Izu–Bonin–Mariana Arc

845:~175 km to ~300 km depth but increases around 400 km, and terminates at ~475 km. B) Central Izu Bonin region. Slab dip is nearly vertical; seismicity tapers off from ~100 km to ~325 km but increases in rate and extends horizontally around 500 km, and terminates at ~550 km. C) Southern Izu Bonin region. Slab dip is ~50°; seismicity is continuous to ~200 km, but a very few anomalous events are evident down to ~600 km. D) Northern Mariana region. Slab dip is ~60°; seismicity is continuous to ~375 km and terminates at ~400 km, but a very few anomalous events are evident down to ~600 km. E) Central Mariana region. Slab dip is vertical; seismicity tapers off slightly between ~275 km and ~575 km, but is essentially continuous. A pocket of deep events around 600 km exists, as well as 1 deep event at 680 km. F) Southern Mariana region. Slab dip is ~55°; seismicity is continuous to ~225 km, with an anomalous event at 375 km. Figure courtesy of Dr. Matt Fouch, 857:

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

923:, 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 ( 263:. 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 Honshū, probably as a result of new subduction along the Nankai Trough. A new episode of rifting to form the Mariana Trough 224:). 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. 188: 131:. 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 293:

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

908:), 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. 215:) 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 no convergence between the Caroline Plate and the Philippine Sea Plate. The IBM arc is not experiencing trench ‘roll-back’, that is, the migration of the 203:– 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 412: 585:). 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 km, 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 ( 285: 569:. 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 ( 441:

is about to descend into a trench starts to bend just outboard of the trench; the seafloor is elevated into a broad swell that is a few hundred meters high and referred to as the "outer trench bulge" or "outer trench rise". The about-to-be subducted plate is highly faulted, allowing seawater to penetrate into the plate interior, where hydration of

673:

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

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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

440:

begins to sink. The IBM trench is devoid of any significant sediment fill; the ~400 m or so thickness of sediments is completely subducted with the downgoing plate. The IBM outer trench swell rises to about 300 m above the surrounding seafloor just before the trench. The lithosphere that

819:

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

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began 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

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locations in volume ~60 km to each side of the lines shown on the map at left. Large variations in slab dip and maximum depth of seismicity are apparent. Distance along each section is measured from the magmatic arc. A) Northern Izu–Bonin region. Slab dip is ~45°; seismicity tapers off from

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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

381:

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

672:

volcaniclastic 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

415:

Geologic relations around the Mariana Trench. Upper left map shows regional setting. Dashed box in regional map (upper left) shows area of detail shown in upper right map. Upper right map shows features up to about 100 km on either side of central Mariana Trench. Dashed line shows location of

249:

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

228:

noted that the arc-parallel slip rate in the forearc reaches a maximum of 30 mm/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

292:

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

258:

Basin. Spreading also began in the northernmost part of the IBM arc about 25 Ma 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,

861:

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

394:

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

321:. 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 219:

towards 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

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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

643:

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

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rise to almost 1000 m 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

115:

The volcanic islands that comprise these island arcs are thought to have been formed from the release of volatiles (steam from trapped water, and other gases) being released from the subducted plate, as it reached sufficient depth for the temperature to cause release of these materials. The

756:), 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 490:‘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 518:

time, whereas the Caroline Islands chain formed over the past 20 million years. Two important basins lie between these chains: the Pigafetta Basin lies between the Marcus-Wake and Magellan chains, and the East Mariana Basin lies between the Magellan and Caroline chains.

254:). 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 878:

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.

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multichannel seismic reflection line 53-53, which is interpreted in lower cross section. Flexure-related faults are outlined in black. Lower figure is a cross-section of the shallow Mariana Subduction Zone along MCS Line 53–54 with numerically annotated features (

2076:

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.; Sliter, W.V. (1993). "Cretaceous Guyots in the Northwest Pacific: An overview of their Geology and Geophysics". In Prigle, M.S.;

824: 475:, 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 116:

associated trenches are formed as the oldest (most western) part of the Pacific plate crust increases in density with age, and because of this process finally reaches its lowest point just as it subducts under the crust to the west of it.

820:

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.

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oceanic 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

483:– 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. 1390:; Hilde, T.W.C.; Bracey, D.R. (1988). "Pre-Cretaceous tectonic evolution of the Pacific plate and extension of the geomagnetic polarity reversal timescale with implications for the origin of the Jurassic 'Quiet Zone'". 385:

The IBM arc system southwest of Guam is markedly different from 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.

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locations; lighter circles represent shallower events, darker circles represent deeper events. Black lines denote cross sectional areas depicted in 6 profiles on right, organized from N to S. Black circles represent

199:, 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 382:

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.

663:

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

250:

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 (

297:

and 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

325:. 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 870:(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, 191:

Cross-section through the shallow part of a subduction zone showing the relative positions of an active magmatic arc and back-arc basin, such as the southern part of the Izu–Bonin–Mariana Arc.

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site 1149, east of the Izu–Bonin segment. The sediments drilled at ODP site 1149 are about 400 m thick and are as old as 134 million years. The sedimentary section is a typical

888:

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 (

1789:

Pringle, M.S. (1992). "Radiometric ages of basaltic basement recovered at sites 800, 801, and 802, Leg 129, Western Pacific Ocean". In R. L. Larson; Y. Lancelot; et al. (eds.).

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one of only two trench-trench-trench triple junctions on Earth. The IBM arc system is bounded on the east by a very deep trench, which ranges from almost 11 km deep in the

1048:. Subduction from Top to Bottom Conference, Avalon CA; held in June 1994. American Geophysical Union Geophysical Monograph. Vol. 96. Washington, D.C. pp. 223–228. 620:

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

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de Ronde, C. E. J.; Massoth, G. J.; Baker, E. T.; Lupton, J. E. (2003). "Submarine hydrothermal venting related to volcanic arcs". In Simmons, S.F.; Graham, I.J. (eds.).

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includes 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

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subducts 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-

581:). 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; ( 395:

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

1598:

Nakamura, T; Nakano, I; Fujimori, H; Yuan, G (1998). "A real-time observation for 3-D structure of ocean phenomena by a 200 Hz ocean acoustic tomography system".

1219: 245:

Simplified tectonic history of the IBM arc system, viewed along E-W profiles. Red corresponds to regions of magmatic activity, blue is magmatically extinct.

2160: 628:, with little carbonate. Carbonates are important near guyots, common in the southern part of the region. Cenozoic sediments are unimportant except for 220:

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 (

143:

Crust and lithosphere produced by the IBM arc system during its ~50 Ma history are found today as far west as the Kyushu–Palau Ridge (just east of the

964:

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.

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intraplate volcanism correspond in time closely to the Cretaceous Superchron. Off-ridge volcanism became increasingly important approaching the

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estimated that intraoceanic arcs combined may contribute hydrothermal emissions equal to ~10% of that from the global mid-ocean ridge system.

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suggested that unbending or thermal stresses in the upper 150 km of the slab may the primary cause of the seismicity. For northern IBM,

277: 2477: 2090: 2009: 1964:

Stern, Robert J.; Bloomer, S. H. (1992). "Subduction zone infancy: Examples from the Eocene Izu–Bonin–Mariana and Jurassic California Arcs".

1620: 1340: 1081: 1351: 1907: 1857: 1419:

Katsumata, Mamoru; Sykes, L.R. (1969). "Seismicity and tectonics of the western Pacific: Izu-Mariana-Caroline and Ryukyu-Taiwan regions".

2138: 1994: 2135:– information about a 2007 geoscientific meeting concerned with the IBM arc, including presentations and posters that can be downloaded. 760:

was penetrated at ODP site 801C during Legs 129 and 185. These are typical mid-ocean ridge basalt that were affected by low-temperature

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built on a submarine platform that lies between 1 and 4 km water depth. Volcanic islands are common in the Izu segment, including

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Iidaka, Takashi; Furukawa, Yoshitsugu (25 February 1994). "Double Seismic Zone for Deep Earthquakes in the Izu–Bonin Subduction Zone".

288:

Simplified bathymetric profiles across the IBM arc system, approximate locations shown in first figure. T indicates position of trench.

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for seven years, along with the overseer of the abandoned plantation and an attractive young Japanese woman. The novel and 1953 film

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orientation to the modern N-S trend. This occurred during mid-Cretaceous time, a ~35–40 Ma interval characterized by a lack of

171:

to less than 3 km where the Ogasawara Plateau enters the trench. The southern boundary is found where the IBM Trench meets the

31: 1636: 2267: 108:, with younger lithosphere in the north and older lithosphere in the south, including the oldest (~170 million years old, or Ma) 1091:

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).

187: 2297: 1201: 329:, where IBM comes onshore in Japan) are found in the southern part of the Bonin segment, where the extinct volcanic islands of 2153: 338:

composition – the shoshonitic province – are found in the transition between the Bonin and Mariana arc segments, including

155:

northeastward and onto southern Honshū, joining up with a complex system of thrusts that continue offshore eastward to the

1063:"Cretaceous Volcanic Sequences and Jurassic Oceanic Crust in the East Mariana and Pigafetta Basins of the Western Pacific" 147:), up to 1,000 km from the present IBM trench. The IBM arc system is the surficial expression of the operation of a 38: The IBM arc system in the Western Pacific. Lines with arrows show approximate locations of E–W profiles across arc. 764:. This crust is overlain by a 3 m thick, bright yellow hydrothermal deposit and about 60 m of alkali olivine 74:; much more of the IBM arc system is submerged below sealevel. The IBM arc system lies along the eastern margin of the 1827:

Scholz, C.H.; Campos, J. (1995). "On the mechanism of seismic decoupling and back arc spreading at subduction zones".

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17th International Conference on Offshore Mechanics and Arctic Engineering; Lisbon; Portugal; held in 5–9 July 1998

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found on the submarine parts of IOCMs give us a chance to study how many of Earth's important ore deposits formed.

2146: 547: 144: 112:. Subduction rates vary from ~2 cm (1 inch) per year in the south to 6 cm (~2.5 inches) in the north. 2392: 1985: 1730: 1554: 1169:"East Mariana Basin tholeiites: Cretaceous intraplate basalts or rift basalts related to the Ontong Java plume?" 1151: 636:

deposited adjacent to Japan and carbonate sediment]]s associated with the relatively shallow Caroline Ridge and

1669:"Pacific Plate subduction beneath the central Mariana and Izu–Bonin fore-arcs: New insights from an old margin" 846: 322: 305:

The magmatic axis of the arc is well defined from Honshū to Guam. This ‘magmatic arc’ is often submarine, with

132: 1607:

Nakanishi, M. (1993). "Expression of Five Fracture Zones in the Northwestern Pacific Ocean". In Prigle, M.S.;

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found a DSZ lying 80 km and 120 km deep, with the two zones separated by 30 35 km. Earthquake

812: 1704:"Are the lower planes of double seismic zones caused by serpentine dehydration in subduction oceanic mantle?" 119:

The IBM arc system is an excellent example of an intra-oceanic convergent margin (IOCM). IOCMs are built on

2487: 2332: 2169: 1274:"Global teleseismic earthquake relocation with improved travel times and procedures for depth determination" 1031: 761: 554:

The age of Western Pacific seafloor has been interpreted from seafloor magnetic anomalies correlated to the

543: 479:

entered the trench 4 – 10 million years ago. However, the composition of the western Pacific seafloor-

172: 2482: 2327: 2245: 733: 693: 677:, where today off-ridge volcanism, shallow bathymetry, and thin lithosphere is known as the 'Superswell' ( 563: 1229:"Effect of recent revisions to the geomagnetic reversal time scale on estimates of current plate motions" 486:

The Pacific Plate seafloor east of the IBM arc system can be subdivided into a northern portion that is

1632:"Magnetic anomaly lineations from Late Jurassic to Early Cretaceous in the west-central Pacific Ocean" 2451: 2212: 2065: 2049: 1973: 1922: 1872: 1836: 1807: 1759: 1718: 1680: 1645: 1578: 1542: 1506: 1457: 1428: 1399: 1366: 1288: 1243: 1180: 1139: 1104: 555: 535: 204: 196: 164: 75: 645: 566: 51: 2124: 2115: 1938: 1481: 1312: 1213: 947: 659:), and at least 650 m of tholeiitic flows and sills in the Nauru Basin, near ODP Site 462. 429: 299: 1858:"A model for the motion of the Philippine Sea Plate consistent with NUVEL-1 and geological data" 1946: 1888: 1265:

Volcanic, geothermal and ore-forming fluids: Rulers and witnesses of processes within the Earth

1007:

was accidentally introduced during World War II and has since devastated native birds on Guam.

452:. Serpentinite thus generated may carry water deep into the mantle as a result of subduction. 151:

and this defines its vertical extent. The northern boundary of the IBM arc system follows the

78:

in the Western Pacific Ocean. It is the site of the deepest gash in Earth's solid surface, the

2435: 2312: 2086: 2015: 2005: 1777: 1734: 1616: 1473: 1336: 1228: 1155: 1077: 1049: 965: 613: 2366: 2272: 2106: 2057: 1981: 1930: 1880: 1844: 1815: 1767: 1726: 1688: 1653: 1586: 1550: 1514: 1465: 1436: 1407: 1374: 1304: 1296: 1251: 1188: 1184: 1147: 1112: 1004: 785: 511: 442: 396: 1320: 2255: 2227: 2194: 1558: 1026: 978: 875: 476: 433: 347: 330: 168: 148: 79: 71: 48: 640:. Strong seafloor currents are probably responsible for this erosion or non-deposition. 2053: 1977: 1926: 1876: 1840: 1811: 1798:

Samowitz, I.; Forsyth, D. (1981). "Double Seismic Zone Beneath the Mariana Island Arc".

1763: 1722: 1684: 1649: 1582: 1546: 1510: 1461: 1432: 1403: 1378: 1370: 1292: 1247: 1143: 1108: 2407: 2379: 2362: 2181: 1658: 1631: 1062: 1021: 1016: 919:

identified 76 volcanic edifices along 1370 km of the Mariana arc, grouped into 60

808: 743:, accumulated mostly in the Cretaceous but also in the last 7 million years (late 652: 637: 425: 359: 264: 260: 216: 200: 83: 2004:. Geophysical Monograph. Vol. 138. American Geophysical Union. pp. 175–222. 276: 2466: 2430: 2422: 2417: 2412: 2402: 2352: 2347: 2317: 2292: 2277: 2240: 2235: 2217: 2207: 2202: 2185: 2085:. Geophysical Monograph. Vol. 77. American Geophysical Union. pp. 307–334. 2078: 1942: 1615:. Geophysical Monograph. Vol. 77. American Geophysical Union. pp. 121–136. 1608: 1494: 1411: 1387: 1192: 1069: 1000: 951: 757: 531: 503: 480: 461: 334: 326: 310: 179:. Thus defined, the IBM arc system spans over 25° of latitude, from 11°N to 35°20’N 160: 152: 120: 109: 94: 67: 1485: 1316: 1076:. Geophysical Monograph. Vol. 77. American Geophysical Union. pp. 77–101. 972:

in the Bonin Islands. Twelve Japanese seamen were stranded in June 1944 on volcanic

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hid out in the wilds of Guam for 28 years before coming out of hiding in 1972. The

867: 740: 629: 625: 609: 449: 156: 124: 1469: 1128:"Pacific microplate and the Pangea supercontinent in the Early to Middle Jurassic" 961:

during the early 19th century. At that time they were known as the Peel Islands.

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Simplified geologic and magnetic map of the western Pacific, based on the work of

346:, south of which the Mariana arc includes volcanic islands (from north to south): 58:. The IBM arc system extends over 2800 km south from Tokyo, Japan, to beyond 17: 2342: 2337: 983: 955: 805: 507: 487: 472: 437: 314: 255: 105: 63: 2177: 1791:

Proceedings of the Ocean Drilling Project, Scientific Results, College Station

969: 841: 828: 797: 784:. This section provides an overview of these data, including a discussion of 781: 748: 605: 515: 469: 445: 318: 208: 102: 90: 55: 1781: 1738: 1159: 1053: 2259: 2173: 1819: 1590: 1518: 1497:; Natland, J.H.; Ito, G. (1990). "The Darwin Rise: Cretaceous Superswell?". 1440: 996: 987: 836: 713: 697: 674: 649: 594: 590: 306: 1477: 1300: 1267:. Society of Economic Geologists Spec. Publ. Vol. 10. pp. 91–110. 892:), or that DSZs represent the locus of serpentine dehydration in the slab ( 827:

Map view of bathymetry and seismicity in the IBM subduction zone using the

284: 1202:"Late Jurassic-Early Cretaceous and oceanic magnetic anomaly block models" 542:. Numbers with asterisks represent scientific drilling sites, especially 30: 1934: 1772: 1747: 1693: 1668: 1117: 1092: 973: 801: 725: 709: 491: 465: 375: 363: 339: 280:

Simplified bathymetric and topographic profile along the IBM magmatic arc

211:

for PH-PA as inferred from the NUVEL-1A model for current plate motions (

98: 862:

faulting mechanism for deep earthquakes is a hotly debated topic (e.g.,

780:

The deep structure of the IBM system has been imaged using a variety of

538:

is shown with arrows, numbers correspond to velocities (mm/year), after

522: 241: 958: 950:

first landed after his epic crossing of the Pacific Ocean in 1521. The

753: 744: 737: 705: 701: 371: 355: 233:

in southern IBM is tectonically more active than that in northern IBM.

230: 2130:

Ring of Fire 2003 investigations in the Mariana arc – including videos

2121:

Ring of Fire 2004 investigations in the Mariana arc – including videos

2112:

Ring of Fire 2006 investigations in the Mariana arc – including videos

1884: 1848: 1748:"Chemical composition of sediments subducting at the Izu–Bonin Trench" 1255: 1093:"Hydrothermal activity and volcano distribution along the Mariana arc" 2061: 1746:

Plank, T.; Kelley, K. A.; Murray, R.W.; Stern, L. Q. (3 April 2007).

1308: 1127: 992: 765: 669: 665: 617:

in the Eastern Pacific and very old seafloor in the Western Pacific.

495: 367: 343: 294: 2133: 1168: 499: 688: 1204:. In W. A. Berggren; D.V. Kent; M.-P. Aubry; J. Hardenbol (eds.). 822: 717: 687: 633: 621: 521: 514:

Ridge. The first two chains formed by off-ridge volcanism during

410: 283: 275: 240: 186: 176: 128: 378:. Mariana volcanoes again becomes submarine south of Anatahan. 2127: 2118: 2109: 1061:

Abrams, L.J.; Larson, R.L.; Shipley, T.H.; Lancelot, Y. (1993).

800:

are essential for locating and understanding the morphology and

721: 351: 342:. The magmatic arc in the Marianas is submarine to the north of 59: 2142: 696:

Site 1149 (see previous figure for location). Far right gives

1227:

DeMets, Charles; Gordon, R.G.; Argus, D.D.; Stein, S. (1994).

578: 1986:

10.1130/0016-7606(1992)104<1621:SZIEFT>2.3.CO;2

1731:

10.1130/0091-7613(2001)029<0299:ATLPOD>2.0.CO;2

1555:

10.1130/0091-7613(1996)024<0027:EOMAPS>2.3.CO;2

1528:"Estimates of modern arc-parallel strain rates in forearcs" 1200:

Channell, J.T.; Erba, E.; Nakanishi, M; Tamaki, K. (1995).

1152:

10.1130/0091-7613(2001)029<0735:PMATPS>2.0.CO;2

656: 589:). The oldest sediments at site 801C are middle Jurassic, 582: 510:-Ogasawara Plateau, the Magellan Seamounts Chain, and the 498:, and islands define three great, WNW-ESE trending chains ( 924: 858: 853: 832: 682: 1995:"An Overview of the Izu–Bonin-Mariana Subduction Factory" 432:

mark where Pacific Plate begins its descent into the IBM

2033:

Von Huene, Roland; Ranero, C. R.; Vannucchi, P. (2004).

732:

The figure above shows the typical sediments drilled at

559: 527: 456:

Geology and composition of the westernmost Pacific Plate

400: 2083:

The Mesozoic Pacific: Geology, Tectonics, and Volcanism

1613:

The Mesozoic Pacific: Geology, Tectonics, and Volcanism

1272:

Engdahl, E.R.; van der Hilst, R.D.; Buland, R. (1998).

1074:

The Mesozoic Pacific: Geology, Tectonics, and Volcanism

935: 916: 905: 573:). The oldest identifiable lineations are M33 to M35 ( 1331:

Gradstein, F.M.; Ogg, J.G.; Smith, A.G., eds. (2005).

1046:

Plate structure and the origin of double seismic zones

660: 212: 1167:

Castillo, P.R.; Pringle, M.S.; Carlson, R.W. (1994).

390:

Behavior and composition of the Western Pacific plate

1630:

Nakanishi, Masao; Tamaki, K.; Kobayashi, K. (1992).

2444: 2361: 2254: 2226: 2193: 954:were a significant stop for water and supplies for 598: 417: 127:built on continental crust, such as Japan or the 1993:Stern, R.J.; Fouch, M.J.; Klemperer, S. (2003). 1350:Green, II, Harry W.; Houston, Heidi (May 1995). 1281:Bulletin of the Seismological Society of America 900:Mariana Arc volcanism and hydrothermal activity 880: 871: 700:and age, 3 columns show vertical variations of 655:in the East Mariana Basin and Pigafetta Basin ( 570: 1667:Oakley, A.J.; Taylor, B.; Moore, G.F. (2008). 884: 816: 539: 2154: 1359:Annual Review of Earth and Planetary Sciences 946:Guam in the southern IBM arc system is where 604:Seafloor spreading in the Pacific during the 436:. The IBM trench is where the Pacific Plate 8: 1829:Journal of Geophysical Research: Solid Earth 1571:Journal of Geophysical Research: Solid Earth 863: 811:, and this is particularly true for the IBM 251: 221: 776:Geophysics of the subducted slab and mantle 302:associated with the IBM forearc or trench. 159:. The intersection of the IBM, Japan, and 2161: 2147: 2139: 1218:: CS1 maint: location missing publisher ( 1856:Seno, T.; Stein, S.; Gripp, A.E. (1993). 1771: 1692: 1657: 1116: 574: 225: 89:The IBM arc system formed as a result of 866:), and has yet to be resolved. Double 854:Engdahl, van der Hilst & Buland 1998 833:Engdahl, van der Hilst & Buland 1998 29: 1569:Menard, H.W. (1984). "Darwin Reprise". 942:Historical importance of IBM arc system 893: 769: 586: 1211: 904:Bathymetry of the Mariana arc region ( 678: 560:Nakanishi, Tamaki & Kobayashi 1992 528:Nakanishi, Tamaki & Kobayashi 1992 401:Von Huene, Ranero & Vannucchi 2004 237:Geologic history of the IBM Arc system 97:. The IBM arc system now subducts mid- 2035:"Generic model of subduction erosion" 2000:. In J. Eiler; M. Hirschmann (eds.). 889: 788:structure at depths >200 km. 259:ultimately producing Earth's largest 7: 2081:; Sliter, W.V.; et al. (eds.). 1752:Geochemistry, Geophysics, Geosystems 1673:Geochemistry, Geophysics, Geosystems 1611:; Sliter, W.V.; et al. (eds.). 1126:Bartolini, A.; Larson, R.L. (2001). 1072:; Sliter, W.V.; et al. (eds.). 728:. Modified from Plank et al. (2006). 661:Castillo, Pringle & Carlson 1994 1379:10.1146/annurev.ea.23.050195.001125 1352:"The Mechanics of Deep Earthquakes" 1173:Earth and Planetary Science Letters 2388:Eastern margin of the Sea of Japan 1659:10.1111/j.1365-246X.1992.tb00126.x 648:. There are 100–400 m thick 195:The IBM arc system is part of the 25: 1637:Geophysical Journal International 995:to drop the first atomic bomb on 407:IBM Trench and outer trench swell 27:Convergent boundary in Micronesia 2268:Aomori Bay West Coast Fault Zone 268:rifts began to form about 2 Ma. 123:and contrast fundamentally with 2298:Itoigawa-Shizuoka Tectonic Line 1493:McNutt, M. K.; Winterer, E.L.; 1421:Journal of Geophysical Research 747:) built on a basement of Early 599:Gradstein, Ogg & Smith 2005 418:Oakley, Taylor & Moore 2008 1335:. Cambridge University Press. 982:is based on these events. The 1: 2002:Inside the Subduction Factory 1470:10.1126/science.263.5150.1116 2478:Geology of the Pacific Ocean 1499:Geophysical Research Letters 1412:10.1016/0040-1951(88)90275-2 1193:10.1016/0012-821X(94)90263-1 540:Seno, Stein & Gripp 1993 139:Boundaries of IBM Arc system 968:was shot down in 1945 near 881:Samowitz & Forsyth 1981 872:Samowitz & Forsyth 1981 571:Bartolini & Larson 2001 2504: 2308:Japan Median Tectonic Line 2288:Futagawa-Hinagu fault zone 1526:McCaffrey, Robert (1996). 1333:A Geologic Time Scale 2004 885:Iidaka & Furukawa 1994 817:Katsumata & Sykes 1969 579:Handschumacher et al. 1988 1906:Stern, Robert J. (2002). 931:Arc hydrothermal activity 768:, 157.4±0.5 Ma old ( 712:, indicators of relative 548:Deep Sea Drilling Program 530:. Relative motion of the 272:IBM Arc system components 145:West Philippine Sea Basin 1871:(B10): 17, 941–17, 948. 1835:(B11): 22, 103–22, 115. 1208:. Tulsa. pp. 51–63. 1206:SEPM Special Publication 864:Green & Houston 1995 847:Arizona State University 608:evolved from a more E-W 252:Stern & Bloomer 1992 222:Scholz & Campos 1995 2333:Philippine Fault System 1820:10.1029/JB086iB08p07013 1702:Peacock, S. M. (2001). 1591:10.1029/JB089iB12p09960 1519:10.1029/GL017i008p01101 1441:10.1029/JB074i025p05923 1185:1994E&PSL.123..139C 1032:South Chamorro Seamount 762:hydrothermal alteration 577:) or perhaps even M38 ( 2328:Northeastern Japan Arc 2246:Philippine Mobile Belt 1301:10.1785/BSSA0880030722 849: 782:geophysical techniques 734:Ocean Drilling Program 729: 694:Ocean Drilling Program 564:Ocean Drilling Program 551: 544:Ocean Drilling Project 421: 289: 281: 246: 192: 47:(IBM) arc system is a 40: 2473:Izu–Bonin–Mariana Arc 2303:Izu–Bonin–Mariana Arc 1915:Reviews of Geophysics 1044:Abers, G. A. (1996). 826: 691: 525: 414: 287: 279: 244: 190: 33: 2452:Boso Triple Junction 2393:Izu–Ogasawara Trench 2213:Philippine Sea Plate 1935:10.1029/2001RG000108 1773:10.1029/2006GC001444 1694:10.1029/2007gc001820 1118:10.1029/2007JB005423 925:de Ronde et al. 2003 859:Nakamura et al. 1998 796:Spatial patterns of 583:Channell et al. 1995 556:geomagnetic reversal 536:Philippine Sea Plate 534:with respect to the 500:Winterer et al. 1993 205:North American Plate 197:Philippine Sea Plate 165:Boso Triple Junction 133:hydrothermal systems 76:Philippine Sea Plate 2054:2004Geo....32..913V 1978:1992GSAB..104.1621S 1966:Geol. Soc. Am. Bull 1927:2002RvGeo..40.1012S 1877:1993JGR....98...17W 1841:1995JGR...10022103S 1812:1981JGR....86.7013S 1793:. pp. 363–372. 1764:2007GGG.....8.4I16P 1723:2001Geo....29..299P 1685:2008GGG.....9.6003O 1650:1992GeoJI.109..701N 1583:1984JGR....89.9960M 1547:1996Geo....24...27M 1511:1990GeoRL..17.1101M 1462:1994Sci...263.1116I 1456:(5150): 1116–1118. 1433:1969JGR....74.5923K 1404:1988Tectp.155..365H 1386:Handschumacher, D; 1371:1995AREPS..23..169G 1293:1998BuSSA..88..722E 1248:1994GeoRL..21.2191D 1144:2001Geo....29..735B 1109:2008JGRB..113.8S09B 1068:. In Prigle, M.S.; 813:Wadati–Benioff zone 646:Ontong-Java Plateau 567:scientific drilling 428:and the associated 62:, and includes the 52:convergent boundary 1908:"Subduction Zones" 1577:(B12): 9960–9968. 1236:Geophys. Res. Lett 999:in 1945. Sergeant 850: 835:. Circles denote 730: 692:Sediment cored at 683:McNutt et al. 1990 657:Abrams et al. 1993 614:magnetic reversals 552: 430:outer trench swell 422: 300:accretionary prism 290: 282: 247: 213:DeMets et al. 1994 193: 173:Kyushu–Palau Ridge 41: 18:Kyushu–Palau Ridge 2460: 2459: 2436:Philippine Trench 2313:Longmenshan Fault 2188:Convergence Zone) 2092:978-0-87590-036-0 2011:978-0-87590-997-4 1972:(12): 1621–1636. 1885:10.1029/93jb00782 1849:10.1029/95jb01869 1806:(B8): 7013–7021. 1622:978-0-87590-036-0 1427:(25): 5923–5948. 1342:978-0-521-78673-7 1256:10.1029/94GL02118 1242:(20): 2191–2194. 1083:978-0-87590-036-0 966:George H. W. Bush 936:Baker et al. 2008 917:Baker et al. 2008 906:Baker et al. 2008 562:and confirmed by 45:Izu–Bonin–Mariana 16:(Redirected from 2495: 2273:Baikal Rift Zone 2163: 2156: 2149: 2140: 2096: 2072: 2070: 2064:. Archived from 2062:10.1130/G20563.1 2039: 2029: 2027: 2026: 2020: 2014:. Archived from 1999: 1989: 1960: 1958: 1957: 1951: 1945:. Archived from 1912: 1902: 1900: 1899: 1893: 1887:. Archived from 1862: 1852: 1823: 1794: 1785: 1775: 1742: 1708: 1698: 1696: 1663: 1661: 1626: 1603: 1594: 1565: 1563: 1557:. Archived from 1532: 1522: 1505:(8): 1101–1108. 1489: 1444: 1415: 1398:(1–4): 365–380. 1382: 1356: 1346: 1327: 1325: 1319:. Archived from 1278: 1268: 1259: 1233: 1223: 1217: 1209: 1196: 1179:(1–3): 139–154. 1163: 1122: 1120: 1087: 1067: 1057: 1005:brown tree snake 921:volcanic centers 876:focal mechanisms 852:More recently, 512:Caroline Islands 397:tectonic erosion 37: 21: 2503: 2502: 2498: 2497: 2496: 2494: 2493: 2492: 2463: 2462: 2461: 2456: 2440: 2357: 2250: 2222: 2189: 2170:Tectonic plates 2167: 2103: 2093: 2075: 2068: 2048:(10): 913–916. 2037: 2032: 2024: 2022: 2018: 2012: 1997: 1992: 1963: 1955: 1953: 1949: 1910: 1905: 1897: 1895: 1891: 1865:J. Geophys. Res 1860: 1855: 1826: 1800:J. Geophys. Res 1797: 1788: 1745: 1706: 1701: 1666: 1629: 1623: 1606: 1597: 1568: 1561: 1530: 1525: 1492: 1447: 1418: 1385: 1354: 1349: 1343: 1330: 1323: 1276: 1271: 1262: 1231: 1226: 1210: 1199: 1166: 1125: 1097:J. Geophys. Res 1090: 1084: 1065: 1060: 1043: 1040: 1027:Mariana Islands 1013: 944: 933: 914: 902: 794: 778: 597:(~162 Ma; 488:bathymetrically 477:subduction zone 458: 434:Subduction Zone 409: 392: 331:Minami Iwo Jima 274: 239: 185: 169:Challenger Deep 161:Sagami trenches 149:subduction zone 141: 93:of the western 80:Challenger Deep 72:Mariana Islands 39: 35: 28: 23: 22: 15: 12: 11: 5: 2501: 2499: 2491: 2490: 2488:Philippine Sea 2485: 2480: 2475: 2465: 2464: 2458: 2457: 2455: 2454: 2448: 2446: 2442: 2441: 2439: 2438: 2433: 2428: 2425: 2420: 2415: 2410: 2408:Okinawa Trough 2405: 2400: 2395: 2390: 2385: 2382: 2380:Mariana Trench 2377: 2371: 2369: 2359: 2358: 2356: 2355: 2350: 2345: 2340: 2335: 2330: 2325: 2320: 2315: 2310: 2305: 2300: 2295: 2290: 2285: 2280: 2275: 2270: 2264: 2262: 2252: 2251: 2249: 2248: 2243: 2238: 2232: 2230: 2224: 2223: 2221: 2220: 2215: 2210: 2205: 2199: 2197: 2191: 2190: 2182:Eurasian Plate 2168: 2166: 2165: 2158: 2151: 2143: 2137: 2136: 2131: 2122: 2113: 2102: 2101:External links 2099: 2098: 2097: 2091: 2073: 2071:on 2011-06-14. 2030: 2010: 1990: 1961: 1903: 1853: 1824: 1795: 1786: 1743: 1717:(4): 299–302. 1699: 1664: 1644:(3): 701–719. 1627: 1621: 1604: 1595: 1566: 1564:on 2011-07-20. 1523: 1490: 1445: 1416: 1392:Tectonophysics 1383: 1347: 1341: 1328: 1326:on 2010-08-06. 1287:(3): 722–743. 1269: 1260: 1224: 1197: 1164: 1138:(8): 735–738. 1123: 1103:(B8): B08S09. 1088: 1082: 1058: 1039: 1036: 1035: 1034: 1029: 1024: 1022:Mariana Trough 1019: 1017:Mariana Trench 1012: 1009: 943: 940: 932: 929: 913: 910: 901: 898: 804:of subducting 793: 790: 777: 774: 638:Caroline Plate 575:Nakanishi 1993 457: 454: 426:oceanic trench 408: 405: 391: 388: 273: 270: 265:back-arc basin 261:back-arc basin 238: 235: 226:McCaffrey 1996 217:oceanic trench 201:Mariana Trough 184: 181: 140: 137: 84:Mariana Trench 49:tectonic plate 34: 26: 24: 14: 13: 10: 9: 6: 4: 3: 2: 2500: 2489: 2486: 2484: 2483:Seismic zones 2481: 2479: 2476: 2474: 2471: 2470: 2468: 2453: 2450: 2449: 2447: 2443: 2437: 2434: 2432: 2431:Manila Trench 2429: 2426: 2424: 2423:Suruga Trough 2421: 2419: 2418:Sagami Trough 2416: 2414: 2413:Ryukyu Trench 2411: 2409: 2406: 2404: 2403:Nankai Trough 2401: 2399: 2396: 2394: 2391: 2389: 2386: 2383: 2381: 2378: 2376: 2373: 2372: 2370: 2368: 2364: 2360: 2354: 2353:Urasoko fault 2351: 2349: 2348:Ulakhan Fault 2346: 2344: 2341: 2339: 2336: 2334: 2331: 2329: 2326: 2324: 2321: 2319: 2318:Neodani Fault 2316: 2314: 2311: 2309: 2306: 2304: 2301: 2299: 2296: 2294: 2293:Idosawa Fault 2291: 2289: 2286: 2284: 2281: 2279: 2278:Haiyuan Fault 2276: 2274: 2271: 2269: 2266: 2265: 2263: 2261: 2257: 2253: 2247: 2244: 2242: 2241:Okinawa Plate 2239: 2237: 2236:Mariana Plate 2234: 2233: 2231: 2229: 2225: 2219: 2218:Yangtze Plate 2216: 2214: 2211: 2209: 2208:Okhotsk Plate 2206: 2204: 2201: 2200: 2198: 2196: 2192: 2187: 2186:Pacific Plate 2183: 2179: 2175: 2171: 2164: 2159: 2157: 2152: 2150: 2145: 2144: 2141: 2134: 2132: 2129: 2125: 2123: 2120: 2116: 2114: 2111: 2107: 2105: 2104: 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Izu–Bonin–Mariana Arc

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