Inter-arc spreading in the Mariana Trough

Bibee, L. Dale; Shor, George G.; Lu, Ruifeng

doi:10.1016/0025-3227(80)90030-4

Cited by 106 publications

(58 citation statements)

References 11 publications

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“…The Ogasawara Plateau collision point migrates northward at $1.2 cm/a (based on Pacific and Philippine Sea Plate relative motion [Sella et al, 2002]), similar to the observed northward propagation of the Marianas rift tip [e.g., Stern et al, 1984]. The Ogasawara Plateau began subducting at the Marianas trench $8 Ma ago [Miller et al, 2006], similar to the Late Miocene onset of Marianas rifting [Karig et al, 1978;Bibee et al, 1980;Hussong and Uyeda, 1981], suggesting a possible relationship between the collision, rotation, and rifting in the Marianas. Collision of the Caroline Plateau with the Yap Trench sometime in the Oligocene to early Miocene [McCabe and Uyeda, 1983] may have had an influence on the early development of the Marianas rift (and possible clockwise rotation of the southern Marianas arc from paleomagnetic studies of Eocene to Miocene rocks [Fuller et al, 1980]).…”

Section: A222 Iransupporting

confidence: 63%

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Collisional model for rapid fore‐arc block rotations, arc curvature, and episodic back‐arc rifting in subduction settings

Wallace

Ellis

Mann

2009

Geochem Geophys Geosyst

102

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[1] We review geophysical and geological data from 23 active and ancient plate boundaries to document a compelling spatial and temporal relationship between collision, plate boundary curvature, rapid tectonic rotations, and the occurrence of back-arc rifting. Our observations support a conceptual model where the change from subduction to collision causes rapid fore-arc rotation (when viewed in a reference frame relative to the bounding tectonic plates), leading to marked plate boundary curvature. Our global compilation reveals that most active back-arc rifts are associated with rapidly rotating fore arcs and nearby collisions. Thus, we propose that collision and rapid fore-arc rotations play a major role in the evolution and kinematics of back-arc basins. We conduct numerical modeling to better understand the physical processes behind these observed rapid tectonic rotations at convergent margins. Our results suggest that the presence of an indentor or choke point in the subduction system (e.g., collision) can generate rapid rotation of the fore arc about a nearby pole and lead to back-arc rifting. The rate of fore-arc rotation and back-arc rifting depends on the incoming indentor velocity and can be greatly enhanced by slab rollback and the presence of a low-viscosity back arc. Where viscosity of the back arc is low, fore-arc rotation dominates; where back-arc viscosity is high, the formation of strike-slip faults and tectonic escape dominates. Our observational and model-derived results illustrate that shallow crustal forces produced by the entry of buoyant features into subduction zones are a fundamental mechanism for the generation of fore-arc block rotations, plate boundary curvature, back-arc rift evolution, and tectonic escape in subduction systems. Rollback of the subducting slab within the mantle will certainly enhance the processes we describe but it is not the only driving force. Wallace, L. M., S. Ellis, and P. Mann (2009), Collisional model for rapid fore-arc block rotations, arc curvature, and episodic back-arc rifting in subduction settings, Geochem. Geophys. Geosyst., 10, Q05001,

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Section: A222 Iransupporting

confidence: 63%

“…See text for discussion. [Lawver et al, 1976;Weissel, 1977;Parson and Hawkins, 1994] Yes Louisville Ridge $5 -4 Ma ago to present [Ruellan et al, 2003] Marianas Marianas Islands L. Miocene-present [Karig et al, 1978;Bibee et al, 1980;Hussong and Uyeda, 1981] Yes Ogasawara plateau (north) and Caroline plateau (south)…”

Section: Examples Of Spatial Coincidence Ofmentioning

confidence: 99%

Collisional model for rapid fore‐arc block rotations, arc curvature, and episodic back‐arc rifting in subduction settings

Wallace

Ellis

Mann

2009

Geochem Geophys Geosyst

102

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“…Os, Oh-shima; Nij, Nii-jima; Myk, Miyake-jima; Mkr, Mikura-jima; Krs, Kurose hole; Hcj, Hachijo-jima; Shc, South Hachijo caldera; Ags, Aoga-shima; Myn, Myojin knoll; Myj, Myojin-sho; Sms, South Sumisu; Ssc, South Sumisu caldera; Trs, Torishima; SB, Shikoku Basin; KS, Kinan sea mount chain; PB, Parece Vela Basin. at 10 Ma, and the consequent seafloor spreading began at 3-4 Ma [Bibee et al, 1980;Yamazaki and Stern, 1997]. Intra-arc rifting west of the present-day volcanic front of the Izu arc started at 2 Ma.…”

Section: Tectonic Settingmentioning

confidence: 99%

Seismological evidence for variable growth of crust along the Izu intraoceanic arc

Kodaira¹,

Sato²,

Takahashi³

et al. 2007

J. Geophys. Res.

145

209

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[1] The processes that create continental crust in an intraoceanic arc setting are a matter of debate. To address this issue, we conducted an active source wide-angle seismic study to examine along-arc structural variations of the Izu intraoceanic arc. The data used were acquired over a 550-km-long profile along the volcanic front from Sagami Bay to Tori-shima. The obtained structural model showed the existence of felsic to intermediate composition middle crust with a P wave velocity (Vp) of 6.0-6.5 km s À1 in its upper part and 6.5-6.8 km s À1 in its lower part. The thickness of the middle crust varied markedly from 3 to 13 km. The underlying lower crust also consisted of two layers (Vp of 6.8-7.2 km s À1 in the upper part and Vp of 7.2-7.6 km s À1 in the lower part). The upper of these layers was interpreted to consist of plutonic gabbro, and the lower layer was interpreted to be mafic to ultramafic cumulates. Average crustal velocities calculated from our model showed remarkable lateral variation, which correlated well with arc volcanism. Low average crustal seismic velocities ($6.7 km s À1

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“…The back-arc spreading process formed the Kyushu-Palau Ridge as a remnant arc at the western edge of the Parece Vela and Shikoku basins. Backarc rifting along the Mariana trough started at 10 Ma, and the consequent seafloor spreading began at 3-4 Ma (Bibee et al, 1980;Yamazaki and Yuasa, 1998). In the Izu arc, intra-arc rifting started to the west of the present-day volcanic front at 2 Ma (e.g., Ishizuka et al, 2002).…”

Section: Introductionmentioning

confidence: 99%

Structural variation of the Bonin ridge revealed by modeling of seismic and gravity data

et al. 2011

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A previous study of a longitudinal profile along the Bonin ridge concluded that remarkably thin forearc crust (<10 km thick) along the northern half of the ridge indicates that the crust there was formed by forearc spreading during the initial stage of subduction along the Izu-Bonin intra-oceanic arc. However, a profile across the Bonin ridge shows a thicker crust. In this study, we construct a model that takes into account seismic and gravity data from both profiles. Re-modeling of the seismic data showed a north-south aligned area of thin crust (∼10 km thick) at the center of the Bonin ridge; this structure was confirmed by gravity data. The seismic data at the eastern end of the across-arc profile suggests that the crust thickens beneath the trenchward slope of the Bonin ridge. However, a petrological model suggests a trenchward extension of forearc oceanic crust that formed during the initial stage of subduction. Although further detailed investigation is required, we suggest that this contradiction can be explained either by the subduction of buoyant crust immediately beneath the forearc oceanic crust, or by the presence of a serpentinized mantle wedge beneath the forearc oceanic crust.

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Inter-arc spreading in the Mariana Trough

Cited by 106 publications

References 11 publications

Collisional model for rapid fore‐arc block rotations, arc curvature, and episodic back‐arc rifting in subduction settings

Collisional model for rapid fore‐arc block rotations, arc curvature, and episodic back‐arc rifting in subduction settings

Seismological evidence for variable growth of crust along the Izu intraoceanic arc

Structural variation of the Bonin ridge revealed by modeling of seismic and gravity data

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