Progress in Earth andPlanetary Science

Philippine Sea Plate inception, evolution, andconsumption with special emphasis on the earlystages of Izu-Bonin-Mariana subduction
Lallemand
Lallemand Progress in Earth and Planetary Science (2016) 3:15
DOI 10.1186/s40645-016-0085-6

Lallemand Progress in Earth and Planetary Science (2016) 3:15
DOI 10.1186/s40645-016-0085-6

REVIEW

Progress in Earth andPlanetary Science

Open AccessPhilippine Sea Plate inception, evolution,and consumption with special emphasis on
the early stages of Izu-Bonin-Mariana
subduction
Serge Lallemand1,2Abstract
We compiled the most relevant data acquired throughout the Philippine Sea Plate (PSP) from the early expeditions
to the most recent. We also analyzed the various explanatory models in light of this updated dataset. The following
main conclusions are discussed in this study. (1) The Izanagi slab detachment beneath the East Asia margin around60–55 Ma likely triggered the Oki-Daito plume occurrence, Mesozoic proto-PSP splitting, shortening and then failure
across the paleo-transform boundary between the proto-PSP and the Pacific Plate, Izu-Bonin-Mariana subduction
initiation and ultimately PSP inception. (2) The initial splitting phase of the composite proto-PSP under the plume
influence at ∼54–48 Ma led to the formation of the long-lived West Philippine Basin and short-lived oceanic basins,part of whose crust has been ambiguously called “fore-arc basalts” (FABs). (3) Shortening across the paleo-transformboundary evolved into thrusting within the Pacific Plate at ∼52–50 Ma, allowing it to subduct beneath the newly
formed PSP, which was composed of an alternance of thick Mesozoic terranes and thin oceanic lithosphere. (4) The
first magmas rising from the shallow mantle corner, after being hydrated by the subducting Pacific crust beneaththe young oceanic crust near the upper plate spreading centers at ∼49–48 Ma were boninites. Both the so-called
FABs and the boninites formed at a significant distance from the incipient trench, not in a fore-arc position aspreviously claimed. The magmas erupted for 15 m.y. in some places, probably near the intersections between
back-arc spreading centers and the arc. (5) As the Pacific crust reached greater depths and the oceanic basinscooled and thickened at ∼44–45 Ma, the composition of the lavas evolved into high-Mg andesites and then arc
tholeiites and calc-alkaline andesites. (6) Tectonic erosion processes removed about 150–200 km of frontal margin
during the Neogene, consuming most or all of the Pacific ophiolite initially accreted to the PSP. The result was
exposure of the FABs, boninites, and early volcanics that are near the trench today. (7) Serpentinite mud volcanoes
observed in the Mariana fore-arc may have formed above the remnants of the paleo-transform boundary between
the proto-PSP and the Pacific Plate.
Keywords: Philippine Sea Plate, Izu-Bonin-Mariana, Subduction initiation, Boninite, Fore-arc basalt, Serpentinite mud
volcano, Back-arc basin, Transform fault, Arc terrane, Plume-ridge interaction

Correspondence: lallem@gm.univ-montp2.fr
1
Géosciences Montpellier, CNRS, University of Montpellier, Montpellier,France2
LIA D3E “From Deep Earth to Extreme Events”, CNRS - MOST, Taipei, Taiwan© 2016 Lallemand. Open Access This article is distributed under the terms of the Creative Commons Attribution 4.0
International License (http://creativecommons.org/licenses/by/4.0/), which permits unrestricted use, distribution, andreproduction in any medium, provided you give appropriate credit to the original author(s) and the source, provide a link to theCreative Commons license, and indicate if changes were made.

Lallemand Progress in Earth and Planetary Science (2016) 3:15

Introduction
The visible part of the Philippine Sea Plate (PSP) has adiamond shape with a maximum north-south length of∼3400 km and a maximum east-west width of ∼2600 km.
Its extent below southwest Japan, the Ryukyu Arc, and thePhilippine Arc (see Fig. 1) is outlined by the Benioff zones
and tomography anomalies (Kao and Chen 1991; Bijwaard
et al. 1998; Wang et al. 2008). Removal of the PSP edges
through tectonic erosion has also been documented, especially along the Izu-Bonin-Mariana (IBM) Trench(Hussong and Uyeda 1981; Bloomer 1983; Fryer et al.
1992; Lallemand 1995). Considering that the eastern
Shikoku, Parece Vela and Mariana basins, which opened
as back-arc basins (Karig 1971a; Uyeda and Ben Avraham1972) during the Neogene, it is clear that the shape andarea of the PSP has changed over time. The PSP subducts
under southwest Japan and the Ryukyu Arc along its
northwestern side, and under the Philippine Arc along its
southwestern side. Conversely, it overrides the PacificPage 2 of 26

Plate along its eastern edge (fringed by the IBM Arc) andits central-western edge (fringed by the Luzon Arc). To
summarize, most of its boundaries consist of subduction
zones except a small divergent segment in the south,
called the Ayu Trough (Fujiwara et al. 1995).
Many authors have contributed to our understandingof the tectono-magmatic evolution of the PSP (e.g.,
Uyeda and Ben Avraham 1972; Hilde and Lee 1984;
Seno and Maruyama 1984; Hickey-Vargas 1991; Stern
and Bloomer 1992; Hall et al. 1995a; Okino et al., 1999;
Deschamps and Lallemand 2002). From among thisgroup, I would like to dedicate this review to Anne
Deschamps who recently departed.
The main objectives of this review paper are as
follows:
 to scan the nature and age of the various parts of

the PSP including the subducted and eroded parts
that represent about one third of its total area.

Fig. 1 Philippine Sea Plate boundaries and toponymy. Plate boundaries (in red) are reported on a bathymetric map based on GEBCO data. Main
faults are represented by thick black lines and active spreading centers by double lines. Red triangles are located on the overriding plates along the
subduction boundaries. Blue dotted lines outline the OIB plateaus. From north to south: Su.T. Suruga Trough, Sa.T. Sagami Trough, Nankai T.
Nankai Trough, A.D.O. Region Amami-Daito-Oki-Daito Region, Bonin Isl. Bonin Islands, O.D.P. Oki-Daito Plateau, O.D.R. Oki-Daito Ridge, U.D. Urdaneta
Plateau, O.D.E. Oki-Daito Escarpment, L.V.F. Longitudinal Valley Fault, H.B. Huatung Basin, G.R. Gagua Ridge, L.V.A. Luzon Volcanic Arc, L.O.F.Z.
Luzon-Okinawa Fracture Zone, B.R. Benham Rise, C.B.F. rift Central Basin Fault rift, M.T. Mariana Trough, M.G.R. Malaguana-Gadao Ridge, Mindanao
F.Z. Mindanao Fracture Zone, Y.T. Yap Trench, P.T. Palau Trench, and A.T. Ayu TroughLallemand Progress in Earth and Planetary Science (2016) 3:15

Page 3 of 26

 to portray the major tectonic events that have

The boundaries of the PSP have changed tremendously
through time. Indeed, most of the so-called “Philippine
mobile belt” still belonged to the PSP during the
Miocene (e.g., Moore and Silver 1982; Lewis and Hayes
1983; Hall 1987; Rangin et al. 1990; Lallemand et al.
1998). In the past, the transpressive plate boundary was
located either west of or within the archipelago. The
reader can refer to Pubellier et al. (2004) among others
for accounts of the huge continental and oceanic sliver
motions of this area during the Neogene. The southeastern boundary, i.e., Mariana and Yap Trenches in particular,considerably lengthened through time to accommodate
the spreading of the West Philippine Basin, PareceVela
Basin, and Mariana Trough (Fig. 1; Deschamps andLallemand 2002; Kobayashi 2004; Okino et al. 2009;
Ribeiro et al. 2013). In this section, we will focus on thevisible part of the present-day PSP, aiming to trace thevarious pieces of the puzzle that result from a multi-stage
tectonic evolution.

dipping Philippine Trench at the latitude of Luzon islandand the northward-dipping Ryukyu Trench at the latitudeof Taiwan. In the vicinity of both islands, the relative convergence between the Eurasian Plate and the PSP is accommodated along several faults, which include theLongitudinal Valley Fault and deformation front in Taiwan(Angelier 1986) and the Philippine Fault and Manila
Trench in Luzon (Pubellier et al. 2004). In the south, theshort Palau Trench extends over a distance of ∼500 km
into a slow-spreading ridge, called the Ayu Trough, which
is supposed to have been active since 25 Ma (Weissel andAnderson 1978; Fujiwara et al. 1995). The southernmost
E-W-trending boundary corresponds to an area of diffuse
strike-slip deformation, which includes the Sorong Fault(Hall 1987). There are two major collisions between active
volcanic arcs carried by the PSP and the adjacent margins.
One is in the west with the Luzon volcanic arc. It has resulted in the Taiwan orogeny since the Pliocene (e.g.,
Angelier 1986; Lallemand et al. 2001; Malavieille et al.
2002). The other is in the north with the IBM arc. It has
resulted in the development of the Izu Collision Zone
since the Upper Miocene (e.g., Taira et al. 1989; Aoike
2001; Arai et al. 2009). Lallemand (2014) described the deformation modes of the subducting PSP associated withthese two arc-continent collisions.
The PSP itself appears as a mosaic of oceanic basins,aseismic ridges, plateaus, fracture zones, volcanic arcs
and fore-arcs, fossil, and active spreading centers. Despite some controversy on the age of the small westernmost Huatung Basin (see Fig. 1), oceanic basins areyounger from west to east.

Present-day boundaries of the PSP

Oceanic basins of the PSP

The PSP was the fastest-moving plate during Cenozoic
times (Zahirovic et al. 2015). Today, the absolute motionof its southern part (∼10 cm/year) in classical reference
frames (DeMets et al. 2010; Seton et al. 2012 or Kreemer
et al. 2014) is comparable to that of the Pacific Plate,which is presently the fastest plate in the world. The highspeed of these two plates is primarily due to the slab pullforce exerted along their northwestern boundaries (i.e.,
Forsyth and Uyeda 1975; Spence 1987; Pacanovsky et al.
1999; Faccenna et al. 2007). The PSP subducts toward thenorthwest along ∼2500 km of the Ryukyu Trench andNankai Trough and 1500 km of the Philippine Trench(Fig. 1). This dominant force controls the northwest motion of the plate. The plate is surrounded by subduction
zones. It is the down-going plate along most of its westernedges, and the overriding plate along its eastern edge
(marked by the Izu-Bonin-Mariana, Yap and Palau
trenches) and the central part of its western edge (marked
by the Manila Trench). There, between Luzon and Taiwan,
the plate boundary is not a single distinct unit because theeastward-dipping Manila Trench overlaps the westward-

The West Philippine Basin (WPB) is the largest of the
PSP oceanic basins at ∼1500 km long and ∼1100 km
wide. It occupies more than one third of the plate’s surface. The main scar, which is east of Luzon and trends
WNW-ESE, was initially called the Central Basin Fault(CBF). Mrozowski et al. (1982) and then Hilde and Lee(1984) demonstrated that symmetric spreading occurredon both sides of that feature, which was thus identified
as a fossil spreading center and renamed the CBF rift. Its
unusual depth, which reaches a maximum of 7900 m,
has been explained by post-spreading amagmatic extension (Fujioka et al. 1999; Deschamps et al. 1999, 2002;
Okino and Fujioka 2003). Several ridge jumps, plateau
emplacements and overlapping spreading centers wereinterpreted by Deschamps et al. (2002, 2008) as the expression of plume-ridge interaction in the image of the
spreading pattern in the North Fiji Basin (Lagabrielle etal. 1997; Faccenna et al. 2010). Taylor and Goodliffe(2004), mainly based on a single line acquired south of
the CBF rift, suggested that the opening direction of thebasin rotated 100° clockwise in the period from 48–49

shaped the PSP such as its inception, subduction
initiation, intraplate deformation including
shortening, rifting and spreading, or tectonic erosion
and subduction along some of its boundaries.
 ultimately, to give rise to new insights into the PSP
tectonic evolution and serve as a guide for new
investigations.

Review
Overview of the non-subducted part of the present-dayPSPLallemand Progress in Earth and Planetary Science (2016) 3:15

to 33 Ma. Another striking difference from the initialmodel proposed by Hilde and Lee (1984) concerns thenorthernmost and southernmost parts of the WPB.
Deschamps and Lallemand (2002) showed that magnetic
lineations trend N-S north of the Oki-Daito escarpment(ODE, Figs. 1 and 2), i.e., perpendicular to the main
trend on both sides of the CBF rift. They postulate that
this piece of oceanic crust was the oldest in the WPB
based on a dated basalt collected at site 294/5. According to their interpretation, rifting may have started assoon as 55 Ma ago behind the proto-Philippine Arc.
Recently, Sasaki et al. (2014) provided new insights on
the southernmost part of the WPB including the Palau
Basin, south of the Mindanao Fracture Zone (FZ, seeFig. 1). Based on three short magnetic profiles across the
Palau Basin and a dolerite sampled along the Mindanao
FZ dated at ∼40 Ma (Ishizuka et al. 2015), they concluded
that the Palau Basin exhibits N-S magnetic lineations, as it
does north of the ODE. Their magnetic model, even poorly
constrained, provides an age of 35–40 Ma, which is quite
young compared to its counterpart in the north. Whatever
the age of this basin, it is now clear that it is made of normal oceanic crust and spreading occurred E-W (in its
present position) south of the Mindanao FZ. The first estimate of the spreading period based on magnetic lineations

Page 4 of 26

by Hilde and Lee (1984) of between 60 and 35 Ma was revised by Deschamps and Lallemand (2002) to from 54 to
33/30 Ma with a short, late extension episode between 30
and 26 Ma. Other authors (Taylor and Goodliffe 2004;
Sasaki et al. 2014) refute the oldest ages proposed by Hildeand Lee (1984) in the southern part of the WPB because it
has been proved that the seafloor fabric changes drasticallysouth of the Mindanao FZ. Unlike most previous authors,
Sasaki et al. (2014) consider a constant spreading rate forthe opening of the WPB and a progressive cessation of
spreading from 37.5 Ma in the southeast to 35.5 Ma in thenortheastern part of the CBF rift.
Hilde and Lee (1984) also supposed that the WPB extended westward in the Huatung Basin across the northsouth trending Gagua Ridge, whereas Deschamps et al.
(2000) argued that dredged gabbros, dated as Early
Cretaceous in the Huatung Basin, invalidated this hypothesis. The age of this small basin is highly controversial. Estimates vary from 131 to 119 Ma (Deschamps etal. 2000) to 52–43 Ma for the northern part and Early
Cretaceous for the southern part (Sibuet et al. 2002), to
44–33 Ma (Hilde and Lee, 1984), 42–33 Ma (Doo et al.
2015), or even ∼ 30-15 Ma (Kuo et al. 2009). Further details and an interesting discussion about this controversy
are available in Eakin et al. (2015).

Fig. 2 Close-up view of the bathymetry of the northern half of the WPB. Details of the Amami-Daito-Oki-Daito region, Gagua Ridge and LuzonOkinawa Fracture Zone are outlinedLallemand Progress in Earth and Planetary Science (2016) 3:15

East of the WPB lies a north-south elongated(∼2500 km long by ∼200–600 km wide) pair of oceanic
basins called Shikoku and Parece Vela. Both basins riftedright after the cessation of spreading in the WPB, i.e.,∼30 Ma ago, then spreading occurred between 29–26
and 15 Ma (Chamot-Rooke et al. 1987; Okino et al.
1994, 1998). Sdrolias et al. (2004) further detailed thekinematics of this “twin-back-arc opening,” characterizing it as the consequence of Pacific slab rollback and
PSP clockwise rotation. The back-arc region ruptured
simultaneously in the north on the Shikoku rift and in
the south on the Parece Vela rift about 2500 km apart.
Spreading centers propagated toward each other andmerged at ∼23 Ma, forming an R-R-R triple junction that
accommodated the difference in the spreading orientations of the two basins. The dramatic change in spreading orientation and rate after 20 Ma is interpreted by
Sdrolias et al. (2004) as the expression of PSP rotation.
The youngest oceanic basin, the Mariana Trough,which is ∼1000 km long and ∼200 km wide, has opened
behind the Mariana Arc since ∼6–8 Ma (Hussong andUyeda 1981; Fryer 1995; Stern et al. 2003; Kato et al.
2003). Many authors have studied the morphological,
geophysical, and petrological characteristics of this basin(Karig 1971b; Baker et al. 1996; Yamazaki and Murakami
1998; Stüben et al. 1998; Martinez et al. 1995, 2000;
Deschamps and Fujiwara 2003; Deschamps et al. 2005).
The asymmetric (full) spreading rate varies from20 mm/year in the north to 40 mm/year in the south(Asada et al. 2007). This is partly responsible for thecurvature of the arc and its stretching, especially southof Guam where a rift crossing the arc and the fore-arc
accommodates the spreading (Ribeiro et al. 2013; Sternet al. 2013).
The Izu-Bonin Arc, north of the Mariana Arc, has also
been affected by trench-perpendicular extension since
2 Ma but the neo-formed intra-arc basin, ∼120 km longand ∼40 km wide, called the Sumisu Rift (Fig. 1), is stillin the rifting stage (Taylor et al. 1990, 1991).
Aseismic ridges and plateaus of the PSP

The PSP oceanic basins are separated by aseismic ridges
and plateaus, except along the eastern edge where active
volcanic arcs bound the Mariana Trough and Sumisu
Rift (see Fig. 1). The longest (∼2600 km) aseismic ridge,
called the Kyushu-Palau Ridge (KPR), trends northsouth in the middle of the plate. It is a remnant arc(Karig 1972) separated from the IBM active volcanic arc
25 Ma ago (Ishizuka et al. 2011a during the opening of
the Shikoku and Parece Vela back-arc basins. It consistsof aligned volcanoes over a width of ∼50–150 km, presenting a marked change in the orientation from NNWSSE to NNE-SSW around ∼23° N. Similarly, the aseismic
West Mariana Ridge is a remnant arc that separated

Page 5 of 26

from the Mariana active volcanic arc ∼7 Ma ago (Karigand Glassley 1970; Gardner 2010). Both the KPR paleoarc on one side and the Izu-Bonin arc and the WestMariana Ridge on the other side are conjugate marginsof the Shikoku and Parece Vela basins.
West of the KPR, there are two regions with aseismic
ridges, a large complex triangular-shaped region, called
the Daito Ridges region or Amami-Daito-Oki-Daito(ADO) region, that lies north of the WPB, and a sharp
linear ridge trending north-south, west of the WPB close
to Taiwan, called the Gagua Ridge (Fig. 2).
The ADO region comprises three ridges from north tosouth: the Amami Plateau, the Daito Ridge, and the OkiDaito Ridge and Plateau (Fig. 2). Tokuyama (1985, 2007),
based on petrology, concluded that the Amami Plateau,composed of three 200-km-long E-W-trending ridges, wasan active island arc before the Eocene (Nishizawa et al.
2014). It is presently subducting beneath the Ryukyu
Arc. South of the Amami Plateau, the Daito Ridge extends E-W for more than 500 km. It also subducts on
its western side and connects with the KPR on its eastern side. Basalts collected there also indicate an island
arc setting (Tokuyama et al. 1986). Further south, theOki-Daito Ridge s.l., which is 700 km long, is composed, from west to east, of the Oki-Daito Rise, theOki-Daito Plateau, and the Oki-Daito Ridge s.s. Volcanic edifices on the Oki-Daito Ridge, as well as in the
Minami-Daito Basin north of it, have similar ocean island basalt (OIB) signatures and an estimated age of
44–48 Ma (Ishizuka et al. 2013). Most of the Daitoridges probably originated from island arcs, based on
their similar velocity structures (Nishizawa et al. 2014)
and their petrology (Hickey-Vargas 2005; Ishizuka et al.
2013). The Oki-Daito Rise, southwest of the main ridge,
is an exception in terms of velocity structure, as it hasa thinner crustal section. Nishizawa et al. (2014) concluded that it is quite clear from velocity structure andmagnetism that the Kita-Daito Basin resulted from thesplitting of the Amami Plateau and Daito Ridge, butthere are no distinctive features indicative of subduction along the southern edge of the Daito Ridge as earlier suggested by Tokuyama et al. (1986).
In the northwestern part of the WPB, we distinguish
two broad highs at equal distances from the CBF rift
(Fig. 2), the Benham Rise east of Luzon and the Urdaneta Plateau south of Okinawa. Ocean Island Basalt(OIB)-like lavas dated at ∼36 Ma were sampled on the
Benham Rise (Hickey-Vargas 1998), and Deschamps etal. (2008) described overlapping spreading centers near
the Urdaneta Plateau. All these observations strongly
support the influence of a mantle plume called the “OkiDaito mantle plume” contemporaneous with the firststages of the WPB rifting and spreading (Deschamps
and Lallemand 2002; Ishizuka et al. 2013). The threeLallemand Progress in Earth and Planetary Science (2016) 3:15

small basins sandwiched between the Daito ridges, i.e.,from south to north the Minami-Daito Basin, the KitaDaito Basin and the Amami-Sankaku Basin, are poorly
known. Their crustal thickness is typical of oceanic crust(Nishizawa et al. 2014), and the few available samples,obtained from drilling in the Minami-Daito Basin, giveages for OIB sills of ∼51 and ∼ 43 Ma (Hickey-Vargas,
1998). E-W-trending magnetic lineations in the KitaDaito Basin are indicative of N-S spreading (Nishizawa
et al. 2014). The Amami-Sankaku Basin was drilled during the last International Ocean Discovery Program(IODP) expedition 351. Preliminary results suggest a~50–55 m.y. old basaltic basement geochemically similar
with “fore-arc basalts” from the IBM arc (see discussion
in section 1.5, Expedition 351 Scientists 2015; Ishizuka
et al. 2015). Finally, the small oceanic basins in the ADO
region are roughly contemporaneous with the first stages
of WPB spreading and could be considered to be the result of short-lived multiple spreading centers originatingfrom the same regional magmatic event (Deschamps andLallemand 2003).
East of Taiwan, the 300 km-long, 4 km-high Gagua
Ridge trends north-south along 123° E. This high separates the small Huatung Basin to the west from the main
WPB to the east. Magnetic lineations of the Huatung
Basin intersect the ridge at an angle of 90°, whichstrongly suggests that the Gagua Ridge was a former
fracture zone (Mrozowski et al. 1982; Hilde and Lee
1984; Deschamps et al. 1998). On the west side of theridge, magnetic lineations of the WPB are highly oblique, so the Gagua Ridge is a non-transform discontinuity (NTD). Velocity and gravity models across the ridge
suggest an episode of westward underthrusting of the
WPB oceanic crust beneath the Huatung Basin(Deschamps et al. 1998; Eakin et al. 2015). The Gagua
Ridge thus represents failed subduction along a former
fracture zone or transform boundary between two
oceanic basins. That episode of short-lived subduction
occurred in the Oligocene according to Deschamps andLallemand (2002), whereas Eakin et al. (2015) favor ayounger Miocene age.
Non-transform discontinuities and fracture zones of the PSP

Among the NTDs and fracture zones observed in thePSP, some are prominent like the Luzon-Okinawa Fracture Zone (LOFZ), or the numerous curved fracturezones that offset the short segments of the Parece Velaspreading center. Others are suspected based on theirorthogonality with the seafloor fabric such as the ODE,the Mindanao FZ, the Gagua Ridge or even the OkiDaito Ridge. The LOFZ consists of a bundle of two tofour parallel NE-SW-trending strike-slip faults offsetting
the westernmost piece of the WPB. It extends from the
mid-point between Luzon Island and Benham Rise to

Page 6 of 26

the Ryukyu Trench south of Miyako Island and thenparallels the trench until at least the fore-arc area off
Okinawa Island (see Figs. 1 and 2 and map in Hsu et al.
2013). It is difficult to estimate the total offset along the
LOFZ because the fossil spreading center west of thefracture zone is entirely subducted beneath the Ryukyu
fore-arc and because its location between the northerntermination of the CBF rift and the LOFZ is not clear.
Based on magnetic identifications, the age of the oceanic
crust west of the LOFZ ranges from 54 Ma in the south
to younger than 47.5 Ma in the north (Doo et al. 2015).
Shinjo and Ishizuka (2015) noticed that all samples collected east of the LOFZ have geochemical plume signatures, contrary to those reported west of the fracturezone. This is a strong argument for a large offset of perhaps several hundred kilometers along that fault zone.
IBM, Yap, and Palau volcanic arcs

The IBM arc is a 3000 km-long intra-oceanic island arc
dated at ∼50 Ma (Cosca et al. 1998). It experienced a
succession of magmatic episodes accompanying, and recording, subduction initiation as well as several periodsof seafloor rifting and spreading. The first spreading
phase, at the origin of the West Philippine Basin, wascontemporaneous with its initiation and building, probably in interaction with the Oki-Daito mantle plume(Ishizuka et al. 2013). The second phase of spreading,resulting in the Shikoku and Parece Vela basins, split thearc ∼25 Ma ago into a remnant arc to the west (thepresent KPR) and the present IBM arc that remained
continuously active. The last spreading episode occurred∼6–8 Ma ago in the Mariana section isolating the WestMariana Ridge to the west from the active Mariana Arc
to the east. The oldest evidences of the initial IBM arc
consist of gabbros and basalts dated ∼51–52 Ma, whichwere found both in the Izu-Bonin fore-arc east of theBonin Islands (Ishizuka et al. 2008, 2011b) and theMariana fore-arc south of Guam (Reagan et al. 2013).
The stratigraphic section of the fore-arc crust consists,from bottom to top, of peridotites, gabbroic rocks, asheeted dike complex, basaltic lava flows, lavas anddikes of boninite and their differentiates, transitional
high-Mg andesites, and tholeiitic and calc-alkaline arclavas (Ishizuka et al. 2014). Reagan et al. (2010) named
the oldest volcanic products “fore-arc basalts (FABs)”,
mainly because they are exposed in the present IBM
fore-arc. This name is ambiguous because (1) theselavas have geochemical affinities with mid-ocean ridge
basalts (MORBs), and (2) because similar lavas of thesame age (∼50–52 Ma) were drilled during IODP Expedition 351 in the Amami-Sankaku Basin (ADO region) west of the KPR (Arculus et al. 2015). This
discovery indicates that the area of initial seafloor
spreading contemporaneous with subduction initiation

Lallemand Progress in Earth and Planetary Science (2016) 3:15

extended from the present-day fore-arc to the region
west of the present-day KPR (Ishizuka et al. 2015). Observations made in the central Mariana Arc indicatethat transitional, and then boninitic lavas, dated ∼44–
48 Ma, overlie the FABs, constituting a coherent suiteof magmatic rocks characteristic of ophiolite assemblages (Reagan et al. 2010). Variations in Cr/(Cr + Al)
atomic ratios of spinels in dunites from the IBM“present-day fore-arc” probably reflect changing melt
compositions from MORB-like to boninitic melts due
to an increase of slab-derived hydrous fluids and/or
melts (Morishita et al. 2011). Similarly, transitional
suites of high-Mg andesites, dated ∼44–45 Ma, preceded the eruption of normal tholeiitic to calc-alkaline
arc magmatism (Ishizuka et al. 2011b).
Fewer data are available for the Yap and Palau arc systems, but it has been established that the Yap arc is nolonger active volcanically since the Late Oligocene or
Miocene, right after its collision with the Caroline Ridge(Hawkins and Batiza 1977; McCabe and Uyeda 1983).
Fujioka et al. (1996) observed ultramafic and gabbroic
rocks along the inner trench slope of the Yap Trenchwith a paleo-Moho discontinuity around 6000 m deep.
Metamorphic and gabbroic rocks from the Yap Arc appear quite similar to those exposed in the Parece Vela
Basin (Ohara et al. 2002). The islands and submergedarc of Palau are thought to be the southern extension of
the KPR (Kobayashi 2004). They consist of 20–38 Ma
arc-type volcanic rocks including basalt, andesite, anddacite fringed by coral limestones (Meijer et al. 1983).
Constraints and speculations on the subducted portionsof the PSP
The slab beneath the Ryukyu and SW Japan arcs

A significant part of the PSP has been subducted beneath the Ryukyu Arc as attested by Wadati-Benioffzone seismicity and regional scale tomographic studies(e.g., Bijwaard et al. 1998; Widiyantoro et al. 1999; Wanget al. 2008; Li and van der Hilst 2010; Wei et al. 2012,2015). A continuous slab-like high-velocity zone (HVZ),
dipping roughly 45°, extends beneath the 1200 km-long
Ryukyu Arc down to ∼300 km depth. This is consistent
with the edge of the seismicity around 250 km according
to Wei et al. (2015), whereas Bijwaard et al. (1998) imaged the high-velocity anomaly deeper, down to at leasta∼500–600 km depth where it merges with the flat-lying
Pacific slab. Lallemand et al. (2001) suspected that the
deepest portion of the PSP slab detached during theUpper Miocene - Lower Pliocene east of the Gagua
Ridge (Fig. 3). Wei et al. (2015) mentioned that the HVZ
extends into the uppermost upper mantle near Taiwan,
but only in VS tomography, which could suggest that an
old and more rigid part of the PSP has penetrated into
the lower mantle there. That deep slab could be

Page 7 of 26

connected with the detached slab east of the Gagua
Ridge (see Fig. 3). Zhao et al. (2012), based on highresolution P-wave tomography, follow the aseismic slab
down to 430 km under Kyushu and 370 km undersouthwest Honshu, though the intraslab seismicity ends
at 180 km deep. We thus estimated the downdip lengthof the PSP aseismic slab beneath SW Japan to be∼700 km (surprisingly, the authors measure 800–
900 km). At the scale of the Ryukyu Trench, we will thus
hypothesize that the subducted portion of the PSP extends ∼700 km northwestward (Fig. 3). PSP imagery beneath southwest Japan is complicated by the fact thatthe subducting Shikoku Basin is very young (30–15 Ma)
and lies above the old subducting Pacific slab. Cao et al.
(2014) confirmed the observation by Zhao et al. (2012)that the P-wave high-velocity anomaly is not continuous
beneath southwest Japan. It is apparently interrupted
by a low-velocity anomaly north of Kyushu, extending northwestward from 80 km to greater depths.
Huang et al. (2013) and Cao et al. (2014) suggestthat the PSP is tearing and forms a slab window corresponding to the KPR. In their model, both thebuoyancy of the KPR and the directional change inthe motion of the PSP play a role in the tearing
process. The corner flow produced by the subducting
Pacific slab, together with its dehydration, probably
heat the PSP slab from below, thus producing lowvelocity anomalies (Zhao et al. 2012), and hiding the
PSP slab dimensions. We will later assume that about
700 km of PSP slab has been subducted beneath the
Ryukyu and southwest Japan arcs.
High intraslab velocity parallel to the trench is consistent with the main spreading direction of the WPB (seegrey arrows in Fig. 3). This is also parallel to LOFZ, andmay reflect fossil anisotropy (Wei et al. 2015). We thus
speculate that the subducted part of the WPB, dextrally
offset along the LOFZ, extends beneath the Ryukyu Arc
up to the latitude of Kyushu. Indeed, if we simply offset
the total width of the WPB measured between the OkiDaito Ridge and the southernmost evidence of WPB
oceanic crust (south of the Mindanao FZ), i.e., 2000 km
at most, we conclude that the oceanic crust of the WPB
may subduct beneath or south of Kyushu if the LOFZ
extends to these latitudes. The ADO region could also
extend beneath Kyushu (Fig. 3) but the steep slab observed there rather supports the subduction of an “old”
oceanic crust. Park et al. (2009) and Yamamoto et al.
(2013) inferred the extent of the KPR beneath the toe ofthe accretionary prism but the LOFZ could plausibly
offset the ridge at a distance of ∼200 km from the trench.
The LOFZ could even offset the KPR northward by ∼150–
200 km (Fig. 3), providing a geometrical explanation to
the following. (1) The change in the trend of the seismicslab isopachs from N20° to N80° occurs beneath theLallemand Progress in Earth and Planetary Science (2016) 3:15

Page 8 of 26

Fig. 3 Oceanic basins with their subducted parts, present and paleo-volcanic arcs and trenches of the PSP. Oceanic basins are outlined with theirrespective ages and the main directions of spreading (grey arrows). Purple and orange dots indicate the present and Eo-Oligo-Lower Miocene volcanicarcs, respectively, associated with the PSP, either caused by the PSP itself or another plate subducting beneath the PSP. The PSP slabs (dotted areas)
have been unfolded and projected at the surface. Note that a small part of the western WPB has subducted beneath the Huatung Basin along
the East side of the Gagua Ridge. The location of the Eo-Oligo-Lower Miocene trench (in orange) has been estimated based on the amount of
IBM arc consumption by tectonic erosion. Mesozoic terrane occurrences in the PSP are reported with green circles, in which the numbers refer
to Table 1 where more details are presented

easternmost part of Honshu and Shikoku islands insteadof beneath Kyushu as would be expected if the KPR were
not offset. (2) We observe two fore-arc embayments(Fig. 1) that could have resulted from KPR subduction
northeast of the present ridge-trench intersection. One iseast of Kyushu. It may have been caused by the non-offset
ridge segment. The other is south of Shikoku. It might
have been caused by the dextrally offset segment. (3) The
slab window, described by Huang et al. (2013) and Cao etal. (2014), attributed to a tear along the “weak” KPR isclearly north of the location it would occupy if it were projected along a straight path with no offset. (4) The buoyant
KPR might contribute to the shallow-dipping slab beneathsouthwest Japan (Gutscher and Lallemand 1999) if it iseast of the slab window rather than west of it. In this case,the width of the subducted Shikoku Basin would be narrower (Fig. 3).

The slab beneath the Philippine Arc

The western part of the WPB is also subducting beneaththe Philippine Trench. Based on the Wadati-Benioffzone, the slab is no longer than 250 km at the latitude of
Mindanao Island and is shorter both north and south ofthere (Lallemand et al. 1998). The subduction can betraced from offshore Mortal Island in the south toLuzon Island in the north (Cardwell et al. 1980). The
short length of the subducted slab as well arc volcanism
ages support a Pliocene age for the start of PSP subduction offshore Mindano. The subduction then propagatedboth northward and southward (Lallemand et al. 1998).
In detail, that region underwent several episodes of subduction, collision, and terrane accretion as depicted bymany authors (McCaffrey et al. 1980; Moore and Silver
1982; Hall 1987; Rangin et al. 1999; Pubellier et al. 2004;
Hall and Spakman 2015).

Lallemand Progress in Earth and Planetary Science (2016) 3:15

Shortening and even subduction of the WPB probably
occurred north of the Philippine Trench along the East
Luzon Trough as attested by a negative gravity anomaly
and compressional features. Lewis and Hayes (1983)
proposed that subduction was active there during the
Oligocene. Such short-lived subduction of the WPB
along its western margin was also proposed by
Deschamps et al. (1998) in the same period with anamplitude decreasing from 200 km in the south to 0near the present intersection between the Gagua Ridgeand the Ryukyu Trench (see Fig. 3). Transpression along
the Gagua Ridge has been also proposed by Eakin et al.
(2015) but during the lower Miocene rather than the
Oligocene.

Estimating margin loss by tectonic erosion along the IBM
Arc

Convergent margins are generally the locus of masstransfers from one plate to the other across the plates’interface. Accretion of crust or sediment may occur,
contributing to a net growth of the upper plate, but sedimentary or crustal erosion (also called tectonic erosion)is also possible, resulting in a net loss of upper plate material. Von Huene and Scholl (1991) estimated thatabout half of the convergent margins were accreting andhalf were erosive. There are two main indicators for a
net global loss of crust at a convergent margin: a significant fore-arc subsidence increasing trenchward together
with a landward retreat of the active volcanic front (vonHuene and Lallemand 1990; Lallemand 1995). Most of
the time, the two indicators are observed to be simultaneous (Fig. 4). Since the PSP is subducting along its
western boundaries, we will focus on its eastern limit,
which includes the IBM, Yap and Palau margins, to determine whether the plate has grown or shrunk.

Page 9 of 26

IBM arc-trench system

The trench-arc distance varies from ∼200 km along the
Izu-Bonin to less than 200 km in the Mariana subduction zones. The Pacific slab always dips more than 50°
and can even reach ∼90° beneath the central Mariana
Arc. The Pacific plate carries numerous seamounts(Fig. 1) into the subduction zone all along that trench(Fryer and Smoot 1985) favoring the dismantlement,
weakening and subsequent consumption of the margin's
front (e.g., Lallemand et al. 1994, Dominguez et al. 1998,
von Huene et al. 2004). As a consequence, the trench
inner slope is steep and no sediment accretion is observed at the toe of the margin. Instead, basement rocks
have been drilled close to the trench and even serpentinite mud volcanoes have been observed all along theMariana fore-arc (Natland and Tarney 1981; Bloomer
1983; Fryer 1992; Lagabrielle et al. 1992b; Fryer et al.
1999). The diversity of metabasic rocks found in one ofthese seamounts can be explained by recycling of forearc materials through tectonic erosion and subductionof the fore-arc (Fryer et al. 2006). The IBM margin has
been classified as one of the most erosive margins in theworld (e.g., von Huene and Scholl 1991; Lallemand1995). Subsidence of the fore-arc of more than 2 km
since ∼ 40 Ma in the Izu-Bonin fore-arc and ∼ 24 Ma in
the Mariana fore-arc has been documented thanks tobenthic foraminifers contained in sediment cores thatare able to record paleo-bathymetry (Kaiho 1992;
Lagabrielle et al. 1992a). In parallel research, Mitchell
et al. (1992) reported volcanic rock outcrops from 17 to
41 Ma at a distance of ∼50 km from the Izu-Bonin
Trench, indicating that the volcanic front has retreatedby at least 150 km during the last 41 Ma (Fig. 4). A
similar history is documented in the Mariana fore-arc
with gabbros and 30–45 Ma volcanic rocks outcroppingnear the trench, supporting a retreat of the volcanic arc

Fig. 4 Sketch showing the shrinking of an active margin undergoing tectonic erosion. Black and grey lines, respectively, outline the present andreconstructed slab’s top and upper plate geometries with respect to a reference line that could be the present volcanic arc

Lallemand Progress in Earth and Planetary Science (2016) 3:15

of at least ∼ 150 km (Hussong and Uyeda 1981; Bloomer1983) (Fig. 4). Johnson et al. (2014) analyzed plutonic
rocks from two dredge sites along a normal fault scarp off
Guam very close to the trench. These rocks were createdfrom boninite parental magmas that were modified into
tonalites and are now part of a midcrustal layer. Their exposure near the trench is another evidence of tectonic erosion processes.
Volcanic arc retreat sometimes results from a shallowing of slab dip, but in this case, and especially in the
Mariana Arc, the present-day slab dip is almost vertical.
Assuming that it has been continually vertical, which isunlikely, the margin’s front has retreated by at least
150 km through consumption of the material constituting the lower section of the margin following a mechanism depicted in Lallemand et al. (1992) or Lallemand(1998). This appraisal is extremely conservative, and amore realistic estimate would consider the margin's retreat to be at least 200 km because the slab dip was
probably shallower in the past and because the oldest
record of arc activity recovered in the fore-arc is younger than the presumed arc initiation at ∼52 Ma (see section 1.5; Ishizuka et al. 2011a). By extension, the wholemargin, from southern Mariana to northern Japan has
been severely affected by tectonic erosion processes during the Neogene and maybe earlier (Lallemand 1995,
1998). The Eo-Oligo-Lower Miocene paleo-arc is locateda very short distance from the trench, varying from a
few kilometers in the Mariana fore-arc to 90 km in
northern Japan where the volcanic arc retreated by∼210 km during the last 23 Ma. This retreat occurred
simultaneously with a subsidence of the margin by morethan 6 km (von Huene and Lallemand 1990). We canthus extend the eastern boundary of the Paleogene PSP
by at least 200 km eastward (Fig. 3).
Southernmost Mariana and Yap trench systems

The southernmost Mariana Arc and Yap segments haveundergone a different story because the southernmost
Mariana arc-trench system stretched E-W in response to
the arc indentation of the Caroline Ridge at ∼ 23 Ma, thespreading of the Parece Vela Basin and the Mariana
Trough (Fujiwara et al. 2000; Martinez et al. 2000; Sternet al. 2013). The activity of the Yap Arc ceased after collision with the Caroline Ridge (McCabe and Uyeda
1983) and strong tectonic erosion narrowed the trench paleo-arc distance to ∼50 km. As a consequence, lower
crustal and even upper mantle sections of the PSP are
exposed on the inner slope of the Yap Trench (Fujiwara
et al. 2000). Significant arc consumption occurred there
at least during the Neogene.
This observation is extremely important for correctlyinterpreting the petrological and chronological data collected along that arc.

Page 10 of 26

Evidences for Jurassic and Cretaceous relics of the
proto-PSP

Most of the PSP consists of Eocene or younger magmatic or sedimentary rocks formed or deposited after its
inception, but from the early beginning of PSP exploration, several evidences of older crust have been reported (see Table 1), attesting to the existence of aJurassic to Early Cretaceous “proto-PSP” (e.g., Ingle et al.
1975; Matsuda et al. 1975; Hussong and Uyeda 1981).
We distinguish between two types of Mesozoic rockoccurrences in the PSP depending on their location
within, or along, the edges of the PSP. Some were observed in a central position like the ADO region. They
necessarily belong to the proto-PSP. Others were observed near the plate boundaries, i.e., along the IBM arc
or Huatung Basin. They might have been accreted after
the PSP formed.
Starting with the ADO region, Matsuda et al. (1975)
reported Late Cretaceous K-Ar ages for whole-rockhornblende tonalites and basalts dredged from theAmami Plateau (7 in Table 1 and Fig. 3). Hickey-Vargas(2005) performed 40Ar/39Ar dating on those tonalites
and obtained an Early Cretaceous age (∼115–118 Ma)that could be attributed to subsequent reheating or another Ar-loss event. Based on the geochemical characteristics of the basalts, she concluded that the Early
Cretaceous subduction zone that formed the Amami
Plateau might have been the site of slab melting compatible with the subduction of a young, hot plate at thattime. The Amami tonalites were probably formed byfractional crystallization from the basaltic magma or partial melting of basaltic arc crust. Mizuno et al. (1978)and Okino and Kato (1992) mentioned that the Daito
and Oki-Daito ridges (10 in Table 1 and Fig. 3) consistedof pre-Eocene basement rocks overlain by middle Eocene
sedimentary rocks. More recently, andesites dredgedon the Daito Ridge (8 and 9 in Table 1 and Fig. 3)
returned 40Ar/39Ar ages of ∼116–119 Ma (Ishizuka et
al. 2011a). Tani et al. (2012) revealed after analyzing
samples collected during a diving cruise conducted in2010 that the ADO region dominantly exposed deep
crustal sections of gabbroic, granitic, and metamorphic rocks with possible continental affinities. Jurassic to Cretaceous zircon U-Pb ages have beenobtained from the plutonic rocks (7 in Table 1 andFig. 3).
Today, the KPR occupies a central position but it constituted the proto-IBM arc and rear-arc before the opening of the Shikoku and Parece Vela basins. As discussed
in section 3, tectonic erosion processes have consumed
the margin’s front, at least during the Neogene. We thus
consider that Cretaceous ages obtained from a volcanic
apron west of the KPR (Ingle et al. 1975; 5 in Table 1
and Fig. 3) or in its southernmost part (Ishizuka et al.

Region (see n° in Fig. 3)

Sample location

Sample nature and dated material

Estimated age

Source1

Dive samples (YK11-07) 32° 14' N–141° 39' E

Andesite, diorite

Cretaceous ~100 Ma (U-Pb) + Paleozoic
and Proterozoic detrital zircons

Tani et al. 20122

Sample 6 K1152 27° 19' N– 143° 00' E

Two pillow basalt lavas beneath gabbro

Middle Jurassic 159.4 ± 0.9 Ma (40Ar/39Ar)

Ishizuka et al. 2011b

Izu-Bonin fore-arc

Tani and Myojinsho 2011

Ishizuka et al. 2012
Mariana fore-arc
3Site 460, DSDP 60 17° 40' N–147° 35' E

Pebble conglomerate with Calpionella
alpinaLate Jurassic to Early Cretaceous (~130–
140 Ma)Azéma and Blanchet 1981

3

Site 460 17° 40' N–147° 35' E

Reworked radiolarians

Upper Cretaceous (Campanian, ~72–83
Ma)

Hussong and Uyeda 1981

3

Site 461 17° 46' N–147° 41' E

Reworked radiolarians“Cretaceous” (~65–135 Ma)

Hussong and Uyeda 1981

4

Dredges 19° 37' N–147° 04' E

Radiolarian cherts

Lower Cretaceous Valanginian ~97–112
Ma and Albian 131–138 Ma

Johnson et al. 1991

4

Dredges 19° 37' N–147° 04' E

Foraminifers in cherts

Lower Cretaceous (Aptian to Albian ~96–
113 Ma)Johnson et al. 1991

4

Dredges 19° 37' N–147° 04' E

MORB metabasalt

Upper Cretaceous 85 Ma (K-Ar)

Johnson et al. 1991

4

Dredges 19° 37' N–147° 04' E

Highly metamorphosed alkali basalt

Upper Cretaceous 71 Ma (K-Ar)

Johnson et al. 1991

Site 290 east of KPR 17° 44' N–133° 28' E

Reworked foraminifers in a volcaniclastic
apron

Cretaceous

Ingle et al. 1975

Dredge in southernmost part of KPR ona ridge between Palau Trench and KPR

Mafic schists of amphibolite togreenschists facies

May have similar age and origin to
Cretaceous Daito Ridge

Ishizuka et al. 2012

Dive samples (YK10-04)

Gabbroic, granitic and metamorphic
rocks

Jurassic to Cretaceous magmatic zircons

Tani et al. 2012

Hornblende tonalite

Lower Cretaceous 69.5 Ma (K/Ar)–117.0 ±1.1 Ma (40Ar/39Ar)

Lallemand Progress in Earth and Planetary Science (2016) 3:15

Table 1 List of samples collected in the PSP providing evidence for a pre-Eocene proto-PSP

WPB
5
KPR
6
ADO region7

25° 54' N–133° 54' E

Tani 2010

27° 53' N–131° 51' E
27° 56' N–132° 02' E
Amami Plateau
7

Dredge 11-17-1 28.07° N–131.63° E

Matsuda et al. 1975
Tokuyama 1985

Dredge 11-17-5 28.08° N–132.02° E

Hornblende tonalite

Lower Cretaceous 75.1 Ma (K/Ar)–115.8 ±0.5 Ma (40Ar/39Ar)

Matsuda et al. 1975
Tokuyama 1985
Hickey-Vargas 2005

Page 11 of 26

Hickey-Vargas 2005
7

7

Dredge 11-9-33

BasaltUpper Cretaceous 82.4 and 85.1 Ma (K/Ar)

Matsuda et al. 1975
Tokuyama 1985

Daito Ridge
8

Short core or dredge ~25.9° N–135.2° E

Andesite

Lower Cretaceous 116.9 ± 0.9 Ma (40Ar/39Ar)

Ishizuka et al. 2011a9

Short core or dredge ~26.0° N–133.1° E

Andesite

Lower Cretaceous

Ishizuka et al. 2011a40

39

118.9 ± 0.4 Ma ( Ar/ Ar)
Oki-Daito Ridge
10

Dredge (unknown exact location)

Alkali basalt

Limit Upper Cretaceous-Paleocene 65 Ma

Okino and Kato 1992

Dredged sample RD19 20.40° N–121.47° E

GabbroLower CretaceousDeschamps et al. 2000

Huatung Basin
11

121.2 ± 4.6 Ma (40Ar/39Ar)
12

Dredged sample RD20 21.49° N–122.69° E

GabbroLower CretaceousDeschamps et al. 2000

123.2 ± 7.8 Ma (40Ar/39Ar)
13

YehYu Creek sample on Lanyu Island 22° N–121.55° E

Red chert float radiolarian

Lower Cretaceous (Barremian ~113–117 Ma)

Deschamps et al. 2000

Outcrops

Ophiolitic suites

Cretaceous

Yumul 2007

Lallemand Progress in Earth and Planetary Science (2016) 3:15

Table 1 List of samples collected in the PSP providing evidence for a pre-Eocene proto-PSP (Continued)

Philippine archipelago
14

Page 12 of 26

Lallemand Progress in Earth and Planetary Science (2016) 3:15

2012; 6 in Table 1 and Fig. 3) are representative of the
proto-PSP prior to its isolation.
Closer to the trench, Mesozoic rocks have also been
discovered along the IBM fore-arc since Deep-Sea Drilling Project (DSDP) expeditions in 1978 (Hussong andUyeda 1981; Bloomer 1983). Late Cretaceous reworked
radiolarians and Upper Jurassic Calpionellids were observed in cherts drilled at sites 460 and 461 in the Mariana fore-arc (Azéma and Blanchet 1981; 3 in Table 1
and Fig. 3). At distances of ∼200 km north of these sites
and more than 50 km arcward of the trench (4 in Table 1
and Fig. 3), dredged cherts, mafic and intermediate lavas,
and intrusive rocks documented the presence of an
ophiolite suite interpreted by Johnson et al. (1991) as accreted fragments of a Cretaceous oceanic plate. The volcanic rocks provided Late Cretaceous K-Ar ages, while
the radiolarians and foraminifers supported an early
Cretaceous age (∼97–138 Ma). More recently, volcanic
rocks have been also sampled in the northern part of the
IBM fore-arc. East of the Bonin Islands, pillow-lavas
were dated at 159.4 ± 0.9 Ma (40Ar/39Ar, Ishizuka et al.
2011b; 2 in Table 1 and Fig. 3), while andesites and diorites east of Aogashima Island gave Cretaceous(∼100 Ma) U-Pb magmatic ages and abundant Paleozoic
to Proterozoic detrital zircons (Tani et al. 2012; 1 inTable 1 and Fig. 3). Such “continental” zircons, together
with the Indian MORB-like isotopic characteristics of
the Jurassic lavas in the Bonin islands region, are substantial evidences for a proto-PSP origin in the vicinityof a continent (Tani et al. 2012; Ishizuka et al. 2012), rather than the allochtonous accreted fragments of Pacificorigin proposed in the Mariana fore-arc by Bloomer(1983) or Johnson et al. (1991).
As discussed in section 1.2, the age of the Huatung
Basin is controversial but we cannot ignore new datings
obtained by Deschamps et al. (2000) on gabbros dredged
in 1980 during a Research Vessel Vema cruise (Mrozowski
et al. 1982). The two dredge sites are located on basement
highs west of the Gagua Ridge (11 and 12 in Table 1
and Fig. 3). They provided Early Cretaceous 40Ar/39Ar
ages of ∼115–131 Ma. Furthermore, ∼113–117 Ma radiolarians were discovered in several red chert float samples, probably collected during the Tungchin andesitic
eruption on Lanyu Island (13 in Table 1 and Fig. 3).
These cherts likely belonged to the former oceanic
plate (Huatung Basin) on which the Miocene volcanicarc was built (Deschamps et al. 2000). Hickey-Vargas et al.
(2008) analyzed the two gabbros and concluded that they
have an Indian MORB Hf-Nd isotopic signature, with Pb
isotope ratios intermediate but closer to Pacific MORBs
than the WPB, which has a strong Indian Pb isotope
signature. For comparison, sources for igneous rocks fromthe Amami Plateau, thought to be an Early Cretaceous
island arc, have Indian Hf and Nd (presubduction mantle)

Page 13 of 26

and Pacific Pb (subduction component) isotope characteristics (Hickey-Vargas et al. 2008).
Except in its northernmost part (north Luzon and the
Batan islands), the Philippine archipelago does not belong to the present-day PSP, but before the inception of
the Philippine Trench in the Late Miocene, it can beconsidered to have been part of the PSP. The Philippine
region has a composite basement containing numerous
ophiolite complexes, most of them being of supra subduction origin (Pubellier et al. 2004). Based on gravity
data, these authors suggested that the present Miocene
volcanic arc in Luzon lies directly on the southern extension of the Huatung Basin. Yumul (2007) provided acompilation of ophiolites all along the mobile belt. Except in a few places, like Zambales or Amnay, most ofthem are Jurassic to Cretaceous in age (14 in Table 1
and Fig. 2). He proposed a zonation from Late Cretaceous amphibolites with quartz-albite metamorphic
soles distributed mainly in the eastern belt, then Early toLate Cretaceous dismembered ophiolites with mostly
tectonic melanges in the central belt and finally Late
Cretaceous to Oligocene ophiolitic complexes in thewestern belt. Such a zonation is discussed by Tani et al.
(2015), who obtained new zircon ages from the northern
ophiolite belts. They showed these to be Eocene in age
and thus probably genetically associated with the WPB
opening. As for the southern ophiolites, in Cebu, Lagonoy and Dinagat, gabbroic and leucocratic rocks associated with the ophiolitic complexes are Jurassic to Late
Cretaceous in age (∼90–200 Ma). Tani et al. (2015) thenconcluded that these Mesozoic ophiolites from thesouthern Philippines may potentially be correlated with
the Mesozoic arc and ophiolitic rocks of the ADO region
before the WPB opening.
Early Eocene isolation of the PSP through subduction
initiation along the proto-IBM Arc

The geodynamic context of the proto-PSP isolation has
long been a matter of debate. The orthogonality of the
CBF rift with the KPR was first interpreted as an indication of plate entrapment. It was proposed that the WPB
resulted from a segment of the Kula-Pacific Ridge andassociated oceanic crust being trapped in the Middle
Miocene (Uyeda and Ben Avraham 1972; Uyeda andMcCabe 1983; Hilde and Lee 1984). A variant of thismodel was later proposed by Jolivet et al. (1989), who
posited that a piece of the North New Guinea/PacificRidge was trapped during the Middle Eocene. Lewis etal. (1982) first proposed a back-arc origin for the formation of the WPB behind the East Mindanao-Samar Arc.
Other authors have also suggested that the WPB opened
as a back-arc basin either behind the East MindanaoSamar Arc (Rangin et al. 1990; Lee and Lawver 1995) or
the proto-IBM Arc (Seno and Maruyama 1984) but with

Lallemand Progress in Earth and Planetary Science (2016) 3:15

poor constraints on the timing and kinematics ofthese events. Based on considerable geological andpaleomagnetic constraints, especially those imposedfrom ocean drilling data and the Philippine islands,
Hall et al. (1995a,b,c) were the first to propose that the
proto-PSP was isolated between two opposing-vergent
subduction zones, and then rotated clockwise while
migrating north from its initial position near the equator.
Hall (2002) later refined the plate tectonic evolution of thewhole western Pacific region. Deschamps and Lallemand(2002) used Hall’s model when providing more details on
the WPB spreading processes. In the earlier stages of
WPB opening, they have accounted for the presence of aplume (Macpherson and Hall 2001) in the generation of
the Benham Rise, Urdaneta Plateau, numerous overlapping spreading centers and ridge jumps. The existence of
this plume, called the “Oki-Daito” plume by Ishizuka et al.
(2013), is supported by numerous petrologic (e.g.,
Hickey-Vargas 1998) and structural (e.g., Deschamps andLallemand 2002; Deschamps et al. 2008) studies. The
updated ages and relative symmetry of the WPB
opening have allowed us to refute the “entrapment model”
and definitely consider the WPB as having been
formed between two facing subduction zones, the East
Mindanao-Samar, also called the proto-Philippine, and theproto-IBM.
Constraints on the age of PSP inception

The age of the shift from proto-PSP to PSP is reasonably
constrained if we accept that the inception of the IBM
subduction establishes the birth of the PSP. However,this point needs to be clarified because, if most authors
agree that the inception of IBM subduction marked theonset of the PSP, there is still a debate about the best
marker for subduction initiation. Ishizuka et al. (2011b)
relates the onset of fore-arc basalt (FAB) magmatism, at
51–52 Ma with the age of initiation of (Pacific) slab sinking, because they are the oldest lavas present on the arcthat are genetically linked with the magma suite observed from the Mariana to the Izu-Bonin fore-arc.
From a petrological point of view, most authors (e.g.,
Stern and Bloomer 1992; Stern et al. 2012; Reagan et al.
2010; Ishizuka et al. 2011b) consider that the FABs
erupted in a fore-arc position close to the paleo-trench,
but we proposed in section 3 that ∼200 km of the margin's front has been removed since the onset of subduction, putting the FABs at a significant distance from theincipient trench at the time of their eruption. This initial
setting was recently confirmed during IODP Exp. 351
with the discovery of rocks similar to the FABs in the
Amami-Sankaku Basin, ∼250 km west of the present-day
trench (∼400–450 km west of the paleo-incipient
trench), which account for the Shikoku Basin opening(Fig. 2, Ishizuka et al. 2015). The seismic structure of the

Page 14 of 26

KPR indicates that the igneous basement of the AmamiSankaku Basin, characterized by FABs, continues beneath the ridge, showing that the earliest arc lies above
the FABs (Arculus et al. 2015). Moreover, FABs are
MORB-like tholeiitic basalts showing little or no masstransfer from a subducting plate (Reagan et al. 2010).
Consequently, the argument that the occurrence of FABs
should date the inception of IBM subduction no longer
stands. By contrast, the first occurrence of boninites,
which required a source of volatiles, certainly marks the
subduction of a hydrated lithosphere. We thus conclude
that the Pacific crust reached a significant depth andmetasomatized the overlying mantle at ∼49–48 Ma.
Considering that the transition from strike-slip movement
along a transform boundary to convergent movement
would unlikely produce high convergence rates (normal
to the boundary) in the earlier stages, subduction inception would reasonably have started a few m.y. earlier,i.e., ∼52–50 Ma is probably a minimum age. Thus we finally converge with the estimate by Ishizuka et al. (2011b)
using a different marker for the onset of IBM subduction.
Deschamps and Lallemand (2002), based on the characteristics of the seafloor between the ODE and the OkiDaito Ridge, estimated the rifting of the WPB tohave occurred around 55 Ma with a start of spreading at ∼54 Ma. This oldest age for the WPB crust
has been confirmed by Doo et al. (2015). Since there
was no IBM subduction when the WPB rifted andspreading began, we should consider that it started
to open behind the proto-Philippine Arc under the
influence of the Oki-Daito plume.
Possible trigger for PSP inception

With respect to what triggered the IBM and thus PSP inception, the following has been documented. (1) The Pacificplate changed its motion at ∼43–50 Ma (Steinberger et al.
2004; Sharp and Clague 2006; Wessel et al. 2006; Whittaker
et al. 2007). Consequently, the timing of this major event ismuch younger than the initiation of subduction along theproto-IBM trench prior to 50 Ma. Furthermore, Faccenna
et al. (2012) showed that the slab pull force that grew along
the IBM (and Tonga-Kermadec) subduction zone largely
contributed to the Pacific plate motion change. (2) The
Oki-Daito plume has also been proposed as another candidate for subduction initiation but again, the oldest rocks
with OIB affinities, which were found in the Minami-Daito
Basin, were dated ∼48.4 Ma (Ishizuka et al. 2013), following
the proto-IBM subduction by no less than 3 m.y. Faccenna
et al. (2010) proposed that the plume might have resulted
from the concomitant return mantle flow generated by thetwo facing subduction zones following a scenario similar to
those of the present North Fiji Basin. Ishizuka et al. (2013)
ruled this hypothesis out considering that the mantle 2 OIB
enrichment, which persisted over 15 m.y., has theLallemand Progress in Earth and Planetary Science (2016) 3:15

characteristics of a very depleted mantle and does not show
evidence of an enriched plume. Plume-induced subduction
initiation has been invoked by Gerya et al. (2015) based ona hotter early Earth, but in a colder Earth where plate tectonics is ongoing, one may consider that the basal drag thatthe plume exerted below the plates might have altered thesmall proto-PSP motion. (3) Spontaneous subduction involving the vertical sinking of older, denser lithospherealong a transform-fracture system, as proposed by many
authors (e.g., Karig 1982; Stern and Bloomer 1992; Shervais
and Choi 2011) can also be ruled out. First of all, reasonable
numerical models indicate that compression across theboundary fault is required (e.g., Toth and Gurnis 1998;
Gurnis et al. 2004; Leng and Gurnis 2011; Leng et al. 2012)
and the classical mode of failure of lithosphere undercompression is localization of the deformation along
conjugated shear bands dipping at an angle of ∼50°,
then failure along one of them and thrust development(e.g., Shemenda 1992). The theoretical conditions usedin numerical models to initiate a “spontaneous” gravitational sinking lithosphere require an extremely young(newly formed) upper plate separated from an old,
dense oceanic plate by a very weak boundary zone andsometimes even a no-slip condition on the down-goingplate (Gerya et al. 2008; Gerya 2012; Leng and Gurnis2015). Secondly, no present or recent subduction onsets, the Philippine, New Hebrides, Flores or Wetar
trench, for example, have involved such gravitational
scenarios. All these recent incipient subductions

Page 15 of 26

required compressional tectonic forces to initiate them(Hall et al. 2003; Lallemand et al. 2005). Thirdly, transpression along a former transform boundary between
two oceanic plates may allow the younger plate to subduct beneath the older as presently observed along the
Hjort Trench (Meckel et al. 2005). (4) The most reasonable trigger is the subduction of the Izanagi-Pacific(IP) Ridge beneath Asia at ∼ 60-55 Ma (Whittaker et al.
2007; O'Connor et al. 2013; Seton et al. 2015). Rapid
subduction of the still-spreading IP ridge, over a vastdistance, likely triggered a chain reaction of tectonic
plate reorganization (Fig. 5). Ridge-push and slab pullforces acting on the Pacific plate changed drastically,
resulting in a switch of the absolute motion from
northwest to west-directed around 55 Ma. Since theAustralian plate absolute motion also changed during
the same period (Whittaker et al. 2007), subduction
systems initiated along the Tonga-Kermadec and IzuBonin-Mariana fracture zones where convergence localized (Hall et al. 2003). The potential giant Izanagi
slab detachment is thought to have changed not only
plate-driven forces such as slab pull or ridge-push, butalso affected the sub-Pacific and sub-East Asia mantle
flow. As such, this mega-event could have also contributed to the occurrence of the Oki-Daito mantle plumeaccompanying the newly formed IBM subduction zone.
The mechanism would reasonably be a return flow
triggered by a combination of factors including the two
facing subduction zones (Faccenna et al. 2010) and theFig. 5 Geodynamic environment of the proto-PSP at 60 Ma and the PSP at 50 Ma. This figure has been modified after Seton et al. (2015). H.B.
Huatung Basin. Mesozoic arc terranes are in green and the newly formed oceanic basins are in orange

Lallemand Progress in Earth and Planetary Science (2016) 3:15

sinking of the detached Izanagi slab on another side(see Fig. 5).
Reconstructed PSP paleo-kinematics

Based on convergent paleomagnetic results, there is arelative consensus on the paleolatitude of the proto-PSPnear the equator (Fig. 5, Hall et al. 1995a,b,c). For many
years, interpretation of paleomagnetic results has been
controversial because declination data have been obtained only from the eastern margin, where subductionrelated tectonic processes may have caused local, rather
than plate-wide, rotations (Hall et al. 1995c). Based on
ODP site 1201, drilled ∼100 km west of the KPR and∼450 km north of the CBF rift, Richter and Ali (2015)
produced new data on the PSP drift since the Middle
Eocene. They have analyzed the WPB basaltic basement(∼47 Ma) and its overlying sedimentary sequence. Paleolatitudes derived from the sedimentary sequence support
the model of northward movement of the plate since the
Eocene. The basaltic basement lay at ∼7 ± 5° S in the
Middle Eocene (see ODP site 1201 on Fig. 5, to be compared with 19° 18' N today). The paleolatitudes determined from site 1201 are consistent with northward
movement of the plate as predicted by Hall (1997) orQueano et al. (2007) and as determined by earlier
paleomagnetic investigations on drill cores or fromonland formations. The PSP decelerated between 50 and
20 Ma with a minimum plate movement at 20 Ma. Any
rotational component of the plate is hard to extract
since the deep-sea cores are not oriented and most azimuthally oriented paleomagnetic data are from plateboundary zone islands, potentially subject to local rotations. Based on drill cores obtained in the ADO region,
Yamazaki et al. (2010) considered that most of thenorthward shift was accomplished between about 50 and
25 Ma with very little northward movement after 15 Ma.
They also present a model in which the PSP rotated 90°
clockwise between 50 and 15 Ma around an Euler polenear 23° N 162° E. Deschamps and Lallemand (2002)
used Hall’s model, which posit a 50° clockwise rotationof the PSP with southward translation between 50 and
40 Ma, no significant movement between 40 and 25 Ma
and 40° clockwise rotation between 25 and 0 Ma for thesouthern part of the plate, and clockwise rotation andnorthward movement between 50 and 0 Ma for thenortheastern part. Despite large uncertainties in rotational motions, they were able, using that model, to account for tectonic interactions with the Huatung Basinalong the eastern margin during the Eocene.
Seton et al. (2015), assuming that the Izanagi slab detachment beneath East Asia was responsible for major
plate reorganization, have examined the consequences
on mantle flow in the Pacific region between ∼ 53 and47 Ma. Their geodynamic calculations, compared with

Page 16 of 26

tomography data, let them argue that the flow changed
from southward before 60 Ma to north-northeastward
after 50 Ma, corroborating the paleolatitudes given by
paleomagnetic data (Hall et al. 1995c, Richter and Ali
2015).
Cretaceous terranes origin

Around ∼ 60–50 Ma, the proto-PSP was located in thesouthern hemisphere (Richter and Ali 2015). A wide
Mesozoic oceanic basin, called the New Guinea ophiolite
back-arc basin, separated the Australian continent fromthe proto-PSP (Hall 2002; Pubellier et al. 2003). Such apaleo-basin is a good candidate for the origin of Early
Cretaceous Huatung Basin rocks with Indian MORB
characteristics (Hickey-Vargas et al. 2008). A strip ofthat New-Guinea Basin was trapped along the complex
transform boundary that separated the Indonesia Arc
from the East Mindanao-Samar Arc (Fig. 5, Deschamps
and Lallemand 2002). Similarly, the Daito ridges show
strong petrological, chronological, and geochemical affinities with the southern Philippine ophiolites (Tani etal. 2015). These terranes probably result from the splitting of the same proto-Philippine island arc region at theearly stages of WPB rifting under the influence of the
Oki-Daito plume (Fig. 5).
Plume-ridge interaction, boninites’ and FABs’ geodynamic
setting

A key point in discussing the early stages of the PSP and
IBM subduction concerns the petrologic and geodynamic
significance of the boninites, which were initially discovered on the Bonin Islands and then at several locations
along the IBM fore-arc up to Palau Island. Boninitic magmatism represents a distinctive style of subduction-related
magmatism, thought to result from melting strongly depleted mantle that is variably metasomatized by slabderived fluids or melts (Crawford et al. 1989; Pearce et al.
1992). Boninites are therefore a rare type of subductionrelated magma. They are much richer in H2O, and require
much more refractory sources than normal island arc
suites. Their genesis requires a depleted mantle peridotite,a source of (C–O–H) volatiles and an abnormally highgeothermal gradient in relatively shallow levels of the
mantle wedge.
Based on present-day fore-arc magma records, they areoften referred to as suprasubduction-zone ophiolites. Several petrologists (Whattam and Stern 2011; Stern et al.
2012) claim that their eruption follows the “subduction initiation rule” in which the magma source changes progressively in composition due to the combined effects of melt
depletion and subduction-related metasomatism. Magmas
progress from early decompression melts of unmodified
fertile mantle to yield “fore-arc” basalts to younger hydrous
flux melts of depleted mantle that has been stronglyLallemand Progress in Earth and Planetary Science (2016) 3:15

modified by subduction-related fluids to yield late high-Mg
andesites and boninitic lavas. Finally, normal arc volcanics(tholeiites) cap the subduction initiation sequence (Stern etal. 2012). Metcalf and Shervais (2008), Reagan et al. (2010)
and Ishizuka et al. (2011b) described the genetic link in themagmatic suite constituting the “present-day fore-arc”
ophiolites along the IBM subduction zone startingfrom the ∼50–52 Ma so-called FABs, then the ∼44–
48 Ma boninite andesites and their differentiates and/or the ∼44–45 Ma, transitional high-Mg andesites,
finally topped by the post 44 Ma arc tholeiites andcalc-alkaline rocks.
Macpherson and Hall (2001) observed that boninitic
magmatism is not recognized in younger subduction
zones of similar dimensions (Crawford et al. 1989) like,for example, the Hjort-Macquarie-McDougall-Puysegur
incipient subduction (Meckel et al. 2005). Macpherson
and Hall (2001) suggest an additional tectonic or thermal factor which could influence the generation of boninites and posit that a mantle plume influenced themagmatic and tectonic evolution of the western Pacificsince the Middle Eocene. Occurrences of recent boninites are reported from the North Tonga Ridge (e.g.,
Falloon et al. 1989), the Valu Fa Ridge in the Lau Basin(Kamenetsky et al. 1997), and the southern New
Hebrides arc (Monzier et al. 1993). Deschamps andLallemand (2003) observed that the geodynamic setting was the same in each of these examples, i.e., eruptions occurred at the intersection between a back-arc
spreading ridge and a volcanic arc. Moreover, basedon their reconstruction of the WPB in 2002, they
noted that the IBM boninites roughly coincided with
the intersection between back-arc rifts or spreading
centers and the proto-IBM arc. Such geodynamic context is exceptional because most of the time, the rift orback-arc spreading center parallels the arc. Specificconditions are needed to make spreading centers andarcs intersect. Among these is the influence of amantle plume that disorganizes the mantle flow in the
back-arc region.
It is highly probable that the FABs that underlie theboninites not only occur in the IBM fore-arc, but also
constitute part of the basement of the short-lived backarc basins in the ADO region (Ishizuka et al. 2015;
Arculus et al. 2015). The occurrence of both FABs andboninites in a modern fore-arc setting is the result of arc
consumption by tectonic erosion after their early emplacement. These lavas were initially emplaced far fromthe incipient trench either in a rear-arc position like theValu Fa lavas, or in a stretched arc at the termination ofa rift like in northern Tonga or in the southern New
Hebrides. In section 7, we propose a scenario for the
early stages of IBM subduction and associated magmatism that satisfies all previous constraints.

Page 17 of 26

Toward an integrative tectono-magmatic model of the
IBM subduction zone

Several paleoreconstructions of PSP evolution have been
proposed (e.g., Uyeda and Ben Avraham 1972; Karig
1975; Seno and Maruyama 1984; Jolivet et al. 1989; Hallet al. 1995a; Lee and Lawver 1995; Hall 2002;
Deschamps and Lallemand 2002; Pubellier et al. 2004;
Honza and Fujioka 2004; Sdrolias and Müller 2006;
Gaina and Müller 2007; Zahirovic et al. 2014; Seton etal. 2015). In this study, we do not pretend to provide acomplete update of PSP tectonic evolution but rather
highlight key phases, especially during the early stages ofthe evolution and IBM subduction initiation, and connect them into an integrated model of evolution thatsatisfies the existing geological, geochemical, geochronological and mechanical constraints.
Proto-PSP environment

The proto-PSP consisted of Mesozoic terranes of various
origins including island arcs such as the Daito ridges
and some Philippine ophiolitic complexes (Hall 2002;
Hickey-Vargas et al. 2008; Tani et al. 2015). At the timeof PSP inception (Fig. 5), there is no clear evidence
whether the Huatung Basin, which probably originatedfrom a larger Mesozoic back-arc basin north ofAustralia, was already trapped or not. If not, the docking
of a strip of that basin through the jump of the plateboundary from the former Gagua fracture zone to another subparallel fracture/transform fault occurred soon
because the trapped piece of Huatung crust moved
northward with the PSP from the very beginning(Deschamps and Lallemand 2002). The simplest configuration that can be derived from the above observations
is that the Mesozoic terranes (∼60 m.y. fossil arcs at thattime) lay behind the active proto-Philippine Arc. Thesefossil arc terranes were separated from the Pacificoceanic plate by a transform fault that allowed the
Izanagi and Pacific plates to subduct beneath East Asia
(e.g., Seton et al. 2015).
Consequences of Izanagi slab detachment

At the end of the Paleocene (∼60–55 Ma), the whole of
East Asia underwent the subduction of the IzanagiPacific active spreading ridge (Whittaker et al. 2007;
Zahirovic et al. 2014). Since the ridge segments were
subparallel to the former margin, the Izanagi plate detached as a whole, resulting in a drastic change inmantle flow dynamics across the whole West Pacific andEast Asia (Seton et al. 2015). This major tectonic event
modified not only the driving forces of the Pacific plate
and thus the plate motion direction, but also those of
the surrounding plates through a change in mantle flow.
In such a context, convergence might have localizedalong the weak fracture zone separating the Pacific plateLallemand Progress in Earth and Planetary Science (2016) 3:15

from the proto-PSP, which was composed of Mesozoic
terranes. Oblique shortening might have started as early
as 60–55 Ma ago, then thrusting localized and subduction of the Pacific plate started. The cumulative downwelling action of the former proto-Philippine
northeastward-vergent subduction and the mantle flow
reorganization following the Izanagi slab detachment
may have triggered localized mantle upwelling, further
called the “Oki-Daito mantle plume” around 50–52 Ma(Fig. 5).
Impact of the Oki-Daito plumeAs in the North Fiji Basin, the proto-PSP split into several “terranes” under the plume’s influence (HickeyVargas et al. 2008; Faccenna et al. 2010). Multiple
spreading centers with various orientations ruptured
the newly formed PSP, especially during the earlier
stages at ∼52–45 Ma. Some of them, especially in the
ADO region, gave rise to short-lived oceanic basins likethe Kita-Daito, Amami-Sankaku or Minami-Daito basinor the piece of the WPB north of the ODE. The plumethus likely triggered basins opening as attested by thepresence of OIB dikes and sills in the Minami-Daito
Basin. The fact that the FAB-like lavas drilled in the
Amami-Sankaku Basin do not exhibit a plume-like geochemical signature may indicate that the spreading
centers propagated outside of the plume’s area of influence. Plateaus, formed by excess magma, or seamounts
with OIB signatures, developed essentially in the northern part of the present WPB, including the MinamiDaito Basin (∼43–51 Ma), Oki-Daito Ridge (∼48 Ma),Oki-Daito Rise (∼40–45 Ma), Urdaneta Plateau (∼40–
36 Ma) and Benham Rise (∼36 Ma) (Ishizuka et al.
2013). Typical failed rifts and propagators characterize
the region between the Urdaneta Plateau and the
Benham Rise (Figs. 1, 2, 3, and 5, Deschamps et al. 2008).
IBM subduction inception

The IBM subduction zone initiated in the region of theformer transform boundary between the splitting Mesozoic terranes that were essentially composed of former
island arcs and the Pacific plate. Since the oldest lavas
that include subduction components (near the KPRDaito Ridge intersection) are ∼48–49 Ma old (Ishizuka
et al. 2011a), we suppose that about 10 m.y. were necessary for the former transform boundary to turn into a
subduction, as suggested by numerical models (Leng andGurnis 2011; Leng et al. 2012). At this stage, it is important to note that subduction did not initiate along atransform fault separating a younger and an older
oceanic plate as has often been described (e.g., Shervais
and Choi 2011; Stern et al. 2012) but along a transformboundary between Mesozoic terranes characterized by acrust ∼20 km thick (Nishizawa et al. 2014) and an

Page 18 of 26

oceanic plate characterized by a ∼6–7 km crust but witha lithosphere of highly variable thickness along the
strike. Indeed, reconstructions by Zahirovic et al. (2014)
and Seton et al. (2015) indicate that the age of the Pacific plate varies from ∼0 in the north to ∼80 Ma in thesouth of the proto-IBM arc. Sdrolias and Müller (2006)
proposed a more restricted age range between 30 and
70 Ma. In any case, it is quite clear that the oceanic
crust (Pacific Plate), whatever its age, will tend to subduct beneath the Mesozoic terranes that are more buoyant if the region undergoes compression. To becomplete, we must admit that young oceanic basins
formed during subduction initiation, so the proto-PSP
ended up consisting of alternating thick Mesozoic arc
terranes and newly formed oceanic crust, as also noticed
by Leng and Gurnis (2015).
The mode of failure along that transform boundary is
unknown, but we can learn from similar known or recent geodynamic contexts. The Australia-Pacific plateboundary south of New Zealand offers an excellent analog to the proto-IBM situation because its former purelytransform boundary evolved into a series of incipient
subductions from Puysegur in the north to Hjort in thesouth. At the latitude of the Puysegur Trench, the young
Tasman oceanic basin (∼10 Ma) began to subduct beneath the Campbell Plateau and Solander Trough in the
Miocene (Lebrun et al. 2003). Detailed investigations
have shown that the former transform fault is still activein the upper part of the Puysegur Ridge. Failure occurredon the Tasman side at a distance from the transform
fault along a shallow-dipping thrust, so that the trench is
now located at ∼20–50 km from the fault (Collot et al.
1995). Similar observations can be done in the Hjort sector with the young Southwest Tasman Basin (∼5–9 Ma)
subducting beneath the Macquarie Ridge Complex,
which includes the Hjort Plateau, since 6–11 Ma(Meckel et al. 2003). Inspired by these recent examples
and by mechanical considerations (e.g., Shemenda 1992),
we suggest that the initial thrusting occurred within the
Pacific plate at a distance of a few tens of kilometersfrom the former transform boundary. The former transform fault probably remained active, partitioning thestrain if we assume that the convergence was oblique fora long time after subduction initiated. Such geometry favors the lateral migration of a fore-arc sliver (McCaffrey
1992; Lallemand et al. 1999). In the proto-IBM case, thefore-arc sliver was likely composed of Pacific oceanic
lithosphere (an ophiolitic wedge of Pacific origin). Considering that the trench-transform distance likely depends on respective lithosphere thicknesses, it may varyalong-strike depending on the plate’s age. Since kinematic reconstructions, in Seton et al. (2015), for example, indicate that the age of the Pacific plate increases
southward from 0 to 80 Ma, we can reasonably assume

Lallemand Progress in Earth and Planetary Science (2016) 3:15

that the Pacific fore-arc sliver will be wider in the south(Fig. 5).
At this stage, it is important to note the difference between spontaneous and forced subduction initiation in ageodynamic context that bears magmatic sources inmind. Indeed, most petrologists (Stern and Bloomer
1992; Shervais and Choi 2011; Stern et al. 2012; Ishizuka
et al. 2014) consider that the asthenospheric mantle invades the gap between “sinking old” and “young buoyant” lithospheres, inducing during fore-arc spreading(FABs and boninites), but since spontaneous subductionis unlikely and “compression is the rule” (Hall et al.
2003), there is no available space for the mantle to reachthe fore-arc region. Consequently, the first lavas erupted
at a significant distance from the incipient trench.
Tectono-magmatic model of PSP inception, IBM subduction
initiation and evolution

Chronologically, we propose the following tectonomagmatic events flow at the scale of the whole IBM system (Figs. 5 and 6):∼60–55 Ma: Izanagi slab detachment beneath the East
Asia margin triggers diffuse shortening across theregion accommodating the transform motion between
the Mesozoic composite proto-PSP and the Pacificoceanic plate.
∼55–52 Ma: mantle flow reorganization after slab
detachment and interaction with local mantle
convection (proto-Philippine subduction) contributed
to the formation of the Oki-Daito plume.
∼54–48 Ma: multiple rifts developed under the
influence of the plume, splitting the composite protoPSP into several ridges separated by short-lived oceanic
basins. Those at the head of the plume were intruded
by OIB sills like the Minami-Daito Basin but others stillshow Indian-ocean MORB signatures in their Pb isotopic composition (Ishizuka et al. 2011b; Ishizuka et al.
2013; Hickey-Vargas et al. 2013). The FABs describedin the Bonin and Mariana fore-arcs belong to thisgroup. These oceanic basins opened back of the transform fault, probably without or with little contamination from the down-going Pacific plate. One of the
spreading centers, subparallel to the proto-Philippine
Arc, gave rise to the oldest crust of the WPB. This wasabandoned after a few m.y. through a ridge jump.
∼52–48 Ma: after several m.y. of diffuse shortening
across the transform boundary region, the deformation
localized along a thrust fault cutting through the
Pacific plate, incorporating a Pacific ophiolite into the
newly formed PSP. Behind the transform fault, the PSP
lithosphere stretched, creating an alternance of thickisland arc remnants and thin oceanic lithosphere(FABs). The width of the Pacific fore-arc sliver wasPage 19 of 26

probably larger in the south where the subducting plate
was older. The subducting Pacific plate probably deformed, with undulations, because the thickness of theoverriding lithosphere varied along-strike from theMesozoic ridges to the young, thin oceanic lithosphere.
The subducting Pacific crust thus reached the mantle
corner sooner beneath the newly formed basins thanbeneath the ridges.
∼49–34 Ma: the first boninites are supposed to have
erupted around ∼ 49-48 Ma, persisting for about
15 m.y (Cosca et al. 1998). Following the geodynamic
setting proposed by Deschamps and Lallemand (2003),
we believe that these lavas did not erupt in a fore-arc
position, but rather in an incipient arc and/or rear-arc
position mostly at the intersection between the spreading centers of the young oceanic basins and the juvenilearc. These are considered to be the first “arc-related
lavas” because they are stratigraphically at the bottomof the volcanic suite, but they were still erupting
15 m.y. after subduction initiation. This clearly indicates, if necessary, that the conditions for their eruption
include a specific geodynamic context including an arcridge intersection as in the Valu Fa Arc (Tonga), rather
than fitting the beginning of subduction.
<45 Ma: high-Ca boninites and high-Mg andesites
sometimes appear atop low-Ca boninites on some
Bonin or Mariana islands (Ishizuka et al. 2006). They
mark the transition between highly depleted mantle
sources and the high degrees of fluxed melting at shallow levels that generated boninites and normal arc volcanism (Reagan et al. 2008). Then, typical arc tholeiites
and calc-alkaline rocks formed, contributing to thegrowth of the IBM Arc. The delay of a few m.y. between the oldest boninites and the oldest arc tholeiites
is simply explained by the time needed for the Pacificcrust to reach the mantle wedge beneath the Mesozoic
ridges and the thickening lithosphere associated with
the FABs.
<40? Ma: tectonic erosion of the frontal margin has
been documented during the Neogene and possibly assoon as the Middle Eocene (Lallemand 1995). It has
been accompanied by fore-arc subsidence/consumption
and volcanic front retreat (Fig. 7). At least 150 km offrontal margin has been subducted and partly recycled
into arc magmatism (Bloomer 1983; Lallemand 1996,
1998). This erosional process permitted the oldest
FABs, arc boninites, and tholeiites to outcrop today
near the trench. Most or all of the Pacific ophiolite has
probably been lost into the subduction zone. Discoveries of Mesozoic cherts and ophiolitic suites in somerare places may represent remnants of the Pacific relics
trapped during subduction initiation as well as pieces of
seamounts offscrapped from the down-going plate later(Johnson et al. 1991). The widespread serpentinite mudLallemand Progress in Earth and Planetary Science (2016) 3:15

Page 20 of 26

Fig. 6 Schematic tectono-magmatic model of IBM subduction initiation and early evolution. Special emphasis has been done on the geodynamic
context of various magma eruptions. The white lines in stage "40 Ma - present" represent the former positions of plate boundaries or the base of
the upper plate in stage "45-40 Ma". TF = transform fault, PAC = Pacific, FAB = Fore-arc basalts

volcanoes observed in the Mariana fore-arc (Fryer et al.
1985, 1999) are very interesting because they are theonly ones known to be active in this context today.
Fluids from the descending plate hydrate the fore-arc
mantle and enable serpentinite muds to rise along faults
to the seafloor (Fryer 2012). Blueschists found in the
mud attest that they originate from depths as great as
25 km and their ascent is probably facilitated by subvertical faults cutting through the fore-arc (Fryer et al.
2006). Following our scenario, we propose that they

form along the segments of the initial paleo-transform
fault zone that have been preserved from erosion. As
suggested above, the Pacific sliver should have been
wider in the Mariana fore-arc because it was thought
to be much older than in the Izu-Bonin fore-arc. Logically, for a constant amount of tectonic erosion along
the IBM fore-arc, the southern part is more likely topreserve Pacific remnants than the northern part. Sucha paleo-transform is a good candidate for both a subvertical faulted zone and hydration, and thus

Lallemand Progress in Earth and Planetary Science (2016) 3:15

Page 21 of 26

Fig. 7 Schematic cross-sections of Izu-Bonin and Mariana fore-arcs at early stage and at present. This cartoon emphasizes the differences in structural
settings that might favor the rise of serpentinite mud diapirs. FABs fore-arc basalts. As in Fig. 4, black and grey lines outline the present and reconstructedslab’s top and upper plate geometries with respect to a reference line that could be the present volcanic arc

serpentinite formation. If this hypothesis is correct, weshould find remnants of the former Pacific ophiolite
trenchward of that zone. The discoveries of Johnson etal. (1991) in the Mariana fore-arc could represent a firstsign that this is the case.

Conclusions
Compiling all the data available on the composite PSP,we were able to depict the earlier stages of PSP evolution
within a coherent integrative approach.
Based on our calculations, the total PSP area can beroughly estimated to cover ∼8.7 106 km2, with about 2/3(∼5.9 106 km2) constituting the present-day visible part of
the PSP, one fourth (∼2.2 106 km2) is already subducted beneath the Ryukyu and Philippine arcs, and the remaining
0.6 106 km2 has been eroded along its eastern boundary.
Based on the timing of events, the most likely trigger
of PSP inception is the Izanagi slab detachment beneaththe East Asia margin. Such a mega-event has been dated
60–55 Ma, which gave enough time for the paleotransform boundary between the Pacific plate and theproto-PSP to localize the deformation, evolve into a subduction zone around 52–50 Ma and produce the firstboninitic lavas a few m.y. later around 49–48 Ma. At thesame time, mantle flow reorganization triggered the formation of the Oki-Daito plume, which triggered, or
enhanced, the splitting of the composite Mesozoic
proto-PSP into several pieces around 54–50 Ma. The

plume also controlled the formation of the long-lived
WPB behind the proto-Philippine Arc, especially in its
northern sector, during the first 15 m.y. of opening. The
IBM trench developed within the Pacific Plate, likely isolating a fore-arc sliver composed of a Pacific ophiolite
bounded arcward by a paleo-transform zone. Later, tectonic erosion of the fore-arc removed most of the Pacificfore-arc material, except in a few areas, like off the Mariana Arc, where some remnants may outcrop, as well as
serpentinite diapirs that might have developed along thealtered paleo-transform relics. The ophiolitic suite presently sampled in the IBM fore-arc was not formed in afore-arc position but at a significant distance (>50 km)
from the incipient trench, which would account for theconsiderable amount of material consumed at the frontof that margin. Consequently, FABs and fortiori boninites are not markers s.s. of subduction initiation. The
so-called “fore-arc basalts” were formed along shortlived spreading ridges, far and out of the influence of the
Pacific subduction, until the slab’s crust reached thedepth of dehydration, favoring the eruption of the boninites. The intersection of numerous spreading centers
and the newly forming arc above a shallow slab satisfied
the necessary conditions for boninite formation. Use of
the word “fore-arc” to characterize these basalts andboninites is genetically not appropriate.
Further investigations and physical experiments areneeded to validate our model.

Lallemand Progress in Earth and Planetary Science (2016) 3:15

Abbreviations
ADO: Amami-Daito-Oki-Daito; CBF: Central Basin Fault; DSDP: Deep-Sea
Drilling Project; FABs: fore-arc basalts; FZ: fracture zone; IBM: Izu-BoninMariana; IODP: International Ocean Discovery Program; IP: Izanagi-Pacific;
KPR: Kyushu-Palau Ridge; LOFZ: Luzon-Okinawa fracture zone; MORBs: midocean ridge basalts; NTD: non-transform discontinuity; ODE: Oki-Daito
Escarpment; OIB: ocean island basalt; PSP: Philippine Sea Plate; WPB: West
Philippine Basin.
Competing interests
The author declares that he has no competing interests.
Authors’ information
The author, after spending the first 2 years of his PhD studies at the Ocean
Research Institute - Tokyo University in the early 1980s, has focused most of
his research studies on understanding subduction processes, with special
emphasis on the Japan and Taiwan areas. He collaborated with Anne
Deschamps during her Master’s and PhD studies as well as during her
post-doctoral research at JAMSTEC between 1997 and 2003. Significant
results on the geodynamics of the Philippine Sea Plate arose from that
intense collaborative period. Anne should have co-authored this review
paper if she had still been alive.
Acknowledgements
I dedicate this review to Anne Deschamps who left us recently and who has
provided crucial constraints on the Gagua Ridge, the Huatung Basin, theMariana Trough and the Izu-Bonin-Mariana arc. Her major contribution,
however, concerns the tectonic evolution of the West Philippine Basin. In
memory of her new insights, especially on the “Central Basin Fault rift,”
Yasuhiko Ohara and Toshiya Fujiwara have suggested naming an oceanic
high fringing the CBF rift in the center of the Philippine Sea Plate the“Deschamps seamount.” Their suggestion was approved unanimously by theIntergovernmental Oceanographic Commission of UNESCO in mid-October
2015. This paper’s cover image shows a detailed map of the Deschamps
seamount (Ohara et al. 2015) and a picture of Anne Deschamps taken in2010 before she explored the East Pacific Rise using the 6000 m deep-sea
submersible Nautile. Thanks to Jean-Yves Royer who provided me with thisphotograph.
I wish to express my deep thanks to the convenors of the special session on“Tectonic evolution of Northeast Asia” at the Japan Geoscience Union
Meeting hold in Makuhari in May 2015, Jonny Wu, Kyoko Okino, Gaku
Kimura, and Cedric Legendre. I also sincerely thank the Japan Geoscience
Union for providing me support for my visit. Anne Delplanque efficiently
redrew my sketches and Stéphane Dominguez kindly provided thebathymetric charts for the cover image and Figs. 1 and 2. Part of this review
was inspired by the scientific exchanges that I had during the JpGU Meetingwith Gaku Kimura, Ken Tani, Ryuichi Shinjo, and Osamu Ishizuka. I was also
inspired by the numerous discussions in the laboratory with Diane Arcay,
Sarah Abecassis, Marguerite Godard, and Fleurice Parat, but the main
substance of the review paper matured from the joint work done with Anne
Deschamps.
Received: 18 November 2015 Accepted: 4 April 2016

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