Hikurangi Plateau subduction a trigger for Vitiaz arc splitting and Havre Trough opening (southwestern Pacific)
←
→
Page content transcription
If your browser does not render page correctly, please read the page content below
https://doi.org/10.1130/G48436.1
Manuscript received 15 May 2020
Revised manuscript received 12 November 2020
Manuscript accepted 15 November 2020
© 2021 The Authors. Gold Open Access: This paper is published under the terms of the CC-BY license.
Hikurangi Plateau subduction a trigger for Vitiaz arc splitting
and Havre Trough opening (southwestern Pacific)
K. Hoernle1,2, J. Gill3, C. Timm1,4, F. Hauff1, R. Werner1, D. Garbe-Schönberg2 and M. Gutjahr1
1
EOMAR Helmholtz Centre for Ocean Research Kiel, 24148 Kiel, Germany
G
2
Institute of Geosciences, Kiel University, 24118 Kiel, Germany
3
Department of Earth and Planetary Sciences, University of California, Santa Cruz, California 95064, USA
4
GNS Science, PO Box 30-368, Lower Hutt 5040, New Zealand
ABSTRACT et al., 2011). It formed at ca. 125 Ma as part
Splitting of the Vitiaz arc formed the Tonga-Kermadec and Lau-Colville Ridges (south- of the Ontong Java–Manihiki–Hikurangi super-
western Pacific Ocean), separated by the Lau Basin in the north and Havre Trough in the plateau, which broke apart shortly after forma-
south. We present new trace element and Sr-Nd-Hf-Pb isotope geochemistry for the Kermadec tion (e.g., Davy et al., 2008; Hoernle et al.,
and Colville Ridges extending ∼900 km north of New Zealand (36°S–28°S) in order to (1) 2010). The basement of the plateau fragments
compare the composition of the arc remnants with Quaternary Kermadec arc volcanism, consists of two distinct geochemical types:
(2) constrain spatial geochemical variations in the arc remnants, (3) evaluate the effect of (1) low-Ti basalts (Kroenke and Kwaimbaita
Hikurangi igneous plateau subduction on the geochemistry of the older arc lavas, and (4) groups on Ontong Java) have isotopically inter-
elucidate what may have caused arc splitting. Compared to the Kermadec Ridge, the Colville mediate compositions similar to that of primi-
Ridge has higher more-incompatible to less-incompatible immobile element ratios and largely tive mantle, and (2) high-Ti basalts (Singallo
overlapping isotope ratios, consistent with an origin through lower degrees of melting of more group on Ontong Java) have enriched mantle
enriched upper mantle in the Vitiaz rear arc. Between ca. 8 and 3 Ma, both halves of the arc 1 (EM1)–type basement with unradiogenic
(∼36°S–29°S) included a more enriched (EM1-type) composition (with lower 206Pb/204Pb and 206
Pb/204Pb but radiogenic Sr isotope ratios
207
Pb/204Pb and higher Δ8/4 Pb [deviation of the measured 208Pb/204Pb ratio from a Northern (e.g., Tejada et al., 2004; Hoernle et al., 2010;
Hemisphere basalt regression line] and 87Sr/86Sr) compared to older and younger arc lavas. Timm et al., 2011; Golowin et al., 2018). Where
High-Ti basalts from the Manihiki Plateau, once joined to the Hikurangi Plateau, could serve stratigraphic information is available, the high-
as the enriched Vitiaz arc end member. We propose that the enriched plateau signature, seen Ti basalts overlie the low-Ti basalts. Between
only in the isotope ratios of mobile elements, was transported by hydrous fluids from the ca. 117 and 79 Ma, spreading along the Osbourn
western margin of the subducting Hikurangi Plateau or a Hikurangi Plateau fragment into Trough paleo–spreading center, now located at
the overlying mantle wedge. Our results are consistent with plateau subduction triggering ∼25.5°S latitude, created ∼3000 km of seafloor
arc splitting and backarc opening. between the Hikurangi and Manihiki Plateaus
(e.g., Mortimer et al., 2019). The northern tip
INTRODUCTION can et al., 1985; Wright et al., 1996; Timm et al., of the subducting Hikurangi Plateau is presently
Volcanic arcs play a key role in the plate 2019; Caratori Tontini et al., 2019). Mechanisms located at ∼36°S.
tectonic paradigm, being the surface expres- for triggering arc splitting, however, are con- Here we present new trace element and Sr-
sion of plate convergence. Nevertheless, little troversial (Sdrolias and Müller, 2006; Wallace Nd-Hf-Pb isotopic data from 40 locations on
is known about the long-term tectonic and geo- et al., 2009). the Kermadec (KR) and Colville (CR) Ridges
chemical evolution of submarine remnant arc Subduction of young igneous oceanic pla- between ∼28°S and 36°S (Fig. S1 in the Supple-
systems formed by arc splitting and backarc teaus is unlikely due to their buoyancy, as dem- mental Material1), recovered primarily on the
basin opening, largely due to their inaccessi- onstrated by the Hikurangi Plateau when it col- R/V Sonne cruise SO255. We show that geo-
bility. Contemporaneous Neogene volcanism on lided with and accreted to the Chatham Rise chemical variations along both ridges are nearly
the Tonga-Kermadec and Lau-Colville Ridges at ca. 105 Ma, becoming part of the Zealandia identical, confirming that they once formed a
(southwestern Pacific Ocean; Fig. 1) supports microcontinent. The present-day Hikurangi Pla- single arc, and that differences between the
the idea that the subparallel ridges were once teau represents a rare example of an oceanic ridges reflect the KR having been the frontal
part of a single volcanic arc (termed the Vitiaz plateau being subducted into Earth’s mantle arc and the CR the rear arc of the Neogene Vitiaz
arc), which split at ca. 5.5–3 Ma to form the Lau beneath the North Island of New Zealand and arc. Some of the late Neogene (8–3 Ma) Vitiaz
Basin and Havre Trough (e.g., Gill, 1976; Dun- the southern Kermadec arc (Fig. 1) (Reyners arc had an enriched composition distinct from
1
Supplemental Material. Supplemental information about the samples and analytical methods, including Fig. S1), Table S1 (geochemical data), and Table S2
(replicates and reference materials). Please visit https://doi.org/10.1130/GEOL.S.13377182 to access the supplemental material, and contact editing@geosociety.
org with any questions.
CITATION: Hoernle, K., et al., 2021, Hikurangi Plateau subduction a trigger for Vitiaz arc splitting and Havre Trough opening (southwestern Pacific): Geology,
v. 49, p. XXX–XXX, https://doi.org/10.1130/G48436.1
Geological Society of America | GEOLOGY | Volume XX | Number XX | www.gsapubs.org 1
Downloaded from http://pubs.geoscienceworld.org/gsa/geology/article-pdf/doi/10.1130/G48436.1/5208662/g48436.pdf
by guest
ca. 8–3 Ma and depleted volcanism perhaps
continuously since the early Miocene.
Plots of isotope ratios versus latitude (with
1° latitude added to CR samples to compen-
sate for northwest-southeast opening of the
Havre Trough) show that isotopic variations are
nearly identical along the KR and CR (Fig. 3),
confirming that they once formed a single vol-
canic arc (Gill, 1976; Timm et al., 2019; Cara-
tori Tontini et al., 2019). The shift to higher
Figure 1. (A) Map showing more-incompatible to less-incompatible ele-
location of the Tonga-Ker- ment ratios in the CR than the KR lavas at simi-
madec arc-backarc system
and Hikurangi Plateau. lar isotopic composition suggests derivation
Red box shows location of of CR lavas through lower degrees of melting
the map in Figure S1 (see beneath the rear arc. KCR lavas with enriched
footnote 1). Base map is compositions were found between 29°S and
from GEBCO_2014 Grid
37°S (corrected CR; Fig. 3) with the strongest
(version 20150318; http://
www.gebco.net). enriched signal being located at ∼33°S, charac-
terized by the lowest 206Pb/204Pb and 207Pb/204Pb
and highest 87Sr/86Sr ratios. Therefore, the
enriched arc signature appears to have been
limited both temporally and spatially, although
more geochronology is necessary to define its
exact duration.
We now review possible origins of the
enriched end member, beginning with the
mantle wedge. Assuming corner flow, enriched
intraplate mantle as found in South Fiji Basin
seamounts and intraplate CR samples could
have flowed from the backarc beneath the
that of the Quaternary Kermadec volcanic arc, (≤18.37) and 207Pb/204Pb (≤15.53) and higher older arc. The South Fiji seamount and intra-
consistent with subduction of the Hikurangi Pla- 87
Sr/86Sr (≥0.7047) at similar 208Pb/204Pb, Nd, plate CR source, however, has higher 206Pb/204Pb
teau or a plateau fragment. The enriched lavas and Hf isotope ratios, indicating an enriched and lower 87Sr/86Sr isotope ratios than the KCR
occur along a segment of the arc where part of mantle (EM1)–type component in the source of lavas and therefore cannot explain the enriched
the forearc is missing, consistent with removal the KCR lavas (between ∼29.5°S and 36.5°S), (EM1-type) signature (Fig. 2). There is also no
by plateau subduction. Plateau collision and sub- not yet found in the Quaternary lavas. evidence of a plume beneath the arc, because
duction is a possible mechanism for causing arc Alkalic seamounts behind and late-stage the enriched lavas show typical subduction zone
splitting and backarc basin opening. cones on the CR (designated “intraplate CR”) incompatible element abundances, e.g., low
have higher Nb/Th (4.3, 9.5–15.5), Ce/Pb (3–32), Ce/Pb (2.0–11.2, n = 74) and Nb/U (0.7–7.6,
RESULTS Nb/U (9–50, LOIA B
C D
Figure 2. 206Pb/204Pb versus 208Pb/204Pb (A), 207Pb/204Pb (B), 87Sr/86Sr (C), and 143Nd/144Nd (D) isotope diagrams for depleted and enriched (EM1-
type; ca. 8–3 Ma) Kermadec Ridge and Colville Ridge lavas, Quaternary Kermadec volcanic arc (QKVA) lavas, Havre Trough backarc (HTBA)
lavas, sediments data, and Manihiki North Plateau samples (Golowin et al., 2018; Timm et al., 2019, and references therein; Hauff et al., 2021;
Gill et al., 2021). In C, the arrow labelled “Subducted sediments” points to the subducted sediment field, which plots above the range in the
diagram. Pacific and Indian mid-oceanic ridge basalt (MORB) is from the PetDB (http://www.earthchem.org/petdb).
explain the enriched composition (Castillo have extended as far north as 29°S. Alterna- propose that between ca. 8 and 3 Ma, high-Ti
et al., 2009; Hoernle et al., 2010). tively, EM1 plateau material may have also plateau basalts with an EM1-type composition,
The Hikurangi Plateau currently subducts been incorporated in the ocean lithosphere similar to Manihiki North Plateau lavas, sub-
south of 36°S, but isotopic evidence suggests (crust and/or mantle) formed directly after ducted beneath the southern Vitiaz arc possibly
that it may underlie the present arc as far north plateau breakup at ca. 117 Ma (Fig. 4). We as far north as ∼29°S.
as ∼32°S (Timm et al., 2014). The enriched
KCR isotopic signature, however, cannot be
explained by the composition of the low-Ti
Hikurangi basement, sampled along ∼50 km
of the Rapuhia scarp (Hoernle et al., 2010).
Detailed sampling and geochemical studies
have also been conducted on the Manihiki Fi g u re 3. Plot of
Plateau, which was once joined to the north- 206
Pb/204Pb versus latitude,
ern part of the Hikurangi Plateau. The high-Ti showing a peak in enrich-
lavas from the Manihiki North Plateau have ment (lowest 206Pb/204Pb)
at 33°S. One degree of
appropriate Pb and Sr isotopic compositions
latitude has been added to
(Timm et al., 2011; Golowin et al., 2018) to Colville Ridge samples to
serve as the EM1 component in the enriched correct for the opening of
KCR lavas (Fig. 2). Although estimates of the the Havre Trough. Refer-
maximum size of the Hikurangi Plateau based ences are as for Figure 2.
on super-plateau reconstructions extend the
plateau to ∼32°S (Timm et al., 2014), it is
possible that a relatively thin finger of plateau
material or plateau fragment, separated from
the western edge of the Manihiki Plateau, may
Geological Society of America | GEOLOGY | Volume XX | Number XX | www.gsapubs.org 3
Downloaded from http://pubs.geoscienceworld.org/gsa/geology/article-pdf/doi/10.1130/G48436.1/5208662/g48436.pdf
by guestsubduction, and (2) Vitiaz arc splitting and
A C Havre Trough opening.
Because there has been only minor clockwise
rotation of the Kermadec forearc from 10 Ma to
the present (Sdrolias and Müller, 2006), another
possible mechanism is removal of forearc litho-
sphere (Wolf and Huismans, 2019). Subduc-
tion of a positive bathymetric anomaly on the
downgoing plate, such as an aseismic ridge or
plateau fragment, would enhance basal litho-
spheric erosion of the overriding plate, result-
ing in subsidence and extension of the margin
B D (Clift et al., 2003). Between 29°S and 34°S,
the lithosphere thickness beneath the forearc
Enriched
thins to ∼10–11 km but reaches thicknesses of
oceanic 16–17 km to the north (25°S–26°S) (Stratford
lithosphere ? et al., 2015; Bassett et al., 2016), which may
reflect basal forearc removal by plateau sub-
duction. In order to explain the absence of the
∼110-km-wide Tonga Ridge (located ∼160 km
from the trench at ∼25°S–26°S) in the forearc
south of ∼30.5°S, Collot and Davy (1998) pro-
posed frontal forearc removal. Removal of a
E large block of the forearc could have resulted in
extension as the overriding plate moved trench-
ward to compensate for forearc removal, and
could explain migration of the arc westward
away from the trench (Keppie et al., 2009)
beginning at ∼30°S and away from the KR into
the eastern Havre Trough south of ∼32°S (Bas-
sett et al., 2016). Thus, lithospheric removal
by plateau collision and subduction could also
be an important mechanism contributing to arc
splitting and backarc basin opening.
Finally, the enriched plateau signal disap-
Figure 4. Model to explain the presence of enriched signal in Kermadec Ridge and Colville pears in the KR and CR volcanism at ca. 3 Ma,
Ridge lavas between ca. 8 and 3 Ma. (A) At ca. 120 Ma, Ontong Java rifts away from the Mani- and normal oceanic crust is presently subduct-
hiki + Hikurangi plateau fragment. (B) At ca. 117–97 Ma, spreading along the Osbourn spreading ing in the region where the enriched signal was
center creates ∼3000 km of seafloor between Manihiki and Hikurangi (Mortimer et al., 2019).
Some oceanic lithosphere formed near rifted margins of plateau fragments may also have observed (29°S–36°S). Once the plateau frag-
enriched plateau-like composition. At ca. 105 Ma, Hikurangi collides with the Gondwana sub- ment fully subducted and thinner “normal” Cre-
duction margin, which later becomes the Chatham Rise of Zealandia. (C) At ca. 10 Ma, the taceous oceanic crust started subducting again,
western margin of Hikurangi is just outboard of the Kermadec–North Island (New Zealand) some slab rollback would have been likely. This
trench. (D) From ca. 8 to 3 Ma, the western Hikurangi margin subducts beneath the Vitiaz arc,
could also have been an important mechanism
which splits into Colville Ridge (CR) and Kermadec Ridge (KR), forming the Havre Trough. (E)
Present configuration. (Modified from Davy et al., 2008; Timm et al., 2014.) causing or contributing to backarc rifting and/
or spreading. We need better constraints on the
timing of Havre Trough opening and plateau
Causes of Arc Splitting and Backarc Basin the incoming plate (e.g., seamount province, subduction in order to constrain the exact mech-
Opening hotspot track, or oceanic plateau) with the anism further.
The causes of splitting of the Vitiaz arc subduction margin. The collision “pins” the As is clear from Ontong Java, plateau col-
into the KR and CR and the formation of the subduction zone, resulting in trenchward rota- lision with a subduction zone will not always
Havre Trough backarc basin are enigmatic. tion of the forearc about the pinned pivot point, result in arc splitting and backarc rifting. Due
Extension in the overriding plate can trig- causing extension, arc splitting, and backarc to its larger size, greater thickness, and younger
ger backarc rifting and/or spreading (Karig, rifting and/or spreading (McCabe, 1984). An age at collision than the Hikurangi plateau mar-
1971). Rollback of the subducting slab causes important criterion for causing backarc opening gin or plateau fragment when it collided with
trench retreat, resulting in extension in the by a collision is that the “indentor enter[s] the New Zealand, the Ontong Java Plateau was too
overriding plate (Jurdy, 1979), but rollback subduction margin just prior to the initiation buoyant and thick to subduct and clogged the
is unlikely to be a major process during sub- of the back-arc rifting event” (Wallace et al., subduction zone, resulting in subduction polar-
duction of thickened plateau crust (e.g., as 2009, p. 9). Based on the presently available ity reversal, so that normal ocean crust could
much as 35 km beneath the Hikurangi Plateau; age and geochemical data, the first evidence again subduct. In summary, there appears to
Reyners et al., 2011). for plateau subduction was at ca. 8 Ma, pre- be a continuum from collision and subduc-
Another mechanism for generating exten- ceding the initial Havre Trough opening at ca. tion of seamount clusters and hotspot tracks
sion in the overriding plate is forearc rotation 5.5–3 Ma (Caratori Tontini et al., 2019), con- resulting in forearc rotation and backarc rift-
caused by collision of a buoyant indentor on sistent with a connection between (1) plateau ing (Wallace et al., 2009), to collision of older
4 www.gsapubs.org | Volume XX | Number XX | GEOLOGY | Geological Society of America
Downloaded from http://pubs.geoscienceworld.org/gsa/geology/article-pdf/doi/10.1130/G48436.1/5208662/g48436.pdf
by guestplateau f ragments causing lithospheric removal Gill, J., Hoernle, K., Todd, E., Hauff, F., Werner, R., Reyners, M., Eberhart-Phillips, D., and Bannister,
(accompanied by arc splitting and backarc open- Timm, C., Garbe-Schönberg, D., Gutjahr, M., S., 2011, Tracking repeated subduction of the
2021, Basalt geochemistry and mantle flow dur- Hikurangi Plateau beneath New Zealand: Earth
ing), to collision of large and thick plateaus over ing early backarc basin evolution: Havre Trough and Planetary Science Letters, v. 311, p. 165–
a long stretch of an arc that shuts down subduc- and Kermadec Arc, southwest Pacific: Geo- 171, https://doi.org/10.1016/j.epsl.2011.09.011.
tion, causing polarity reversal in oceanic sub- chemistry Geophysics Geosystems, https://doi. Sdrolias, M., and Müller, R.D., 2006, Controls on
duction zones. org/10.1029/2020GC009339 (in press). back-arc basin formation: Geochemistry Geo-
Golowin, R., Portnyagin, M., Hoernle, K., Hauff, physics Geosystems, v. 7, Q04016, https://doi
F., Werner, R., and Garbe-Schönberg, D., .org/10.1029/2005GC001090.
ACKNOWLEDGMENTS 2018, Geochemistry of deep Manihiki Plateau Stratford, W., Peirce, C., Funnell, M., Paulatto, M.,
We thank the shipboard and scientific crews of R/V crust: Implications for compositional diver- Watts, A.B., Grevemeyer, I., and Bassett, D.,
Sonne for a successful SO255 cruise; S. Hauff, K. sity of large igneous provinces in the Western 2015, Effect of Seamount subduction on forearc
Junge, and U. Westernströer for analytical support; Pacific and their genetic link: Chemical Geol- morphology and seismic structure of the Tonga-
O. Ishizuka, B. Jicha, and B. Stern for helpful formal ogy, v. 493, p. 553–566, https://doi. org/10.1016/ Kermadec subduction zone: Geophysical Journal
reviews; I. Grevemeyer for helpful comments; and the j.chemgeo.2018.07.016. International, v. 200, p. 1503–1522, https://doi
German Federal Ministry of Education and Research Hauff, F., Hoernle, K., Gill, J., Werner, R., Timm, C., .org/10.1093/gji/ggu475.
(BMBF) (grant 03G0255A), GEOMAR Helmholtz Garbe-Schönberg, D., Gutjahr, M., and Jung, S., Tejada, M.L.G., Mahoney, J.J., Castillo, P.R., Ingle,
Centre (Kiel, Germany), and GNS Science (New Zea- 2021, R/V SONNE Cruise SO255 “VITIAZ”: S.P., Sheth, H.C., and Weis, D., 2004, Pin-prick-
land) for funding this project. An integrated major element, trace element and ing the elephant: Evidence on the origin of the
Sr-Nd-Pb-Hf isotope data set of volcanic rocks Ontong Java Plateau from Pb-Sr-Hf-Nd isotopic
REFERENCES CITED from the Colville and Kermadec Ridges, the Qua- characteristics of ODP Leg 182 basalts, in Fit-
Ballance, P.F., Ablaev, A.G., Pushchin, I.K., Pletnev, ternary Kermadec volcanic front and the Havre ton, J.G., et al., eds., Origin and Evolution of the
S.P., Birylina, M.G., Itaya, T., Follas, H.A., and Trough backarc basin (version 1.0): Interdisci- Ontong Java Plateau: Geological Society [Lon-
Gibson, G.W., 1999, Morphology and history plinary Earth Data Alliance (IEDA), https://doi don] Special Publication 229, p. 133–150, https://
of the Kermadec trench–arc–backarc basin– .org/10.26022/IEDA/111723 (accessed October doi.org/10.1144/GSL.SP.2004.229.01.09.
remnant arc system at 30 to 32°S: Geophysical 2020). Timm, C., Hoernle, K., Werner, R., Hauff, F., van den
profile, microfossil and K-Ar data: Marine Geol- Hoernle, K., Hauff, F., van den Bogaard, P., Werner, Bogaard, P., Michael, P., and Coffin, M.F., and
ogy, v. 159, p. 35–62, https://doi.org/10.1016/ R., Mortimer, N., Geldmacher, J., Garbe-Schön- Koppers, A., 2011, Age and geochemistry of the
S0025-3227(98)00206-0. berg, D., and Davy, B., 2010, Age and geochem- oceanic Manihiki Plateau, SW Pacific: New evi-
Bassett, D., Kopp, H., Sutherland, R., Henrys, S., istry of volcanic rocks from the Hikurangi and dence for a plume origin: Earth and Planetary
Watts, A.B., Timm, C., Scherwath, M., Greve- Manihiki oceanic plateaus: Geochimica et Cos- Science Letters, v. 304, p. 135–146, https://doi
meyer, I., and de Ronde, C.E.J., 2016, Crustal mochimica Acta, v. 74, p. 7196–7219, https://doi .org/10.1016/j.epsl.2011.01.025.
structure of the Kermadec arc from MANGO .org/10.1016/j.gca.2010.09.030. Timm, C., et al., 2014, Subduction of the oceanic
seismic refraction profiles: Journal of Geophysi- Hofmann, A.W., Jochum, K.P., Seufert, M., and White, Hikurangi Plateau and its impact on the Ker-
cal Research: Solid Earth, v. 121, p. 7514–7546, W.M., 1986, Nb and Pb in oceanic basalts: New madec arc: Nature Communications, v. 5, 4923,
https://doi.org/10.1002/2016JB013194. constraints on mantle evolution: Earth and Plan- https://doi.org/10.1038/ncomms5923.
Caratori Tontini, F., Bassett, D., de Ronde, C.E.J., etary Science Letters, v. 79, p. 33–45, https://doi Timm, C., de Ronde, C.E.J., Hoernle, K., Cousens,
Timm, C., and Wysoczanski, R., 2019, Early .org/10.1016/0012-821X(86)90038-5. B., Wartho, J.-A., Caratori Tontini, F., Wysoc-
evolution of a young back-arc basin in the Havre Jurdy, D.M., 1979, Relative plate motions and the zanski, R., Hauff, F., and Handler, M., 2019,
Trough: Nature Geoscience, v. 12, p. 856–862, formation of marginal basin: Journal of Geo- New age and geochemical data from the South-
https://doi.org/10.1038/s41561-019-0439-y. physical Research, v. 84, p. 6796–6802, https:// ern Colville and Kermadec Ridges, SW Pacific:
Castillo, P.R., Lonsdale, P.F., Moran, C.L., and doi.org/10.1029/JB084iB12p06796. Insights into the recent geological history and
Hawkins, J.W., 2009, Geochemistry of mid- Karig, D.E., 1971, Origin and development of mar- petrogenesis of the Proto-Kermadec (Vitiaz) Arc:
Cretaceous Pacific crust being subducted along ginal basins in the western Pacific: Journal of Gondwana Research, v. 72, p. 169–193, https://
the Tonga-Kermadec Trench: Implications for the Geophysical Research, v. 76, p. 2542–2561, doi.org/10.1016/j.gr.2019.02.008.
generation of arc lavas: Lithos, v. 112, p. 87–102, https://doi.org/10.1029/JB076i011p02542. Todd, E., Gill, J.B., Wysoczanski, R.J., Hergt, J.M.,
https://doi.org/10.1016/j.lithos.2009.03.041. Keppie, D.F., Currie, C.A., and Warren, C., 2009, Wright, I.C., Leybourne, M.I., and Mortimer, N.,
Clift, P.D., Pecher, I., Kukowski, N., and Hampel, A., Subduction erosion modes: Comparing finite 2011, Hf isotopic evidence for small-scale hetero-
2003, Tectonic erosion of the Peruvian forearc, element numerical models with the geologi- geneity in the mode of mantle wedge enrichment:
Lima Basin, by subduction and Nazca ridge cal record: Earth and Planetary Science Let- Southern Havre Trough and South Fiji Basin back
collision: Tectonics, v. 22, 1023, https://doi ters, v. 287, p. 241–254, https://doi. org/10.1016/ arcs: Geochemistry Geophysics Geosystems, v. 12,
.org/10.1029/2002TC001386. j.epsl.2009.08.009. Q09011, https://doi.org/10.1029/2011GC003683.
Collot, J.Y., and Davy, B., 1998, Forearc structures McCabe, R., 1984, Implications of paleomagnetic Turner, S.P., and Hawkesworth, C.J., 1998, Using geo-
and tectonic regimes at the oblique subduction data on the collision related bending of island chemistry to map mantle flow beneath the Lau
zone between the Hikurangi Plateau and the arcs: Tectonics, v. 3, p. 409–428, https://doi Basin: Geology, v. 26, p. 1019–1022, https://doi
southern Kermadec margin: Journal of Geo- .org/10.1029/TC003i004p00409. .org/10.1130/0091-7613(1998)0262.3.CO;2.
doi.org/10.1029/97JB02474. Magoni, C., Calvert, A.T., and Bosch, D., Wallace, L.M., Ellis, S., and Mann, P., 2009, Colli-
Davy, B., Hoernle, K., and Werner, R., 2008, Hikurangi 2007, Oligocene–Miocene tectonic evolution sional model for rapid fore-arc block rotations,
Plateau: Crustal structure, rifted formation, and of the South Fiji Basin and Northland Plateau, arc curvature, and episodic back-arc rifting in
Gondwana subduction history: Geochemistry SW Pacific Ocean: Evidence from petrology subduction settings: Geochemistry Geophys-
Geophysics Geosystems, v. 9, Q07004, https:// and dating of dredged rocks: Marine Geol- ics Geosystems, v. 10, Q05001, https://doi
doi.org/10.1029/2007GC001855. ogy, v. 237, p. 1–24, https://doi.org/10.1016/ .org/10.1029/2008GC002220.
Duncan, R.A., Vallier, T.L., and Falvey, D.A., 1985, j.margeo.2006.10.033. Wolf, S.G., and Huismans, R.S., 2019, Mountain build-
Volcanic episodes at Eua, Tonga Islands, in Mortimer, N., Gans, P.B., Palin, J.M., Mef- ing or backarc extension in ocean-continent sub-
Scholl, D.W., and Vallier, T.L., eds., Geology fre, S., Herzer, R.H., and Skinner, D.N.B., duction systems: A function of backarc lithospheric
and Offshore Resources of Pacific Island Arcs— 2010, Location and migration of Miocene– strength and absolute plate velocities: Journal of
Tonga Region: Houston, Texas, Circum-Pacific Quaternary volcanic arcs in the SW Pacific Geophysical Research: Solid Earth, v. 124, p. 7461–
Council for Energy and Mineral Resources, Earth region: Journal of Volcanology and Geother- 7482, https://doi.org/10.1029/2018JB017171.
Science Series, v. 2, p. 281–290. mal Research, v. 190, p. 1–10, https://doi Wright, I.C., Parson, L.M., and Gamble, J.A., 1996,
Gill, J.B., 1976, Composition and age of Lau .org/10.1016/j.jvolgeores.2009.02.017. Evolution and interaction of migrating cross-arc
Basin and Ridge volcanic rocks: Implica- Mortimer, N., van den Bogaard, P., Hoernle, K., Timm, volcanism and back-arc rifting: An example from
tions for evolution of an interarc basin and C., Gans, P.B., Werner, R., and Riefstahl, F., 2019, the southern Havre Trough (35°20′–37°S): Jour-
remnant arc: Geological Society of Amer- Late Cretaceous oceanic plate reorganization nal of Geophysical Research, v. 101, p. 22,071–
ica Bulletin, v. 87, p. 1384–1395, https://doi and the breakup of Zealandia and Gondwana: 22,086, https://doi.org/10.1029/96JB01761.
.org/10.1130/0016-7606(1976)872.0.CO;2. doi.org/10.1016/j.gr.2018.07.010. Printed in USA
Geological Society of America | GEOLOGY | Volume XX | Number XX | www.gsapubs.org 5
Downloaded from http://pubs.geoscienceworld.org/gsa/geology/article-pdf/doi/10.1130/G48436.1/5208662/g48436.pdf
by guestYou can also read
