JOURNAL OF PETROLOGY
VOLUME 50
NUMBER 8
PAGES 1553^1573
2009
doi:10.1093/petrology/egp041
Geochemical Differences of the Hawaiian Shield
Lavas: Implications for Melting Process in the
Heterogeneous Hawaiian Plume
ZHONG-YUAN REN1*, TAKESHI HANYU2, TAKASHI MIYAZAKI2,
QING CHANG2, HIROSHI KAWABATA2, TOSHIRO TAKAHASHI2,
YUKA HIRAHARA2, ALEXANDER R. L. NICHOLS2 AND
YOSHIYUKI TATSUMI2
1
KEY LABORATORY OF ISOTOPE GEOCHRONOLOGY AND GEOCHEMISTRY, GUANGZHOU INSTITUTE OF
GEOCHEMISTRY (GIG), CHINESE ACADEMY OF SCIENCES (CAS), 511 KEHUA STREET, WUSHAN, GUANGZHOU
510640, CHINA
2
INSTITUTE FOR RESEARCH ON EARTH EVOLUTION (IFREE), JAPAN AGENCY FOR MARINE^EARTH SCIENCE
AND TECHNOLOGY (JAMSTEC), 2^5 NATSUSHIMA-CHO, YOKOSUKA, KANAGAWA 237-0061, JAPAN
RECEIVED JULY 3, 2008; ACCEPTED JUNE 6, 2009
ADVANCE ACCESS PUBLICATION JULY 7, 2009
Numerous geochemical studies have indicated that the Hawaiian
mantle plume consists of several distinct components. However, their
origin remains controversial, with a number of different interpretations having been proposed. We present new major element, trace
element and high-precision Sr^Nd^Pb^He isotope data for a suite
of fresh submarine lavas erupted by the Koolau, Kilauea and Loihi
volcanoes, which are widely believed to have sampled three distinct
Hawaiian plume components. The Sr and Nd isotope compositions
of the Loihi lavas are similar to those of Kilauea lavas. However,
our double-spike Pb isotopic data show that Loihi lavas have both
Kilauea-like and Loihi-like compositions. This discovery implies
that the Loihi source region contains a Kilauea-like (‘Kea’) mantle
component. Our new data support the existence of three major types
of intrinsic plume component: a Loihi component, an ‘enriched’
(Koolau) component and a ‘depleted’ (Kea) component. We propose
that the Loihi component is a common component, forming the
matrix in the Hawaiian mantle plume, and that the isotopic differences between the various shield lavas reflect different mixing proportions of the Loihi component and recycled oceanic crust
components (EM-1-like and HIMU-like). The Koolau component
contains a higher proportion of EM-1, whereas the Kea component
contains a higher proportion of HIMU. EM-1- and HIMU-like
recycled oceanic crust components are distributed on a fine scale
Ocean island basalts (OIBs) provide important information about the composition and evolution of the mantle.
Since White (1985) and Zindler & Hart (1986) identified
several distinct mantle components (isotopic endmembers) based on studies of OIB, many models have
been proposed to explain their nature and origin (Hart,
1988; Weaver, 1991; Chauvel et al., 1992; Hauri & Hart,
1993; Hofmann, 1997; Lassiter & Hauri, 1998; Blichert-Toft
et al., 1999; Tatsumi, 2000; Eisele et al., 2002; Stracke et al.,
2003, 2005; Salters & Stracke, 2004), including mantle
*Corresponding author. Telephone: 86-20-85292969.
Fax: 86-20-85291510. E-mail: [email protected]
ß The Author 2009. Published by Oxford University Press. All
rights reserved. For Permissions, please e-mail: journals.permissions@
oxfordjournals.org
throughout the peridotitic matrix within the Hawaiian plume.
Both components are present in the sources beneath Kea- and
Loa-trend volcanoes. We infer that the thermal structure and spatially distributed compositional heterogeneity of the plume are important in controlling the isotopic composition of lavas from a given
Hawaiian volcano.
KEY WORDS:
Hawaii; mantle plume; source components; melting
process
I N T RO D U C T I O N
JOURNAL OF PETROLOGY
VOLUME 50
differentiation, subduction zone related recycling of oceanic lithosphere and melt extraction at mid-ocean ridges.
In many studies, researchers have often assumed that
there are a limited number of end-member components in
the mantle (e.g. HIMU, EM-1, EM-2, DMM) and that
mixing of these components can produce most of the isotopic variability in OIBs (e.g. Zindler & Hart, 1986).
However, it is reasonable to infer that throughout geological time subduction has continuously introduced rocks
with different compositions into the mantle. Therefore,
each OIB source may have its own unique composition, or
components, which have evolved individually from other
OIB sources (e.g. Stracke et al., 2003).
The Hawaiian^Emperor volcanic island and seamount
chain represents one of the best examples of mantle plume
volcanism. It is located on the Pacific plate and samples
material from the deep mantle (Wilson, 1963; Morgan,
1971; Frey et al., 1994). Hawaiian volcanoes evolve through
four major eruptive stages (e.g. Clague & Dalrymple,
1987): pre-shield, shield, post-shield, and rejuvenation.
Each stage produces rocks of distinct chemical and isotopic
composition. The shield phase produces about 95% of the
total volume of volcanic rocks, and, as a result, it is likely
to provide the most direct information about the bulk composition of the mantle plume (Clague & Dalrymple, 1987).
Numerous geochemical studies have shown that the
Hawaiian mantle plume is chemically and isotopically heterogeneous and there has been much debate about whether
it consists of two (Bennett et al., 1996; Lassiter & Hauri,
1998; Blichert-Toft et al., 1999), three (Staudigel et al., 1984;
Eiler et al., 1996, 2003; Hauri, 1996) or four (Abouchami
et al., 2000; Mukhopadhyay et al., 2003) distinct components, and how these components originated.
Most of the data reported for Hawaiian volcanoes
have been obtained for subaerial samples, which represent only the final eruptive stage. Additionally, the subaerial rocks are frequently affected by low-temperature
alteration (Chen et al., 1991; Frey et al., 1994; Ren et al.,
2004). To gain a deeper insight into the compositional variability of the Hawaiian magmas and the structure and
dynamics of the underlying mantle plume, the Hawaii
Scientific Drilling Project was undertaken (e.g. Hauri
et al., 1996; Kurz et al., 1996; Lassiter et al., 1996; BlichertToft & Albare'de, 1999; DePaolo et al., 2001; Blichert-Toft
et al., 2003; Eisele et al., 2003; Kurz et al., 2004; Rhodes
& Vollinger, 2004; Bryce et al., 2005; Huang & Frey,
2005), which has provided important information on
mantle plume structure and melting processes. In addition, lavas from the submarine parts of the Hawaiian
volcanoes are commonly fresh and have provided important information on the composition of the Hawaiian
volcanoes (see Garcia et al., 1989; Clague et al., 1995;
Takahashi et al., 2002; Ren et al., 2004, 2005, 2006; Hanyu
et al., 2005, 2007).
NUMBER 8
AUGUST 2009
In this study, we present major element, trace element,
and high-precision Sr^Nd^Pb^He isotopic data for a suite
of fresh lavas from the submarine Koolau, Kilauea and
Loihi volcanoes. These volcanoes are widely considered to
have sampled three distinct Hawaiian plume components
(e.g. Eiler et al., 1996; Hauri, 1996). We discuss the number
of distinct mantle components and their possible origins
necessary to explain the isotopic variability of Hawaiian
shield lavas and propose a model of a heterogeneous
Hawaiian plume in which the heterogeneities are uniformly distributed.
S A M P L E S A N D A N A LY T I C A L
TECH NIQUES
Samples
Seven lava samples from the Loihi seamount, five from the
submarine Puna Ridge of Kilauea volcano, two from the
submarine S507 site (possibly part of Mauna Loa),
and six from the Makapuu stage lavas of Koolau volcano
(two from subaerial flows, four from submarine flows;
Tanaka et al., 2002) have been analyzed. Detailed sample
localities are shown in Figs 1 and 2, and rock types are
given in Table 1. These samples were collected during
Japan^USA Hawaiian cruises, between 1998 and 2003,
using the Japan Agency for Marine^Earth Science and
Technology (JAMSTEC) vessel, R.V. Yokosuka equipped
with Shinkai 6500, a manned submersible (Takahashi
et al., 2002, and papers therein).
The sampled lavas vary considerably in mineralogy
ranging from weakly phyric (52 vol. % phenocrysts) to
highly olivine phyric (up to 40 vol. %). Olivine is the dominant phenocryst type in most samples, with some samples
also containing clinopyroxene plagioclase. Phenocrysts
other than olivine make up 51 vol. %. The olivine crystals
are generally euhedral and undeformed, containing inclusions of chromite and glass, although some are resorbed
and kink banded. Chromite also occurs as small crystals
(05 mm) in the groundmass. Clinopyroxene crystals are
usually euhedral and commonly sector zoned. They form
as glomeroporphyritic aggregates with plagioclase in some
of the lavas. Plagioclase generally forms small (05 mm),
subhedral to euhedral crystals, although rare rounded or
embayed plagioclase crystals are present in some lavas.
Analytical techniques
All sample preparation and analyses were performed at
the Institute for Research on Earth Evolution (IFREE),
JAMSTEC. Rock powders were prepared following the
procedure of Ren et al. (2006). For Sr, Nd, and Pb isotope
analyses, to eliminate secondary minerals and alteration
products, the dried powders were leached in distilled 15N
HCl at 1008C for 4 h prior to acid dissolution and analysis
(e.g. Ren et al., 2006).
1554
REN et al.
HAWAIIAN SHIELD LAVA GEOCHEMISTRY
Hawaiian Islands
Submarine Makapuu
Kea trend
Koolau volcano
OAHU
MOLOKAI
MAUI
Haleakala volcano
LANAI
Submarine Hana Ridge
KAHOOLAWE
KO
Loa trend
0
MK
MH
Kilauea volcano
H
HAWAII
100Km
ML
Submarine
Puna Ridge
S507
LOIHI
Fig. 1. Map of the Hawaiian islands, showing the location of the main volcanoes and the Kea and Loa volcano trends. ML, Mauna Loa; MK,
Mauna Kea; H, Hualalai; KO, Kohala; MH, Mahukona. Sample locations from the submarine Makapuu stage of Koolau volcano, Loihi seamount (on the Loa trend), and submarine Kilauea volcano (on the Kea trend) are labeled with stars.
Major elements, and Zr and Nb were measured using
X-ray fluorescence (XRF) spectrometry. Major elements
were measured at the Key Laboratory of Isotope
Geochronology and Geochemistry, Guangzhou institute
of Geochemistry following the procedure of Ren et al.
(2004) and Zr, Nb were measured at IFREE, JAMSTEC
following the procedure of Tatsumi et al. (2006). Rare
earth element abundances and some other trace elements
(Sc, Rb, Sr, Y, Cs, Ba, Pb, Th, and U) were determined
by inductively coupled plasma mass spectrometry (ICPMS) using an Agilent 7500s system following the procedures described by Chang et al. (2003). Analytical accuracy
and precision for ICP-MS analyses, estimated from
repeated measurements of international standards, were
better than 10% and 2^5%, respectively.
Prior to isotope analysis, Sr and Nd were isolated by
cation-exchange chromatography, using HCl and a-HIBA
(a-hydroxy iso-butyricacid). Sr was purified using a
micro-column filled with 50 ml of Sr resin (Eichrom
Technologies, IL, USA). Pb was isolated by anionexchange chromatography after dissolution in HF^HBr.
All chemical procedures were carried out in a Class 100
clean room. Sr, Nd, and Pb isotope measurements were
performed using static multi-collection mass spectrometry,
employing a Finnigan TRITON TI (Thermo Fisher
Scientific, MA, USA), equipped with nine Faraday cup
collectors. The analyses of Sr and Nd isotopes followed the
methods of Tatsumi et al. (2006), and the analysis of Pb followed the methods of Miyazaki et al. (2003). Total procedural blanks for Sr, Nd, and Pb were less than 10 pg, 3 pg,
and 6 pg, respectively. Normalizing factors used to correct
the mass fractionation of Sr and Nd during the measurements were 86Sr/88Sr ¼ 01194 and 146Nd/144Nd ¼ 07219.
Analyses of standards NIST 987 and JNdi-1 over the measurement period provided 87Sr/86Sr ¼ 0710257 07 (2SD)
(n ¼13), and 143Nd/144Nd ¼ 0512100 11 (2SD) (n ¼15),
respectively. Lead isotope ratios were measured using the
double-spike method, following a procedure similar to
that described by Thirlwall et al. (2000). All the data were
corrected for mass-fractionation using a 207Pb^204Pb
double-spike that had previously been calibrated against
208
Pb/206Pb ¼100016 of NIST T 982 (Catanzaro et al.,
1968). NIST 981 (25 ng) was treated as an unknown
during the measurement period and gave 206Pb/204Pb ¼
207
Pb/204Pb ¼15501 0002,
and
16944 0003,
208
204
Pb/ Pb ¼ 36731 0007 (2SD, n ¼ 5).
We analyzed He isotope compositions in olivines. Rock
samples were crushed using a jaw crusher and olivine
phenocrysts were handpicked under a binocular microscope. The typical olivine grain size was 05^15 mm.
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JOURNAL OF PETROLOGY
VOLUME 50
NUMBER 8
AUGUST 2009
Fig. 2. Bathymetric maps of (a) North Flank of Oahu Island, and (b) Loihi seamount, showing sample localities (circles). Bathymetric maps
are complied from (a) Kairei cruise KR98-08 and Yokosuka cruise YK99-07 SeaBeam data, and (b) Kairei cruise KR98-09 and Yokosuka
cruise YK99-07 SeaBeam 2100 data. Marked localities were sampled by Shinkai 6500 JAMSTEC (1999).
The selected crystals were leached in warm (708C) 5%
HNO3 to remove surface contaminants, then washed ultrasonically with acetone, ethanol and distilled water.
Samples were loaded in crushing tubes for in vacuo crushing, and then the crushing tubes were baked out for 1day
to reduce the blank level. Measurements of noble gas abundances and isotope ratios were performed on a sector-type
mass spectrometer (GVI-5400). He isotope ratios were normalized by repeated measurements of the in-house standard gas from Kaminoyama well (568 Ra). The other
isotope ratios and noble gas abundances were calibrated
by repeated measurements of diluted air. Neon isotope
ratios were corrected for interference of 40Ar2þ and
CO22þ on 20Neþ and 22Neþ, respectively. Typical blank
levels by crushing are 3 10^12, 1 10^12 and 06 10^12
cm3 STP for 4He, 20Ne and 36Ar, respectively. The analytical procedure used for all noble gases has been described
in more detail by Hanyu et al. (2007).
R E S U LT S
There have been numerous previous petrological and geochemical investigations of Hawaiian shield lavas, and not
surprisingly, some characteristics of the samples from this
study have already been reported. Thus, in this section we
will only briefly summarize the general characteristics of
the lavas, before focusing on those new features revealed
by our data.
Major elements
All the samples analyzed in this study (Table 2) are tholeiitic basalts or picrites, except for WAF-36. This sample
is from the subaerially erupted Makapuu stage of the
Koolau volcano (Haskins & Garcia, 2004) and is an alkalic
basalt (Tanaka et al., 2002). The analysed samples
have K2O/P2O5 within the range of magmatic values of
15^22 (Wright & Fiske, 1971). The potentially mobile elements, such as K, correlate with abundances of immobile
elements, such as Nb, suggesting that the samples are
fresh. Except for WAF-36, all the lavas have MgO contents
greater than 65 wt %, suggesting that their compositions
are affected mainly by olivine crystallization.
Of the samples analyzed in this study, the Loihi lavas
have the highest CaO, TiO2 and Fe2O3, and lowest SiO2
contents at a given MgO content. The Kilauea lavas have
higher TiO2 and CaO contents and lower SiO2 contents
than the Koolau (Makapuu) lavas at the same MgO content. The Koolau (Makapuu) lavas have the lowest CaO
and TiO2, and highest SiO2 contents at a given MgO content (except for the alkalic basalt WAF-36). Because these
1556
REN et al.
HAWAIIAN SHIELD LAVA GEOCHEMISTRY
Table 1: Sample localities and rock types used for analyses
Run
Sample
Locality
Mbsl
Rock type
MgO
Olivine
Olivine
Cpx
Plag
(wt %)
ph
mph
mph
mph
Gmass
Alteration
Loihi
R1
S490-2
1884460 N, 15581140 W
4657
pillow lava, picrite
2325
30
5
65
weak
R2
S490-3
1884470 N, 15581140 W
4598
pillow lava, picrite
2297
29
6
65
weak
R3
S490-6
1884520 N, 15581130 W
4426
pillow lava, picrite
2728
40
3
57
weak
R4
S491-5
1884610 N, 15581040 W
4137
piritic pillow lava
1657
14
6
80
weak
R5
S491-7
1884620 N, 15581070 W
4047
pillow lava, picrite
2326
25
2
73
fresh
R6
S493-2
1885320 N, 15581000 W
4411
pillow lava, picrite
2447
25
8
1
66
fresh
R7
S494-6
188505N, 1558138W
2323
pillow lava, olivine basalt
1036
5
2
01
03
926
weak
02
755
fresh
Kilauea
R8
S492-4
1984800 N, 15481910 W
3958
picritic pillow lava
1822
19
5
03
R9
S492-5
1984780 N, 15481920 W
3961
sheet flow, picritic lava
1775
18
9
04
R10
S492-6
1984780 N, 15481940 W
3953
sheet flow, picritic lava
1650
17
2
R11
S506-6B
19821320 N, 154833390 W
5096
picrite
2005
20
7
73
moderate
R12
S506-7A
19821370 N, 154833400 W
5016
pillow fragment, picrite
2034
13
10
77
moderate
726
fresh
81
fresh
Mauna Loa?
R13
S507-1B
18854860 N, 155826750 W
3455
olivine basalt
1106
9
3
88
weak
R14
S507-5B
18855860 N, 155827560 W
2732
picrite
2254
23
8
69
weak
R15
WAF-36
Wheeler Air Force drilling core
1803
basalt
491
1
1
98
moderate
R16
WAF-39
Wheeler Air Force drilling core
1943
olivine basalt
1257
9
2
89
moderate
R17
S500-1
2185140 N, 15784540 W
2980
pillow lava, olivine-rich basalt
1308
20
1
785
weak
R18
S500-5B
21850980 N, 157845550 W
2696
pillow lava, picrite
2045
29
3
R19
S500-6
2185080 N, 15784620 W
2815
pillow lava, picrite
2046
29
15
R20
S500-9A
2185050 N, 15784620 W
2602
pillow basalt
693
2
2
Koolau
05
68
weak
695
weak
96
weak
Mbsl, meters below sea level; ph, phenocryst; mph, microphenocryst; cpx, clinopyroxene; plag, plagioclase; Gmass,
groundmass.
intershield differences are not a function of MgO content,
which is largely controlled by the crystal^liquid differentiation processes, they may reflect differences in the parental
magma compositions.
Major element ratios, such as Al2O3/CaO and TiO2/
Na2O, that would not be affected by just olivine crystallization (Frey et al., 1994) correlate strongly among the
Hawaiian lavas. In the Koolau (Makapuu) lavas Al2O3/
CaO is higher and TiO2/Na2O lower, whereas in the
Loihi and Kilauea lavas the opposite is the case. The
Loihi lavas have the lowest Al2O3/CaO. Samples from the
S507 site have ratios between those of the Koolau
(Makapuu) and Kilauea lavas.
slightly higher in the Koolau (Makapuu) lavas than in
the Kilauea and Loihi lavas. Abundances of incompatible
trace elements, such as Th, Ba, La, Ce, Nb, Zr, P2O5, and
Sr, are positively correlated with each other (not shown).
Similar correlations have been observed in the Hawaiian
shield volcanoes previously and have been interpreted to
reflect magmatic differentiation and partial melting processes (e.g. Frey et al., 1994). Trace element ratios, such as
Zr/Nb, Sr/Nb, and La/Nb, correlate well with each other,
and these ratios are higher in the Koolau (Makapuu)
lavas than in the Kilauea lavas, and lowest in the Loihi
lavas. Samples from the S507 site have ratios between
those of the Koolau (Makapuu) and Kilauea lavas.
Trace elements
Sr^Nd^Pb^He isotopes
Trace element abundances are reported in Table 2.
As shown in previous studies (e.g. Frey et al., 1994), Ni correlates positively with MgO content, whereas Sr and Zr
show inverse correlations. At a given MgO content, Ni is
The Kilauea and Loihi lavas have lower 87Sr/86Sr,
and higher 143Nd/144Nd, 206Pb/204Pb, 207Pb/204Pb, and
208
Pb/204Pb than those from Mauna Loa (Table 3, Fig. 3).
The Koolau (Makapuu) lavas have the highest 87Sr/86Sr,
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JOURNAL OF PETROLOGY
VOLUME 50
NUMBER 8
AUGUST 2009
Table 2: Major element and trace element compositions of the studied samples
Volcano:
Loihi
Kilauea
Mauna Loa?
Run:
R1
R2
R3
R4
R5
R6
R7
R8
R9
R10
R11
R12
Sample:
S490-2
S490-3
S490-6
S491-5
S491-7
S493-2
S494-6
S492-4
S492-5
S492-6
S506-6B
S506-7A S507-1B S507-5B
R13
R14
SiO2
4386
4389
4308
4601
4359
4379
4719
4720
4716
4793
4585
4623
4954
4620
TiO2
167
169
138
219
160
151
239
187
188
177
181
183
184
136
Al2O3
722
725
581
962
709
693
1174
935
954
1057
811
814
1200
809
Fe2O3
1392
1421
1425
1388
1400
1373
1396
1305
1295
1227
1296
1319
1271
1276
MnO
016
015
015
016
016
016
016
015
014
014
014
014
015
015
MgO
2325
2297
2728
1657
2326
2447
1036
1822
1775
1650
2005
2034
1106
2254
CaO
723
736
618
916
758
726
1091
805
804
903
794
821
980
675
Na2O
134
130
101
197
130
108
209
151
165
167
127
125
191
123
K2O
030
028
020
047
033
026
039
032
034
032
037
035
029
020
P2O5
015
015
011
022
015
013
022
018
018
017
017
017
017
012
LOI
077
068
012
015
004
015
027
010
004
006
144
025
029
034
Total
9985
9993
9932
10010
9909
9915
9914
9979
9960
10028
10010
10009
9917
9906
Sc
214
214
19
261
242
232
322
218
217
212
231
210
229
174
Co
981
976
1105
776
1009
101
60
7503
7303
6506
9152
766
4904
Ni
11027
10687
13479
6765
10692
11315
2428
Rb
Sr
534
222
521
223
369
170
Y
134
135
109
Zr (XRF)
776
789
616
Nb (XRF)
94
96
71
751
735
533
Ba
La
Ce
Pr
Nd
792
192
268
123
782
191
267
124
579
144
201
948
901
301
197
114
142
123
118
285
388
178
622
214
461
199
704
322
564
245
575
249
543
272
572
255
59
244
408
251
817
12055
32
181
81
125
98
99
89
89
95
72
52
860
653
1023
792
821
780
839
771
537
438
811
271
123
655
162
229
107
109
272
392
185
876
222
321
154
896
226
328
157
853
216
315
150
102
921
233
342
167
172
2733
97
101
187
8617
689
108
177
10448
119
107
183
680
780
119
181
7954
136
196
226
8353
106
855
217
316
153
198
146
951
711
694
180
267
132
527
137
205
101
Sm
309
318
245
448
314
276
495
404
416
402
450
411
384
Eu
108
107
0861
153
106
0963
171
145
146
146
157
146
141
288
107
Gd
337
340
270
482
340
301
536
466
472
464
512
468
463
346
Tb
051
0527
0426
0748
0523
0459
0837
0706
0719
0692
0759
070
0731
0543
Dy
290
301
239
425
300
264
490
400
406
397
430
389
429
319
Ho
056
0562
0458
0817
0568
0498
0948
0754
077
0757
0794
0722
0829
0603
Er
148
148
122
218
153
131
252
20
204
20
206
187
224
164
Tm
0196
0201
0161
0295
0198
0174
0343
0257
0264
0258
0261
0236
030
0207
Yb
116
118
094
172
123
106
206
157
160
153
159
143
177
130
Lu
0169
0175
0139
0256
0181
0157
0296
0224
0227
0216
0222
0198
0251
0185
Hf
233
234
183
332
231
164
358
145
247
292
283
321
244
108
Pb
0704
0699
0540
109
0773
0662
10
0720
0691
0659
0613
0593
0617
0596
Th
0583
0580
0417
0890
0599
0451
0744
0662
0683
0636
0705
0638
0447
0353
U
0181
0180
0129
0297
0178
0138
0232
0221
0228
0213
0246
0222
0221
0107
(continued)
1558
REN et al.
HAWAIIAN SHIELD LAVA GEOCHEMISTRY
Table 2: Continued
Volcano:
Koolau
Run:
R15
R16
R17
R18
R19
R20
Sample:
WAF-36
WAF-39
S500-1
S500-5B
S500-6
S500-9A
SiO2
4864
5040
5004
4748
4739
5200
TiO2
298
207
162
137
157
210
Al2O3
1656
1162
1177
885
856
1381
Fe2O3
1309
1281
1159
1210
1246
1194
MnO
011
013
014
014
014
014
MgO
491
1257
1308
2045
2046
693
CaO
843
694
827
650
620
969
Na2O
381
226
207
167
180
250
K2O
081
053
038
031
039
058
P2O5
045
035
019
016
021
026
LOI
036
051
012
004
014
025
10016
10020
9927
9907
9931
10020
Sc
133
160
239
201
151
271
Co
3825
5631
579
801
7185
5241
11183
Total
Ni
Rb
Sr
Y
Zr (XRF)
Nb (XRF)
Ba
142
107
680
282
194
128
164
565
926
386
240
149
126
169
La
171
144
Ce
426
344
Pr
Nd
626
303
488
229
515
314
421
246
167
140
975
821
9939
582
251
167
107
415
1163
721
379
221
131
64
53
80
86
704
575
759
905
786
650
199
164
29
24
141
117
880
222
319
153
105
265
389
187
Sm
785
585
377
319
405
506
Eu
272
202
135
113
138
178
Gd
825
631
416
350
446
554
Tb
117
0924
0642
0535
0667
0841
Dy
645
518
367
309
373
489
Ho
118
096
0692
0588
0697
0914
Er
302
254
185
154
186
243
Tm
0377
0329
0246
0206
0238
0324
Yb
228
196
149
123
145
191
Lu
0320
0275
0217
0179
0205
0281
Hf
498
431
282
233
214
373
Pb
172
143
0910
0708
0901
113
Th
0922
0920
0438
0367
0564
0579
U
0252
0285
0146
0117
0179
0194
LOI, loss weight on ignition; negative values indicate gain
weight on ignition.
and the lowest 143Nd/144Nd and 206Pb/204Pb among the
Hawaiian shield lavas. Samples from site S507 have isotope
ratios similar to those of the Mauna Loa lavas (Table 3,
Fig. 3a and b). The 87Sr/86Sr and 143Nd/144Nd isotope
ratios measured in this study for the Loihi lavas are similar
to those for the Kilauea lavas. The similarity between
Kilauea and Loihi was previously noted by Garcia et al.
(1995). However, Sr and Nd isotope data do not provide the same level of volcano-specific resolution as
Pb isotope data (Abouchami et al., 2005). In the
208
Pb/204Pb^206Pb/204Pb diagram (Fig. 3d), the fields for
Loihi and Kilauea defined by high-precision triplespike Pb isotope data are clearly distinct and do not overlap. Loihi lavas have higher 208Pb/204Pb at a given
206
Pb/204Pb than Kilauea lavas. However, new doublespike Pb isotopic data for Loihi seamount lavas obtained
in this study (S491-5, S491-7, S493-2) have lower
208
Pb/204Pb at a given 206Pb/204Pb, and plot in the
Kilauea field (Fig. 3d). This is an important observation
because it implies that Loihi’s source region includes a
Kilauea-like (‘Kea’) mantle component. This observation
challenges the interpretation that the Loihi lavas represent
a mantle component (the Loihi component) that is distinct
from the Kea component (Eiler et al., 1996; Hauri, 1996).
The helium concentration in fluid inclusions in olivine
varies from 13 10^9 to 330 10^9 cm3 STP/g (Table 4),
which is within the normal range of helium concentrations
for olivines from Hawaii (Kurz et al., 1996). There is no systematic correlation between the measured 3He/4He and
helium concentration, suggesting that the helium isotopic
ratios are not strongly influenced by post-eruptive production of radiogenic 4He. The 3He/4He values for the Loihi
lavas, ranging from 226 to 307 Ra, are among the highest
measured in Hawaiian basalts to date (Fig. 4). The
Kilauea lavas have ratios ranging from 92 to 153 Ra, the
S507 samples from 177 to 188 Ra, and the Koolau
(Makapuu) lavas from 129 to 148 Ra. Across all the
Hawaiian shield volcanoes, 3He/4He ratios do not correlate
strongly with Sr, Nd, or 208Pb/204Pb isotopic ratios (see
Fig. 4). However, there are broad correlations between He
and Sr, Nd, and 208Pb/204Pb within lavas from a single
volcano (Fig. 4). Some samples show elevated 20Ne/22Ne,
21
Ne/22Ne, and 40Ar/36Ar compared with atmospheric
values. 20Ne/22Ne and 21Ne/22Ne are positively correlated
and define a trend that overlaps with the Loihi^Kilauea
trend (e.g. Honda et al., 1991). Honda et al. (1991) suggested
that this could be ascribed to the involvement of a less
degassed component in the mantle source, which is supported by the high 3He/4He.
DISCUSSION
In the following discussion we consider: (1) the number of
distinct mantle components; (2) the possible origins of the
components required to explain the isotopic variations in
1559
JOURNAL OF PETROLOGY
VOLUME 50
NUMBER 8
AUGUST 2009
Table 3: Sr^Nd^Pb isotope compositions of the studied samples
Sample
143
2SE
87
2SE
206
2SE
207
2SE
208
R1
S490-2
R2
S490-3
0512958
0000013
0512944
0000010
0703586
0000009
18440
0002
15482
0002
38182
0005
0703587
0000008
18436
0001
15477
0001
38178
R3
S490-6
0512944
0004
0000015
0703589
0000008
18434
0002
15468
0002
38151
R4
S491-5
0005
0512958
0000009
0703580
0000008
18491
0004
15481
0004
38146
R5
0010
S491-7
0512970
0000011
0703580
0000008
18450
0002
15475
0001
38131
0004
R6
S493-2
0512920
0000007
0703581
0000008
18495
0003
15476
0003
38175
0007
R7
S494-6
0512946
0000012
0703538
0000009
18354
0002
15472
0002
38101
0005
R8
S492-4
0512927
0000012
0703610
0000008
18457
0003
15478
0003
38113
0007
R9
S492-5
0512949
0000007
0703604
0000008
18523
0003
15489
0003
38139
0006
R10
S492-6
0512948
0000008
0703598
0000009
18517
0003
15482
0002
38113
0006
R11
S506-6B
0512982
0000006
0703599
0000007
18568
0004
15484
0003
38121
0008
R12
S506-7A
0512977
0000009
0703578
0000008
18583
0002
15495
0001
38154
0004
Run
Nd/144Nd
Sr/86Sr
Pb/204Pb
Pb/204Pb
Pb/204Pb
2SE
Loihi
Kilauea
Mauna Loa?
R13
S507-1B
0512905
0000008
0703707
0000007
18202
0003
15467
0002
38001
0006
R14
S507-5B
0512923
0000006
0703717
0000008
18240
0002
15467
0002
38022
0006
Koolau
R15
WAF-36
0512718
0000008
0704137
0000015
17846
0002
15433
0002
37757
0005
R16
WAF-39
0512740
0000009
0704075
0000007
17857
0002
15444
0002
37759
0006
R17
S500-1
0512780
0000011
0703995
0000007
17873
0002
15451
0002
37776
0005
R18
S500-5B
0512788
0000007
0703967
0000009
17876
0003
15452
0002
37774
0006
R19
S500-6
0512826
0000008
0703892
0000007
17950
0003
15454
0003
37816
0008
R20
S500-9A
0512773
0000008
0703974
0000009
17867
0002
15451
0002
37775
0004
All powders were leached in distilled 15N HCl at 1008C for 4 h prior to acid dissolution and analysis. Measured
ratios for standard materials were 87Sr/86Sr ¼ 0710257 07 for NBS987 (n ¼ 13, 2s), 143Nd/144Nd ¼ 0512100 11 for
JNdi-1 (n ¼ 15, 2s), and standard deviations for 206Pb/204Pb ¼ 16944 0003, 207Pb/204Pb ¼ 15501 0002, and
208
Pb/204Pb ¼ 36731 0007 for NIST 981 (2s, n ¼ 5).
the Hawaiian shield lavas; (3) the implications of our new
data for models of the Hawaiian plume.
Mantle components in the source of the
Hawaiian pre-shield and shield lavas
Our new 87Sr/86Sr, 143Nd/144Nd, and 206Pb/204Pb data,
combined with data from previous studies, show nearlinear correlations (Fig. 3a and b), suggesting binary
mixing of two source components; the ‘Koolau’ and ‘Kea’
components, as proposed previously by a number of
researchers (Bennett et al., 1996; Lassiter & Hauri, 1998;
Blichert-Toft et al., 1999). This is further supported by the
near-linear trends of Sr^Nd isotope ratios when plotted
against major and trace element ratios (Fig. 5). However,
the Loihi lavas have higher 3He/4He (Kurz et al., 1995;
Eiler et al., 1996; Valbracht et al., 1997) and 208Pb/204Pb at
a given 206Pb/204Pb compared with other Hawaiian shield
lavas (Abouchami et al., 2005; this study) (Figs 3d and 4),
suggesting that a third source component is present.
This ‘Loihi’ component has also been identified in previous
studies (e.g. Staudigel et al., 1984; Garcia et al., 1995; Kurz
et al., 1995; Eiler et al., 1996; Hauri et al., 1996; Hanyu et al.,
2005, 2007). If the Pb isotope systematics of Mauna Kea
are examined in detail even three source components
appear to be insufficient (Abouchami et al., 2000, 2005;
Eisele et al., 2003). In 208Pb/204Pb^206Pb/204Pb space, Pb
isotope data for lavas from single Hawaiian volcanoes
define distinct linear arrays (see Fig. 3d; and Abouchami
et al., 2005, fig. 2a). Eisele et al. (2003) found that the Pb isotope compositions of lavas from the HSDP-2 of Mauna
Kea display three distinct arrays, which they referred to
as ‘Kea-lo8’, ‘Kea-mid8’, and ‘Kea-hi8’. These three arrays
converge to a common end-member and were interpreted
in terms of mixing of three unradiogenic end-members
with a more radiogenic end-member. Previously published
Pb isotope data from the submarine Hana Ridge lavas,
Haleakala volcano (Ren et al., 2006), where the precision
of the Pb isotopic data is similar to that using the Pb
1560
REN et al.
(a)
15.58
“Fresh”
Altered Oceanic Crust
0.5131
0.5128
204
Pb/ Pb
Kilauea
0.5130
0.5129
(c)
Koolau
Mauna Loa
Hawaii
Upper Mantle
East Pacific
Rise MORB
Loihi
207
Nd/ 144Nd
143
Kilauea
Haleakala
Loihi
S507
0.5132
HAWAIIAN SHIELD LAVA GEOCHEMISTRY
Koolau
0.5127
Koolau
15.46
Loihi
Mauna Loa
15.38
17.6 17.8
0.5125
0.702 0.7025 0.703 0.7035 0.704 0.7045 0.705
87
15.50
Kilauea
15.42
WAF-36
0.5126
15.54
18.2 18.4 18.6 18.8
18
206
86
Sr/ Sr
0.704
(d)
Koolau
WAF-36
Mauna Loa
Loihi Kilauea
Pb/204 Pb
0.705
204
Pb/ Pb
38.4
Kea-hi8
Loihi
38.2
Loa
38.0
Kilauea
Koolau
Kea-lo8
208
87
86
Sr/ Sr
(b)
0.703
Kea
37.8
0.702
17.6 17.8 18
Mauna Loa
Hawaii
Upper Mantle
East Pacific Rise MORB
18.2
19
37.6
17.7
18.4 18.6 18.6 19
206
Pb/204Pb
17.9
18.1
18.3
206
204
Pb/
18.5
18.7
Pb
Fig. 3. (a) 87Sr/86Sr vs 143Nd/144Nd, (b) 206Pb/204Pb vs 87Sr/86Sr, (c) 206Pb/204Pb vs 207Pb/204Pb, and (d) 206Pb/204Pb vs 208Pb/204Pb for the
Hawaiian lavas measured in this study compared with fields for Loihi, Kilauea, Mauna Loa and Koolau compositions determined in other studies. Fields in (a) and (b): Kilauea, Mauna Loa and Koolau (Makapuu) are from Lassiter et al. (1996), Pietruszka & Garcia (1999) and
Tanaka et al. (2002); data for Loihi lavas are from Garcia et al. (1993, 1995, 1998). East Pacific Rise mid-ocean ridge basalt (MORB) and
Hawaii upper mantle are from Pietruszka & Garcia (1999, fig. 6). Fields in (c) and (d): Loihi, Kilauea, Mauna Loa and Koolau lavas are
from triple-spike Pb isotope data of Abouchami et al. (2000, 2005). The ‘Kea-hi8’ (grey) and ‘Kea-lo8’ fields are from Eilele et al. (2003), whereas
their ‘Kea-mid8’ field almost overlaps the Kilauea field. The line in (d) defines the boundary between Loa- and Kea-trend lavas (from
Abouchami et al., 2005). The Pb isotope data from this study and the Pb isotope data of Abouchami et al. (2005) have been corrected for mass
fractionation using the NIST 981 Pb isotopic values: 206Pb/206Pb ¼16944, 207Pb/204Pb ¼15501, 208Pb/204Pb ¼ 36731. The 2s error bars are
given in the corner of the diagrams. In the 87Sr/86Sr vs 143Nd/144Nd (a) and 206Pb/204Pb vs 87Sr/86Sr (b) diagrams, isotopic ratios for Loihi
lavas from this study plot within the Kilauea field. However, our double-spike Pb isotope data for Loihi lavas (d) exhibit both Loihi-like and
Kilauea-like compositions, as defined by the triple-spike Pb isotope data of Abouchami et al. (2005). Pb isotopic compositions from the Hana
Ridge lavas, Haleakala volcano (Ren et al., 2006), plotted in (d), display the same array as ‘Kea-lo8’.
double-spike technique, display a similar trend to that of
the Kea-lo8 array (Eisele et al., 2003), distinct from those
of the Loihi and Kilauea lavas defined by Abouchami
et al. (2005) (Fig. 3d), and do not project towards Koolau
compositions. These observations suggest that more
than three isotopically distinct components are required
to produce the complete range of isotopic compositions
observed in the Hawaiian shield lavas. However, principal
component analysis has indicated that the isotopic variations in the shield lavas appear to be dominated by mixtures of three components, namely Loihi, Koolau and
Kea (e.g. Hauri, 1996; Blichert-Toft et al., 2003). Eiler et al.
(1996) also found that the isotopic compositions of each of
their samples could be explained as a mixture of these
three components using a least-squares approach.
The origins of the source components
The origin of the Loihi, Koolau, and Kea components has
been discussed in a number of studies (Eiler et al., 1996;
Hauri, 1996; Lassiter & Hauri, 1998; Blichert-Toft et al.,
1999, 2003; Norman & Garcia, 1999; Pietruszka & Garcia,
1999; Ren et al., 2005, 2006; Salters et al., 2006; Hanyu
et al., 2007). Loihi lavas have high 3He/4He ratios and as a
result many researchers believe that the Loihi component
comes from a less degassed mantle reservoir that retains
1561
JOURNAL OF PETROLOGY
VOLUME 50
some of its primordial helium (e.g. Kurz et al., 1982, 2004;
Hanyu et al., 2007).
The geochemical characteristics of the Makapuu lavas
from the Koolau volcano (believed to best represent
the Koolau component) have been interpreted in terms of
derivation of the lavas from a source that contains EM-1like ancient recycled oceanic crust, including a small
amount of pelagic sediment (e.g. Eiler et al., 1996; Hauri,
1996; Lassiter & Hauri, 1998; Blichert-Toft et al., 1999;
Huang & Frey, 2005). However, it has also been suggested
that they were derived from a mantle plume source that
contained ancient depleted lithospheric material (Norman
& Garcia, 1999; Salters et al., 2006). A component consisting of ancient recycled oceanic crust, including pelagic
sediments, is likely to have higher 87Sr/86Sr, and lower eNd
NUMBER 8
AUGUST 2009
and 206Pb/204Pb than depleted mantle (Weaver, 1991),
which is what is observed in the Koolau (Makapuu) lavas.
Pelagic sediments commonly have a high Pb abundance
and low U/Pb (McCullouch & Gamble, 1991; Weaver,
1991). Although modern pelagic sediments are, for the
most part, too radiogenic to explain the low 206Pb/204Pb
of the Makapuu lavas, it is expected that ancient pelagic
sediments will have much lower 206Pb/204Pb. In addition,
owing to their low U/Pb, even over their long-term evolution, ancient pelagic sediments will not become enriched
in 206Pb/204Pb through the radioactive decay of U
(Weaver, 1991; Hauri, 1996). Furthermore, the derivation of
the Koolau component from recycled oceanic crust plus a
small amount of pelagic sediment can also explain the Os
isotope composition of the Makapuu lavas (Lassiter &
Table 4: Noble gas abundances and their isotopic ratios in the glass and olivine from studied samples
Run
Sample
Weight
Crushing
(g)
(strokes)
Abundance (cm3 STP/g)
4
He
20
36
Ne
–9
(10 )
(10
84
Ar
–12
)
(10
–12
)
132
Kr
(10
Xe
–12
)
(10–12)
Loihi
R1
S490-2 (g)
1853
428
213
178
R2
S490-3 (ol)
1335
884
101
157
R3
S490-6
1028
R4
S491-5 (ol)
1589
R5
S491-7
0596
50
S491-7 duplicate
0606
30
(stepwise)
0606
70
R6
S493-2 (ol)
1577
R7
S494-6 (g)
2189
50
674
104
0349
153
286
605
572
169
0122
620
241
492
215
0248
614
738
235
0194
163
274
135
00878
165
268
0849
00553
706
319
0903
00643
326
236
586
158
297
156
398
172
13
Kilauea
R8
S492-4 (ol)
1211
R9
S492-5
0529
50
R11
S506-6B
1108
50
R12
S506-7A
1123
30
(stepwise)
1123
70
S506-7A duplicate
0467
70
R13
S507-1B
0515
50
R14
S507-5B
1136
30
(stepwise)
1136
40
660
50
128
147
181
0571
00426
188
244
254
0616
00826
693
229
0547
00692
331
160
0431
00272
580
309
0677
0138
335
159
128
106
Mauna Loa?
860
132
348
116
203
389
123
00989
130
388
0377
115
0298
00383
Koolau
R16
WAF-39
058
729
348
431
622
0166
R17
S500-1 (ol)
0604
255
229
421
881
0324
R18
S500-5B (ol)
1502
546
540
874
188
00810
R19
S500-6 (ol)
1548
562
664
684
158
0104
(continued)
1562
REN et al.
HAWAIIAN SHIELD LAVA GEOCHEMISTRY
Table 4: Continued
Run
Sample
Isotope ratios
3
He/4He
20
Ne/22Ne
21
Ne/22Ne
38
Ar/36Ar
38
Ar/36Ar
00290 00010
01883 00013
3178 34
01882 00017
5632 74
Loihi
R1
S490-2 (g)
272 14
R2
S490-3 (ol)
303 12
R3
S490-6
307 04
01885 00015
9539 90
R4
S491-5 (ol)
250 19
1054 109
00355 00087
01883 00007
7508 67
R5
S491-7
267 03
1112 015
00323 00015
01868 00018
3063 29
S491-7 duplicate
261 07
01890 00023
1411 13
(stepwise)
265 10
01895 00032
5951 59
R6
S493-2 (ol)
246 10
01885 00015
7239 41
R7
S494-6 (g)
218 05
01888 00005
3170 06
01875 00336
7905 1100
992 010
967 018
00290 00013
Kilauea
R8
S492-4 (ol)
146 07
R9
S492-5
153 03
984 009
00291 00007
01876 00027
1160 11
R11
S506-6B
92 04
1020 039
00303 00011
01854 00022
6053 65
R12
S506-7A
104 03
01865 00022
2099 20
(stepwise)
105 08
S506-7A duplicate
102 04
01882 00025
1337 13
R13
S507-1B
177 06
R14
S507-5B
188 02
(stepwise)
189 04
Mauna Loa?
1124 015
00337 00008
01861 00029
674 65
01857 00046
7838 75
01918 00032
3433 33
Koolau
R16
WAF-39
129 04
966 008
00287 00005
01886 00013
2082 29
R17
S500-1 (ol)
143 06
985 017
00290 00013
01866 00007
2969 11
R18
S500-5B (ol)
144 05
985 016
00297 00017
01870 00012
3663 16
R19
S500-6 (ol)
148 04
980 015
00298 00014
01871 00006
3626 09
Data are from Kaneoka et al. (2002). g, glass; ol, olivine. Analytical uncertainty indicates one standard deviation in
the measured value. He isotope ratios are nomalized by atmospheric value (140 10–6).
Hauri, 1998), as well as their Hf isotope compositions
(Blichert-Toft et al., 1999).
The trace element characteristics of the Hawaiian lavas
[for example, the distinctive negative Th^U anomalies
(Fig. 6), and Th/La and Th/Ba values (Fig. 7) lower than
those of primitive mantle] suggest that the Hawaiian
source contains a significant amount of recycled oceanic
lower crust (Hofmann et al., 1993; Sobolev et al., 2000; Ren
et al., 2005, 2006).
The origin of the Kea component has been discussed
by many workers (e.g. Tatsumoto, 1978; Stille et al., 1986;
Eiler et al., 1996; Hauri, 1996; Lassiter et al., 1996;
Lassiter & Hauri, 1998; Pietruszka & Garcia, 1999;
Mukhopadhyay et al., 2003; Wang et al., 2003; Hanyu et al.,
2007). Lassiter & Hauri (1998), Pietruszka & Garcia
(1999), Ren et al. (2006) and Hanyu et al. (2007) have
proposed that the Kea-like compositions are derived
from melting of a long-term depleted component within a
heterogeneous Hawaiian plume, rather than from the
assimilation of hydrothermally altered oceanic crust into
plume-derived melts (Eiler et al., 1996; Wang et al., 2003),
or melting of upper mantle lithosphere or asthenosphere
beneath Hawaii (e.g. Tatsumoto, 1978; Stille et al., 1986;
Hauri, 1996; Lassiter et al., 1996).
Some studies have argued that the ‘depleted’ Kea component is derived from ‘young’ HIMU-like (515 Ga)
recycled oceanic crust (Thirlwall, 1997; Eisele et al., 2003).
However, melting experiments (Kogiso et al., 1998;
Takahashi & Nakajima, 2002) have indicated that picritic
primary magmas [e.g. 16^17 wt % MgO for Haleakala
(Chen, 1993; Wagner et al., 1998; Ren et al., 2004) and
Kilauea (Clague et al., 1995) shield volcanoes cannot be
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(a)
VOLUME 50
Loihi
Koolau
35
NUMBER 8
Kilauea
Haleakala
AUGUST 2009
S507
Loihi
Plume core?
25
Loihi
20
15
4
Koolau
10
3
He/ He (R/Ra)
30
5
Kea
HIMU
0
0.7034
0.7036
0.7038
87
(b)
EM-1
Kilauea
Mauna Loa
Mauna Kea
0.7040
0.7042
86
Sr/ Sr
35
3
4
He/ He (R/Ra)
Loihi
EM-1
30
Plume core?
25
Loihi
20
15
10
5
0.5127
Kilauea
Mauna Loa
Koolau
Mauna Kea
Kea
0.5128
0.5129
143
Nd/
(c)
35
0.5131
HIMU
144
Nd
Loihi
Loihi
25
20
15
Koolau
10
Kea
3
4
He/ He (R/Ra)
30
5
HIMU
Kea trend
EM-1
Loa trend
0
0
10
20
∆
30
208
Pb/
40
204
50
60
Pb
Fig. 4. He isotopic variations for Hawaiian volcanoes, compared with (a) 87Sr/86Sr, (b) 143Nd/144Nd, and (c) 208Pb/204Pb isotopic variations.
Fields for Loihi, Kilauea, Mauna Kea, Mauna Loa are from Kurz et al. (2004); field for Mauna Kea in (b) is from Bryce et al. (2005).
208Pb/204Pb indicates deviation of 208Pb/204Pb at a given 206Pb/204Pb from the Northern Hemisphere Reference line, defined as
208Pb/204Pb ¼100[208Pb/204Pbmeas ^ (1209 206Pb/204Pbmeas þ15627)] (Hart, 1984). High values of 208Pb/204Pb indicate 208Pb/204Pb values
that are relatively high (for a particular 206Pb/204Pb on a Pb^Pb diagram), suggesting elevated values of Th/U. The boundary line defining
the Loa- and Kea-trends is from Abouchami et al. (2005). Assumed endmember components are shown as ‘Loihi’, ‘Kea’, and ‘Koolau’. The Sr,
Nd, and Pb isotopic data are from Ren et al. (2006), He isotopic data for the Haleakala lavas are from Hanyu et al. (2007). The other He isotopic
data for Hawaiian lavas are from this study and Kaneoka et al. (2002) (see Table 4).
1564
REN et al.
2.2
Al2O3/CaO
1.8
Loihi
Kilauea
S507
Koolau
(b)
2.2
WAF-36
WAF-36
1.8
Haleakala
Al2O3/CaO
(a)
HAWAIIAN SHIELD LAVA GEOCHEMISTRY
1.4
1.4
1.0
1.0
0.6
0.6
0.7035 0.7036 0.7037 0.7038 0.7039 0.7040 0.7041 0.7042
87
6
8
10
Sr/ Sr
(c)
(d)
1.6
1.2
1
16
18
1.0
0.8
0.6
0.6
0.7035 0.7036 0.7037 0.7038 0.7039 0.7040 0.7041 0.7042
WAF-36
1.2
0.8
87
14
1.6
1.4
WAF-36
La/Nb
La/Nb
1.4
12
Zr/Nb
86
0.5127
86
0.5128
0.5129
143
Sr/ Sr
Nd/ 144Nd
Fig. 5. Compositional correlations (a) 87Sr/86Sr vs Al2O3/CaO, (b) Zr/Nb vs Al2O3/CaO, (c) 87Sr/86Sr vs La/Nb, and (d)
Nb. Trace element data and isotopic data for Haleakala lavas are from Ren et al. (2004, 2006).
derived from simple melting of recycled oceanic basalt.
Direct partial melting of a basaltic crustal protolith yields
partial melts that are too low in NiO and MgO, and too
high in SiO2 to generate Hawaiian tholeiites (Herzberg,
2006). Furthermore, this model is also inconsistent
with the higher 3He/4He of the Kea lavas, because if the
Kea-like source is recycled oceanic crust it should be
degassed and would have low 3He/4He. Hanyu et al.
(2007) proposed that the Kea component is not a distinct
mantle end-member but a sub-component that is a mixture
of the Loihi component (or less-degassed component) and
a HIMU component. If the Kea component is derived
from mixing of the HIMU and Loihi components, then,
as indicated by Fig. 4, the Kea component should have
lower 3He/4He, 87Sr/86Sr and 208Pb/204Pb than the Loihi
component, as HIMU has low 3He/4He, 87Sr/86Sr and
208Pb/204Pb (Zindler & Hart, 1986). We also propose
that the Koolau component is not a distinct pure
end-member component but a sub-component that is
derived by mixing Loihi and EM-1 components (Fig. 4).
0.5130
143
Nd/144Nd vs La/
Because the EM-1-like component has lower 3He/4He and
143
Nd/144Nd, and higher 87Sr/86Sr and 208Pb/204Pb than
the Loihi component, the Koolau component would be
expected to have He, Sr, Nd, and Pb isotope compositions
between those of the Loihi and EM-1-like components.
In addition, there are probably some other minor components in the Hawaiian plume source, for example, the
common radiogenic and un-radiogenic end-members as
defined in the Mauna Kea source (Eisele et al., 2003).
Monte Carlo modeling shows that these end-members
could be derived from ‘young recycled oceanic crust’
(515 Ga) components that have different differentiation
ages and variable m and k values (Eisele et al., 2003). Such
a model is consistent with the idea that recycled oceanic
crust exists in the Mauna Kea source based on trace element compositions (Hofmann & Jochum, 1996). From a
study of melt inclusions, Ren et al. (2005) inferred that
recycled oceanic crust retains its distinct geochemistry,
forming streaks or ribbons distributed throughout the
entire plume.
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VOLUME 50
Loihi
Primitive Mantle Normalized
25
20
15
10
5
0
Rb Th Nb La Pb Sr Nd Zr Ti Tb Y Er Yb
Ba U K Ce Pr P Sm Eu Gd Dy Ho Tm Lu
(b)
Kilauea- S507
Primitive Mantle Normalized
25
20
15
10
5
0
(c)
Primitive Mantle Normalized
25
S507
Rb Th Nb La Pb Sr Nd Zr Ti Tb Y Er Yb
Ba U K Ce Pr P Sm Eu Gd Dy Ho Tm Lu
Koolau
WAF-36
20
15
10
5
0
Rb Th Nb La Pb Sr Nd Zr Ti Tb Y Er Yb
Ba U
K Ce Pr P Sm Eu Gd Dy Ho Tm Lu
Fig. 6. Primitive mantle (Sun & McDonough, 1989) normalized
trace element patterns, adjusted to 176 wt % MgO, for (a) Loihi,
(b) Kilauea-S507, and (c) Koolau (Makapuu) lavas.
NUMBER 8
AUGUST 2009
We propose that the Loihi component is a common component forming the peridotite matrix of the Hawaiian
plume, because variations between He and radiogenic isotopes for the Kea- and Loa-trend volcanoes converge on
the Loihi component on the high 3He/4He side. The isotopic compositions of the various shield lavas reflect different
mixing proportions of the Loihi component and recycled
ancient oceanic crust components (EM-1-like and HIMUlike) in the source. The recycled oceanic crust may include
pelagic sediments that have evolved to an EM-1-like
composition (Weaver, 1991; Hauri, 1996; Lassiter & Hauri,
1998; Blichert-Toft et al., 1999), or may not include sediments and have a relatively young differentiation age and
variable m and k values that have evolved to ‘young
HIMU-like’ compositions (Thirlwall, 1997; Eisele et al.,
2003).
On the basis of a melt inclusion study of Koolau
(Makapuu) and Haleakala (Hana Ridge) lavas, Ren et al.
(2005) inferred that the Hawaiian lavas are derived from
the mixing of melts with distinct compositions that may
have originated from different sources. We prefer liquid^
liquid mixing rather than solid^solid mixing, because the
melt inclusions represent liquids with distinct compositions
derived from partial melting of a heterogeneous plume
source that have not been homogenized in a magma chamber (e.g. Ren et al., 2005).
It has been suggested that these plume source components could be pyroxenites (Ren et al., 2004) formed
during the initial interaction between ambient peridotite
mantle and melt from recycled oceanic crust during upwelling in the plume (e.g. Sobolev et al., 2000, 2005, 2007; Ren
et al., 2006; Hanyu et al., 2007). We infer that during the formation of the pyroxenites the isotopic signature of the
recycled oceanic crust (EM-1-like and HIMU-like) would
be transferred to the Loihi-like peridotite mantle. The pyroxenites would mostly exhibit coherent isotopic signatures
from the recycled oceanic crust, because the concentrations of Sr, Nd, and Pb are so low in the peridotite that
even small amounts of partial melt originating from
recycled oceanic crust would have a strong influence on
these elements, without significantly changing mineral
compositions and proportions (Sobolev et al., 2000).
The secondary pyroxenite may be distributed randomly
in the peridotite matrix. Mixing of melts derived from
the peridotite matrix and this secondary pyroxenite could
generate picritic melts (Takahashi & Nakajima, 2002;
Herzberg, 2006) with Sr, Nd, and Pb isotope compositions
between Loihi and EM-1, or Loihi and HIMU (Fig. 4).
The Loa-trend and the Kea-trend
The loci of the main shield volcanoes of the Hawaiian
Islands follow two parallel curved lines, known as the
Loa (or southwestern) trend and the Kea (or northeastern) trend (Fig. 1; Jackson et al., 1972). It has long been suggested that these two volcanic trends are geochemically
1566
REN et al.
HAWAIIAN SHIELD LAVA GEOCHEMISTRY
1.2
(Th/La)n
1.0
0.8
0.6
0.4
0.2
Loihi
Kilauea
S507
Koolau
0.0
0.0
0.2
0.4
0.6
0.8
1.0
1.2
(Th/Ba)n
Fig. 7. Primitive mantle (Sun & McDonough, 1989) normalized Th/La vs Th/Ba (Hofmann & Jochum, 1996) in the basaltic Hawaiian lavas.
distinct (e.g. Tatsumoto, 1978; Hauri et al., 1996; Lassiter
et al., 1996), and are related to the position of the volcanoes
relative to the axis of the Hawaii plume. Recently,
Abouchami et al. (2005) illustrated the trends’ isotopic
distinction using high-precision triple-spike Pb isotope
data in 208Pb/204Pb vs 206Pb/204Pb and 207Pb/204Pb vs
206
Pb/206Pb diagrams. However, Ren et al. (2005) reported
the discovery of both Kilauea-like (Kea) and Mauna
Loa-like (Loa) major element and trace element compositions in olivine-hosted melt inclusions, and even within
single rock samples, from Haleakala (Hana Ridge) (Keatrend) and Koolau (Makapuu) shield (Loa-trend) volcanoes. Ren et al. (2006) also found that during the growth
of the Haleakala shield whole-rock trace element and Sr,
Nd, Pb isotope compositions shifted from Kilauea-like
(Kea) in submarine lavas from the Hana Ridge, to
Mauna Loa-like (Loa) in subaerial lavas from
Honomanu. All of this is inconsistent with the existence of
two geochemically distinct trends. The compositional
trends from the current Pu’u O’o eruption suggest that
both Kilauea- and Mauna Loa-like components are present within Kilauea’s mantle source region (Marske et al.,
2007).
In this study, the high-precision 208Pb/204Pb and
206
Pb/204Pb isotopic ratios of some of the Loihi lavas are
similar to those of the Kilauea lavas defined by
Abouchami’s triple-spike Pb isotope data (Fig. 3c and d),
despite the fact that Loihi is believed to sample the Loa
trend composition (Hauri, 1996; Lassiter et al., 1996;
Abouchami et al., 2005).
Both Kea and Loa characteristics appear to occur in the
Loihi lavas as well as in those from Haleakala (West &
Leeman, 1987; Ren et al., 2006), Mauna Kea (Eisele et al.,
2003), Kilauea (Marske et al., 2007), and Koolau (Jackson
et al., 1999; Tanaka et al., 2002; Haskins & Garcia, 2004).
On a large scale, general geochemical differences exist
between whole-rocks from the Kea- and Loa-trend volcanoes (e.g. Abouchami et al., 2005), and on a small scale,
the two geochemical trends can exist within a single
shield and even within a single rock sample, regardless
of the specific geographical location of the volcano.
Therefore, the Kea and Loa components must be distributed finely throughout the mantle source beneath the
Kea- and Loa-trend volcanoes.
M E LT I N G P RO C E S S E S I N T H E
H E T E RO G E N E O U S H AWA I I A N
P LU M E
Parental magma compositions and
melting processes
A parental magma composition, with an MgO content
of 176 wt %, was inferred from melt inclusion and host
olivine compositions (data from Ren et al., 2005) in
the Hana Ridge lavas, following the procedure of
Danyushevsky et al. (2000). To permit comparison between
lavas at the same MgO content, and discover more
about their mantle source compositions and the melting
processes in the mantle plume (e.g. Hauri, 1996;
Mukhopadhyay et al., 2003; Ren et al., 2004, 2006), we
adjusted the major element data for the Loihi, Kilauea,
the S507 site and Koolau lavas to 176 wt % MgO by
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JOURNAL OF PETROLOGY
VOLUME 50
(a) 0.7043
(d)
WAF-36
AUGUST 2009
0.7043
WAF-36
0.7038
Sr/ 86Sr
0.7041
Loihi
Kilauea
0.7036
0.7038
87
87
Sr/ 86Sr
0.7041
NUMBER 8
0.7036
S507
Koolau
(b) 0.7033
0.7033
0.5
16
1.0
Zr/Nb
14
(e)
12
2.5
0.51305
0.51295
Nd/ 144 Nd
10
8
FeO* (wt.% adjusted)
2.0
Al 2 O 3 /CaO (adjusted)
WAF-36
6
0.51285
143
(c)
1.5
0.51275
13
WAF-36
0.51265
5
12
WAF-36
6
7
8
9
10
11
12
CaO (wt.% adjusted)
11
10
44
45
46
47
48
49
50
51
SiO 2 (wt.% adjusted)
87
86
Fig. 8. (a) SiO2 vs Sr/ Sr, (b) SiO2 vs Zr/Nb, (c) SiO2 vs FeO, (d) Al2O3/CaO vs 87Sr/86Sr, and (e) CaO vs 143Nd/144Nd adjusted for fractionation to a parental magma composition containing 176 wt % MgO (see text for explanation).
addition or subtraction of Fo87 olivine (e.g. Ren et al., 2004)
(Fig. 8).
These adjusted major element compositions show
systematic variations. SiO2 contents increase, CaO and
FeO contents decrease, and Al2O3/CaO increases in the
order Loihi^Kilauea^Mauna Loa (S507 site)^Makapuu
(Fig. 8). The adjusted SiO2, CaO, FeO, and Al2O3/CaO
also correlate well with isotopic (e.g. Sr, Nd, Pb) and
trace element ratios (e.g. Zr/Nb, La/Nb, Sr/Nb) (Fig. 8).
Sobolev et al. (2005, 2007) and Herzberg (2006) have
demonstrated that pyroxenite sources generate melts with
higher SiO2, and lower Ca and Mg contents than peridotite sources. Therefore the pattern of major element compositions, and the correlations with isotope ratios, from
Loihi to Kilauea to Mauna Loa to Koolau, may reflect
changes in the source composition or mixing proportions
of melts from the Loihi component and ancient recycled
oceanic crust components. In other words, the higher
SiO2, and lower Ca contents in the Makapuu lavas compared with that of the Loihi lavas suggest that the Koolau
melt is derived from mixing of melts of peridotite and pyroxenite, and that this melt contained a higher proportion
of pyroxenite melt than the Loihi melt. The Loihi lavas
have the lowest SiO2 and highest Ca contents among the
Hawaiian lavas, suggesting that the Loihi melt is derived
from melting of a source with a more dominant peridotite
lithology than the Kilauea or Koolau sources. The
Kilauea lavas have higher SiO2 and lower Ca contents
than the Loihi lavas, but lower SiO2 and higher Ca contents than the Koolau lavas, suggesting that the proportion
1568
REN et al.
HAWAIIAN SHIELD LAVA GEOCHEMISTRY
of the melt derived from melting of pyroxenite is smaller
than that in the Koolau melts but greater than that in the
Loihi melt.
The SiO2 and FeO contents of basalts are both sensitive
indicators of the degree and mean pressure of melting
(Kogiso et al., 1998). For example, a higher extent of melting leads to a higher SiO2 and a lower FeO content in the
melt (Frey et al., 1994; Yang et al., 1996). The adjusted SiO2
and FeO contents in the Loihi and Kilauea tholeiites
(Fig. 8) suggest that from Loihi to Kilauea, within the
Hawaii mantle plume, the degree of melting increases
and the pressure of melting decreases (e.g. Garcia et al.,
1995, 1998).
Geochemical structure of the plume and
partial melting processes
Some researchers have proposed that a concentrically
zoned mantle plume can account for the geochemical characteristics of the Hawaiian lavas (e.g. Hauri et al., 1996;
Kurz et al., 1996; Lassiter et al., 1996; DePaolo et al., 2001;
Bryce et al., 2005). An alternative model, involving a concentrically zoned, but asymmetrically heterogeneous,
plume has been proposed by Kurz et al. (2004), based on
the different temporal evolution of Mauna Kea and
Mauna Loa. However, based on the overall Pb isotopic differences between the Kea- and Loa-trend shield volcanoes,
together with small-scale heterogeneities within the
stratigraphic sequences of Mauna Kea and Koolau,
Abouchami et al. (2005) argued against concentric compositional zoning of the plume. Instead, they proposed the
existence of a compositionally zoned mantle plume in
which the zoning is left to right bilaterally asymmetric.
Blichert-Toft et al. (2003) also argued against a compositionally zoned mantle plume and proposed a model in
which the heterogeneities are distributed vertically like a
stack of ‘pancakes’, which are sampled consecutively by
the volcanoes. Ren et al. (2005, 2006), based on a study of
melt inclusion compositions, combined with whole-rock
compositions, originally proposed a Hawaiian mantle
plume characterized by more random heterogeneity than
would be present in a compositionally zoned mantle
plume. They suggested that ancient recycled oceanic crust
is distributed throughout the entire plume and that the isotopic composition of lavas from a given Hawaiian volcano
(at a given time) is governed by the thermal structure of
the plume and the solidus temperature of the heterogeneous source lithologies within the plume. The proportion
of the recycled oceanic crust component sampled by the
melt is higher in the later stages of Hawaiian shields as
the volcanoes migrate away from the central axis of the
plume. This can be summarized as disequilibrium melting
within a heterogeneous mantle plume. Ito & Mahoney
(2005) proposed a model for the flow and melting of a
heterogeneous mantle. They assumed that the mantle is
composed of enriched mantle peridotite, pyroxenite and
depleted mantle peridotite with distinct trace-element and
isotopic compositions and with different melting temperatures. The enriched mantle peridotite and pyroxenite both
begin melting deeper than the depleted mantle peridotite
and the magma composition is assumed to be controlled
by perfect mixing of the fractional melts.
Based on the above observations, we propose a heterogeneous Hawaiian mantle plume model, modified from that
of Ren et al. (2005, 2006). This model could explain
the observed intershield geochemical variations of the
Hawaiian lavas. To a first order, the isotopic variations in
the Hawaiian shield lavas appear to be dominated by a
mixture of three components: the Loihi component, the
relatively ‘enriched’ Koolau component, and the relatively
‘depleted’ Kea component (Fig. 4). The Koolau component
probably consists of a higher proportion of the EM-1-like
component, whereas the Kea component may contain a
higher proportion of the HIMU-like component.
Overall, geochemical differences exist between the
whole-rocks of the Kea- and Loa-trend volcanoes, possibly
reflecting NE^SW asymmetric heterogeneities in the
Hawaiian plume (e.g. Abouchami et al., 2005). However,
in detail, similar differences can also exist within a single
shield, and even within a single sample of lava, suggesting
a more random heterogeneity than would be present in a
compositionally zoned mantle plume. We speculate that
the plume may entrain its peridotite matrix (Loihi component) from the lower mantle and mix with recycled oceanic crust components (EM-1 and HIMU) that have been
stirred and stretched, but still retain a distinct geochemistry, and form streaks or ribbons distributed throughout
the entire plume. The recycled oceanic crust components,
EM-1-like and HIMU-like, are distributed finely within
the peridotitic matrix of the Hawaiian plume, and both
are present in the mantle sources beneath the Kea- and
Loa-trend volcanoes. Overall, the Loa source has a higher
proportion of the EM-1 than the HIMU component,
whereas the Kea source contains a higher proportion of
HIMU than EM-1. However, the opposite can occur occasionally in the Loihi sources (so that they have a Kilauealike mantle component, as observed in this study), Mauna
Kea sources (so that they have a Loihi-like mantle component; Eisele et al., 2003), Kilauea sources (so that they
have a Mauna Loa-like mantle component; Marske et al.,
2007), Haleakala sources (so that they have a Mauna Loalike mantle component; Ren et al., 2006), and Koolau
sources (so that they have a Kilauea-like mantle component; Jackson et al., 1999; Tanaka et al., 2002; Haskins &
Garcia, 2004).
Both the thermal structure of the plume and the spatial
distribution of compositional heterogeneities appear to be
important in controlling the isotopic composition of
lavas from a given Hawaiian volcano. In other words, the
melting points of the different materials control which
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JOURNAL OF PETROLOGY
VOLUME 50
component dominates in the lavas erupted at each shield
volcano (Ren et al., 2005, 2006). The melting depth
decreases in the mantle plume during the progressive
growth of the Hawaiian shield volcanoes (as indicated by
the shallowing melting depth from Loihi to Kilauea suggested by the adjusted SiO2 and FeO contents), because
the temperature drops as the volcanoes migrate away
from the central axis of the plume towards the margins
with the plate motion (DePaolo & Stolper, 1996). During
the pre-shield and early stages of shield growth, the
magma source is located within the core of the plume.
The resulting high temperatures were able to generate
melts not only from the pyroxenite component (forming a
silica-rich melt from the recycled oceanic crust which interacts with the surrounding peridotite), but also from the
more refractory component (peridotite from the lower
mantle), to form alkalic melts relatively deeper (e.g. preshield Loihi lavas). The compositions of these melts, generated in the plume center, become progressively more
silica-saturated with time, reflecting higher degrees of partial melting as the depth of melting decreases, until finally
tholeiitic melts are formed (e.g. up sequence in Loihi and
Kilauea lavas) (Garcia et al., 1995, 1998).
The large variation in He isotope ratios over only a
few thousand years also implies that the plume is highly
heterogeneous, containing both high- and low-3He/4He
source materials (Kurz et al., 2004). There is a varying contribution from undegassed (Loihi component) and
degassed (recycled oceanic crust components) sources.
The high 3He/4He in the Loihi lavas and the overall
decrease in 3He/4He in lavas erupted during the later
stages of volcanism at other volcanoes suggest that Loihi
is close to the present-day center of the Hawaiian hotspot
(Kurz et al., 1996, 2004), because during initial melting at
the core of the plume, volatiles would be preferentially
extracted into the melt (Valbracht et al., 1996; DePaolo
et al., 2001; Hanyu et al., 2005). The Loihi component from
the lower mantle may be more enriched in He than the
recycled oceanic crust component, and as a result, in the
early stages of melting, the plume melt would contain
high amounts of He with high 3He/4He ratios. In contrast,
lavas from some of the late stages of the Hawaiian shields
have both isotopically ‘enriched’ (e.g. lavas from the late
stage of the Mauna Loa shield, Kurz et al., 1995; the
Honomanu stage of the Haleakala shield, Ren et al., 2006;
and Makapuu stage of the Koolau shield, Tanaka et al.,
2002; Haskins & Garcia, 2004), and ‘depleted’ characteristics (e.g. lavas from the late stage of the Mauna Kea
shield, see Bryce et al., 2005, fig. 13; and the Kohala shield,
Eiler et al., 1996). These ‘enriched’and ‘depleted’ characteristics are accompanied by lower 3He/4He ratios, implying
that the proportion of degassed subducted oceanic crust
components (e.g. EM-1 or HIMU) contributing to the
melt may be higher relative to the peridotitic matrix in
NUMBER 8
AUGUST 2009
the later stages of the Hawaiian shield volcanoes as volcanoes migrate from the plume axis to the margin. This is
because the mantle source of the later-stage lavas is located
sufficiently far from the mantle plume center for the temperature to be lower. Here plume components with lower
melting points (e.g. pyroxenite) would be preferentially
sampled by the melt.
CONC LUSIONS
Our data show that the isotope ratios of Sr, Nd, and Pb
exhibit near-linear correlations with major element ratios
(e.g. Al2O3/CaO, TiO2/Na2O) and trace element ratios
(e.g. Zr/Nb, Sr/Nb, and La/Nb). The Sr and Nd isotope
compositions of Loihi and Kilauea lavas are indistinguishable. However, in terms of 208Pb/204Pb vs 206Pb/204Pb the
Loihi lavas have both Loihi- and Kilauea-like compositions. This implies that Loihi’s source region contains
both Loihi- and Kilauea-like (‘Kea’) mantle components.
Overall, whole-rock geochemical differences exist between
the Kea- and Loa-trend volcanoes. However, the spatial
geochemical differences (defined on a geographical basis
as the Kea- and Loa-trends) can also exist within a single
shield, and even within a single sample, regardless of the
specific geographical location of the volcano. We infer that
the recycled oceanic crust, EM-1- and HIMU-like mantle
components derived from recycled oceanic crust are distributed finely throughout a peridotite matrix within the
Hawaiian plume, and that both components are present
in the mantle sources beneath the Kea- and Loa-trend volcanoes. Overall, the Loa source has a higher proportion
of EM-1 than the HIMU component, whereas the Kea
source contains a higher proportion of HIMU relative to
EM-1. However, the opposite can occasionally occur
within the Hawaiian mantle source regions (e.g. in the
mantle beneath Loihi, Mauna Kea, Kilauea, Haleakala,
and Koolau volcanoes). To explain these geochemical differences we propose a model in which disequilibrium melting is occurring within a heterogeneous mantle plume,
modified from that of Ren et al. (2005, 2006). The model
indicates that both the thermal structure and spatial distribution of compositional heterogeneities within the plume
appear to be important in controlling the isotopic composition of lavas from a given Hawaiian volcano. In other
words, the melting points of the different materials will
control which component is dominant in the lavas erupted
at each shield volcano.
AC K N O W L E D G E M E N T S
Z-.Y.R. acknowledges support from a JSPS Fellowship.
We thank E. Takahashi, who kindly provided the
Hawaiian lava samples. The paper benefited from helpful
comments on an earlier version of the manuscript from
V. Salters, J. Lassiter, S.-C. Huang and an anonymous
1570
REN et al.
HAWAIIAN SHIELD LAVA GEOCHEMISTRY
reviewer. We thank the Editor M. Wilson and M. Garcia,
J. Blichert-Toft and M. Rhodes for constructive reviews.
We are grateful to M. R. Reid and R. K. Workman for
comments and suggestions.
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