least to the first approximation. Although the IBM arc deforms internally – and in fact in the south a small plate known as the Mariana Plate is separated from the Philippine Sea Plate by a spreading ridge in the Mariana Trough- it is still useful to discuss approximate rates and directions of the Philippine Sea Plate with its lithospheric neighbors, because these define, to a first order, how rapidly and along what streamlines material is fed into the Subduction Factory. The Philippine Sea Plate (PH) has four neighboring plates: Pacific (PA), Eurasian (EU), North American (NA), and Caroline (CR). There is minor relative motion between PH and CR; furthermore, CR does not feed the IBM Subduction Factory, so it is not discussed further. The North American plateincludes northern Japan, but relative motion between it and Eurasia is sufficiently small that relative motion between PH and EU explains the motion of interest. The Euler pole for PH-PA as inferred from the NUVEL-1A model for current plate motions [DeMets et al., 1994] lies about 8°N, 137.3°E, near the southern end of the Philippine Sea Plate. PA rotates around this pole CCW ~1°/Ma with respect to PH. This means that relative to the southernmost IBM, PA is moving NW and being subducted at about 20-30 mm/y, whereas relative to the northernmost IBM, PA is moving WNW and twice as fast. At the south end of IBM, there is almost now convergence between the Caroline Plate and the Philippine Sea Plate.It should be noted that the IBM arc is not experiencing trench ‘roll-back’, that is, the migration of the oceanic trenchtowards the ocean. The trench is moving towards Eurasia, although a strongly extensional regime is maintained in the IBM arc system because of rapid PH-EU convergence. The nearly vertical orientation of the subducted plate beneath southern IBM exerts a strong “sea-anchor” force that strongly resists its lateral motion. Back-arc basin spreading is thought to be due to the combined effects of the sea-anchor force and rapid PH-EU convergence (Scholz and Campos, 1995). The obliquity of convergence between PA and the IBM arc system change markedly along the IBM arc system. Plate convergence inferred from earthquake slip vectors is nearly strike-slip in the northernmost Marianas, adjacent to and south of the northern terminus of the Mariana Trough, where the arc has been ‘bowed-out’ by back-arc basin opening, resulting in a trench which strikes approximately parallel to the convergence vectors. Convergence is strongly oblique for most of the Mariana Arc system but is more nearly orthogonal for the southernmost Marianas and most of the Izu-Bonin segments. McCaffrey (1996) noted that the arc-parallel slip rate in the forear reaches a maximum of 30mm/yr in the northern Marianas. According to McCaffrey, this is fast enough to have produced geologically significant effects, such as unroofing of high-grade metamorphic rocks, and provides one explanation for why the forearcin southern IBM is tectonically more active than that in northern IBM.
Geologic history of the IBM Arc system
The evolution of the IBM arc system is among the best known of any convergent margin. Because IBM has always been an arc system under strong extension, its components encompass a broad area, from the Palau-Kyushu Ridge to the IBM trench (see first-right figure). In general, the oldest components are farthest west, but a complete record of evolution is preserved in the forearc. The IBM subduction zone began as part of a hemispheric-scale foundering of old, dense lithosphere in the Western Pacific (Stern and Bloomer, 1992). The beginning of true subduction localized the magmatic arc close to its present position, about 200 km away from the trench, and allowed the sub-forearc mantle to stabilize and cool. The arc stabilized until about 30 Ma, when it began to rift to form the Parece Vela Basin. Spreading also began in the northernmost part of the IBM arc about 25Ma and propagated south to form the Shikoku Basin. Parece Vela and Shikoku basin spreading systems met about 20 Ma and the combined Parece Vela Basin-Shikioku Basin continued widening until about 15 Ma, ultimately producing Earth's largest
back-arc basin. The arc was disrupted during rifting but began to build again as a distinct magmatic system once seafloor spreading began. Arc volcanism, especially explosive volcanism, waned during much of this episode, with a resurgence beginning about 20 Ma in the south and about 17 Ma in the north. Tephra from northern and southern IBM show that strong compositional differences observed for the modern arc have existed over most of the arc's history, with northern IBM being more depleted and southern IBM being relatively enriched. About 15 Ma, the northernmost IBM began to collide with Honshu, probably as a result of new subduction along the Nankai Trough.A new episode of rifting to form the Mariana Trough back-arc basinbegan sometime after 10 Ma, with seafloor spreading beginning about 3-4 Ma. Because disruption of the arc is the first stage in forming any back-arc basin, the present Mariana arc volcanoes cannot be older than 3-4 Ma but the Izu-Bonin volcanoes could be as old as ~25 Ma. The Izu interarc rifts began to form about 2 Ma.
IBM Arc system components
The three segments of IBM (figure to right) do not correspond to variations on the incoming plate. Boundaries are defined by the Sofugan Tectonic Line (~29°30’N) separating the Izu and Bonin segments, and by the northern end of the Mariana Trough back-arc basin (~23°N), that defines the boundary between the Bonin and Mariana segments. Forearc, active arc, and back arc are expressed differently on either side of these boundaries (see figure below).The forearc is that part of the arc system between the trench and the magmatic front of the arc and includes uplifted sectors of the forearc situated near the magmatic front, sometimes called the ‘frontal arc’. The IBM forearc from Guam to Japan is about 200 km wide. Uplifted portions of the forearc, composed of Eocene igneous basement surmounted by reef terraces of
Eoceneand younger age, produce the island chain from Guam north to Ferdinand de Medinilla in the Marianas. Similarly, the Bonin or Ogasawara Islands are mostly composed of Eocene igneous rocks. There is no accretionary prismassociated with the IBM forearc or trench.The magmatic axis of the arc is well defined from Honshu to Guam. This ‘magmatic arc’ is often submarine, with volcanoesbuilt on a submarine platform that lies between 1 and 4 km water depth. Volcanic islands are common in the Izu segment, including O-shima, Hachijojima, and Miyakejima. The Izu segment farther south also contains several submarine felsic calderas. The Izu arc segment is also punctuated by inter-arc rifts. The Bonin segment to the south of the Sofugan Tectonic Line contains mostly submarine volcanoes and also some that rise slightly above sealevel, such as Nishino-shima. The Bonin segment is characterized by a deep basin, the Ogasawara Trough, between the magmatic arc and the Bonin Islands forearc uplift. The highest elevations in the IBM arc (not including the Izu Peninsula, where IBM comes onshore in Japan) are found in the southern part of the Bonin segment, where the extinct volcanic islands of Minami Iwo Jimaand Kita Iwo Jimarise to almost 1000 meters above sealevel. The bathymetric high associated with magmatic arc of the Izu and Bonin segments is often referred to as the Shichito Ridge in Japanese publications, and the Bonins are often referred to as the Ogasawara Islands. Volcanoes erupting lavas of unusual composition – the shoshonitic province - are found in the transition between the Bonin and Mariana arc segments, including Iwo Jima. The magmatic arc in the Marianas is submarine to the north of Uracas, south of which the Mariana arc includes volcanic islands (from north to south): Asuncion, Maug, Agrigan, Pagan, Alamagan, Guguan, Sarigan, and Anatahan. Mariana volcanoes again becomes submarine south of Anatahan.The back-arc regions of the three segments are quite different. The Izu segment is marked by several volcanic cross-chains which extend SW away from the magmatic front. The magmatically-starved Bonin arc segment has no back-arc basin, inter-arc rift, or rear-arc cross chains. The Mariana segment is characterized by an actively spreading back arc basin known as the Mariana Trough. The Mariana Trough shows marked variations along strike, with seafloor spreading south of 19°15’ and rifting farther north.The IBM arc system southwest of Guam is markedly different than the region to the north. The forearc region is very narrow and the intersection of backarc basin spreading axis with the arc magmatic systems is complex.
Behavior and composition of the Western Pacific plate
Everything on the Pacific plate that enters the IBM trench is subducted. The next section discusses some modifications of the lithosphere just prior to its descent and the age and composition of oceanic crust and sediments on the Pacific plate adjacent to the trench. In addition to subducted sediments and crust of the Pacific plate, there is also a very substantial volume of material from the overriding IBM forearc that is lost to the subduction zone by
tectonic erosion(von Huene et al., 2004).
IBM Trench and outer trench swell
. Serpentinite thus generated may carry water deep into the mantle as a result of subduction.
Geology and composition of the westernmost Pacific plate
Pacific platesubducts in the IBM trench, so understanding what is subducted beneath IBM requires understanding the history of the western Pacific. The IBM arc system subducts mid- Jurassicto Early Cretaceous lithosphere, with younger lithosphere in the north and older lithosphere in the south. It is not possible to directly know the composition of subducted materials presently being processed by the IBM Subduction Factory – what is now 130 km deep in the subduction zoneentered the trench 4 – 10 million years ago. However, the composition of the western Pacific seafloor- oceanic crust- sediments, crust, and mantle lithosphere - varies sufficiently systematically that, to a first approximation, we can understand what is now being processed by studying what lies on the seafloor east of the IBM trench.
The Pacific plate seafloor east of the IBM arc system can be subdivided into a northern portion that is bathymetrically ‘smooth’ and a southern portion that is bathymetrically rugged, separated by the Ogasawara Plateau. These large-scale variations mark distinct geologic histories to the north and south. The featureless north is dominated by the Nadezhda Basin. In the south, crude alignments of
seamounts, atolls, and islands define three great, WNW-ESE trending chains (Winterer et al., 1993): the Marcus Island- Wake Island- Ogasawara Plateau, the Magellan SeamountsChain, and the Caroline IslandsRidge. The first two chains formed by off-ridge volcanism during Cretaceoustime, whereas the Caroline Islands chain formed over the past 20 million years. Two important basins lie between these chains: the Pigafetta Basinlies between the Marcus-Wake and Magellan chains, and the East Mariana Basinlies between the Magellan and Caroline chains.
The age of Western Pacific seafloor has been interpreted from
seafloor magnetic anomaliescorrelated to the geomagnetic reversaltimescale (Nakanishi et al., 1992) and confirmed by Ocean Drilling Program scientific drilling. Three major sets of magnetic anomalies have been identified in the area of interest. Each of these lineation sets comprises M-series (mid-Jurassic to mid-Cretaceous) magnetic anomalies that are essentially "growth rings" of the Pacific Plate. These anomaly sets indicate that the small, roughly triangular Pacific plate grew by spreading along three ridges (Bartolini and Larson, 2001). The oldest identifiable lineations are M33 to M35 (Nakanishi, 1993) or perhaps even M38 (Handschumacher et al., 1988). It is difficult to say how old these lineations and the older crust might be; the oldest magnetic lineations for which ages have been assigned are M29 (157 Ma; (Channell et al., 1995). Magnetic lineations as old as M29 are not known from other oceans, and the area in the Western Pacific that lies inside the M29 lineation - that is, crust older than M29 - is on the order of 3x106 km2, about a third of the size of the United States. ODP site 801 lies on seafloor that isconsiderably older than M29 and the MORB basement there yields Ar-Ar ages of 167±5 Ma (Pringle, 1992). The oldest sediments at site 801C are midde Jurassic, Callovianor latest Bathonian(~162 Ma; Gradstein et al., 2005).
Seafloor spreading in the Pacific during the
Cretaceousevolved from a more E-W 'Tethyan' orientation to the modern N-S trend. This occurred during mid-Cretaceous time, a ~35-40 Ma interval characterized by a lack of magnetic reversals known as the Cretaceous Superchron or Quiet Zone. Subsequently, the location of N-S trending spreading ridges relative to the Pacific Basin migrated progressively to the east throughout Cretaceous and Tertiary time, resulting in the present marked asymmetry of the Pacific, with very young seafloor in the Eastern Pacific and very old seafloor in the Western Pacific.
Sediments being delivered to the IBM trench are not thick considering that this some of Earth's oldest seafloor. Away from seamounts, the pelagic sequence is dominated by chert and pelagic clay, with little carbonate. Carbonates are important near guyots, common in the southern part of the region. Interestingly, Cenozoic sediments are unimportant except for
volcanic ashand Asian loessdeposited adjacent to Japan and carbonate sediments associated with the relatively shallow Caroline Ridgeand Caroline plate. Strong seafloor currents are probably responsible for this erosion or non-deposition.
The compositions of sediments being subducted beneath the northern and southern parts of the IBM arc are significantly different, because of the Cretaceous off-ridge volcanic succession in the south that is missing in the north. Lavas and volcaniclastics associated with an intense episode of intraplate volcanism correspond in time closely to the Cretaceous Superchron. Off-ridge volcanism became increasingly important approaching the
Ontong-Java Plateau. There are 100-400m thick tholeiitic sillsin the East Mariana Basinand Pigafetta Basin(Abrams et al., 1993), and at least 650m of tholeiitic flows and sills in the Nauru Basin, near ODP Site 462. Castillo et al. (1994) suggest that this province may reflect the formation of a mid-Cretaceous spreading system in the Nauru and East Mariana basins. Farther north, deposits related to this episode consist of thick sequences of Aptian- Albianvolcaniclastic turbidites shed from emerging volcanic islands, such as preserved at DSDP site 585 and ODP sites 800 and 801. A few hundred meters of volcaniclastic deposits probably characterizes the sedimentary succession in and around the East Mariana and Pigafetta basins. Farther north, at DSDP sites 196 and 307 and ODP site 1149, there is little evidence of mid-Cretaceous volcanic activity. It appears that the Aptian-Albian volcanic episode was largely restricted to the region south of present 20°N latitude. Paleomagnetic and plate kinematic considerations place this broad region of off-ridge volcanism in the present vicinity of Polynesia, where today off-ridge volcanism, shallow bathymetry, and thin lithosphere is known as the 'Superswell' (Menard, 1984; McNutt et al., 1990).
The figure above shows the typical sediments drilled at
Ocean Drilling Programsite 1149, east of the Izu-Bonin segment. The sediments drilled at ODP site 1149 are about 400m thick and are as old as 134 million years. The sedimentary section is a typical pelagic stratigraphy, accumulated mostly in the Cretaceous but also in the last 7 million years (late Neogene) built on a basement of Early Cretaceousoceanic crust. The lowermost portion is carbonate and chert, the next layer is very chert-rich, the third layer is clay-rich. This is followed by a long depositional hiatus before sedimentation resumes ~6.5 Ma (Late Miocene), with deposition of volcanic ash, clay, and windblown dust. The stratigraphy east of the Mariana segment differs from that being subducted beneath the Izu-Bonin segment in having a much greater abundance of Early Cretaceous intra-plate volcanics and flood basalts.About 470m of oceanic crustwas penetrated at ODP site 801C during Legs 129 and 185. These are typical mid-ocean ridge basaltthat were affected by low-temperature hydrothermalalteration. This crust is overlain by a 3m thick, bright yellow hydrothermal deposit and about 60 m of alkali olivine basalt, 157.4±0.5 Ma old (Pringle, 1992).
Geophysics of the subducted slab and mantle
The deep structure of the IBM system has been imaged using a variety of geophysical techniques. This section provides an overview of these data, including a discussion of
mantlestructure at depths >200 km.
Spatial patterns of
seismicityare essential for locating and understanding the morphology and rheologyof subducting lithospheric slabs, and this is particularly true for the IBM Wadati-Benioff zone(WBZ). Katsumata and Sykes (1969) first outlined the most important features of the IBM WBZ. Their study detected a zone of deep earthquakes beneath the southern Marianas and provided some of the first constraints on the deep, vertical nature of subducting Pacific lithosphere beneath southern IBM. They also found a region of reduced shallow seismicity (≤70 km) and an absence of deep (≥ 300 km) events beneath the Volcano Islands adjacent to the junction of the Izu Bonin and Mariana trenches, where the trench trends nearly parallel to the convergence vector.
More recently, Engdahl et al. (1998) provided an earthquake catalog containing improved locations (Figure 10). This data set shows that, beneath northern IBM, the dip of the WBZ steepens smoothly from ~40° to ~80° southwards, and seismicity diminishes between depths of ~150 km and ~300 km (Figures 11a c). The subducted slab beneath central IBM (near 25°N; Fig. 11c) is delineated by reduced seismic activity that nevertheless defines a more vertical orientation that persists southward (Figures 11d f).Deep earthquakes, here defined as seismic events ≥300 km deep, are common beneath parts of the IBM arc system (Figures 10, 11). Deep events in the IBM system are less frequent than for most other subduction zones with deep seismicity, such as Tonga/Fiji/Kermadec and South America. Beneath northern IBM, deep seismicity extends southward to ~27.5°N, and a small pocket of events between 275 km and 325 km depth exists at ~22°N. There is narrow band of deep earthquakes beneath southern IBM between ~21°N and ~17°N, but south of this there are extremely few deep events. Although early studies assumed that seismicity demarcated the upper boundary of the slab, more recent evidence has shown that many of these earthquakes occur within the slab. For instance, a study by Nakamura et al.  showed that a region of events beneath northernmost IBM region occur ~20 km beneath the top of the subducting plate. They propose that transformational faulting, which occurs when metastable olivine changes to a more compact spinel structure, produces this zone of seismicity. Indeed, the faulting mechanism for deep earthquakes is a hotly debated topic (e.g., [Green and Houston, 1995] ), and has yet to be resolved. Double seismic zones (DSZs) have been detected in several parts of the IBM subduction zone, but their locations within the slab as well as interpretations for their existence vary dramatically. Beneath southern IBM, Samowitz and Forsyth  found a DSZ lying 80 km and 120 km deep, with the two zones separated by 30 35 km. Earthquake focal mechanisms indicate that the upper zone, where most events occur, is in downdip compression, while the lower zone is in downdip extension. This DSZ is located at a depth where the curvature of slab is greatest; at greater depths it unbends into a more planar donfiguration. Samowitz and Forsyth  suggested that unbending or thermal stresses in the upper 150 km of the slab may the primary cause of the seismicity. For northern IBM, Iidaka and Furukawa  used a refined earthquake relocation scheme to detect a DSZ between depths of 300 km and 400 km, which also has a spacing of 30 35 km between the upper and lower zones. They interpreted data from S to P converted phases and thermal modeling to propose that the DSZ results from transformational faulting of a metastable olivine wedge in the slab. Recent work suggests that compositional variations in the subducting slab may also contribute to double seismic zone [Abers, 1996] , or that DSZs represent the locus of serpentine dehydration in the slab [Peacock, 2001] .
Mariana Arc Volcanism and Hydrothermal Activity
Bathymetry of the Mariana arc region (Baker et al., 2008), showing all 51 edifices presently named along the volcanic front between 12°30’N and 23°10’N. Hydrothermally or volcanically active submarine edifices are labeled red; active subaerial edifices are labeled green. Inactive submarine and subaerial edifices are labeled in smaller black and green font, respectively. For all edifices, caldera labels are in bold italics. Black circles (20-km diameter) identify those volcanic centers composed of multiple individual edifices. Solid red line is the backarc spreading center.
Baker et al. (2008) identified 76 volcanic edifices along 1370 km of the Mariana arc, grouped into 60 ‘‘volcanic centers,’’ of which at least 26 (20 submarine) are hydrothermally or volcanically active. The overall volcanic center density is 4.4/100 km of arc, and that of active centers is 1.9/100 km. Active volcanoes lie 80 to 230 km above the subducting Pacific plate, and ~25% lie behind the arc magmatic front. There is no evidence for a regular spacing of volcanoes along the Mariana arc. The frequency distribution of volcano spacing along the arc magmatic front peaks between 20 and 30 km and shows the asymmetric, long-tail shape typical for many other arcs. The first global compilation of arc volcanoes using recent bathymetric data estimated that arcs that are at least partially submarine have a population of almost 700 volcanoes, of which at least 200 are submerged (de Ronde et al., 2003).
Arc Hydrothermal Activity
Baker et al. (2008) estimated that intraoceanic arcs combined may contribute hydrothermal emissions equal to ~10% of that from the global mid-ocean ridge system.
*Abrams, L.J., Larson, R.L., Shipley, T.H., and Lancelot, Y., 1993. ""Cretaceous Volcanic Sequences and Jurassic Oceanic Crust in the East Mariana and Pigafetta Basins of the Western Pacific" in M.S. Prigle, W.W. Sager, W.V. Sliter, and S. Stein (eds.) The Mesozoic Pacific: Geology, Tectonics, and Volcanism, Geophysical Monograph 97, American Geophysical Union, 77-101.
*Baker, E.T., Embley, R.W., Walker, S.L., Resing, J.A., Lupton, J.E., Nakamura, K.-I., de Rode, C. E. J., Massoth, G. J. 2008. Hydrothermal activity and volcano distribution along the Mariana arc. J. Geophys. Res.113, B08S09, doi:10.1029/2007JR005423, 2008.
*Bartolini, A., and Larson, R.L., 2001. "Pacific microplate and the
Pangeasupercontinent in the Early to Middle Jurassic" Geology 29, 735-738.
*Castillo, P.R., Pringle, M.S., and Carlson, R.W., 1994. "East Mariana Basin tholeiite: Cretaceous intraplate basalts or rift basalts related to the Ontong Java plume?" Earth and Planetary Science Letters 123, p. 139-154.
*Channel, J.T., Erba, E., Nakanishi, M., and Tamaki, K., 1995. "Late Jurassic-Early Cretaceous and oceanic magnetic anomaly block models", in W. A. Berggren, D.V. Kent, M.-P. Aubry, and J. Hardenbol, SEPM Special Publication, Tulsa, p. 51-63.
*DeMets, C., R.G. Gordon, D.D. Argus, and S. Stein, 1994. "Effect of recent revisions to the geomagnetic reversal time scale on estimates of current plate motions", Geophys. Res. Lett., 21, 2191-2194.
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*Engdahl, E.R., R.D. van der Hilst, and R. Buland, 1998. ""Global teleseismic earthquake relocation with improved travel times and procedures for depth determinatio." Bulletin of the Seismological Society of America, 88, p. 722-743.
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*Handschumacher, D.W., Sager, W.W., Hilde, T.W.C. and Bracey, D.R., 1988. "Pre-Cretaceous tectonic evolution of the Pacific plate and extension of the geomagnetic poarity reversal timescale with implications for the origin of the Jurassic "Quiet Zone". Tectonophysics 155, 365-380.
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*Plank, T., Kelley, K. A., Murray, R.W., Stern, L. Q., 2007. "Chemical composition of sediments subducting at the Izu-Bonin Trench". Geochemistry, Geophysics, Geosystems, 8.
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*Scholz, C.H., and Campos, J., 1995. "On the mechanism of seismic decoupling and back arc spreading at subduction zones" Journal of Geophysical Research-B, 100, 22,103-22,115.
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*Stern, R.J., Fouch, M.J., and Klemperer, S., 2003. “An Overview of the Izu-Bonin-Mariana Subduction Factory” in J. Eiler and M. Hirschmann (eds.) Inside the Subduction Factory, Geophysical Monograph 138, American Geophysical Union, 175-222.
*von Huene, R., Ranero, C. R., and Vannucchi, P., 2004. "Generic model of subduction erosion". Geology 32, 913-916.
*Winterer, E.L., Natland, J.H., Van Waagsbergen, R.J., Duncan, R.A., McNutt, M.K., Wolfe, C.J., Silva, I.P., Sager, W.W., and Sliter, W.V., 1993. "Cretaceous Guyots in the Northwest Pacific: An overview of their Geology and Geophysics" in M.S. Prigle, W.W. Sager, W.V. Sliter, and S. Stein (eds.) The Mesozoic Pacific: Geology, Tectonics, and Volcanism, Geophysical Monograph 97, American Geophysical Union, 307-334.
Northern Mariana Islands
* [http://volcano.und.edu/vwdocs/volc_images/southeast_asia/mariana/basic_geology.htm] - VolcanoWorld about the Mariana arc subaerial volcanoes
* [http://www.pmel.noaa.gov/vents/marianas/multimedia06.html] -
NOAARing of Fire 2006 investigations in the Mariana arc - cool videos etc.
* [http://oceanexplorer.noaa.gov/explorations/04fire/welcome.html] -
NOAARing of Fire 2004 investigations in the Mariana arc - cool videos etc.
* [http://oceanexplorer.noaa.gov/explorations/03fire/welcome.html] -
NOAARing of Fire 2003 investigations in the Mariana arc - cool videos etc.
* [http://vids.myspace.com/index.cfm?fuseaction=vids.channel&ChannelID=33358833] - interview with Dr. R. Embley about NOAA studies of Mariana submarine volcanoes
* [http://www.nsf-margins.org/IBM07/] - information about a 2007 geoscientific meeting concerned with the IBM arc, including presentations and posters that can be downloaded.
* [http://www.volcano.si.edu/world/region.cfm?rnum=0804] - Volcanoes of the IBM arc
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