Earth and Planetary Science Letters 304 (2011) 135–146
Contents lists available at ScienceDirect
Earth and Planetary Science Letters
j o u r n a l h o m e p a g e : w w w. e l s ev i e r. c o m / l o c a t e / e p s l
Age and geochemistry of the oceanic Manihiki Plateau, SW Pacific: New evidence for
a plume origin
Christian Timm a,⁎,1, Kaj Hoernle a, Reinhard Werner a, Folkmar Hauff a, Paul van den Bogaard a,
Peter Michael b, Millard F. Coffin c,2, Anthony Koppers d
a
IFM-GEOMAR Leibniz Institute of Marine Sciences, Wischhofstr. 1–3, 24148 Kiel, Germany
Department of Geoscience, The University of Tulsa, Tulsa, OK 74104, USA
Atmosphere and Ocean Research Institute, University of Tokyo, Kashiwa-shi, Chiba 277–8568, Japan
d
College of Oceanic and Atmospheric Sciences, Oregon State University, Corvallis, OR 97331–5503, USA
b
c
a r t i c l e
i n f o
Article history:
Received 9 August 2010
Received in revised form 24 January 2011
Accepted 26 January 2011
Available online 20 February 2011
Editor: R.W. Carlson
Keywords:
Manihiki Plateau
oceanic large igneous province
40
Ar/39Ar age dates
major and trace element and Sr–Nd–Hf–Pb
isotope geochemistry
volatiles
Greater Ontong Java Event
a b s t r a c t
We present 40Ar/39Ar age and geochemical (major and trace element and Sr–Nd–Hf–Pb isotope) data from
submarine samples recovered from the basement of the Manihiki Plateau during the R/V Sonne research
expedition SO193. The samples, predominately tholeiites, with minor occurrences of basaltic andesites and
hawaiites, give a mean age of 124.6 ± 1.6 Ma from four different localities on the plateau. Based on TiO2 content,
we define two groups of volcanic rocks that differ in trace element and isotopic compositions. Partial melting
modeling suggests that the low-Ti group lavas were derived through large degrees of melting (c. 30%) of a
peridotitic source at mantle potential melting temperatures of c. Tp = 1510 °C, more than 100 °C above the
ambient mantle potential melting temperature. Since the primary water contents of both groups of lavas are low
(0.1–0.3g wt.%) and the source is peridotitic, excess temperature is most likely the reason for the large degrees of
melting producing the large volume of plateau basalts, consistent with the involvement of a mantle plume. The
incompatible element contents of the low-Ti group lavas show a multistage history with enrichment in the most
incompatible elements of a previously highly depleted source. They have isotopic compositions similar to
enriched mid-ocean-ridge basalt (EMORB) and similar to the common focal zone (FOZO) component. The high-Ti
group lavas have more enriched incompatible element compositions overall. Their isotopic compositions tend
towards an enriched mantle (EMI)-type endmember, similar, although less extreme, than lavas from the Pitcairn
Islands. The geochemistry of the Manihiki Plateau can best be explained by a plume containing three
components: 1) a dominant peridotitic FOZO-type component, 2) delaminated EMI-type subcontinental
lithospheric mantle (SCLM), and 3) a HIMU (recycled oceanic crustal)-type component possibly in the form of
eclogite/pyroxenite. The similarity in age and geochemical composition of Manihiki, Hikurangi and Ontong Java
basement lavas, including volcanism in some adjacent basins, suggests that the Greater Ontong Java Volcanic
Event covered c. 1% of the Earth's surface with volcanism.
© 2011 Elsevier B.V. All rights reserved.
1. Introduction
Large Igneous Provinces (LIPs) belong to the most extreme
volcanic events on Earth, during which large volumes of volcanic
rocks can be produced within a short time period (e.g. Self et al.,
2008). Several models have been proposed for the formation of LIPs.
Most authors attribute LIP formation to the arrival of a starting-plume
head, resulting in extensive melting of upwelling lower mantle in the
upper asthenosphere (e.g. Campbell et al., 1989; Campbell, 1998,
2003; Courtillot et al., 2003; Fitton and Godard, 2004; Hauff et al.,
⁎ Corresponding author. Tel.: + 64 4 570 4391; fax: + 64 4 570 2600.
E-mail address: c.timm@gns.cri.nz (C. Timm).
1
Now at GNS Science, 1 Fairway Dr, Avalon, Lower Hutt, New Zealand.
2
Now at Institute for Marine and Antarctic Studies, University of Tasmania, Hobart,
Tasmania 7001, Australia.
0012-821X/$ – see front matter © 2011 Elsevier B.V. All rights reserved.
doi:10.1016/j.epsl.2011.01.025
2000; Hoernle et al., 2010; Ingle et al., 2007; Larson, 1991a,b, 1997;
Mahoney, 1987; Mahoney and Spencer, 1991; Mahoney et al., 1993:
Tejada et al., 1996, 2002, 2004). Such starting plume heads may
broaden laterally to diameters of ~2500 km when they pond at the
base of the lithosphere (Griffiths and Campbell, 1991; Richards et al.,
1989). High magma production rates occur at the initial stage, which
led to the formation of some LIPs within geologically short time scales
of several millions of years (e.g. Duncan and Pyle, 1988; Peate, 1997;
Renne et al., 1995). Other models include the formation of LIPs through
1) increased melt production by plume–ridge interaction (Mahoney,
1987; Mahoney et al., 1993), 2) upwelling and subsequent extensive
melting induced by a meteoritic impact (Ingle and Coffin, 2004; Jones
et al., 2002; Rogers, 1982), 3) extension and decompression melting
(plate separation model; Anderson, 1996, 2000; Hames et al., 2000; King
and Anderson, 1998), 4) enhanced partial melting due to the presence of
eclogite (Cordery et al., 1997; Korenaga, 2005; Yasuda et al., 1997),
136
C. Timm et al. / Earth and Planetary Science Letters 304 (2011) 135–146
5) accumulation of smaller volcanic terranes by subduction processes
(Hoernle et al., 2004a), and 6) delamination of subcontinental
lithospheric mantle followed by upwelling and decompression melting
(e.g. Anderson, 2005; Hales et al., 2005). Cretaceous LIPs in the Pacific
Ocean include the Ontong Java, Hikurangi, and Manihiki plateaus and
the Hess, Shatsky and Magellan rises.
Several models have been proposed for the formation of the
Manihiki Plateau. Winterer et al. (1974) proposed its formation during
active rifting in mid-Cretaceous time, near or at the triple junction
between the Pacific, Antarctic and Farallon plates, whereas Mahoney
and Spencer (1991) invoked the arrival of a plume head beneath the
oceanic lithosphere. Beiersdorf et al. (1995) conducted a more detailed
study on volcanic rocks from a seamount (“Mt. Eddie”) near Deep Sea
Drilling Project (DSDP) Site 317, proposing the involvement of a plume
head in the generation of the Manihiki Plateau basement. Larson (1997)
instead favored the combination of plume activity and rifting. The
presence of a paleo-spreading center, the Osbourn Trough, midway
between the Manihiki and Hikurangi plateaus and evidence that the
Rapuhia Scarp at the northern margin of the Hikurangi Plateau is a rifted
margin, has led to the proposal that the Hikurangi and Manihiki plateaus
might have once been connected (Billen and Stock, 2000; Hoernle et al.,
2004b, 2010; Worthington et al., 2006). It has also been proposed that
the Ontong Java, Hikurangi, and Manihiki plateaus possibly formed as a
single mega-plateau (covering ~1% of the earth surface), which shortly
after formation broke up forming the separate plateau fragments (Davy
et al., 2008; Taylor, 2006).
Until the marine expedition with R/V Sonne (SO193), few samples had
been recovered from the Manihiki Plateau. Analyzed and/or dated
igneous rock samples only exist from: 1) DSDP Site 317 (Hoernle et al.,
2010; Jackson et al., 1976; Mahoney and Spencer, 1991), 2) a few dredge
locations from the 1900 m high Mt. Eddie seamount and from the base of
the Manihiki Atoll (Beiersdorf et al., 1995) and 3) from four locations
along the flanks of the Danger Island Troughs (Clague et al., 1976; Ingle
et al., 2007). Consequently the age and composition of the Manihiki
Plateau are not well constrained. The uppermost 2 km of the Manihiki
Plateau crust, however, is exposed along the Danger Island and Suvorov
troughs (Fig. 1), and the northern margin of the High and West Plateaus,
making the plateau basement accessible to sampling by dredging. During
the SO193 expedition, igneous rocks were recovered from 70 basement
and seamount sites, making the Manihiki Plateau the most extensively
sampled submarine plateau to date. Here we present new 40Ar/39Ar age
(from 5 samples) and geochemical (major and trace element and Sr–Nd–
Hf–Pb isotope from 17 samples) data from volcanic rocks recovered from
seven Manihiki basement sites during SO193 (Fig. 1), in order to improve
our understanding of the temporal and geochemical evolution and
ultimately the origin of the Manihiki LIP and test the existing models for
the formation of LIPs. Data from the remaining locations, which contained
younger, primarily alkalic, volcanism will be published separately.
2. Geological and tectonic setting
The Manihiki Plateau is located in the SW Pacific extending from ~3°S
to ~16°S and from 159°W to ~169°W. It covers an area of ~770,000 km2
(Coffin and Eldholm, 1994) and has an estimated overall volume of
8.8 million km3 (Eldholm and Coffin, 2000). The plateau is bordered by
the Tokelau Basin to the west, the Samoan Basin to the south, and the
Penrhyn and Central Pacific basins to the east and north, respectively. The
plateau lies in water depths of ~3000 m, up to 2000 m above the
surrounding Cretaceous seafloor, which is located in water depths of
~4000–5000 m (Fig. 1). The crustal thickness of the Manihiki Plateau is
believed to range between 15 and 25 km (Hussong et al., 1979; Mahoney
and Spencer, 1991; Viso et al., 2005). Numerous seamounts and some of
the westernmost Cook Islands (e.g. the Manihiki and Rakahanga atolls
and the Danger Islands) are scattered across the entire plateau. Based on
geophysical surveys from the 1960s and early 1970s, Winterer et al.
(1974) subdivided the Manihiki Plateau in three major morphological
units: (1) the ‘High Plateau’ in the east, (2) the ‘North Plateau’, and the (3)
the ‘Western Plateaus’ (Fig. 1). Deep fault systems, which are considered
to be failed rift systems (e.g. Hoernle et al., 2010; Larson et al., 2002;
Mahoney and Spencer, 1991; Viso et al., 2005), separate these units. The
N–S trending Danger Island Troughs (named after the atolls at its
southern end) separate the High from the Western Plateaus. They consist
of three en echelon fault-bounded (up to ~6200 m deep) basins. The
Danger Island Troughs bifurcate south of 10°S into the Suvorov Trough in
the east and the southern Danger Island Troughs in the west.
A broad basin separates the High and the North plateaus. The High
Plateau encompasses ~400,000 km2 above the 4000 m contour interval
and represents the largest and shallowest morphological unit of the
Manihiki Plateau. The center of the High Plateau lies in average water
depths of ~2500 to 3000 m. According to Winterer et al. (1974), acoustic
basement of the plateau has a flat relief and is covered by ≥1 km pelagic
and/or volcaniclastic sediments. The Western Plateaus represent the
second largest morphological unit of the Manihiki Plateau, encompassing ~250,000 km2 above the 5000 m contour interval, located in average
water depths of ~3500 to 4000 m. The North Plateau, encompassing
~60,000 km2 above the 4500 m depth, forms the smallest portion of the
Manihiki Plateau and is as shallow as ≤1500 mbsl. The central and
western portions are characterized by rough topography, which
becomes less pronounced as a result of being covered by ≤1 km of
sediment (Winterer et al., 1974). Seamounts and atolls are concentrated
in the marginal parts of the Manihiki Plateau.
One K/Ar age of 106.0± 3.5 Ma was determined on an igneous
basement sample drilled at DSDP Site 317 (Lanphere and Dalrymple,
1976), which is significantly younger than the directly overlying
sediment ~116 Ma (Sliter, 1992). Two 40Ar/39Ar ages from tholeiitic
basalts from DSDP Site 317 of 116.8±3.7 and 116.4 ±5.1 Ma (Hoernle
et al., 2010) agree well with the age of the overlying sediment and are
within error of an 40Ar/39Ar age of 117.9 ±3.5 for a tholeiitic sample
dredged from the Danger Island Troughs (Ingle et al., 2007). The ages of
these tholeiitic samples and an 40Ar/39Ar age of 99.5±0.7 Ma for an
alkalic sample from the Danger Island Troughs also suggest that at least
two episodes of volcanism are recorded on the Manihiki Plateau (Ingle
et al., 2007). Three samples from Mt. Eddie seamount on the High Plateau
yielded K/Ar total fusion ages of 81.6, 75.2 and 75.1 Ma, providing
additional evidence for a late alkalic stage (Beiersdorf et al., 1995).
During plateau formation in Early Cretaceous time, the seafloor drilled
at DSDP Site 317 was located at shallow water depths of 200–300 m
(possibly even subaerial), based on geochemical, sedimentological, and
paleontological evidence in the deposited volcaniclastic material (Ai et al.,
2008; Clift, 2005; Ito and Clift, 1998; Jenkyns, 1976). Shortly after the
plateau was emplaced, it is believed that the Tongareva triple junction
initiated, causing extension together with mantle upwelling, causing
incipient rifting along the Danger Islands and Suvorov troughs at about
120–118 Ma (Larson et al., 2002; Viso et al., 2005). Shortly thereafter,
renewed spreading formed the present eastern margin (Manihiki Scarp)
and possibly the southern margin as a result of asymmetric spreading
between the Manihiki and Hikurangi plateaus (Billen and Stock, 2000;
Davy et al., 2008). A zircon age of 115 Ma for the seafloor exposed at the
Wishbone Scarp just north of the Hikurangi Plateau indicates that the
breakup of the Manihiki and Hikurangi plateaus at the Osbourn Trough
spreading center happened at ~116 Ma, shortly after formation of these
plateaus (Mortimer et al., 2006). After formation and ensuing breakup,
the Manihiki Plateau cooled and subsided. Lithospheric subsidence,
however, was less than that of normal seafloor (Clift, 2005).
3. Results
3.1.
40
Ar/39Ar dating
A detailed list of the 40Ar/39Ar age data is presented in Table 1
(analytical method; age spectra and analytical data are in Supplementary file 1–4). All errors reported in this paper are stated as 2σ.
C. Timm et al. / Earth and Planetary Science Letters 304 (2011) 135–146
137
Fig. 1. Bathymetric map of the Manihiki Plateau. Black and white dots represent sample locations where the plateau basement has been recovered, including the location of DSDP Site
317. White diamonds are sample locations reported in Clague et al. (1976) and Ingle et al. (2007). Numbers beneath some sample numbers are the respective 40Ar/39Ar ages DSDP
site 317 ages are taken from Hoernle et al. (2010). Lower left inset map shows the general location of the Manihiki Plateau. OT = Osbourn Trough.
Our six new 40Ar/39Ar ages of plateau phase volcanic rocks from
four different locations from the Manihiki Plateau range from 126.0 ±
1.5 to 122.9 ± 1.6 Ma and are within error of each other. Glass sample
DR52, dredged along the northern margin of the High Plateau,
produced 40Ar/39Ar step-heating ages of 126.0 ± 1.5 (IFM-GEOMAR
geochronology laboratory) and 123.8 ± 0.8 Ma (Oregon State geochronology laboratory). Ages of 124.5 ± 1.5 Ma and 122.9 ± 1.6 Ma
(both IFM-GEOMAR) were obtained on glass samples dredged along
the eastern flank of the southern Danger Island Troughs (at location
DR26). Feldspar step-heat ages of 125.2 ± 8.3 Ma (DR18) and 125.0 ±
2.1 Ma (DR46) were obtained from samples from the lower eastern
flank of the Suvorov Trough and from a volcanic structure in the basin
between the North and High plateaus, respectively. In summary, our
new 40Ar/39Ar data set indicates that the main part of the Manihiki
Plateau basement may have formed within a geologically short period
of intense volcanism at 124.6 ± 1.6 Ma.
3.2. Geochemical characteristics of the plateau-phase lavas
Major element compositions (normalized to 100% on a volatile-free
basis) of volcanic rocks from the plateau basement range from tholeiitic
basalts to basaltic andesites (after Le Maitre et al., 2002; except for two
samples with MgO b 9.2 wt.% that extend to lower SiO2, suggesting
clinopyroxene and plagioclase in addition to olivine fractionation in
these samples). Relatively low loss of ignition (LOI b 2.5 wt.%) and P2O5
(b0.13 wt.%) suggests that the influence of seawater alteration on the
chemistry of the selected whole rock samples was minor. Nevertheless,
highly variable ratios of some large ion lithophile elements (LILEs) to
rare earth elements (REEs) and high field strength elements (HFSEs)
(e.g. (K, Rb)/Yb and U/(Nd, Nb)) in the whole rock samples suggest that
some of the LILEs have been affected by seawater alteration. The glasses,
on the other hand, do not show evidence of mobilization of LILEs. We
therefore concentrate on immobile trace elements in this study, which
138
C. Timm et al. / Earth and Planetary Science Letters 304 (2011) 135–146
Table 1
Results of step-heating
40
Ar/39Ar analyzes of the Manihiki basement.
Sample
Group
Run/Lab No.
Plateau age (Ma) ± 2s
MSWD
Probability
% 39Ar in plateau
No. of steps
Dated material and type of analysis
SO193
SO193 DR52–2
High-Ti
1.07
2.00
1.02
1.02
0.93
48.3
64.6
12 to 19
9 to 19
Glass step-heating
Glass step-heating
High-Ti
71.0
76.0
13 to 24
6 to 16
Glass step-heating
Glass step-heating
SO193
SO193
SO193
SO193
Low-Ti
High-T
Low-Ti
Low-Ti
127.1 ± 2.6
125.5 ± 1.8
126.0 ± 1.5
124.2 ± 0.9
123.7 ± 0.9
123.8 ± 0.8
125.2 ± 8.3
125.0 ± 2.1
124.5 ± 1.5
122.9 ± 1.6
0.38
0.03
0.31
SO193 DR52-2a
1st /52-2gls
2nd /52-2gl2
Wtd. Mean
1st/3 G1-10
2nd/3 G2-10
Wtd. Mean
DR18-4Bfs2
DR46-1fss
DR26-1gls
DR26-7gls
1.06
2.10
1.50
0.57
0.39
0.05
0.10
0.84
92.3
58.9
90.2
80.3
3 to 19
12 to 18
5 to 19
8 to 18
Feldspar step-heating
Feldspar step-heating
Glass step-heating
Glass step-heating
DR18-4B
DR46-1
DR26-1
DR26-7
a
University of Oregon ages.
Bold ages are used in the text and figures.
Number of Analyses
11
Manihiki (FOZO)
Manihiki (EMI)
Ontong Java (FOZO)
Ontong Java (EMI)
Hikurangi
9
7
tions (less radiogenic Nd, Hf, and Pb, but more radiogenic Sr isotope
ratios than the low-Ti rocks; Figs. 4 and 5a–d, Table 2), confirming that
their differences in TiO2 cannot solely be explained by fractional
crystallization.
Manihiki basement glasses have relatively low and variable H2O
contents and H2O/Ce ratios similar to MORB (Michael, 1995) and OJP
glasses (Michael, 1999; Roberge et al., 2004). The high-Ti glass (DR522) has low H2O/Ce like some EM1-type glasses (e.g., Dixon et al.,
2004), while the low-Ti glasses have higher H2O/Ce (400) like some
MORB and OJP glasses. Dissolved CO2−
3 contents in these same glasses
show that they erupted deep enough below the sea surface to prevent
H2O loss by degassing: thus the low H2O contents and ratios are
believed to be primary. The primary water contents of the Manihiki
100
a)
Ontong Java
(Kwaimbaita)
Ontong Java
(Singgalo)
Hikurangi
10
Rock/PRIMA (Hofmann, 1988)
generally correlate well with TiO2 and each other, show similar
compositions to related glass samples and show smooth patterns on
multi-element diagrams (e.g. Figs. 3 and 4; Supplementary Table 1).
Based on TiO2 content, the volcanic rocks can be grouped into a lowTi (TiO2 b 0.90 wt.%; MgO = 2.3–13.7) and a high-Ti group (TiO2 0.90 wt.%; MgO= 3.3–9.1). Fractional crystallization processes cannot
explain the difference in TiO2 at the same MgO. At a given MgO content,
SiO is generally higher and FeOt, Na2O, and P2O5 are mildly to
moderately incompatible elements (e.g. heavy (H) and middle (M)
rare earth elements (REE), Zr, Hf and Y) than in the high-Ti group and
average N-MORB Th, Nb, Ta and La abundances than the high-Ti group
(Fig. 3a). Whereas the U-shaped multi-patterns of the low-Ti group
lavas are distinct from N-MORB, the high-Ti group lavas show relatively
flat multi-element patterns between normal (N) and enriched (E)
MORB lavas (Fig. 3a). In the glass samples, the large ion lithophile
element (LILE; Rb, Ba, U, and K) within the low- and high-Ti group lavas
is generally similar. In addition, moderately to less incompatible trace
element ratios (e.g. (Nd, Sm)/Yb, (Tb/Yb)N and Zr/Y; Fig. 4a–e) are
higher in the high-Ti group. The Manihiki basement samples form
reasonably good correlations on radiogenic isotope correlation diagrams, suggesting that alteration has not destroyed the primary isotopic
signatures of the samples. The low-Ti group samples overlap the isotopic
range of the common focal zone (FOZO) component after Hauri et al.
(1994) (FOZO A) and Stracke et al. (2005) (FOZO B). Their compositions
are also similar to the dominant Kwaimbaita/Kroenke-type lavas from
the Ontong Java Plateau (e.g. Mahoney et al., 1993; Tejada et al., 1996,
2002) and the Hikurangi Plateau A lavas (Hoernle et al., 2010), but
extend to less radiogenic Sr and more radiogenic Pb isotopic compositions or towards more HIMU-like compositions (Fig. 5a–d). The high-Ti
group, similar in composition to the less common Singgalo lavas,
generally has more enriched mantle one (EM1)-type isotopic composi-
Osbourn Seamounts
1
0.1
Ontong Java
(Kroenke)
Low-Ti group lavas (wr)
High-Ti group lavas (wr)
Low-Ti group (Ingle et al., 2007)
High Ti group (Ingle et al., 2007)
Th Nb La Ce Pr Nd Sm Hf Zr Eu Gd Tb Dy Ho Y Er Tm Yb Lu
100
b)
EMORB
10
NMORB
1
5
Low-Ti group lavas (gl)
High-Ti group lavas (gl)
3
0.1
1
80
90
100
40Ar/39Ar
110
120
130
Age (Ma)
Fig. 2. 40Ar/39Ar ages of Manihiki (medium gray), Ontong Java (light gray) and
Hikurangi (black) basement lavas, including an age from the Danger Island Troughs
(Ingle et al., 2007) and two ages from DSDP Site 317 (Hoernle et al., 2010). Ages from
the Ontong Java Plateau are from Mahoney et al. (1993), Tejada et al. (1996) and Tejada
et al. (2002) and those from the Hikurangi Plateau are from Hoernle et al. (2010).
Samples from Manihiki (high-Ti group) and Ontong Java (Singgalo group), which have
enriched (EMI-type) compositions, are marked with a cross.
Rb Th Nb K
Ce Pr Sr Sm Zr Eu Tb Ho Er Yb
Ba U
Ta La Pb Nd P
Hf
Ti Gd Dy Y
Tm Lu
Fig. 3. a) Immobile incompatible element patterns on a multi-element diagram of the
Manihiki basement lavas normalized to primitive mantle (Hofmann, 1988). Additional
Manihiki data (black and white diamonds) are from Ingle et al. (2007). The dark gray
field shows the range in primitive-mantle-normalized whole rock incompatible
element abundances of the Hikurangi Plateau, whereas the medium gray field shows
the field for the incompatible element contents of the Ontong Java Plateau. (Fitton and
Godard, 2004; Mahoney et al., 1993; Tejada et al., 2002, 2004 and from Hoernle et al.,
2010). E- and N-MORB (after Sun and McDonough, 1989) are added as reference.
b) Primitive mantle normalized multi-element diagram of the glass samples.
139
C. Timm et al. / Earth and Planetary Science Letters 304 (2011) 135–146
1.4
a)
8
c)
r2
1.2
= 0.85
4
0.8
r2 = 0.73
0.6
2
0.4
b)
εNd(t)
(Tb/Yb)N
6
1.0
15
d)
r2 = 0.61
13
3
9
2
εHf(t)
Zr/Y
11
7
1
0
0.0
2
r = 0.79 (ZrXRF)
5
3
0.5
1.0
1.5
2.0
2
r = 0.78
20
Low-Ti group lavas (FOZO)
High-Ti group lavas (EMI)
19
Low-Ti group lavas (gl)
(t)
High-Ti group lavas (gl)
206Pb/204Pb
TiO2 (wt %)
e)
18
LT group literature data
HT group literature data
0.0
0.5
1.0
1.5
2.0
2.5
TiO2 (wt %)
Fig. 4. TiO2 (wt%) correlates well with a) (Tb/Yb)N, b) Zr/Y, c) εNd(t), d) εHf(t) and e) 206Pb/204Pb (t) in the Manihiki basement rocks, where N denotes normalized to primitive
mantle and t the initial isotopic composition at the age of sample formation. The low-Ti group (LT) lavas, compared to the high-Ti rocks (HT), have lower (Tb/Yb)N and Zr/Y but
higher εNd(t), εHf(t) and 206Pb/204Pb (t). Additional Manihiki data are from Ingle et al. (2007), Mahoney and Spencer (1991) and Hoernle et al. (2010). Light gray rectangles are data
from the Ontong Java Plateau (from the GEOROC database and Fitton and Godard, 2004; Mahoney et al., 1993; Tejada et al., 1996, 2002, 2004).
glasses are low and fall into the range for the Kwaimbaita/Kroenke
glasses from Ontong Java (0.1–0.3 wt.%). This is surprising for DR52,
which has an isotopic composition more similar to the Singgalo lavas
from Ontong Java. The Singgalo glasses have higher primary water
contents of 0.4–0.5 wt.%. In addition, the low and high-Ti group
Manihiki glasses have lower S contents (c. 0.05 wt.%) than glasses
from the Ontong Java Plateau (0.09–0.11 wt.%; Roberge et al., 2004)
and MORB (e.g. Wallace and Carmichael, 1992).
4. Discussion
4.1. Similar ages and geochemistry of the Manihiki, Ontong Java
and Hikurangi Plateau basements
The Manihiki Plateau basement volcanic rocks have similar ages and
geochemical compositions to the Ontong Java and Hikurangi Plateau
fragments. Our new 40Ar/39Ar age data from four new Manihiki
basement locations yield an age of 124.6 ± 1.5 Ma (Fig. 1). The age of
117.9 ± 3.5 Ma (2σ) determined from a sample from the Danger Island
Troughs (Ingle et al., 2007) and the DSDP Site 317 sample with an age of
116.4 ± 5.1 Ma (Hoernle et al., 2010) overlap the youngest age in this
study within error. The age of 116.8 ± 3.7 Ma from DSDP Site 317 lies
slightly outside of the 2σ error for the youngest sample dated in this
study at 122.9 ± 1.6 Ma, suggesting that the uppermost part of the
plateau drilled at Site 317 may be slightly younger than basement lavas
dredged at from the Danger Islands and Suvorov troughs and the
northern margins of the plateau. Taken together the ages for the
Manihiki basement localities fall in the range of 117–126 Ma. This age
range overlaps with the main pulse of activity at Ontong Java ranging
from 119 to 129 Ma (Mahoney et al., 1993; Tejada et al., 1996, 2002) and
includes the oldest age from the Hikurangi Plateau of 118 ± 4.0 Ma
(Hoernle et al., 2010), consistent with all three plateaus having formed
contemporaneously with a peak in activity between 121 and 125 Ma
(Fig. 2).
Despite the large extent of the Ontong Java Plateau, samples from the
basement analyzed thus far form three very restricted geochemical
groups: 1) the dominant Kwaimbaita-type lavas, found throughout the
plateau, which are characterized by relatively flat incompatible element
patterns on multi-element diagrams and isotopic compositions similar
to E-MORB, 2) the Kroenke group lavas that are characterized by higher
MgO contents and lower incompatible element abundances than the
Kwaimbaita group lavas but have similar incompatible element and
isotopic ratios and have been interpreted as parental to the Kwaimbaita
group lavas (and thus these two groups will be referred to collectively
henceforth), and 3) the Singgalo group lavas that have more enriched
incompatible element characteristics and more EMI-type isotopic
compositions (e.g. Fitton and Godard, 2004; Tejada et al., 1996, 2002,
2004). The Hikurangi Plateau lavas (group A) have very similar
geochemical characteristics to the Kwaimbaita/Kroenke group lavas
from Ontong Java, whereas one sample (group B) has a composition
similar to the Singgalo group lavas (Hoernle et al., 2010). As noted
above, the Manihiki basement rocks also form two distinct geochemical
groups: 1) a low-Ti group with isotopic compositions ranging from the
Kwaimbaita/Kroenke type lavas from Ontong Java (and Hikurangi) to
HIMU or FOZO (B)-like compositions, and 2) a high-Ti group with
isotopic compositions similar to the Singgalo lavas from Ontong Java
with more EM1-type compositions than the low-Ti group lavas. The
similarity in age and geochemical composition of the Manihiki, Ontong
Java and Hikurangi Plateaus is consistent with these plateaus having
been formed by the same event and as a single mega-plateau (e.g.
Taylor, 2006; Davy et al., 2008), but does not require formation as a
single plateau.
140
C. Timm et al. / Earth and Planetary Science Letters 304 (2011) 135–146
12
FOZO A (t)
0.703
b)
15.5
Ptc (t)
Ptc (t)
a)
Pacific
MORB (t)
0.705
0.704
87Sr/86Sr
20
EMI
(t)
Hikurangi
Seamounts (t)
d)
FOZO B (t)
εHf(t)
5
r
eA
tl
an
OS (t ) Pacific
MORB (t )
Hikurangi
Seamounts (t)
ray
M
0
Ptc (t)
Osbourn
Seamounts (t)
Pacific
MORB (t)
EMI
-1
38
HIMU
t)
c(
Pt
-5
-3
EMI
1
3
5
7
9
11 17
18
19
Low-Ti group lavas (FOZO)
HT group literature data
High-Ti group lavas (EMI)
OJP-Kwaimbaita/Kroentke
High-Ti group lavas (gl)
37
21
206Pb/204Pb(t)
εNd(t)
Low-Ti group lavas (gl)
20
208Pb/204Pb(t)
39
FOZO A (t)
10
40
HIMU
FOZO B (t)
FOZO A (t)
15
15.7
15.6
Hikurangi OS (t)
Seamounts (t)
0.702
FOZO B (t)
207Pb/204Pb(t)
0
HIMU
Osbourn
Seamounts (t)
Seawater
alteration
4
2
Marine
Sediments (t)
FOZO A (t)
6
15.8
Hikurangi
Seamounts (t)
FOZO B (t)
8
εNd(t)
c)
Pacific MORB (t)
10
OJP-Singallo
Hikurangi A
Hikurangi B
LT group literature data
Fig. 5. a) Initial 87Sr/86Sr vs. initial εNd, b) initial εNd vs. initial εHf, c) initial 206Pb/204Pb vs. 207Pb/204Pb and d) 206Pb/204Pb vs. 208Pb/204Pb. To minimize the seawater alteration effect
the 87Sr/86Sr age correction of the samples DR 26–1 (wh) and DR 47–1 a Rb/Sr ratio of 0.27 was assumed. Additional Manihiki data are from Hoernle et al. (2010), Ingle et al. (2007),
Mahoney and Spencer (1991). Pacific MORB is based on data from Meyzen et al. (2007), the Pitcairn (Ptc) field is based on data from Eisele et al. (2002) and the Hikurangi and
Osbourn Seamount (OS) fields are based on data from Hoernle et al. (2010). Mantle array in Fig. 5b is as defined in Geldmacher et al. (2003). Also shown are the FOZO-type
Kwaimbaita/Kroenke (white rectangles), the EMI-type Singgalo (black rectangles) formations of the Ontong Java Plateau (from Mahoney et al., 1993; Tejada et al., 1996, 2002, 2004)
and the FOZO-type Hikurangi A (white triangles) and EMI-type Hikurangi B (black triangles) after Hoernle et al. (2010). MORB data have been corrected for radiogenic ingrowth over
125 Ma assuming 87Rb/86Sr = 0.005, 147Sm/144Nd = 0.25, 176Lu/177Hf = 0.04, μ = 10 and κ = 40. FOZO fields (FOZO A after Hauri et al., 1994 and FOZO B after Stracke et al., 2005) have
been age corrected assuming 87Rb/86Sr = 0.015, 147Sm/144Nd = 0.1, 176Lu/177Hf = 0.005, μ = 12 and κ = 80. The Pitcairn data have been age corrected assuming 87Rb/86Sr = 0.01,
147
Sm/144Nd = 0.2, 176Lu/177Hf = 0.03, μ = 8 and κ = 80.
Although there is no discernable difference in the ages of the highand low-Ti volcanic rocks on Manihiki, all basement samples drilled at
DSDP Site 317 belong to the high-Ti group. Based on the stratigraphy,
they formed at the end of the plateau stage of volcanism, which is
consistent with the Singgalo Formation lavas in Central Malaita and at
DSDP Site 807 on the Ontong Java Plateau being stratigraphically
younger than the main Kwaimbaita/Kroenke phase (Tejada et al.,
2002). It is, however, noteworthy that the lavas from the Ontong Java
and Hikurangi Plateau basements with ages younger than 116 Ma have
Kwaimbaita/Kroenke (low-Ti) type compositions, rather than Singgalo
(high-Ti) type compositions (Fig. 2). Below we will evaluate the
geochemical data from the low- and high-Ti group volcanic rocks
separately to elucidate the origin of both geochemical groups and to
assess which processes were responsible for the excess volcanism that
formed the Manihiki Plateau.
4.2. Low-Ti-group volcanic rocks — evidence for an upwelling thermal
anomaly (mantle plume)
The CaO concentration of very mafic volcanic rocks (MgO N 9 wt.% to
minimize the possible effects of fractionation of clinopyroxene and
plagioclase) can be used to determine if the melts were derived from
peridotitic and/or pyroxenitic sources (Herzberg and Asimow, 2008). The
CaO content of the most mafic low-Ti group volcanic rocks from the
Manihiki Plateau ranges from 10.3 to 12.6 wt.%, falling into the field of
peridotite partial melts defined by Herzberg and Asimow (2008)
(Fig. 6a). The sample with low MgO (6.4 wt.%) also has low CaO
(8.6 wt.%) but high Al2O3 (16.7), reflecting primarily clinopyroxene
fractionation. The low Zr/Hf (b39), Sr/Y (b7), and CaO/Al2O3 (b0.9)
further support derivation from a peridotitic source. In accordance with
melting pressures N30 kb (see below), the low FeOt contents (8.9–
9.6 wt.%) in the mafic low-Ti volcanic rocks (MgO N 9 wt.%) point to
derivation from a depleted peridotitic source similar to mantle peridotite
KLB-1 with a forsterite content in the olivine of 89.1 mol% (Hirose and
Kushiro, 1993).
The fresh glass samples can be used to evaluate the volatile contents
of the melts forming the Manihiki basement rocks. The melts for the
Manihiki glass samples (high- and low-Ti groups) had low H2O (0.18–
0.26 wt.%), similar to MORB (Michael, 1995) and the Kwaimbaita/
Kroenke lavas from the Ontong Java Plateau (Michael, 1999; Roberge
et al., 2004). This is supported by H2O/Ce of 140–430, which overlaps
with those from Ontong Java (200–400) and MORB (120–410). The low
H2O of the melts indicates a fairly dry mantle source for the Manihiki
Plateau rocks, which precludes flux melting to produce the observed
large degrees of melting and large volumes of lavas.
Since the volatile content of the melts appears to have been low, we
use the method of Herzberg and Asimow (2008) to evaluate the
temperatures and pressures of melting and the degrees of melting. The
primary composition of the three low-Ti group Manihiki tholeiite
samples (two whole rock and one glass; which only had olivine on the
liquidus) can be calculated by using the Primelts2 program. The
calculated primary-melt composition of these lavas can be generated
141
0.283014
0.282947
0.283019
0.282999
–
0.282992
0.282827
0.283095
0.282861
0.282873
a)
0.283488 (7)
0.283238 (53)
0.283132 (5)
–
0.283141 (6)
–
0.283036 (4)
0.282923 (3)
0.283214 (5)
0.282925 (5)
0.282932 (4)
CaO (wt%)
L - Ol
L - Ol
- Cpx
- Plag
Peridotite Partial Melts
+Cpx
3
10
0.47b
0.37
0.58b
1.00b
0.68
0.50
0.78
0.65
0.82
0.87b
0.83
1.03
=1
3.8
1-
0.2
74
Mg
O
5
12
% Melt fraction 0 10 20 30 40
b)
FeO (wt%)
10
50
4 Gpa
11
L+Ol
-Ol
+Ol
9
3 GPa
8
-Ol
7
6
0
Measured
Calculated
2 GPa
10
20
30
MgO (wt%)
Fig. 6. a) Diagram showing MgO vs. CaO. The dashed line marks at MgO= 9 wt.% the onset
of clinopyroxene and plagioclase fractionation. High concentrations of CaO in the mafic
basement lavas (MgON 9 wt.%) from the Manihiki Plateau are consistent with their
derivation from a peridotitic source. Light gray rectangles are data from the Ontong Java
Plateau (from the GEOROC database and Fitton and Godard, 2004; Mahoney et al., 1993;
Tejada et al., 1996, 2002). Additional data for the high-Ti rocks comes from Hoernle et al.
(2010). b) Diagram showing MgO vs. FeOt modified after Herzberg and Asimow (2008).
Primary melt compositions of three Low-Ti group lavas (two whole rock and one glass
sample) were calculated by using the Primelts2 program. The primary melt composition of
these lavas corresponds to c. 30% partial melting, which is broadly consistent with the
extent of partial melting for volcanic basement lavas from the Ontong Java Plateau (e.g.
Tejada et al., 2002). Furthermore the FeOt concentration relates to melting pressures of c.
3.2 GPa, which corresponds to the melting depth of c. 100 km.
Modified after Herzberg and Asimow, 2008.
2.97
1.48
5.25
5.34
5.26
5.25
5.47
4.83
7.38
3.92
7.52
10.5
11.2
11.4
12.3
0.512931 (6)
0.512954 (3)
0.512895 (2)
0.512897 (3)
0.512899 (4)
0.512895 (3)
0.512901 (2)
0.512907 (3)
0.512735 (2)
0.513015 (5)
0.512773 (2)
0.512749 (2)
0.512738 (2)
0.512745 (2)
0.512741 (3)
0.512809
0.512785
0.512776
0.512785
0.512782
0.512782
0.512789
0.512745
0.512564
0.512859
0.512616
0.512587
0.512590
0.512584
0.512590
0.86
0.88
0.84
0.85
0.21
0.09
0.41
0.36
0.46
0.60
0.48
0.52
0.19
0.14
0.19
0.20
0.14
0.05
0.32
0.30d
0.12
0.18
0.26
0.38
5 6 7 SOLIDUS
Pi (GPa)
-Cpx
Ca
O
0.23
20.000 (16) 19.498 15.632 (12) 15.608 39.719 (32) 39.080 0.23
0.21
20.311 (1)
19.778 15.659 (1) 15.653 39.920 (2) 39.141 –
20.223 (1)
19.725 15.677 (1) 15.653 40.111 (4) 39.103 0.25
20.310 (1)
19.892 15.679 (1) 15.659 39.921 (2) 39.305 –
20.291 (1)
20.035 15.675 (1) 15.662 39.894 (2) 39.534 18.475 (1)
18.213 15.517 (1) 15.505 38.272 (2) 38.149 0.17
18.802 (1)
17.904 15.501 (1) 15.495 38.224 (4) 38.154 0.32
19.848 (1)
19.325 15.723 (1) 15.697 39.360 (3) 39.136 0.23
18.494 (1)
17.918 15.504 (1) 15.476 38.372 (3) 38.148 18.124 (1)
17.939 15.508 (1) 15.499 38.363 (2) 38.136 0.45
18.120 (1)
17.862 15.509 (1) 15.496 38.355 (2) 38.077 18.273 (1)
17.889 15.524 (1) 15.505 38.424 (2) 38.193 18.270 (1)
17.820 15.529 (1) 15.507 38.424 (2) 38.222 0.45
0.21 0.14
0.05
4
Pyroxenite Partial Melts
d
c
b
a
Glass samples.
Pb measured by laser ablation ICPMS.
For age correction an 87Rb/86Sr of 0.27 has been assumed.
Assumed.
0.73
0.51
1.27
1.21
1.25
1.20
1.24
1.59
2.56
1.25
2.41
3.47
3.38
3.72
3.76
0.703648
0.703639
0.702559
–
0.702864
0.702769
0.702781
0.703542
0.704611
0.703747c
0.705484
0.704628
0.705657
0.704338
0.704391
0.705574 (6)
0.704100 (5)
0.703348 (5)
–
75.6
0.703331 (5)
82.7
0.703277 (2)
83.8
0.703274 (3)
7.44 0.707422 (6)
191
0.704722 (5)
67.5
0.704227 (5)
194
0.705585 (6)
125
0.704723 (6)
185
0.705885 (3)
130
0.704650 (6)
143
0.704526 (5)
125
8.33
125
3.15
125 11.3
125
125
6.87
125
8.18
125
8.05
125
5.61
125
4.16
125 28.1
125
3.82
125
2.30
125
8.19
125
7.88
125
3.76
SO193DR18-1
SO193DR18-4B
SO193DR26-1
SO193DR26-1a
SO193DR26-2
SO193DR26-3a
SO193DR26-10a
SO193DR38-2
SO193DR46-1
SO193DR47-2
SO193DR49-1
SO193DR52-1A
SO193DR52-2a
SO193DR52-3A
SO193DR52-3B
22.2
32.8
73.8
176
143
15
0.17
0.27
0.65
–
0.60
–
1.32
1.14
0.67
2.42
2.63
177
204
204
204
204
204
204
144
Age Rb
Sample
Table 2
Sr–Nd–Hf–Pb isotope ratios.
Sr
87
Sr/86Srm
87
Sr/86Sri
Sm
Nd
143
Nd/
Ndm
144
Nd/
Ndi
U
Th
Pb
206
Pb/
Pbm
206
Pb/
Pbi
207
Pb/
Pbm
207
Pb/
Pbi
208
Pb/
Pbm
208
Pb/
Pbi
Lu
Hf
176
Hf/
Hfm
177
Hf/
Hfi
C. Timm et al. / Earth and Planetary Science Letters 304 (2011) 135–146
by c. 30% partial melting of a (garnet–) peridotite at a pressure of
c. 3.2 GPa, corresponding to a depth of partial melting of c. 105 km
(Fig. 6b). Mantle potential temperatures of 1503 °C (SO193DR18-4B),
1509 °C (SO193DR26-10) and 1516 °C (SO193DR26-13) were calculated for the three samples. These temperatures are about 160 °C above the
average ambient mantle potential temperature of 1350 °C, slightly
above the average for ocean island basalts (~1480 °C), and similar to
average temperatures for LIPs, but about 40 °C less than those calculated
for Ontong Java melts (Herzberg and Gazel, 2009). The lower calculated
melting temperatures for the Manihiki basement rocks, combined with
lower crustal thickness for the plateau, are consistent with the lower
overall magma production during the formation of the Manihiki
compared to the Ontong Java Plateau or portions of a mega-plateau.
In addition to the low total FeO, the moderately to mildly
incompatible element abundances and ratios also indicate derivation
of the low-Ti group lavas from a depleted source. The low TiO2, Na2O,
P2O5 and moderately incompatible trace element contents (e.g. MREE,
Zr, and Hf) and the low moderately to less incompatible element
ratios (e.g. (Nd, Sm, Tb)/Yb, Zr/Y) of the low-Ti group support a
combination of greater dilution through higher degrees of partial
melting and/or derivation from a more depleted source compared to
the high-Ti lavas and N-MORB (Fig. 4a–b). Despite the evidence for
source depletion, the enrichment of the most incompatible elements
(e.g. Th, Nb and La), compared to less incompatible elements (e.g. Zr,
Hf and the M- and HREE), can be explained by enrichment through
small degree melts. Ratios of highly to moderately incompatible
elements correlate well with Pb isotope ratios in the low-Ti volcanic
rocks: for example, 206Pb/204Pb isotope ratios correlate positively with
Th/Zr (r2 = 0.80), Th/Hf (r2 = 0.77), Th/Sm (r 2 = 0.78), Nb/Zr
142
C. Timm et al. / Earth and Planetary Science Letters 304 (2011) 135–146
(r2 = 0.82), Nb/Hf (r2 = 0.82), Nb/Sm (r2 = 0.84), La/Zr (r2 = 0.89),
La/Hf (r2 = 0.82) and La/Sm (r2 = 0.82) (not shown). The good
correlation with these highly immobile incompatible element ratios
suggests that the Pb isotope composition of the low-Ti samples, which
include four fresh glass samples, cannot be explained by posteruption alteration. In conclusion, the aforementioned correlations
indicate that the component causing the source enrichment is not
only highly enriched in the most incompatible elements but also has
radiogenic Pb isotope ratios and therefore could be a HIMU (high
time-integrated μ (U/Pb))-type component.
As pointed out by Ingle et al. (2007), the unusual incompatible
element characteristics (depletion of moderately relative to mildly
incompatible elements and enrichment of highly relative to moderately
incompatible elements) of the low-Ti group lavas from the Danger Island
and Suvorov troughs (our data) require a multistage source history. Ingle
and colleagues attributed the incompatible element characteristics to
initial depletion of a mantle wedge of a subduction zone through melt
extraction and subsequent introduction of melts from subducted
volcaniclastic sediments, which implies that the Manihiki low-Ti volcanic
rocks were derived from a distinct source compared to the Ontong Java
Kwaimbaita/Kroenke (and Hikurangi A) type rocks. We will discuss an
alternative model that can also relate the Manihiki to Ontong Java and
Hikurangi sources. On Sr–Nd–Pb–Hf isotope correlation diagrams, the
low-Ti group volcanic rocks largely overlap the FOZO-type mantle source
fields of Hauri et al. (1994) (FOZO A) and Stracke et al. (2005) (FOZO B),
projected back to 125 Ma (Fig. 5a–d), suggesting that FOZO-type lower
mantle may be involved in the generation of the low-Ti group lavas. We
note, however, that the incompatible element characteristics of the lowTi basalts (very low moderately incompatible element abundances and
extreme depletion of the moderately compared to mildly and highly
incompatible elements) are distinct from any oceanic basalts for which
data has been published thus far (Ingle et al., 2007), including OIBs with
isotopic compositions falling within the range of the FOZO A and FOZO B
components. Therefore we feel that a FOZO B type source for the Manihiki
rocks is unlikely.
The only rocks to date that have been found related to the Greater
Ontong Java Event that have similarly depleted incompatible element
contents and characteristics to the mildly and moderately incompatible
elements of the low-Ti group lavas from Manihiki are samples from the
Osbourn Seamounts (Tuatara and Moa Seamounts) adjacent to the
northwest margin of the Hikurangi Plateau, which are also highly
depleted in the highly incompatible elements (Fig. 3a). These rocks have
the appropriate isotopic compositions and depleted incompatible
element abundances to serve as the depleted endmember for the
basement array formed by the Ontong Java and Hikurangi Plateaus and
the previously published Manihiki basement data (Hoernle et al., 2010).
Despite the extremely depleted incompatible element compositions of
the Osbourn Seamount samples, the isotopic compositions are similar to
E-MORB or the FOZO A component of Hauri et al. (1994) with more
radiogenic Nd, Hf and Pb but less radiogenic Sr isotopic compositions
than the Kwaimbaita/Kroenke and Hikurangi A lavas. The less
radiogenic Sr and more radiogenic Pb isotopic composition of the lowTi group rocks, which include fresh glass samples and therefore the
unradiogenic Sr similar to the radiogenic Pb cannot simply be explained
by post-eruption alteration, and could reflect minor addition of a HIMUtype component, similar in composition to late-stage volcanism on the
Hikurangi, Ontong Java and Manihiki Plateaus (Hoernle et al., 2008,
2009, 2010; Ingle et al., 2007; Tejada et al., 1996). This HIMU-type
component could be present in the source as pyroxenite/eclogite,
possibly ultimately derived from recycled oceanic crust. Addition of
small degree melts from ancient recycled oceanic crust to a source
similar to the Osbourn Seamounts could explain the isotopic and trace
element compositions of the low-Ti melts. One possible scenario is that
recycled ocean crust (in the form of eclogite/pyroxenite) is contained in
a depleted peridotitic matrix with a composition similar to the Osbourn
Seamount source. Upon upwelling of such a source, the eclogite
(especially if carbonated) would form melts that metasomatize the
surrounding depleted peridotitic mantle (e.g. Dasgupta et al., 2007;
Timm et al., 2009). Melting of such a source upon further upwelling
could generate the low-Ti melts.
4.3. High-Ti-group lavas — contribution of subcontinental lithospheric
mantle
Now we will discuss the origin of the high-Ti group lavas and their
role in the generation of the Manihiki Plateau. Whereas all but one of
the low-Ti samples had MgO N 9.3 wt.%, all of the high-Ti samples have
MgO b 9.1 wt.%. Fractionation of clinopyroxene and plagioclase is
likely to have lowered the CaO and Al2O3 contents of the high-Ti
Manihiki samples (Fig. 6a). Therefore, their parental melts are likely to
have had higher CaO contents and thus also to have been derived from
a peridotitic source. Alternatively the low MgO and CaO could reflect
derivation from a pyroxenitic source. The low CaO/Al2O3 (b0.9), Sr/Y
(b9.5) and Zr/Hf (b39.5) ratios of all Manihiki basement samples,
however, also favor derivation from a peridotitic rather than
pyroxenitic/eclogitic source. Therefore both the low- and high-Ti
group rocks appear to be derived from melting of peridotitic sources.
The differences in trace element and isotopic compositions between
the groups, however, require that at least two distinct peridotitic
source components were involved in the formation of the plateau
basement.
The high-Ti group has minor and trace element characteristics
similar to DSDP Site 317 samples (e.g. Hoernle et al., 2010; Ingle et al.,
2007; Mahoney and Spencer, 1991). The generally flat immobile,
primitive-mantle-normalized incompatible element distribution on
multi-element diagrams of the high-Ti group volcanic rocks suggests a
common mantle source for the widely-distributed dredge samples
that is very similar to the source for the Ontong Java, Singgalo and the
Hikurangi B basement lavas (Fig. 5).
Following Hirose and Kushiro (1993) and Walter (1998), the TiO2
concentration in mafic volcanic rocks mainly depends on the degree of
partial melting and/or pressure conditions, behaving like a moderately
incompatible element. Thus the high TiO2, combined with high Na2O,
P2O5 and moderately incompatible trace element contents (e.g. MREE, Zr,
and Hf) and the low moderately to less incompatible element ratios (e.g.
(Nd, Sm, Tb)/Yb, Zr/Y), of the high-Ti group lavas could represent lower
degrees of partial melting at greater depths and/or derivation from a
more enriched source. Generally higher FeOt and lower SiO2 at a given
MgO are also consistent with greater depths of melting (Hirose and
Kushiro, 1993) in the formation of the high-Ti group lavas. Low ratios of
(Th, U, Ba, Rb, Pb, and K)/Zr in the glass sample argue against the addition
of a marine sedimentary or fluid-bearing component into the high-Ti
group rocks, which is consistent with the low H2O content and H2O/Ce
ratio of 140 in the high-Ti glass sample (DR52-2; H2O= 0.19 wt.%). Lack
of evidence for a significant role of fluids in the generation of the high-, as
well as low-, Ti group lavas excludes flux-melting from being a major
melting mechanism for all Manihiki basement lavas. The general origin of
the EMI-type source component, however, is controversial (see Lustrino
and Dallai, 2003 and Geldmacher et al., 2008 for summaries). In the SW
Pacific, the Pitcairn archipelago exemplifies one EMI-type locality, where
the EMI-type component has been attributed to incorporation of
continentally- derived material containing various proportions of pelagic
sediments (e.g. Eisele et al., 2002). The absence of typical depletions in Th,
Nb, and Ta in the Manihiki basement lavas argues against the
involvement of significant amounts of continental crust (Fig. 3), which
is also consistent with the eruption of the Manihiki Plateau through
oceanic crust within the Pacific Ocean (which was larger in Cretaceous
time; e.g. Mueller et al., 2008) far away from active subduction zones and
continents. There is a striking similarity in radiogenic isotopic composition between the high-Ti group Manihiki basement lavas and lavas from
Hawaiian volcanoes Mauna Loa and Koolau, which gives valuable
insights into the origin of enriched mantle (Fig. 7).
C. Timm et al. / Earth and Planetary Science Letters 304 (2011) 135–146
12
Pacific
MORB (t)
10
εNd(t)
8
6
4
FOZO B (t)
Osbourn
Seamounts (t)
Kilauea
Loihi
Mauna Loa
Koolau
FOZO A (t)
Hikurangi
Seamounts (t)
2
0
17.0
Ptc (t)
18.0
19.0
20.0
206Pb/204Pb(t)
Fig. 7. 206Pb/204Pb (t) vs. εNd (t). The low-Ti group lavas from Manihiki overlap the
Kwaimbaita/Kreonke group rocks from Ontong Java but extend to more radiogenic Pb
isotopic compositions, suggesting involvement of an additional component, not yet
observed in the plateau basement lavas from the Ontong Java and Hikurangi Plateaus.
Hawaiian lavas (data from the GEOROC database) have been age corrected for radiogenic
ingrowths assuming 147Sm/144Nd= 0.202 and μ = 12. Since the Hawaiian lavas are the
classical example for lower mantle source plume-related melts, the similarity of Hawaiian
lavas and those from the Manihiki/Ontong Java/Hikurangi Plateau suggests a lower mantle
source for the lavas of the “Greater Ontong Java Event”.
The sub-continental lithospheric mantle (SCLM) composed of residual
lherzolite and harzburgite may be the best source for the EMI-type
component. Throughout the complex geological history of the SCLM,
several geological processes may have produced trace element enrichment and depletion (see Geldmacher et al., 2008 for a summary).
Although spinel peridotite xenoliths from continental lithosphere
commonly show strongly fractionated incompatible-element patterns
(e.g. McDonough, 1990), multiple melting episodes and refertilization of
Achaean SCLM (e.g. Griffin et al., 2009) may ultimately have smoothed the
trace element distribution. Drilled DSDP Site 527 lavas from the EMI-type
Walvis Ridge in the southern Atlantic for which SCLM has been proposed
as the possible origin (e.g. Gibson et al., 2005; Salters and Sachi-Kocher,
2010) show similar trace element patterns to the high-Ti Manihiki lavas.
Even if the trace element composition is more enriched, large degrees of
partial melting during plateau formation may produce relatively flat trace
element patterns. Finally it has been demonstrated that depleted
subcontinental lithosphere also plays an important role in the EMI-type
Koolau lavas (Salters et al., 2006). Delamination could transfer EMI-type
SCLM to a zone of neutral buoyancy, such as the 660 km upper–lower
mantle or the core–mantle boundary (Elkins-Tanton, 2007; O'Reilly et al.,
2009; Timm et al., 2010).
4.4. Geodynamic model of the Manihiki Plateau
New age data from four additional widely distributed locations on
the Manihiki Plateau provide further support that the Manihiki Plateau
was formed during the “Greater Ontong Java Event”, which includes the
Ontong Java, Manihiki and Hikurangi Plateaus and possibly the related
volcanism in the East Marianas, Lyra and Nauru Basins around Ontong
Java (Fitton and Godard, 2004). This event was the most extreme
volcanic episode on Earth during the Phanerozoic (covering c. 1% of the
Earth's surface), requiring an extreme melting event. Increased partial
melting through plume–ridge interaction as proposed for the formation
of the Ontong Java Plateau (Mahoney, 1987; Mahoney et al., 1993)
cannot sufficiently explain the eruption of such large volumes of lavas
across the entire plateau with similar ages (124.6 Ma). Furthermore, the
relatively high CaO at a given MgO and the low Sr/Y and Zr/Hf are MgO
inconsistent with plateau formation through partial melting of an
upwelling primarily eclogitic source as proposed by Korenaga (2005).
High partial melting temperatures and the presumed proximity to
spreading centers argue against the plate separation model. No evidence
for a meteorite impact (e.g. the presence of shocked quartz, iridium
143
anomaly or associated tsunami deposits) has been found at c. 125 Ma.
The low H2O content in the Manihiki submarine glasses (184–
258 ppm), similar to water content from the Ontong Java Plateau
lavas and MORB (170 ± 30 and 140 ± 40 ppm H2O, respectively;
Roberge et al., 2004) excludes flux melting as the major mechanism
for generating the high degrees of melting and large volumes of
magmatism. Together with evidence for significant uplift in the early
phase of volcanic activity at Manihiki (i.e. evidence for shallow water or
subaerial formation), the high temperatures and low volatile contents
support the presence of a thermal and probably also compositional
anomaly, thus favoring the plume hypothesis.
Two major components have been previously identified in volcanism
associated with the Greater Ontong Java Event: 1) the regionally
dominant Kwaimbaita/Kroenke component (with Kroenke-type melts
being parental to the Kwaimbaita lavas) with flat incompatible element
patterns and isotopic compositions similar to the FOZO of Hauri et al.
(1994), and 2) the stratigraphically younger Singgalo component with
more enriched incompatible element abundances and EMI-type isotopic
signatures. The Manihiki low-Ti volcanic rocks have similar Nd and Hf
isotopic compositions, but they have distinct incompatible element
abundances and more radiogenic Pb but less radiogenic Sr isotope ratios
than the Kwaimbaita/Kroenke and Hikurangi A lavas. As discussed above,
a multistage history involving at least two distinct source components is
required: 1) one with more depleted incompatible element abundances
than the Kwaimbaita/Kroenke lavas (possibly similar to those of the
Osbourn seamounts located just off the conjugate rifted margins of the
Hikurangi and Manihiki Plateaus), and 2) one with enriched highly
incompatible elements and radiogenic Pb and less radiogenic Sr, similar
to the late-stage HIMU-type alkalic volcanism on the plateaus. In
summary, at least three distinct components are required to explain
the geochemistry of the Manihiki basement lavas: 1) Osbourn seamount,
possibly FOZO-type, 2) HIMU-type and 3) EM1-type components.
The Kwaimbaita/Kroenke component at Ontong Java can either be
a mixture of the Osbourn and Singgalo (or more extreme EMI-type
component such as sampled at Pitcairn) components. Alternatively
the compositions of the Osbourn and Kwaimbaita/Kroenke lavas
could reflect heterogeneity in the FOZO-type source. It has been
proposed that the FOZO component represents a common and
ubiquitous component present in the lower mantle (Hart et al.,
1992; Hauri et al., 1994; Stracke et al., 2005; Zindler and Hart, 1986),
although the proposed compositions for FOZO show considerable
variation (see Stracke et al., 2005, for a summary). It is, however, to be
expected that this component, if it indeed represents the composition
of the lower mantle, will also vary regionally as is the case with MORB,
which shows that the upper mantle is regionally heterogeneous.
Excluding the Manhiki low-Ti lavas, the remaining plateau basement
lavas (Kwaimbaita/Kroenke, Hikurangi A, Singgalo, Hikurangi B and the
Manihiki high-Ti groups) and Osbourn Seamounts form a very similar
isotopic array to the lavas from the Hawaiian volcanoes of Kilauea, Loihi
and Mauna Loa with the Osbourn samples overlapping the field for
Kilauea (e.g. Fig. 7). High 3He/4He ratios in lavas from Kilauea, Loihi, and
Mauna Loa (e.g. Farley and Neroda, 1998), together with the presence of
low velocity zones beneath the Hawaiian volcanoes (e.g. Montelli et al.,
2004, 2006; Nolet et al., 2006), strongly argue for a lower mantle origin
of the Hawaiian plume. The similarity of the isotopic composition of the
Hawaiian volcanoes and the Manihiki basement lavas provides further
support that the Manihiki, Ontong Java and Hikurangi Plateaus were
derived from similar, but heterogeneous source in the lower mantle (e.g
Hoernle et al., 2010; Tejada et al., 2002).
During Late Jurassic and Early Cretaceous times, the Panthalassa
(proto-Pacific) Ocean was more extensive than today (e.g. Mueller et al.,
2008). The emplacement of the Manihiki Plateau nearly in the center of
the Pacific Ocean argues against the direct involvement of continental
crust and/or sediments. Thermal erosion and delamination of the SCLM
during the breakup of Gondwana and subsequent recycling into the
upper mantle and subsequent storage at a thermal boundary layer (such
144
C. Timm et al. / Earth and Planetary Science Letters 304 (2011) 135–146
as the 660 km boundary) have been proposed for the origin of the EMItype signature in the southern Atlantic and Indian Oceans (Geldmacher
et al., 2008; Hawkesworth et al., 1986; O'Reilly et al., 2009). Gondwana
SCLM could also have been delaminated during subduction around the
proto Pacific Ocean. If delamination of SCLM has been an ongoing process
since ancient times (O'Reilly et al., 2009), the SCLM could have developed
into a widespread enriched mantle reservoir along the transition zone or
enriched pockets could be distributed throughout the Earth's mantle
down to the D″ layer at the core–mantle boundary. A plume, initiated at
the core mantle boundary, could entrain significant amounts of such
enriched material while rising through the mantle, as well as HIMU-type
recycled oceanic crust in the form of eclogite/pryoxenite.
It, however, cannot be excluded that all three of the components
(FOZO-type, EM1-type and HIMU-type) in the basement lavas were
derived from the plume source, e.g. the D″ boundary layer. Delaminated
subcontinental lithospheric mantle could contain all three of these
components. Depleted harzburgitic portions of the subcontinental
lithosphere can have highly depleted incompatible element and overall
depleted isotopic compositions resulting from depletion related to crust
formation and later magmatism. Various metasomatic processes can
cause enrichment of the subcontinental lithosphere, leading to an EM1type composition for example through carbonatite metasomatism and a
HIMU-type composition through metasomatism with very low-degree
silica-undersaturated melts (e.g. see Geldmacher et al., 2008).
Based on experimental results, pyroxenite/eclogite and enriched
mantle peridotite will begin melting at deeper depth compared to
depleted upper mantle (e.g. Dasgupta et al., 2006, 2007; Hirschmann,
2000; Hirschmann and Stolper, 1996). Therefore the first melts would
be derived from more fertile parts of the plume, for example pyroxenite/
eclogite with a HIMU-type composition and the enriched peridotite
with an (EMI)-type composition. Entrained parts of the plume, which
would then become progressively more diluted with increasing degree
of partial through decompression as the plume ascended.
Recent studies of seismic tomography in the south Pacific show a
large low-velocity zone located beneath the transition zone extending
down to the lower mantle (Li et al., 2008; Suetsugu et al., 2009;
Tanaka et al., 2009). Small plumes rising from a stalled super-plume
are believed to be responsible for the formation of the ocean islands of
French Polynesia (Suetsugu et al., 2009). Assuming its existence since
mid-Cretaceous time, this super-plume could explain the formation of
not only the Manihiki Plateau but also the Greater Ontong Java Event
(Hoernle et al., 2010; Larson, 1991a,b) (Fig. 8). Larson (1991a,b)
attributed the intense magmatism/volcanism in the Pacific Basin
during mid-Cretaceous time to an even larger superplume (c. 6000 to
10,000 km in diameter), which he proposed formed at c. 125 Ma at
the core–mantle boundary. Significant uplift should have accompanied the arrival of such a large-scale upwelling event, which could
account for the shallow water to subaerial formation of parts of the
Manihiki Plateau. A super-plume, stalled at the transition zone (as
shown by Li et al., 2008; Suetsugu et al., 2009; Tanaka et al., 2009) and
feeding a widespread swarm of secondary plumes, would also result
in less significant uplift than impingement of the super-plume at the
base of the lithosphere. Such a model could also explain why the
temperatures calculated for Ontong Java and Manihiki lavas, despite
the magnitude of this event, are lower than strong plumes such as
Hawaii. In conclusion, we favor the formation of the Manihiki Plateau
and possibly the Greater Ontong Java Event through numerous
secondary plumes coming off a newly arrived heterogeneous superplume head stalled at the transition zone with at least three distinct
compositional endmembers.
Fig. 8. Schematic model for the origin of the Manihiki Plateau and possibly also for the
Ontong Java and Hikurangi Plateaus. A deep derived (FOZO-type) superplume, most
likely from a thermal boundary layer such as the core–mantle boundary (CMB), ascends
until the transition zone at c. 660 km, either already containing or entraining domains
of EMI-type SCLM and eclogite/pyroxenite with HIMU-type compositions (recycled
ocean crust (ROC)) during its ascent. The EMI-and HIMU-type components are sampled
at lower degrees of melting and the FOZO type at higher degrees of melting.
plateau formation continuing until c. 117 Ma. Therefore its formation
was contemporaneous with the Ontong Java and Hikurangi Plateaus.
2) The geochemical data suggest the presence of two groups of
basement lavas with different minor and trace element and
isotopic compositions: a) High-Ti group, compositionally similar
to the Singgalo lavas on the Ontong Java Plateau, with an EMI-type
isotopic composition, and b) Low-Ti group of lavas ranging in
composition from the Kwaimbaita/Kroenke lavas at Ontong Java to
more HIMU-like compositions. Following the methods of Herzberg
and Asimow (2008), we propose that both groups formed through
partial melting of peridotite. Calculated primary partial melts for
the low-Ti group lavas were formed through c. 30% partial melting
at mantle potential temperatures of c. 1510 °C, falling into the
average mantle potential temperature for the formation of LIPs
(Herzberg and Gazel, 2009). The incompatible element and
isotopic composition of the low-Ti group lavas can best be
explained by the enrichment of a highly depleted source (similar
in composition to the Osbourn Seamounts located adjacent to the
rifted northeast margin of the Hikurangi Plateau) with small
degree melts from a HIMU-type source, similar to the source of
late-stage alkalic volcanism on each of the plateaus. This is the first
time that involvement of a HIMU-type component has been
identified in the Greater Ontong Java volcanism.
3) Based on shallow emplacement (e.g. Ai et al., 2008) and evidence for
unusually high degree of melting, and strongly elevated melting
temperatures, the plume head theory can best explain the origin of
the Manihiki Plateau. The plume head may have stalled at the
transition zone, consistent with the present occurrence of the
superplume beneath the SW Pacific.
Supplementary materials related to this article can be found online
at doi:10.1016/j.epsl.2011.01.025.
Acknowledgements
5. Conclusions
1) The Manihiki Plateau formed in Early Cretaceous time primarily at
124.6 ± 1.6 Ma but with volcanism associated with the late stages of
We thank Dagmar Rau, Jan Fietzke and Silke Hauff for their
technical assistance with major element and isotopic analyses. We are
grateful to SO193 Captain Mallon, his crew, and the shipboard
scientists for their expert support. A. Ehmer and J. Leppin helped with
C. Timm et al. / Earth and Planetary Science Letters 304 (2011) 135–146
processing of the SIMRAD data. Constructive reviews from two
anonymous reviewers helped to improve the manuscript. Richard
Carlson is thanked for editorial handling and additional comments.
The German Ministry of Education and Research (BMBF; Grant SO193
Manihiki) and German Research Foundation (DFG; Grant HO1833/191 to cover costs for a substitute to cover KH's teaching load during
preparation of the manuscript) are thanked for providing funds to
carry out and publish this study. Fig. 1 was prepared with GMT public
domain software (Wessel and Smith, 1995).
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