tapraid4/zqn-ajsc/zqn-ajsc/zqn01010/zqn2165d10a metzgerm S⫽18 3/11/11 16:51 Art:
[American Journal of Science, Vol. 310, December, 2010, P. 1210 –1249, DOI 10.2475/10.2010.02]
ACCRETIONARY OROGEN AND EVOLUTION OF THE JAPANESE
ISLANDS—IMPLICATIONS FROM A Sr-Nd ISOTOPIC STUDY OF THE
PHANEROZOIC GRANITOIDS FROM SW JAPAN
BOR-MING JAHN*,**
ABSTRACT. The Japanese Islands represent a segment of a 450 Ma old subductionrelated orogen developed along the western Pacific convergent margin, and most
tectonic units are composed of late Paleozoic to Cenozoic accretionary complexes and
their high P/T metamorphic equivalents. The formation of the Japanese Islands has
been taken as the standard model for an accretionary orogeny. According to Maruyama
(1997), the most important cause of the orogeny is the subduction of an oceanic ridge,
by which the continental mass increases through the transfer of granitic melt from the
subducting oceanic crust to the orogenic belt. Sengor and Natal’in (1996) named the
orogenic complex the “Nipponides,” consisting predominantly of Permian to Recent
subduction-accretion complexes with very few fragments of older continental crust. These
authors pointed out the resemblance in orogenic style between Japan and the Central
Asian Orogenic Belt (CAOB). The present work uses new and published Sr-Nd isotopic
data from the literature to test the statements made by these authors. A large
proportion of the granitoids from SW Japan have high initial 87Sr/86Sr ratios, negative
␧Nd(T) values and Proterozoic Sm-Nd model ages. The Japanese isotopic data are in
strong contrast with those of two celebrated accretionary orogens, the Central Asian
Orogenic Belt and Arabian-Nubian Shield, but are quite comparable with those
observed in SE China and Taiwan, or in classical collisional orogens in the European
Hercynides and Caledonides. This raises questions about the bulk composition of the
continental crust in SW Japan, or the type of material accreted in accretionary
complexes, and negates the hypothesis that the “Nipponides” contains very few
fragments of older continental crust. The subduction-accretion complexes in Japan are
composed mainly of recycled continental crust, probably of Proterozoic age. This
study supports the idea that proto-Japan was initially developed along the southeastern
margin of the South China Block.
Key words: Accretionary orogen, accretionary complex, Japanese Islands, Sr-Nd
isotope tracer, Mesozoic granitoids, Nipponides, crustal growth, juvenile/recycled
crust, Central Asian Orogenic Belt (CAOB), Arabian-Nubian Shield (ANS), SE China,
Taiwan.
introduction
Accretionary orogens are known to be the most important sites of continental
growth and mineralization (for example, Windley, 1992; Sengor and others, 1993;
Sengor and Natal’in, 1996; Jahn, 2004; Kovalenko and others, 2004; Condie, 2007;
Cawood and others, 2009). They include Archean greenstone belts, Proterozoic
orogens (for example, the Birimian of West Africa, Svecofennian of S. Finland,
Cadomian of NW Europe, and the Arabian-Nubian Shield or ANS), Late Neoproterozoic to Mesozoic orogens of the Central Asian Orogenic Belt (CAOB), as well as
Paleozoic to Recent orogens of the circum-Pacific, including the Canadian Cordillera,
and the Caribbean. Accretionary orogens consist of accretionary wedges containing
material eroded from the upper plate and accreted from the downgoing plate, plus
island arcs, ophiolites, oceanic plateaux, old continental blocks, metamorphic rocks
and syn- and post-orogenic granitoids (for example, Cawood and others, 2009; Isozaki
and others, 2010). In the past two decades, studies of accretionary orogens in the
* Institute of Earth Sciences, Academia Sinica, P. O. Box 1-55, Nangang, Taipei 11529, Taiwan
** Present address: Department of Geosciences, National Taiwan University, P. O. Box 13-318, Taipei,
106 Taiwan; [email protected]
1210
Fn*
tapraid4/zqn-ajsc/zqn-ajsc/zqn01010/zqn2165d10a metzgerm S⫽18 3/11/11 16:51 Art:
Bor-Ming Jahn
1211
Canadian Cordillera (Samson and others, 1989; Samson and Patchett, 1991), CAOB
(Sengor and others, 1993; Sengor and Natal’in, 1996; Jahn, 2004; Kovalenko and
others, 2004) and ANS (Stern, 1994, 2002, 2008; Stein and Goldstein, 1996) have
confirmed the massive generation of juvenile granitoid crust in the Neoproterozoic
and Phanerozoic. This important period of crustal growth was seldom recognized or
down-graded in the classic models of continental growth (Armstrong, 1981; Reymer
and Schubert, 1984; McCulloch and Bennett, 1994; Taylor and McLennan, 1995), but
is gaining appreciation in the last two decades (for example, Samson and others, 1989;
Sengor and others, 1993; Jahn, 2004; Kovalenko and others, 2004; Condie, 2007).
The Japanese Islands represent a segment of a 450 Ma old subduction-related
orogen developed along the western Pacific convergent margin, and most tectonic
units are composed of late Paleozoic to Cenozoic accretionary complexes (AC) and
their high P/T metamorphic equivalents (Isozaki, 1996; Isozaki and others, 2010).
Japan appears to provide an ideal model of oceanward growth of an active continental
margin by subduction-accretion processes. In fact, the formation of the Japanese
Islands has been taken as the classic model for accretionary orogeny and often serves as
an example for understanding the crustal evolution of the CAOB and other accretionary orogens (Sengor and Natal’in, 1996; Condie, 2007; Cawood and others, 2009).
According to Maruyama (1997), the most important cause of the orogeny is the
subduction of an oceanic ridge, by which the continental mass increases through the
transfer of granitic melt from the subducting oceanic crust and/or the mantle wedge
to an orogenic belt. Sengor and Natal’in (1996) named the Japanese orogenic
complex the “Nipponides,” which consists predominantly of Permian to Recent
subduction-accretion complexes with very few fragments of older continental crust.
These authors pointed out the resemblance in orogenic style between Japan and the
CAOB, and further emphasized the large mass proportion of the accretionary complex
relative to older continental crust. By implication, the accretionary complex in Japan
must be quite “juvenile” as a whole, and consists mainly of mantle-derived crustal
materials. In this scenario, voluminous granitic melts emplaced in SW Japan and
elsewhere in the Japanese Islands would and should possess Sr-Nd isotopic signatures
indicative of juvenile crust, as observed in many parts of the CAOB or ANS. In the first
instance, this appears to be in agreement with the absence of Precambrian rocks in
Japan. However, the available Sr-Nd isotopic data from the literature and the new
analyses presented here of Cretaceous granites from the Sanyo Belt, Miocene granites
from the Shimanto Belt, and Quaternary granites from the Japan Alps, indicate that
they are in strong contrast with those observed in the CAOB and ANS. In fact, the
isotopic signatures are more comparable with those observed in SE China and Taiwan,
or in classical collisional orogens, such as the European Hercynides and Caledonides.
In this paper, I will summarize the available Sr-Nd isotopic data for granitic rocks
generated in the Japanese Islands from the Paleozoic to Recent, and argue that, in
addition to the accreted oceanic mafic rocks, the exposed continental crust in SW
Japan was produced mainly by remelting or recycling of Proterozoic crust; whereas
juvenile crust of mantle-derivation constitutes only a small proportion. This is contrary
to what was predicted by Sengor and Natal’in (1996) for the “Niponides” with respect
to the importance of the lithological assemblages of an “ocean plate stratigraphy.” I will
conclude that the subduction-accretion complexes in Japan are composed mainly of
recycled continental crust, probably of Proterozoic age for the main part. On the other
hand, the isotopic data support the tectonic evolution model that proto-Japan was
developed initially along SE China as a part of Cathaysia and shared the same
geochemical and isotopic characteristics as the South China Block (sensu lato; Isozaki
and Maruyama, 1991; Maruyama and others, 1997; Isozaki and others, 2010). The
microcontinent was later separated from SE China and drifted northeastward to form
proto-Japan.
tapraid4/zqn-ajsc/zqn-ajsc/zqn01010/zqn2165d10a metzgerm S⫽18 3/11/11 16:51 Art:
1212
Bor-Ming Jahn—Accretionary orogen and evolution of the Japanese Islands—
methodology and source of data
In this paper, the technique of radiogenic isotope tracers (Sr-Nd) will be adopted
to discuss the generation of the continental crust of Japan. The tracers are in a way
comparable to the genetic code (DNA) in biology. The continental crust comprises a
variety of lithologic types; some of them represent “recycled” products of ancient crust,
whereas others show “juvenile” character if they are produced by melting of mantle
peridotites or remelting of mantle-derived rocks such as basalts or andesites. A terrane
composed only of island arc or ophiolite assemblages has clearly a juvenile nature, but
a terrane comprising essentially granitic rocks, like that of SW Japan or Transbaikalia,
cannot be easily classified as juvenile or recycled. In this case, the isotope tracer
technique is the most powerful tool in the determination of the proportion of the
mantle component in the making of a continent.
While basaltic rocks are the most commonly used material in studies of the
composition and evolution of the upper mantle, the genesis and evolution of the
continental crust must be understood through studies of granitoids because they are
generally produced by melting of the middle to lower crust, and hence serve as an
excellent probe for the bulk of the continental crust. In the specific case of the
Japanese Islands, only granitic rocks will be examined.
The source of data used in this paper is mainly from the literature (see Appendix
1), supplemented by new analyses on fourteen Late Cretaceous granitoids from the
Sanyo Belt of SW Japan, two Miocene granitoids from the Shimanto belt of southern
Shikoku and two Pleistocene granodiorites (Takidani Pluton) from the Japan Alps in
north-central Japan (table 1). The complete set of new chemical and isotopic analyses,
as well as zircon age determinations, will be published separately in a paper dedicated
to the petrogenetic study (Jahn and others, in preparation). Only the Sr-Nd isotopic
data (Appendix 1) will be used in this paper for discussion and illustration.
general geological and tectonic setting of the japanese islands
The Japanese Islands are composed mainly of subhorizontal nappe piles of an
accretionary complex (AC) and their metamorphic equivalents with late Paleozoic to
Cenozoic ages (Faure, 1985; Isozaki, 1996; Isozaki and Maruyama, 1991; Isozaki and
others, 2010). Japan is divided into several geologic units with broadly four periods of
accretion: Permo-Triassic, Jurassic, Cretaceous and Tertiary (Faure and others, 1986;
Taira and others, 1989; Ichikawa, 1990; Isozaki and Maruyama 1991). The accreted
nappe-pile structures are best preserved and studied in SW Japan (for example, Faure,
1985; Faure and others, 1986), so the present study deals only with the crustal
evolution of SW Japan.
According to Maruyama and others (1997), Japan originated from a rifted
continental margin about 750 to 700 million years ago, when the South China Block
rifted apart from the Neoproterozoic supercontinent Rodinia to open the PaleoPacific Ocean (Hoffman, 1991; Dalziel, 1992; Powell and others, 1993; Park and others,
1995). Since the tectonic inversion from a passive continental margin to an active
convergent margin at ca. 450 Ma, proto-Japan has grown asymmetrically oceanward for
nearly 400 km across-arc, through successive subduction of the “Pacific plate,” which
included the Farallon, Izanagi-Kula, Pacific and Philippine Sea plates. It was in the
Miocene that proto-Japan converted to an island arc isolated from mainland Asia
through the opening of the Japan Sea.
At present, Japan is situated at the junction of four distinct plates: the Eurasian,
Philippine Sea, Pacific and North American. The Eurasian plate includes SW Japan
(western Honshu, Shikoku and Kyushu) and the Ryukyu Islands, whereas NE Japan
and Hokkaido together belong to the North American plate. The Philippine Sea plate
is subducting northwestwards at a rate of 4 cm/yr under SW Japan along the Nankai
Trough and Ryukyu trench. The Pacific plate is subducting at a rate of 10 cm/yr
beneath NE Japan, with its leading slab reaching a depth of 660 km under Beijing,
T1b
tapraid4/zqn-ajsc/zqn-ajsc/zqn01010/zqn2165d10a metzgerm S⫽18 3/11/11 16:51 Art:
Implications from a Sr-Nd isotopic study of the Phanerozoic granitoids
1213
China, as revealed by a tomographic study (Zhao and others, 2007; see also a review by
Isozaki and others, 2010). Within the main island (Honshu), NE Japan collided against
SW Japan and formed a high mountain chain (elevation ⬎2000 m) called the “Japan
Alps.” The mountain chain extends across the Honshu arc and is uplifting very rapidly
since 2 Ma (based on our zircon U-Pb and fission track data; Jahn and others, in
preparation). Two of our analyzed granitoid samples reported herein were collected
from the Takidani pluton (or stock) of the Japan Alps (fig. 1).
The predominance of accretionary complexes and the association of detached
continental fragments in Japan suggest that the Japanese Islands have developed
mainly through convergence between oceanic and continental plates along active
margins (Isozaki, 1997; Isozaki and others, 2010). Isozaki (1996) stated that several
major oceanic plates have subducted beneath the South China Block margin, leaving
more than 10 distinct AC (accretionary complex) belts (now reduced to 9 AC belts,
based on the latest reappraisal of the geotectonic framework of Japan, by Isozaki and
others, 2010). All the AC belts occur as thin subhorizontal fault-bounded geologic
bodies, that is, nappes, and show a clear downward and oceanward younging polarity
(Isozaki and Itaya, 1991; Isozaki and Maruyama, 1991). Numerous oceanic fragments
derived from subducted oceanic plates, including deep-sea sediments and seamount
basalts and reef limestone, were accreted to Japan.
In the tectonic evolution of the Japanese Islands, the Permo-Triassic tectonics is
regarded as most important because the basic framework of the Japanese orogenic
belts was established and stabilized at that time (Isozaki, 1996). The occurrence of
Permo-Triassic tectonic units is well developed in SW Japan and the Ryukyu Islands. By
contrast, Permo-Triassic rocks are rarely recognized in NE Honshu and Hokkaido,
except the Hitachi-Takanuki Belt at the southern tip of NE Japan.
Figure 1 shows two major components of the Permo-Triassic orogen in SW Japan:
(1) the accretionary complexes and their high-P metamorphic equivalents, which were
generated by subduction of the Farallon plate, and (2) the continent-continent
collisional orogenic units, as represented by the Hida and Oki belts (Isozaki, 1996,
1997). In the Ryukyu Islands, the high-P metamorphic AC on Ishigaki Island, close to
Taiwan, represents the southwestern extension of the Permo-Triassic accretionary
orogen in SW Japan.
The Median Tectonic Line (MTL) is a prominent strike-slip fault running
through most of SW Japan. It divides SW Japan into two zones: the “Inner Zone” on the
back-arc side, and the “Outer Zone” on the fore-arc side (fig. 1). In the Outer Zone, the
post-Jurassic accretionary complexes are arranged to show oceanward younging from
the Cretaceous to Miocene (Taira and others, 1988), and beyond to the present
accretionary prism at the Nankai Trough. No collision-related Permo-Triassic units
have been identified. The deep parts of the accretionary complexes are exposed as a
low-pressure to high-pressure regional metamorphic belt, which includes the famous
Sanbagawa Belt. The Sanbagawa Belt is generally non-eclogitic and consists mainly of
meta-sedimentary rocks and mafic schists. Most meta-sedimentary rocks are pelitic to
psammistic schists and phylites, with rare metachert (quartz schist) and calcareous
schists. However, several eclogite bodies occur in the Besshi and Kotsu areas on
Shikoku Island (Okamoto and others, 2000; Ota and others, 2004; Utsunomiya and
others, 2011). Conspicuous Miocene granitic rocks also occur on the Pacific side of SW
Japan. These granitoids intrude into the Cretaceous and Tertiary accretionary complexes, and they were likely produced by remelting of the Shimanto accretionary
complex (Stein and others, 1996; Shinjoe, 1997).
In the Inner Zone (fig. 1), Cretaceous to Paleogene granitoids are extensively
distributed. Note that the majority of granitic intrusions were emplaced in the
Cretaceous, and they intruded into the pre-Cretaceous accretionary complexes which
include regional metamorphic rocks. The intrusive granitoids are associated with
F1
60
BJ06-204
R12915
15
1.9
R12911
15
1.9
BJ03-2
BJ06-201a
85
72TO-287
BJ06-202b
85
85
6910-157A
85
6910-105
74
TKM 3
74
74
TKM 2
TKM 6
74
TKM 1
67
64
6911-211
74
64
75T-175A
TKM 4
64
6911-213
TKM 5
72
Age
(Ma)
70N-508
Sample
No.
Hotaka Dake area,
Japan Alps
Hotaka Dake area,
Japan Alps
Kashiwajima, SW
Shikoku
Kashiwajima, SW
Shikoku
Shimanto Belt, S
coast Shikoku
Miyoshi mine area
Kaneishi quarry,
Hirukawa
Odou rive dam-site,
Ohtsu
Misuji water-fall,
Ohtsu
Miyamachi,
Shigaraki-cho
Kouga Golf,
Kozai-cho
Kouga Golf, south
end
Myokanji,
Kozai-cho
Takamatsu-cho,
Okayama
Miyoshi mine
gulch, Okayama
Sosha, Okayama
Matsuda quarry,
Naegi
Iwamoto quarry,
Hirukawa
Shinden, Hirukawa
Locality
Table 1
mélange belt
Takidani
Takidani
S Okayama
S Okayama
S Okayama
S Okayama
Tanakami
Tanakami
Tanakami
Tanakami
Tanakami
Tanakami
Naegi West
Naegi West
Naegi West
Naegi East
Pluton name
or formation
mudstone
gt-bio granite
hb-bio
granodiorite
hb-bio
granodiorite
bio granite
fine biotite
leucogranite
fine biotite
granite
very fine
leucogranite
med. biotite
granite
co. biotite
granite
co. biotite
granite
fine biotite
granite
fine biotite
granite
co. biotite
granite
hb-bio granite
co. biotite
granite
med. biotite
granite
med. biotite
granite
biotite granite
Rock
type
21.6
209
34.9
4.99
7.63
458
137
102.9
126.5
126.2
148
141
295.1
107
80.1 328.3
9.17
10.0
163.2
3.87
3.21
3.38
1.05
0.706
177
122
114
2.62
42.3
7.74
65.9
18.8
209
6.34
188
67.5
77.4
Sr
8.61
86
Rb
87
4.80
101.5
5.40
14.6
12.6
68.5
383
390
148
307
354
260
176
340
223
346
338
335
204
[Rb] [Sr]
(ppm) (ppm)
Sr
137
141
148
12
12
13
11
13
80.1
107
9
8
8
11
16
22
26
458
383
390
148
307
354
260
9
10
340
176
6
7
8
20
9
±2σm
223
346
338
335
Sr
204
86
87
0.71242
0.70797
0.70797
0.70732
0.70748
0.70708
0.70904
0.70998
0.70671
0.71337
0.70849
0.70737
0.71052
0.69855
0.71108
0.70757
0.70853
0.70811
0.70810
I(Sr)
85
86
86
50
83
67
72
97
71
108
64
65
64
73
85
86
87
77
85
68
75
106
71
119
64
66
65
81
4.72
7.13
6.93
6.07
4.03
7.87
7.20
7.29
4.75
6.90
12.60
5.84
6.22
7.60
6.21
9.25
7.18
7.10
7.06
25.49
32.46
30.83
29.52
19.85
22.20
21.80
22.09
21.64
22.29
33.67
22.44
25.92
21.69
24.23
25.47
23.50
23.09
31.94
TM (Ma) [Sm] [Nd]
TM (Ma)
(I = 0.708) (I = 0.707) (ppm) (ppm)
0.1119 0.512329
0.1328 0.512393
0.1359 0.512387
0.1243 0.512469
0.1227 0.512462
0.2132 0.512446
0.1997 0.512427
0.1995 0.512419
0.1327 0.512400
0.1871 0.512147
0.2283 0.512185
0.1572 0.512145
0.1450 0.512048
0.2118 0.512257
0.1548 0.512084
0.2195 0.512223
0.1847 0.512198
0.1858 0.512220
144
Nd
143
Nd
Nd
0.1335 0.512175
Sm
144
147
6
8
12
14
6
5
4
4
5
6
14
6
4
5
5
4
7
4
3
-6.0
-4.8
-4.9
-3.3
-3.4
-3.7
-4.1
-4.3
-4.6
-9.6
-8.8
-9.6
-11.5
-7.4
-10.8
-8.1
-8.6
-8.2
-9.0
-5.4
-4.7
-0.43
-0.32
-0.31
-0.37
-3.3
-4.8
-0.38
0.08
0.02
0.01
-0.33
-0.05
0.16
-0.20
-0.26
0.08
-0.21
0.12
-0.06
-0.06
-0.32
1614
1580
1581
1756
1661
1800
1268
1281
1220
1699
1229
1424
1492
1160
1152
1306
1232
1245
1099
1108
134373 1256
7699
7675
1409
5660
-10456 1694
2696
2433
58909 1557
2743
-26628 1621
4939
5014
1848
TDM-1 TDM-2
f
(Sm/Nd) (Ma) (Ma)
-3.4
-3.9
-4.1
-4.3
-3.9
-9.5
-9.1
-9.2
-11.0
-7.6
-10.4
-8.3
-8.5
-8.1
-8.5
±2σm εNd(0) εNd(T)
1214
Sr-Nd isotopic data of granitoids and sediments of accretionary complexes from SW Japan
tapraid4/zqn-ajsc/zqn-ajsc/zqn01010/zqn2165d10a metzgerm S⫽18 3/11/11 16:51 Art:
Bor-Ming Jahn—Accretionary orogen and evolution of the Japanese Islands—
240
180
BJ06-211
BJ06-212
Shimanto Belt, S
coast Shikoku
Shimanto Belt, S
coast Shikoku
Shimanto Belt, S
coast Shikoku
Shimanto Belt, S
coast Shikoku
Shimanto Belt, S
coast Shikoku
Jurassic AC in
Inuyama
Jurassic AC in
Inuyama
Triassic AC near
Inuyama
Inuyama area,
Aichi Prefecture
Locality
rhythmic
layer
rhythmic
layer
mélange belt
mélange belt
mélange belt
mélange belt
mélange belt
Pluton name
or formation
73.1
siltstone
31.4
409.0
44.8
basaltic sill
35.5
79.1 105.1
82.3
49.0
168.2
mudstone
mudstone
37.5
13.9
red chert
chert
25.8
siltstone
493.5
161
22.5
red chert
siltstone
240.6
[Rb] [Sr]
(ppm) (ppm)
38.7
Rock
type
Sr
86
87
0.723833
0.317 0.708468
0.722299
2.18
0.724548
0.728854
6.71
3.46
0.822 0.709406
0.443 0.708648
0.132 0.706805
6.38
Sr
Sr
0.466 0.708632
86
Rb
87
13
11
10
13
12
15
11
11
11
±2σm
0.70766
0.71486
0.71167
0.71570
0.70871
0.70827
0.70669
0.71839
0.70823
I(Sr)
4.61
6.08
2.66
1.10
1.75
2.12
5.05
4.79
2.80
18.81
28.32
13.29
5.34
7.44
10.93
21.61
23.93
15.17
TM (Ma)
TM (Ma) [Sm] [Nd]
(I = 0.708) (I = 0.707) (ppm) (ppm)
Nd
0.1482 0.512660
0.1298 0.512179
0.1210 0.512447
0.1245 0.512140
0.1422 0.512476
0.1173 0.512452
0.1413 0.512904
0.1210 0.512229
144
143
Nd
Nd
0.1116 0.512296
Sm
144
147
6
12
20
6
8
12
6
6
8
0.4
-9.0
-3.7
-9.7
-3.2
-3.6
5.2
-8.0
-6.7
1.5
-6.9
-2.0
-8.1
-2.7
-3.0
5.6
-7.4
-6.0
±2σm εNd(0) εNd(T)
-0.25
-0.34
-0.38
-0.37
-0.28
-0.40
-0.28
-0.38
-0.43
1139
1759
1155
1722
1435
1103
519
1512
1273
826
1570
1129
1625
1112
1116
426
1478
1358
f
TDM-1 TDM-2
(Sm/Nd) (Ma) (Ma)
(1) Rb-Sr model ages (TM, in Ma) are calculated assuming initial 87Sr/86Sr ratio of 0.708 and 0.707.
(2) The one-stage model age (TDM-1) is calculated assuming a linear Nd isotopic growth of the depleted mantle reservoir from εNd(T) ⫽ 0 at 4.56 Ga to ⫹10 at the
present time.
TDM-1 ⫽ 1/␭ ln[(143Nd/144Nd)s ⫺ 0.51315]/[(147Sm/144Nd)s ⫺ 0.2137]), where s ⫽ sample, ␭ ⫽ decay constant of 147Sm (0.00654 Ga-1). The two-stage model age
(TDM-2) is obtained assuming that the protolith of the granitic magmas has a Sm/Nd ratio (or fSm/Nd value) of the average continental crust (Keto and Jacobsen, 1987).
TDM-2 ⫽ TDM1 ⫺ (TDM1 ⫺ t)(fcc ⫺ fs)/(fcc ⫺ fDM), where fcc, fs, fDM ⫽ fSm/Nd are values of the average continental crust, the sample and the depleted mantle,
respectively.
In our calculation, fcc ⫽ ⫺0.4 and fDM ⫽ 0.08592 are used, and t ⫽ the intrusive age of granite. To obtain meaningful model ages, TDM were calculated for samples
with f(Sm/Nd) ranges from ⫺0.2 to ⫺0.6 (Wu and others, 2002).
co ⫽ coarse, med ⫽ medium, hb ⫽ hornblende, bio ⫽ biotite, gt ⫽ garnet.
180
60
BJ06-208
180
60
BJ06-207b
BJ06-209
60
BJ06-210
60
BJ06-206
60
BJ06-205
BJ06-207a
Age
(Ma)
Sample
No.
Table 1
(continued)
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Bor-Ming Jahn—Accretionary orogen and evolution of the Japanese Islands—
Granitoid
Accretionary complex
Metamorphic belt
Hida
Tertiary
Cretaceous - Tertiary
Jurassic - Cretaceous
Cretaceous
Jurassic - Cretaceous
Pre-Jurassic
Jurassic
Pre-Jurassic
4
1
ultramafic rock
6
11
Sedimentary rock
Cenozoic volcanic rock
2
Oki
12
n
Sani
Cretaceous volcanic rock
5
San
yo
Takidani
8
ke
o
Ry
12
7
10
6
8
3
8
8
MTL
9
200 km
Kashiwajima
Fig. 1. General geologic map of SW Japan. The Median Tectonic Line (MTL) separates the granitoiddominated terrane to the north from the Mesozoic-Cenozoic accretionary wedge to the south. The granitoid
terrane is divided into three granitic belts (Ryoke, Sanyo and Sanin) based on the type of mineral deposits
and oxygen fugacity (Ishihara, 1971). New isotopic analyses were done on granitic rocks from the Sanyo Belt,
a small granite pluton (or plug) at Kashiwajima on SW Shikoku Island, and the Takidani granodiorite of the
Japan Alps. Their localities are given in table 1. The numerals in yellow circles correspond to the following
literature data sources with the localities of study areas given in Appendix 1: (1) Arakawa (1990), Arakawa
and Shimura (1995), (2) Arakawa (1989), Arakawa and Shimura (1995), (3) Fujii and others (2000), (4)
Iizumi and others (2000), (5) Ishioka and Iizumi (2003), (6) Kagami and others (1992), (7) Kagami and
others (2000), (8) Morioka and others (2000), (9) Nakajima and others (2004), (10) Shinjoe (1997), (11)
Takagi and Kagami (1995), (12) Terakado and Nohda (1993).
coeval rhyolites and ignimbrites even though much of this cover series has been
eroded to expose the intrusive rocks. In addition, a few collisional belts, or nonaccretionary units (Hida and Oki belts, fig. 1), occur in the northern part, and they are
composed of polymetamorphic gneiss and schist complexes, with Triassic (230 Ma)
regional metamorphism of intermediate pressure facies (Komatsu, 1990).
Ishihara (1971) made a detailed study of the granitoids and associated ore
deposits. He divided the Inner Zone into three metallogenic provinces, from south to
north, a Barren, a Tungsten, and a Molybdenum Province (see also Ishihara and
Murakami, 2006). The three provinces correspond to the Ryoke, Sanyo and Sanin Belts
as delineated by Murakami (1974) on the basis of granite petrography and age data.
Subsequently, in a study of opaque mineral in the granitoids, Ishihara (1977) classified
the Sanin Belt as belonging to the magnetite-series, whereas the two other belts belong
to the ilmenite-series. The magnetite-series rocks contain higher Fe2O3/FeO ratios
than the ilmenite-series rocks.
The lithological types in the Inner Zone are more extensive than granitoids and
acid volcanic rocks alone. In fact, the Ryoke belt is a plutonic-metamorphic terrane
that comprises unmetamorphosed pre-Cretaceous accretionary complexes with highlevel granites, as well as high-grade, but low P/T, metasediments with migmatites and
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gneissic granites. Granitic rocks are dominant over metamorphic rocks. Based on the
apparent along-arc variation of isotopic ages, it has been suggested that the Ryoke and
Sanyo granitoids were produced by Cretaceous subduction of the Kula-Pacific ridge
and that the magmatism migrated eastward with passage of the ridge along the SW
Japan margin (for example, Nakajima, 1994). However, such eastward migration of
magmatic activities has not been verified.
Isozaki and others (2010) described that the continental side of the MTL (⫽ Inner
Zone) is composed of a 15 km-thick lower crust of unknown composition, a 20
km-thick granitic upper crust and thin roof-pendants of Paleozoic to Jurassic AC
(⫹meta-AC) units at the surface. These AC units are characterized by subhorizontal
stacks of multiple fault-bounded units, previously recognized as “nappes,” with a gentle
dip towards the Eurasian continent.
sample descriptions
In this paper new Sr-Nd isotopic analyses (table 1) of samples, including granitoids, siltstones and cherts, are used in graphic representations. The collection of these
samples was not systematic and different samples serve different purposes. The new
data only supplement the existing large dataset in the literature used in this paper (see
Appendix 1). The granitic rocks were collected by S. Ishihara from four plutons (Naegi
East, Naegi West, Tanakami, and S. Okayama) of the Sanyo Belt, SW Japan. The age
information was obtained from the literature. The Naegi granites were dated at 64 to
72 Ma (K-Ar mineral ages) by Ishihara and others (1988). The Tanakami granites have
K-Ar biotite ages of 73.3 and 74.7 Ma for the central part, but 67.9 Ma for the eastern
part of the pluton (Sawada and Itaya, 1993). For the granites of the Okayama area, a
muscovite greisen from the Miyoshi mine was dated at 86.6 Ma by the K-Ar method
(Ishihara and others, 1988), whereas a whole-rock Rb-Sr isochron age of 84 Ma was
obtained for the southern Okayama batholith (Kagami and others, 1988).
Two hornblende-biotite granodiorite samples from the Takidani pluton of the
Japan Alps and two biotite granites from the Kashiwajima pluton of SW Shikoku were
also analyzed. The emplacement ages of these granitoids have been firmly established
at 1.9 Ma for Takidani and 15 Ma for Kashiwajima by the SHRIMP zircon U-Pb method.
The complete geochronological data (zircon U-Pb, zircon fission-track, biotite and
K-feldspar Ar-Ar) will be reported in another paper (Jahn and others, in preparation).
The Takidani pluton is the youngest plutonic intrusive in the world. In addition,
sedimentary rocks from the Shimanto Belt and a Jurassic to Triassic accretionary
complex (Inuyama area) were also included for analysis. This was to test the source of
the sediments from the “ocean plate stratigraphy,” long considered to be the principal
component of the accretionary complexes of Japan.
sr-nd isotope data
For the new samples, Sr and Nd isotopic compositions were analyzed at the
University of Rennes 1 (France) and the Institute of Earth Sciences, Academia Sinica
(Taiwan). In both laboratories the analyses were performed using two similar Finnigan
MAT-262 Thermal Ionization Mass Spectrometers (TIMS). Mass fractionation was
corrected against 86Sr/88Sr ⫽ 0.1194 and 146Nd/144Nd ⫽ 0.7219. All isotopic ratios
were finally adjusted against the standard salts of NBS-987 Sr ⫽ 0.710250 and La Jolla
Nd ⫽ 0.511860. The in-run precisions as shown in the analytical tables are expressed as
2 standard errors (2 sigma-mean), and they are approximately equal to 0.1 epsilon
unit. However, the external precisions based on long-term duplicate analyses on
standard salts yielded about 0.4 epsilon unit.
All the new and literature Sr-Nd data used in the present paper are summarized in
Appendix 1 and further illustrated in figures 2, 3, 4 and 5. Figure 2 shows a plot of
initial 87Sr/86Sr ratios as a function of intrusive ages of granitoids and depositional ages
of sedimentary rocks (siltstone and mudstone). The new data for granitoids are
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Fig. 2. Initial Sr isotopic ratios (⫽ISr) of granitoids and sedimentary rocks of two accretionary
complexes from SW Japan. A line at ISr ⫽ 0.705 is drawn for reference. Granitoids with ISr lower than this line
are considered “juvenile” and those with values higher than 0.710 are mainly “recycled.” The proportion of
the recycled crustal component increases with increasing ISr values. Data sources: New data (table 1); Kagami
and others (1992, 1995), Terakado and Nohda (1993), Arakawa and Shinmura (1995), Stein and others
(1996), Shinjoe (1997), Ishioka and Iizumi (2003), Takagi (2004). All the data used in this figure can be
found in table 1 and Appendix table.
expressed as solid red circles (Sanyo belt and Takidani granodiorite of the Japan Alps)
and solid yellow circles (Kashiwajima, Shimanto belt, SW Shikoku). The new analyses
of siltstones and cherts from the accretionary complex are shown with solid blue and
green circles. The rest are literature data. Based on the dataset of 565 analyses,
important points can be outlined as follows: (1) All granitoids are younger than 250
Ma, but the majority of them were emplaced in the Cretaceous (145-65 Ma); Triassic
and Jurassic granites are relatively rare. (2) Most granitic rocks are characterized by
initial 87Sr/86Sr ratios higher than 0.705, which is a value typically observed for
granitoids of the Central Asian Orogenic Belt (for example, Jahn, 2004). (3) Granitoids with initial 87Sr/86Sr ratios lower than 0.705 are mainly from the Jurassic Hida
Belt (185-190 Ma), or were emplaced in the Early Cretaceous (140-100 Ma) and
Cenozoic (50-10 Ma). The low ratios suggest that these granitic rocks were likely
produced by remelting of mantle-derived rocks (gabbros), or a lithological assemblage
containing a large proportion of mantle component (accreted ocean plate stratigraphy). (4) The high initial 87Sr/86Sr ratios (ISr value) indicate that the generation of
granitic rocks must have involved a participation of much older rocks. That is, a
significant proportion of Precambrian crust is required in the source regions for the
generation of these granites. Although no Precambrian rocks have been identified in
Japan, the presence of protoliths with Precambrian heritage in the middle to lower
crust is strongly implied.
Figure 3 illustrates the variation of initial 143Nd/144Nd ratios, expressed as εNd(T)
values, in the granitic rocks of different ages. Note that the number of data points
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Fig. 3. Nd isotopic compositions of granitoids and sedimentary rocks from SW Japan. “Juvenile”
granitoids are generally characterized by positive εNd(T), whereas granitoids of recycled origin have negative
values. Samples show negative values as low as ⫺15. Data sources: New data (table 1), Kagami and others
(1992, 1993), Arakawa and Shinmura (1995), Stein and others (1996), Shinjoe (1997), Ishioka and Iizumi
(2003), Takagi (2004).
(235) is reduced to about a half of the Sr isotope data. However, the distribution of
data points, with respect to the reference line of εNd(T) ⫽ 0, form an impressive mirror
image of the Sr isotope data (fig. 2). The majority of the data points show negative
values. Granitic rocks with a large proportion of mantle component are expected to
have positive εNd(T) values, as commonly observed in granitoids of the CAOB or ANS
(see later sections), but this is not the case for SW Japan. The scenario shown in figure
3 indicates that most of the granitic rocks were derived by melting of protoliths with a
large proportion of recycled crust of Precambrian age.
εNd(T) and ISr values are commonly anti-correlated in most rocks. Figure 4 shows
that the majority of granitoids from SW Japan fall in the fourth quadrangle of the
εNd(T) vs (87Sr/86Sr)o (⫽ISr) diagram, which is segmented by two reference lines—a
horizontal zero εNd(T) line (or CHUR, Chondritic Uniform Reservoir) and a vertical
line of ISr ⫽ 0.7045 for Earth’s primitive mantle (PM). The data array is very similar to
that commonly observed for crustal rocks. Most mantle-derived mafic rocks and
“juvenile” granitoids would reside in the second quadrangle, but only a few granitoids
of SW Japan are found there. Granitoids of the Hida Belt are distinguished from the
bulk of the Japanese granitic rocks and have Sr-Nd isotope compositions close to the
reference point of the primitive Earth (⫽ intersection of the two reference lines).
The Sr-Nd isotopic characteristics of the Japanese granitoids indicate that they
had a long crustal residence time. Figure 5 shows a plot of εNd(T) vs depleted-mantle-
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Fig. 4. εNd(T) vs (87Sr/86Sr)o plot for granitoids and sedimentary rocks from SW Japan. The majority of
granitoid data points fall in the fourth quadrangle, suggesting their “recycled” nature. Data sources as in
figure 3.
based single-stage and 2-stage model ages (TDM-1 and TDM-2). The reason for using the
2-stage model age calculation is that some of the new analyses were obtained on highly
differentiated granitic rocks with the lanthanide tetrad effect, which often leads to
aberrant very large or negative model ages due to the increase of Sm/Nd ratios in the
final stage of differentiation (Jahn and others, 2001). In figure 5, while the intrusive
ages of the granitoids are younger than 250 Ma (shown by the yellow band), their
model ages are much older, from ca. 700 to over 2000 Ma. This suggests that the
protoliths of the granitoids contain a significant proportion of Precambrian crust. The
scenario is much the same as that for the Cenozoic sedimentary rocks of Taiwan, to be
illustrated in a later section.
discussion
Together with the Japanese Islands, the Central Asian Orogenic Belt (CAOB) and
the Arabian-Nubian Shield (ANS) are three well-known “young” accretionary orogens
formed in the Neoproterozoic or later. Therefore, a comparison between the three
accretionary orogens in terms of their crustal development could be instructive.
Numerous Sr-Nd isotopic analyses have confirmed that much of the crustal mass of the
CAOB and ANS is juvenile, produced by melting of accreted island arc assemblages.
The process may include melting of mantle peridotites (for basalts and andesites),
remelting of mantle-derived basaltic and andesitic rocks, and/or fractional crystallization of basaltic and andesitic magmas (for granitoids). Juvenile crust has substantially
contributed to the growth of the continent in the CAOB and ANS (Sengor and others,
1993; Stern, 1994, 2002, 2008; Jahn and others, 2000a, 2000b; Jahn, 2004; Kovalenko
and others, 2004; Eyal and others, 2010).
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Fig. 5. εNd(T) vs TDM (depleted-mantle-based model ages) plot for granitoids from SW Japan. Because
some granites show the REE tetrad effect, which produced aberrant age values in the single-stage TDM
calculation, the 2-stage model ages (TDM-2) values for the granitoids are also calculated for comparison
(inset). The figure shows that TDM ranges from ca. 700 to 2000 Ma, except for the granitoids of the Hida Belt.
Data sources as in figure 3.
Comparison with the CAOB
The Central Asian Orogenic Belt (CAOB) covers an immense surface area (ca. 5.3
million km2) and spans from the Urals in the west to the Pacific coast in the east. It
represents about 11 percent of Asia. NE China is also included even though most of it
has been named as the “Manchurides” by Sengor and Natal’in (1996). The Nd isotopic
characteristics of granitoids from the different terranes of the CAOB are summarized
and illustrated in figure 6.
NE China and Inner Mongolia.—In NE China, more than 350 granitic bodies were
emplaced in the Great Xing’an (or Khinggan), Lesser Xing’an and Zhangguangcai
Ranges, and mostly during Mesozoic times (Wu and others, 2011). The granites are
composed mainly of I-type and subordinate A-type granites (Wu and others, 2000,
2002, 2003a, 2003b). They are accompanied by extensive Mesozoic and Tertiary acid
volcanic rocks. Isotope tracer analysis and age determination of deep-drill cores from
the Songliao Basin in central NE China revealed that the Basin is underlain by granitic
rocks and deformed granitic gneisses of Phanerozoic age (Wu and others, 2001).
Precambrian zircons have been identified, but they are substantially rarer (Wu and
others, 2011). Based on the time-space distribution of the granitic rocks, Wu and
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15
15
A
NE China
I nner M ongolia
Hida B elt, J apan
Depleted mantle
10
5
5
CH UR
0
ε Nd(T )
εNd(T )
K azakhstan
X injiang - A ltai M tns
X injiang -J unggar
X injiang - A latau M tns
Depleted mantle
10
-5
E ar ly-middle
P roter ozoic crust
-10
CH UR
0
-5
E ar ly-middle
P roterozoic crust
-10
-15
B
-15
-20
-20
Ar chean crust
-25
0
100
200
300
400
500
600
700
800
Ar chean cr ust
-25
900 1000
0
100
200
300
Intr usive Age (M a)
15
Depleted M antle
10
400
500
600
700
800
900 1000
Intr usive Age (M a)
15
C
10
Post-collisional granites (CAOB) D
Depleted Mantle
5
CH UR
0
-5
ε Nd(T)
ε Nd(T )
5
E ar ly-middle
P roter ozoic crust
0
-10
-10
-15
-15
C aledonides
Hercynides
Pr e-Riphean (in Caled)
Pr e-Riphean (in Hercy )
-20
-25
0
100
200
300
400
CHUR
-5
Early-middle
Proterozoic crust
NE China
East Junggar
Inner Mongolia
Transbaikalia
W Altai-Sayan
Ar chean crust
-20
Archean crust
Data: Kovalenk o and others (1996)
500
600
700
Intr usive Age (M a)
800
900 1000
-25
100
150
200
250
300
350
400
450
500
Intrusive Age (Ma)
Fig. 6. εNd(T) vs. intrusive ages of granitic rocks from the Central Asian Orogenic Belt. Data sources:
(A) NE China (Wu and others, 2000, 2002; Jahn and others, 2001), Inner Mongolia (Chen and others,
2000), and Hida Belt (Arakawa and Shimura, 1995; Arakawa and others, 2000). (B) Kazakhstan (Heinhosrt
and others, 2000; Kröner and others, 2008), Xinjiang—Altai Mountains (Zhao and others, 1993; Wang and
others, 2009), Junggar (Han and others, 1997; Chen and Jahn, 2002), Alatau (Zhou and others, 1995). (C)
Data for Mongolia and Transbaikalia (Kovalenko and others, 1996, 2004). (D) Post-collisional granites (NE
China: Wu and others, 2002; East Junggar: Chen and Jahn, 2002; Inner Mongolia: Hong and others, 1996;
Jahn, unpublished; Transbaikalia: Jahn and others, 2009; western Sayan-Gorny Altai: Kruk and others, 2001).
others (2011) suggested that the Jurassic granites in the Zhangguangcai Range were
probably related to Paleo-Pacific plate subduction, whereas the Early Cretaceous
granites in the Great Xing’an Range resulted from delamination or extension of the
previously thickened lithosphere.
In Inner Mongolia, several periods of granitic intrusion took place from Devonian
to Jurassic times. The samples used in this study came from a Paleozoic anorogenic
A-type suite (280 Ma; Hong and others, 1995, 1996), an arc-related calc-alkaline
magmatic belt composed of gabbroic diorite, quartz diorite, tonalite and granodiorite
(SHRIMP zircon age ⫽ 309 ⫾ 8 Ma, Chen and others, 2000) and a Mesozoic
collision-type granitic suite comprising monzogranite (adamellite), granodiorite and
leucogranite (Rb-Sr isochron age of 230 ⫾ 20 Ma; Chen and others, 2000).
Figure 6A shows that the majority (75%) of the samples have positive εNd(T)
values. Most of the samples with negative εNd(T) values came from the Precambrian
Jiamusi Massif (εNd(200 Ma) ⫽ ⫺7 to ⫺12). Such a close relationship between the
isotopic compositions of granitoids and the ages and nature of their intruded “basement” rocks is also demonstrated by the granitoids from northern Xinjiang (Hu and
others, 2000) and Mongolia (Kovalenko and others, 1996, 2004; Jahn and others,
2004). The lowering of the εNd(T) values was effected by the participation of old crustal
rocks in their magma genesis.
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Xinjiang and Kazakhstan.—A variety of Phanerozoic granitoids occur throughout
northern Xinjiang. As for the case of NE China, the majority of granitoids have positive
εNd(T) values which suggest a dominance of the mantle component in the generation
of these rocks (fig. 6B). This is particularly true for the granitoids from the E and W
Junggar terranes (Zhao and others, 1993; Han and others, 1997; Chen and Jahn,
2004). The Junggar Basin is covered by Cenozoic desert sands and thick continental
basin sediments (ⱖ10 km) of Permian and younger ages. Drilling records indicate
little deformation within the basin, suggesting stability of the basement at least since
the Permian (Coleman, 1989). The nature of the Junggar basement has been much
debated; some consider that it represents a micro-continent with Precambrian basement (Wu, 1987), whereas others regard it as trapped Paleozoic oceanic crust of
various origins (Feng and others, 1989; Hsü, 1989; Coleman, 1989; Carroll and others,
1990). Surrounding the Junggar Basin are exposed numerous ophiolites in the East
and West Junggar terranes, as well as in its southern margin. These terranes can be
appropriately referred to as “island-arc assemblages,” and no rocks of Precambrian age
have been documented. Coleman (1989) considered these terranes as oceanic arc
assemblages, and compared them with those in the present western Pacific. Based on a
trace-element and Sr-Nd isotopic study, Chen and Jahn (2004) concluded that the
basement is most likely underlain by Early to Middle Paleozoic arc rocks and oceanic
crustal assemblages that were trapped during the Late Paleozoic tectonic consolidation
of Central Asia. This is consistent with the very young model ages ranging from 400 to
1000 Ma (400 to 600 Ma in a two-stage model) for the Junggar granites (fig. 6B).
Also shown in figure 6B, the granitoids emplaced in the Chinese Altai composite
terrane show a wide range of isotopic composition and model ages (Hu and others,
2000; Wang and others, 2009). A tight relationship between the isotopic compositions
of granitoids and the nature of their basement rocks can be established. The Sm-Nd
isotope study by Hu and others (2000) revealed that the basement rocks of the Altai
and Tianshan were largely produced in the Proterozoic. The parallel manifestation of
isotopic compositions and model ages between basement rocks and intrusive granites
argues for the significant role of crustal “contamination” in the genesis of the
Phanerozoic granitoids. An implication is that the presence of old Precambrian
microcontinents is significant in the accretionary history of Central Asia (Kröner and
others, 2007). A more quantitative study on the proportion of the mantle component
in the crust of the Altai Mountains was presented by Wang and others (2009).
Heinhorst and others (2000) undertook a comprehensive study of mineralization
in association with a variety of magmatic rocks in east-central Kazakhstan. Although the
types of mineralization (Au, Cu, rare-metal, or REE) may be related to a particular
magmatic suite or a lithological variety, most granitic rocks have positive εNd(T) values
irrespective of their bulk compositions and types of mineralization (Heinhorst and
others, 2000). The granitoids were intruded in several episodes: 450 and 300 Ma for
magmatic suites with gold mineralization, about 300 Ma for granitoids with rare-metal
mineralization, and ca. 250 Ma for A-type granites with REE mineralization. There is a
slight tendency for an increase of εNd(T) with younger ages of the rocks. Single-stage
model ages for all cases are between 400 and 1500 Ma.
Mongolia and Transbaikalia.—Figure 6C shows the Nd-Sr isotopic compositions of
granitoids from the northern belt of central Mongolia to Transbaikalia. This area has
been extensively studied by Kovalenko and others (1996, 2004). These authors
delineated four isotope provinces (Precambrian, “Caledonian,” “Hercynian,” and
“Indonesian”), which coincide with three tectonic zones of corresponding ages for the
northern belt of the CAOB, and with one (Indonesian) in Inner Mongolia and NE
China (Kovalenko and others, 2004).
The Transbaikalian and northern Mongolian terranes roughly correspond to the
“Barguzin” belt and “Caledonides” of Kovalenko and others (2004). The Baydrag
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Bor-Ming Jahn—Accretionary orogen and evolution of the Japanese Islands—
terrane is the only early Precambrian microcontinent containing granulitic and
amphibolitic gneisses of Archean age. The Barguzin Belt and the Hangay-Hentey Basin
are known to be “composite” terranes comprising Proterozoic and Phanerozoic
formations. The Hangay-Hentey Basin is intruded by impressive amounts of Early
Palaeozoic to Mesozoic granitoids. The granitoid belt extends to Transbaikalia and
further to the Sea of Okhotsk.
As shown in figure 6C, the Phanerozoic granites emplaced into “Caledonian” and
“Hercynian” provinces have positive εNd(T) values, suggesting their juvenile characteristics, whereas those intruded into the Baydrag and the composite terranes (Barguzin
and Hangay-Hentay) show εNd(T) values from positive to negative, indicating variable
contributions of Precambrian crust in the generation of the granitic rocks. Note that
some Late Neoproterozoic to Early Palaeozoic granites (600-500 Ma) have εNd(T)
values as high as ⫹10, suggesting their derivation from an almost pure depleted mantle
component (⫽100% basaltic and/or andesitic source).
Most plutons and batholiths of the CAOB have calc-alkaline characteristics typical
of subduction zone magmatism, but the emplacement of voluminous granites of the
alkaline and peralkaline series also deserves attention. Petrogenetically, these rocks are
akin to the A-type granites, which are generally known to form in post-collisional
extensional environments (for example, Jahn and others, 2009). Figure 6D summarizes the isotopic characters of this kind of granite from the CAOB. The majority of
these rocks possess positive εNd(T) values; only a few show negative values. All of them
have young model ages (TDM) from 500 to 1300 Ma. This indicates that the source of
post-accretionary granitoids in the CAOB is dominated by the mantle-derived component.
Comparison with the ANS
The Arabian-Nubian Shield (ANS) is well-known as one of the best examples for
crustal growth in the Neoproterozoic. The crust of the ANS is essentially juvenile
formed by protracted accretion of island arc terranes (Bentor, 1985; Stern, 1994, 2002;
Stein and Goldstein, 1996; Meert, 2003; Jarrar and others, 2003; Johnson, 2003;
Johnson and Woldehaimanot, 2003; Stoeser and Frost, 2006; Stern and others, 2010).
Island arc accretion is thought to have ended in the ANS by ⬃700 Ma and was followed
by continental collision at 640 to 650 Ma (Stern, 1994, 2002, and references therein).
The Late Neoproterozoic post-collisional stage of tectonomagmatic evolution of the
ANS commenced at ⬃640 Ma. Transition from collision to extension occurred at ⬃600
Ma (Stern, 1994; Garfunkel, 1999; Genna and others, 2002; Jarrar and others, 2003)
and was finally followed with a stable craton and platform setting (Garfunkel, 1999).
The evolution of the ANS (⬃820 to 570 Ma) involved vast amounts of granitoid
magmatism, thought to be well correlated with the changing tectonic setting (Bentor,
1985; Stern and Hedge, 1985; Bentor and Eyal, 1987; Kröner and others, 1990; Stern,
1994; Garfunkel, 1999; Moghazi, 1999, 2002; Jarrar and others, 2003, 2008; Johnson,
2003; Johnson and Woldehaimanot, 2003; Katzir and others, 2007b; Stern and others,
2010). Four stages of magmatic activity are recognized: (1) island arc magmatism
including early medium-K calc-alkaline plutons (now gneisses) and metavolcanic rocks
occurred at ⬃820 to 740 Ma; (2) late syn-collisional medium- to high-K calc-alkaline
granitoids and gabbro that bear evidence for penetrative deformation and low-grade
metamorphism intruded at ⬃670 to 635 Ma; (3) the most voluminous post-collisional
(undeformed) high-K calk-alkaline gabbro-granodiorite-granite suite formed at ⬃640
to 610 Ma; and (4) within-plate alkaline and peralkaline granite suites preceded by
intensive bimodal volcanism at ⬃600 to 550 Ma.
Eyal and others (2010) recently conducted a petrological and geochemical study
of 27 calc-alkaline and alkaline plutons/complexes and one dike swarm from the Sinai
Peninsula, in the northern part of the ANS. Granites of the alkaline suite were studied
in 16 plutons ranging in size from 1 to 400 km2, some of which are central plutons in
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ring complexes. The most celebrated example is the Katherina ring complex (Katzir
and others, 2007a), in which granite is intrusive into volcanic rocks and ring dikes and
often shows miarolitic texture, indicating crystallization at shallow depth. The majority
of alkaline plutons are composed of syenogranite, alkali feldspar granite and peralkaline granite.
The granitoids from the northern ANS were emplaced during the period of ca.
750 to 550 Ma. The available Sm-Nd isotope data indicate that all the rock types are
characterized by positive εNd(T) values with no exception (figs. 7A, 7B, 7C, and 7D).
Two-stage model ages vary from ca. 860 to 1200 Ma for the calk-alkaline suite, and from
ca. 800 to 1100 Ma for the alkaline suite. Single-stage model ages are quite similar to
the two-stage model ages, suggesting that fSm/Nd values for most rocks are close to that
of the average continental crust (ca. ⫺0.4). The Nd model ages suggest that little
Archean or early Proterozoic rocks exist in the lower to middle crust of the northern
ANS. This inference is supported by the U-Pb dating of individual zircon grains from
various plutonic rocks (Be’eri-Shlevin and others, 2009). The petrogenesis and sequence of emplacement for the alkaline and post-collisional granitoids from the Sinai
Peninsula have been discussed in detail by Eyal and others (2010).
Comparison Between Japan, CAOB and ANS
The distinction in Nd isotopic composition between the granitoids formed in the
three classic accretionary orogens (Japan, CAOB, and ANS) is clearly demonstrated.
The entirely positive εNd(T) values for the ANS granitoids suggest that they were
produced by partial melting of mantle-derived protoliths with little contribution from
much older rocks. More specifically, granitoids were generated by differentiation of
mantle-derived dioritic magma in the early stage of arc formation; by remelting of
mantle-derived arc rocks in later stages, with only very small amounts of PreNeoproterozoic crustal component; and by remelting of underplated basic rocks in
post-orogenic stages.
The dominance of positive εNd(T) values for the CAOB granitoids indicates that
most granitoids are “relatively juvenile,” and that others have witnessed a greater
contribution from Archean to early Proterozoic micro-continents, hence producing
granitoids with negative εNd(T) values. By contrast, the granitoids from SW Japan have
dominantly negative εNd(T) values and relatively high initial 87Sr/86Sr ratios (⬎0.707),
suggesting involvement of a significant amount of recycled crustal rocks. Their
formation and emplacement in Japan do not imply a net growth of the continental
crust. If the granitoids were derived by partial melting of accreted terranes, it suggests
that the essential component of the accreted material is recycled crust of ultimately
Precambrian derivation. In fact, abundant clasts of Proterozoic granites and gneisses
(up to 1.8 Ga of age) were found in the Jurassic conglomerate of the Mino-Tanba
accretionary complex (Shibata and Adachi, 1974). Maruyama (1997) hypothesized
that the most important cause of the orogeny in SW Japan is the subduction of an
oceanic ridge, by which the continental mass increases through the transfer of granitic
melt from the subducting oceanic crust to the orogenic belt. The present analysis of
Sr-Nd isotopic data does not support such a hypothesis.
Comparison with SE China and Taiwan
While the Nd isotopic characteristics of the Japanese accretionary orogen can be
distinguished from those of the CAOB and ANS, they are surprisingly comparable with
that of well-known “collisional orogens,” such as the Caledonides and Hercynides of
western Europe (Jahn and others, 2000a, 2000b; Jahn, 2004), the Paleozoic to
Mesozoic orogens of SE China, and the Cenozoic orogen of Taiwan. Chen and Jahn
(1998) made a synthesis of the crustal evolution in SE China based on extensive Nd
and Sr isotopic data compiled from the pre-1998 literature for intrusive granitoids,
volcanic, sedimentary and metamorphic rocks from three major tectonic units of SE
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12
10
8
Southern Israel
6
εNd(T)
A
DM
Elat schists
4
2
granitic gneisses
0
CHUR
-2
-4
Granitoids & rhyolites
Mafic dikes and trachydolerites
Elat schists
-6
-8
-10
0
100
200
300
400
500
600
700
800
900
1000
Age (Ma)
12
10
8
Southwestern Jordan
6
εNd(T)
B
DM
Araba Complex
4
Aqaba Complex
2
0
CHUR
-2
-4
Granitoids of Aqaba Complex
A-type granites - Humrat-Feinan suite
Monzogabbro, monzodiorite, Q monzodiorite
-6
-8
-10
0
100
200
300
400
500
600
700
800
900
1000
Age (Ma)
Fig. 7. εNd(T) vs. intrusive ages of granitic rocks from the northern part of the Arabian Nubian Shield.
(A) Southern Israel (Data sources: Beyth and others, 1994; Stein and Goldstein, 1996; Mushkin and others,
2003). (B) SW Jordan (Jarrar and others, 2003).
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10
Sinai Peninsula
Egypt
8
6
εNd(T)
C
DM
4
2
0
CHUR
-2
-4
Granitoids of Katherina Complex
Granitoids - Kid area (SE Sinai)
Syenogranites - Kid area
-6
-8
-10
0
100
200
300
400
500
600
700
800
900
1000
Age (Ma)
12
10
Eastern Desert
Egypt
8
6
εNd(T)
D
DM
4
2
0
CHUR
-2
Granites - Wadi El-Imra district
Gabbro-diorite complex Wadi El-Imra district
Granitoids - Gebel El-Urf area
-4
-6
-8
-10
0
100
200
300
400
500
600
700
800
900
1000
Age (Ma)
Fig. 7. (continued) (C) Sinai Peninsula (Katherina Complex: Stein and Goldstein, 1996; Katzir and
others, 2007a, 2007b; Eyal and others, 2010. Kid area, SE Sinai: Moghazi and others, 1998). (D) Eastern
Desert (Wadi El-Imra: Furnes and others, 1996; Gebel El-urf area: Moghazi, 1999). Data compilation by Boris
Litvinovsky.
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Fig. 8. (A) εNd(T) vs. intrusive age plot of granitic rocks from the South China Block (Yangtze and
Cathaysia). Data sources: Chen and Jahn, 1998 and references therein; additional data from Hsieh and
others (2008), Jiang and others (2009), Li and others (2007), Wan and others (2010), Wang and others
(2007), Yu and others (2007). (B) εNd(T) vs. model age plot of granitic rocks from South China Block. Data
sources as for (A).
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1229
China: Dabie, Yangtze and Cathaysia. In the present compilation, literature data
published since 1999 are included with the pre-1998 data. The combined data are
illustrated in figure 8. Phanerozoic granitoids from SE China were emplaced from
about 470 to 80 Ma, and are characterized by negative εNd(T) values from ⫺17 to about
0, with a few exceptions (fig. 8A). The granitoids have depleted-mantle-based model
ages (TDM) of 500 to 2800 Ma, but are mainly in the range of 1000 to 2200 Ma (fig. 8B).
The model age data indicate that the most important crustal formation events took
place in the Proterozoic, possibly with a very minor proportion produced in the Late
Archean. I defend this statement even though an increasing number of Archean zircon
grains have been identified in recent years in the Yangtze craton (for example, Zheng
and others, 2006; Zheng and Zhang, 2007). In summary, the crustal evolution in SE
China, including the Yangtze Craton and Cathaysia, is distinctly different from the
Archean-dominated North China Block (Chen and Jahn, 1998). Interestingly, the
ranges of εNd(T) and TDM are very similar to those of the Hercynian and Caledonian
belts in Europe (Jahn and others, 2000a, 2000b; Jahn, 2004).
The island of Taiwan is geologically young. The oldest rocks are the marble
sequences from the Tanan’ao Complex in the east and from the “Peikang High” in the
west of the island, which were dated at about 250 Ma using their Sr isotopic compositions and the Pb-Pb isochron technique (Jahn and others, 1992). Granitic intrusions
are rare. A few small plutons of Cretaceous granitoids were emplaced in the Tanan’ao
Complex, whereas a small Jurassic granite stock occurs within the schist belt of the
southern Central Range (Yui and others, 2009). The mountain belts were formed by
the collision between the Eurasian and the Philippine Sea plates. A close geological
correlation between Taiwan and SE China has long been established using geochronological and geochemical data of the Mesozoic granitoids and the Late Permian
carbonates (Jahn and others, 1986, 1990, 1992; Lan and others, 1996, 1997, 2002, 2008;
Chen and Jahn, 1998; Yui and others, 2009).
Figure 9 summarizes the Nd isotopic composition and model ages of granitoids
and metasedimentary rocks from Taiwan. The main figure is a plot of εNd(T) vs
one-stage model age (TDM-1), whereas the inset is a plot of εNd(T) vs two-stage model
age (TDM-2). In both representations, the εNd(T) values are shown to vary from zero to
⫺16, except for four analyses of the Early Jurassic granites (191 Ma) from Taiwan (Yui
and others, 2009). Single-stage model ages vary from 700 to 2000 Ma. This scenario is
surprisingly similar to that of SW Japan (fig. 5). The Sm-Nd isotopic data of sedimentary rocks from Japan and Taiwan are shown in figure 10 for comparison. In this figure,
lines radiating from the depleted mantle reference point (DM) represent calculated
model ages (TDM). The model ages of sediments from Taiwan range from ca. 1200 to
2300 Ma, whereas those from Japan show a wider range from 700 to 2600 Ma. The
younger model ages of Japan indicate that these sedimentary rocks contain a higher
proportion of the mafic component from the “ocean plate stratigraphy.” Nevertheless,
the dominance of model ages between 1200 to 2500 Ma suggests that the sedimentary
rocks represent recycled Precambrian protoliths. Note that recent zircon geochronology of the Cenozoic sedimentary rocks in Taiwan has revealed many zircon grains of
Archean age (Shao and others, 2010). In fact, the Cenozoic accretionary wedge of
Taiwan is dominated by sediments of Cathaysian derivation.
tectonic implications
Since the early Paleozoic, westward subduction of the Paleo-Pacific plate has
governed the tectonic evolution of the eastern Eurasian margin by building wide belts
of accretionary wedge along trench and plate-marginal volcanic-plutonic belts (Isozaki,
1996, 1997; Kimura, 1997; Maruyama, 1997; Maruyama and others, 1997; Isozaki and
others, 2010). In the preceding sections, only SW Japan was discussed because the
pattern of crustal growth of the Paleozoic to Mesozoic accretionary complexes is best
exemplified in SW Japan, due to the rapid Quaternary uplift and erosion of the
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Fig. 9. εNd(T) vs. model age plots of granitoids and metasedimentary rocks from Taiwan. (A) TDM-1 model
ages are calculated with a single-stage model in which the Sm/Nd ratio of a rock is assumed to be identical to that
of its protolith. (B) TDM-2 model ages are obtained with a two-stage model in which the protolith of the first stage
is assumed to have evolved as the average continental crust with 147Sm/144Nd ⫽ 0.12, or f(Sm/Nd) ⫽ ⫺0.4 (see
footnote of table 1). Data sources: Chen and others (1990), Lan and others (2008). Because some granites show
the REE tetrad effect, which produced aberrant age values in the single-stage TDM calculation, the 2-stage model
ages (TDM-2) values are also calculated for comparison (B).
Cenozoic cover. SW Japan is composed, from the continental side to ocean, of nine
accretionary complex units (Oeyama, Renge, Akiyoshi, Suo, Ultra-Tanba, Mino-TanbaChichibu, Sanbagawa, Northern Shimanto and Southern Shimanto belts (Isozaki and
others, 2010). The units have almost the same rock assemblages of the “ocean plate
stratigraphy,” including MORB-type basalt, chert, hemipelagic mudstone, limestone,
turbidite or sandstone and conglomerate. The ocean plate stratigraphy records the
history of sedimentation on the ocean floor as it travels from a ridge to a trench. In the
scheme of tectonic evolution presented by Isozaki (1996) and Maruyama (1997),
Mesozoic granitoids appear to be generated by melting of the subducted oceanic crust
(see fig. 11), or produced in the middle to lower crust apparently overlain by the
accretionary complexes. However, it is not clearly shown whether the protoliths of the
granitoids were the accretionary complexes or the old Yangtze lower crust. The idea of
slab melting for the genesis of the vast amounts of granitic rocks (Maruyama, 1997) was
deemed unlikely from the present analysis.
The revelation of the dominantly Precambrian heritage for granitoids of SW
Japan is critical to the tectonic reconstruction of the Japanese Islands. An important
question is why, in terms of the Sr-Nd isotopic compositions, the Japanese accretionary
orogen is so different from other accretionary orogens, such as the CAOB and ANS. By
contrast, the accretionary orogens of SW Japan are more comparable with the
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Fig. 10. Comparison of Sm-Nd isotopic compositions of sedimentary and metasedimentary rocks from
Taiwan and Japan. Lines radiating from DM (depleted mantle) represent depleted mantle model ages
(single-stage model). The data for Japan (Kagami and others, 2006) are more scattered than the data for
Taiwan. The “young” sediments (500-1000 Ma) of Japan are likely to contain more materials from the ocean
plate stratigraphy, such as siltstones from the early Tertiary accretionary complex of the Shimanto Belt in
southern Shikoku.
collisional orogens in SE China, Taiwan, and even the European Caledonides and
Hercynides. On the other hand, the similarity of isotopic signatures between Japan and
SE China supports the models of tectonic evolution and paleogeographic position of
proto-Japan proposed by Maruyama and others (1997) and Sengor and Natal’in
(1996). Both models proposed that the Pre-Cenozoic accreted terranes were developed along the continental margin of SE China (fig. 11). According to Maruyama and
others (1997), the Ryoke low P/T and the Sanbagawa high P/T belts, as well as the
Shimanto accretionary complex, began to develop close to the present coast of SE
China in the Late Cretaceous (ca. 90 Ma). In the model of Sengor and Natal’in (1996),
the South Japan microcontinent was initially separated from SE China (near Fujian) in
the Early Jurassic (ca. 160 Ma). By 145 Ma, at the Jurassic/Cretaceous boundary, the
constituent terranes of the microcontinent began to migrate northeastwards by
transpression. They arrived and docked at the Eurasian margin to the east of the
“Manchurides” in the Oligocene. The Japan Sea was later opened and thus rearranged
and formed the essential framework of the present Japanese Islands.
If the two models as described above are accepted, the similar Nd isotopic
signatures between SW Japan, SE China and Taiwan can be satisfactorily explained.
The terranes or tectonic units of SW Japan were thus initially formed at the continental
margin of SE China. Since they are part of the South China Block, the granitoid
formation and crustal evolution in SW Japan must have shared the same processes and
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Fig. 11. Paleogeographic reconstruction of Late Cretaceous Japan at ca. 90 Ma (Maruyama and others,
1997). Note that the Ryoke granitic belt, the Sanbagawa high P/T schist belt and the Shimanto accretionary
complex were developed along the continental margin in proximity of SE China. The cross-section depicts a
“transfer” of granitic magmas from the subducting slab or melting of the lower crust and possibly the
accretionary complexes.
conserved similar isotopic signatures. Using the age information, Sr-Nd isotopic signature
and geochemical data of the end-Permian marble sequence and Cretaceous granitoids of
the Tanan’ao Complex, Jahn and others (1992) hypothesized that the paleogeographic
position of proto-Taiwan was situated to the south of Guangdong Province. This hypothesis
has later been supported by an exhaustive monazite age study of the Tertiary sandstones of
Taiwan (Yokoyama and others, 2007), and a zircon age study of Early Tertiary andesite and
rhyolite (Chen and others, 2010). Because the crustal and tectonic development of SW
Japan and Taiwan took place in the proximal SE part of the South China Block, their
sharing of Sr-Nd isotopic characteristics is clearly explained.
conclusions
In a recent review on accretionary orogens, Cawood and others (2009) stated that
accretionary orogens form at intraoceanic and active continental margin plate boundaries. They include the supra-subduction zone forearc, magmatic arc and back-arc
components. They further separated accretionary orogens into retreating and advancing types. The case of Japan is of the retreating type. Similarly, in a discussion on
tectonic models for accretion of the Central Asian Orogenic Belt, Windley and others
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(2007) summarized that the CAOB was formed by accretion of island arcs, ophiolites,
ocean islands, seamounts, accretionary wedges, oceanic plateaux and microcontinents
in a manner comparable with that of circum-Pacific Mesozoic-Cenozoic accretionary
orogens. In both syntheses, accretionary orogens appear to consist dominantly of rocks
of mantle origin; hence granitoids derived by remelting of these rocks are generally
“juvenile.” This is generally true for the CAOB and ANS.
However, the present study argues that accretionary orogens could be distinguished by the nature of the accreted lithological assemblages. Orogens with dominantly island arc assemblages would witness generation of granitoids with juvenile
characters. This is best exemplified by the granitoids of the ANS and many parts of the
CAOB. By contrast, orogens with accretionary complexes with a large proportion of
recycled Precambrian crust relative to mantle-derived rocks would produce granitic
rocks with a more crustal signature. This is represented by the Japanese Islands. The
Sr-Nd isotopic compositions of Japanese granitoids shown in figures 2 to 5 indicate that
the source regions varied from dominantly mantle-derived rocks to an assemblage with
a large proportion of recycled Precambrian crust. This implies that the proportion of
eroded Precambrian crust in the trench to the ocean plate stratigraphy was very
variable in the subducted accretionary complexes during the Mesozoic. Alternatively,
the accreted fragments, including MORB, basalts of seamounts and ocean plateaux,
have not significantly participated in the generation of granitic magmas.
In conclusion, accretionary orogens can be distinguished by the nature of
accreted lithologic assemblages. The Arabian-Nubian Shield contains the highest
proportion of mantle-derived rocks, or island arc suites, and juvenile granitoids. SE
Japan shows the opposite scenario. Though the CAOB was mainly developed through
accretion of island arcs, it also contains accreted Precambrian continental fragments.
This is well demonstrated by the isotopic compositions of granitoids from west-central
Mongolia (Jahn and others, 2004; Kovalenko and others, 2004) and the Chinese Altai
Mountains (Hu and others, 2000; Wang and others, 2009). Finally, this study demonstrates that, despite the well-documented accretionary complexes (Isozaki and others,
2010), the generation of extensive granitoids in SW Japan was probably dominated by
remelting of Precambrian crustal sources underlying the “thin” roof-pendants of
accretionary complexes (Isozaki and others, 2010). The oceanic component of the
“ocean plate stratigraphy” has not participated to a significant amount in the production of the continental crust in SW Japan. On the other hand, the isotopic data support
the idea that proto-Japan was initially developed along the southeastern part of the
South China Block, as advocated by several authors (Isozaki, 1996, 1997; Sengor and
Natal’in, 1996; Maruyama and others, 1997; Isozaki and others, 2010).
acknowledgments
This article is dedicated to Professor Alfred Kröner, a highly distinguished scholar
and long-time friend, in honor of his 70th birthday. The content of this paper was first
presented in 2006 in the second ERAS International Workshop on “Accretionary
orogens and Continental Growth,” held at Kochi University, Japan, and convened by
Gaku Kimura and Yukio Isozaki. I benefited from discussions with many participants
during the meeting. The company of Kazu Okamoto and Aoki-san during the sample
collection of Miocene granites at Kashiwajima, SW Shikoku, is highly appreciated.
Shunso Ishihara provided a suite of granite samples from the Sanyo belt and the
analytical results are used in this paper. Nicole Morin (Rennes), Po-Hsuan Lin and
Masako Usuki (Taipei) helped in the laboratory work. Kazu Okamoto taught me some
geology of Japan. The assistance of Atsushi Utsunomiya, Qingguo Zhai, and Po-Hsuen
Lin in the preparation of this paper is deeply acknowledged. The paper was improved
by the comments and suggestions of Michel Faure, Fuyuan Wu and Simon Wilde. This
work is supported by NSC-Taiwan grant numbers 96-2116-M-001-004, 97-2752-M-002003-PAE; 97-2116-M-001-011; 98-2116-M-001-009.
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Appendix
Table A1
Rb-Sr and Sm-Nd isotope data of granitoid rocks (granites, qz-diorite, tonalite, granodiorite,
adamelite (monzogranite), adakitic granite, granophyre) from Japan
Sample
No.
Age Rb
Sr
(Ma) (ppm) (ppm)
87
87
86
86
Rb
Sr
Sr
Sr
I (Sr)
Sm
Nd
(ppm) (ppm)
147
143
144
144
Sm
Nd
Nd
Nd
εNd(0) fSm/Nd εNd(T) TDM-1 TDM-2
(Ga) (Ga)
Arakawa, Y., 1990 Two types of granitic intrusions in the Hida belt, Japan: Sr isotopic and chemical characteristics of the Mesozoic Funatsu
granitic rocks. Chemical Geology, 85, 101-117
UB01
195
31.3 650
0.70530
UB06
195
58.3 572
0.70531
UB08
195
50.2 449
0.70528
UB09
195
96.3 281
0.70537
UB10
195
66.9 470
0.70521
UB11
195 142
289
0.70537
UB12
195 142
248
0.70541
ON01234*1 195
53
649
—
ON01230*1 195
43.6 746
0.70732
SN102
195
56.81 959.3
0.70725
SN101
195 107.3 547.9
0.70940
SN0-2
195 116
336
0.70979
TG02
195
67.03 532.8
0.70664
TG05
195 100
546
0.70654
YT06
YT07
YT08
YT10
YT14
YT18
YT20
YT21
YT24
YT11
YT28
YT29
IN01
IN02
IN03
YT12
YT19
YT22
YT23
Hd03
Hd04
Hd06
Hd08
Hd09
Hd13
Hd18
185
185
185
185
185
185
185
185
185
185
185
185
185
185
185
185
185
185
185
185
185
185
185
185
185
185
Ng01
Ng02
Ng03
Ng08
185
185
185
185
Hs02
190
Hs03
190
Hs04
190
Hs05
190
Hs108
190
Iori intrusion
Ir01
190
Ir02
190
Ir03
190
Ir04
190
Ir05
190
Ir06
190
Ir07
190
190
Ir08
190
Ir09
30.4 580
38.7 508
39.3 578
29.2 598
41.8 572
53.2 462
51.1 633
36.1 726
50.7 738
48.6 697.7
55.1 377
49.8 884
60.4 465
58
637
61.3 538.1
53.1 768
76
470.2
54
668
52.8 696
47.8 777.1
66.1 862.7
59.1 605.5
61.7 606.2
42.2 1213
34.1 1011.1
172.6 205.6
0.15
0.22
0.20
0.14
0.21
0.33
0.23
0.14
0.20
0.20
0.42
0.16
0.38
0.26
0.33
0.20
0.47
0.23
0.22
0.18
0.22
0.28
0.29
0.10
0.10
2.43
0.707290
0.707440
0.707370
0.707410
0.708520
0.707600
0.708040
0.707430
0.707010
0.707350
0.707830
0.707130
0.707730
0.709050
0.709300
0.706480
0.707260
0.706820
0.706690
0.706950
0.706270
0.707630
0.709290
0.706200
0.706680
0.716950
0.70689
0.70686
0.70685
0.70704
0.70796
0.70672
0.70742
0.70705
0.70649
0.70682
0.70672
0.70670
0.70674
0.70836
0.70843
0.70595
0.70603
0.70620
0.70611
0.70648
0.70569
0.70689
0.70851
0.70594
0.70642
0.71055
643.2
625
686.2
683.2
0.20
0.26
0.23
0.35
0.706720
0.706960
0.707580
0.709780
0.70620
0.70627
0.70697
0.70886
48.7 653.9
46.4 678
91.3 484.3
89
481.7
35.4 1147.1
0.22
0.20
0.55
0.53
0.09
0.704980
0.704980
0.706160
0.705980
0.704740
0.70440
0.70444
0.70469
0.70454
0.70450
0.707810
0.707900
0.706770
0.706870
0.707400
0.707220
0.707290
0.707890
0.707550
0.70658
0.70682
0.70642
0.70636
0.70668
0.70661
0.70678
0.70695
0.70632
44.1
56.6
54.5
82.6
80.3 510
73
527
46.3 1032
49.7 767
64.2 696
64.3 828
54.6 837
76.5 636
84.4 535
0.46
0.40
0.13
0.19
0.27
0.23
0.19
0.35
0.46
tapraid4/zqn-ajsc/zqn-ajsc/zqn01010/zqn2165d10a metzgerm S⫽18 3/11/11 16:52 Art:
1235
Implications from a Sr-Nd isotopic study of the Phanerozoic granitoids
Table A1
(continued)
Sample
No.
Age Rb
Sr
(Ma) (ppm) (ppm)
87
87
86
86
Rb
Sr
Sr
Sr
I (Sr)
Sm
Nd
(ppm) (ppm)
147
143
144
144
Sm
Nd
Nd
Nd
εNd(0) fSm/Nd εNd(T) TDM-1 TDM-2
(Ga) (Ga)
Arakawa, Y., 1990. Two types of granitic intrusions in the Hida belt , Japan: Sr isotopic and chemical characteristics of the Mesozoic Funatsu
granitic rocks. Chemical Geology, 85, 101-117
Kegachidake intrusion
Kg02*
185.8 78.2 373
0.61 0.706470 0.70487
Kg03*
185.8 103.2 147.7
2.02 0.710310 0.70497
Kg07*
185.8 134
226.5
1.71 0.709380 0.70485
Kg09*
185.8 130.7 184
2.06 0.710290 0.70486
Okumayama intrusion
Ok01
190
46.9 370
0.37 0.705750 0.70476
Ok02
190
57
355
0.47 0.706270 0.70501
Ok05
190
78.4 430
0.53 0.706460 0.70503
Komagatake intrusion
Km03*
192.6 51.4 612
0.24 0.706090 0.70542
Arakawa Y. and Shinmura T., 1995. Nd-Sr isotopic and geochemical characteristics of two constrasting types of calc-alkaline plutons in the
Hida belt, Japan. Chemical Geology, 124, 217-232
TYPE-1 PLUTON
UB03
184
0.70528 2.41 12.71 0.1146 0.512551
-1.7 -0.42 0.2
0.92
0.95
UB05
184
0.70539 2.85 12.53 0.1373 0.512570
-1.3 -0.30 0.1
1.16
0.95
UB10
184
0.70521 3.82 28.08 0.0822 0.512591
-0.9 -0.58 1.8
0.65
0.85
UB11
184
0.70536 3.33 19.83 0.1016 0.512633
-0.1 -0.48 2.1
0.70
0.81
UB12
184
0.70539 3.23 19.74 0.0990 0.512635
-0.1 -0.50 2.2
0.69
0.80
OK01
190
46.9 370
0.37 0.705750 0.70476 2.79 13.13 0.1283 0.512510
-2.5 -0.35 -0.8
1.14
1.04
OK25
190
0.70550 2.42 10.89 0.1344 0.512750
2.2 -0.32 3.7
0.77
0.66
TYPE-2 PLUTON
SN03
190
5.03 29.13 0.1044 0.512060 -11.3 -0.47 -9.0
1.52
1.73
SN04
190
4.54 28.58 0.0961 0.512085 -10.8 -0.51 -8.3
1.38
1.67
ON32
190
3.88 24.32 0.0963 0.512416
-4.3 -0.51 -1.9
0.95
1.15
OM03
190
5.72 32.30 0.1071 0.512402
-4.6 -0.46 -2.4
1.07
1.18
OM04
190
3.13 12.11 0.1562 0.512624
-0.3 -0.21 0.7
1.39
0.89
OM05
190
3.47 14.88 0.1408 0.512406
-4.5 -0.28 -3.2
1.55
1.22
YT06
190
4.67 19.49 0.1448 0.512459
-3.5 -0.26 -2.2
1.53
1.14
YT22
190
10.05 24.40 0.2489 0.512674
0.7
0.27 -0.6
-2.08
0.94
YT29
190
4.03 27.38 0.0890 0.512413
-4.4 -0.55 -1.8
0.90
1.14
Hd03
190
7.41 47.47 0.0944 0.512402
-4.6 -0.52 -2.1
0.96
1.17
Hd13
190
5.25 29.04 0.1393 0.512443
-3.8 -0.29 -2.4
1.45
1.16
Hd18
190
2.57 13.50 0.1152 0.512012 -12.2 -0.41 -10.2
1.76
1.82
GY2120
190
86.6 637
0.39 0.710600 0.70954 2.07 11.32 0.1105 0.511965 -13.1 -0.44 -11.0
1.75
1.89
GY1717
190 240
741
0.94 0.715180 0.71264 1.84 10.51 0.1058 0.511936 -13.7 -0.46 -11.5
1.71
1.93
GY2403
190 178
592
0.87 0.715070 0.71273 3.52 25.27 0.0842 0.511820 -16.0 -0.57 -13.2
1.56
2.08
Fujii and others, 2000. Sr-Nd isotopic systematics and geochemistry of the intermediate plutonic rocks from Ikoma mountains,
Southewest Japan: evidence for a sequence of Mesozoic magmatic activity in the Ryoke belt. The Island Arc, 9, 37-45
K95091204-3
K 94101010
K 96030105
K 96030101
K 96061902
K 96061903
K 96070302
K 96070303
K95091203-1
F 95072106
F 95072107
F 95072109
F 96022502-1
F95022502-2
F 96022503
F 94103002
F 94103008
F 96071904
F 96071907-1
F 94080404
161
161
161
161
161
161
161
161
161
121
121
121
121
121
121
121
121
121
121
121
20
33
40
85.9
47
49
24
30
9
78
468
532
430
434
455
427
453
486
368
342
0.13
0.18
0.27
0.57
0.30
0.33
0.16
0.18
0.07
0.66
0.707446
0.707684
0.707866
0.708566
0.707955
0.708035
0.707702
0.707737
0.707424
0.708615
0.70716
0.70727
0.70725
0.70726
0.70727
0.70728
0.70734
0.70732
0.70727
0.70749
67
73
78
79
79
98
76
78
69
415
383
383
388
359
399
406
400
417
0.46
0.55
0.59
0.59
0.65
0.71
0.54
0.57
0.48
0.708335
0.708480
0.708493
0.708538
0.708727
0.708752
0.708518
0.708502
0.708364
0.70754
0.70753
0.70748
0.70752
0.70761
0.70753
0.70759
0.70753
0.70754
1.95
3.53
5.55
4.01
5.76
5.60
4.40
5.40
4.47
0.65
4.52
8.74
17.20
24.60
17.90
21.50
21.20
17.10
20.10
15.10
3.26
21.50
0.1347
0.1244
0.1363
0.1353
0.1619
0.1595
0.1551
0.1621
0.1792
0.1202
0.1270
0.512358
0.512355
0.512304
0.512362
0.512338
0.512312
0.512394
0.512315
0.512336
0.512302
0.512303
-5.5
-5.5
-6.5
-5.4
-5.9
-6.4
-4.8
-6.3
-5.9
-6.6
-6.5
6.55 39.30 0.1280 0.512317
5.21 16.70 0.1879 0.512315
-0.32
-0.37
-0.31
-0.31
-0.18
-0.19
-0.21
-0.18
-0.09
-0.39
-0.35
1.29
1.28
1.38
1.28
1.36
1.40
1.26
1.40
1.39
1.36
1.37
-6.3
-6.3
-4.2
1.53
-4.0
1.36
-5.3
1.66
-4.1
1.53
-5.1
2.38
-5.6
2.35
-3.9
1.96
-5.6
2.45
-5.5
3.57
-5.4
1.38
-5.5
1.49
(Age 161 Ma)
-0.35 -5.2
1.48
-0.04 -6.2
4.87
8.66 45.20 0.1159 0.512303
-6.5
-0.41 -5.3
1.32
1.35
7.92 29.80 0.1609 0.512336
6.41 23.20 0.1667 0.512335
6.38 24.50 0.1576 0.512340
-5.9
-5.9
-5.8
-0.18 -5.3
-0.15 -5.4
-0.20 -5.2
2.34
2.63
2.19
1.36
1.37
1.35
1.35
1.43
tapraid4/zqn-ajsc/zqn-ajsc/zqn01010/zqn2165d10a metzgerm S⫽18 3/11/11 16:52 Art:
1236
Bor-Ming Jahn—Accretionary orogen and evolution of the Japanese Islands—
Table A1
(continued)
Sample
No.
Age Rb
Sr
(Ma) (ppm) (ppm)
87
87
86
86
Rb
Sr
Sr
Sr
I (Sr)
Sm
Nd
(ppm) (ppm)
147
143
144
144
Sm
Nd
Nd
Nd
εNd(0) fSm/Nd εNd(T) TDM-1 TDM-2
(Ga) (Ga)
Iizumi and others, 2000. Sr-Nd isotope ratios of gabbroic and dioritic rocks in a Cretaceous-Paleogene grainte terrain, Southwest Japan. The
Island Arc, 9, 113-127
4110205
82.9 129
199
1.88 0.709426 0.70700
4.77 26.10 0.1110 0.512392 -4.8 -0.44 -3.9
4110206
82.9 98
225
1.26 0.708696 0.70710
5.45 26.50 0.1240 0.512394 -4.8 -0.37 -4.0
AG005
82.9 79
313
0.73 0.706692 0.70580
3.92 19.20 0.1230 0.512596 -0.8 -0.37
0.0 correct
950915
82.9 63
336
0.54 0.706577 0.70590
5.10 23.90 0.1290 0.512572 -1.3 -0.34 -0.6
Omishima
82.9
0.70580
—
4110302
82.9 98
264
1.07 0.708008 0.70660
4.99 31.80 0.0950
—
4110303
82.9 99
274
1.05 0.707317 0.70600
4.82 25.30 0.1150
—
4110309
82.9 119
328
1.05 0.706770 0.70540
4.96 26.30 0.1140 0.512565 -1.4 -0.42 -0.5 correct
KO-005
82.9 129
324
1.15 0.706181 0.70470
5.25 28.60 0.1110 0.512664
0.5 -0.44
1.4
TMS-01
82.9 31
399
0.23 0.706802 0.70650
4.68 25.20 0.1120 0.512571 -1.3 -0.43 -0.4
TMO20
82.9 99
306
0.94 0.705540 0.70430
3.20 15.50 0.1250 —
TMO11
82.9 68
334
0.59 0.706100 0.70530
4.47 24.40 0.1110 0.512626 -0.2 -0.44
0.7
6010507
82.9 73
301
0.70 0.708388 0.70750
4.96 25.10 0.1190 0.512389 -4.9 -0.40 -4.0 correct
6010505
82.9 94
268
1.02 0.708681 0.70740
5.34 27.80 0.1160 0.512390 -4.8 -0.41 -4.0
6010402
82.9 122
315
1.12 0.708782 0.70730
5.93 28.20 0.1270 0.512370 -5.2 -0.35 -4.5
6062205
82.9 66
277
0.69 0.707548 0.70670
5.52 27.70 0.1200 0.512408 -4.5 -0.39 -3.7
4103002
85.2 82
384
0.62 0.707138 0.70630
6.71 34.20 0.1190 0.512322 -6.2 -0.40 -5.3 correct
5081901
85.2 51
386
0.38 0.707076 0.70660
6.18 29.80 0.1250 0.512431 -4.0 -0.36 -3.3
32219
85.2 41
491
0.24 0.706272 0.70600
3.84 18.60 0.1250 0.512421 -4.2 -0.36 -3.5
6062203
85.2 93
341
0.79 0.707419 0.70640
4.19 22.80 0.1110 0.512391 -4.8 -0.44 -3.9
6062204
85.2 91
348
0.76 0.707447 0.70650
4.07 22.10 0.1110 0.512378 -5.1 -0.44 -4.1 correct
6062101
85.2 46
632
0.21 0.706685 0.70640
3.04 15.60 0.1180 0.512446 -3.7 -0.40 -2.9
7690503
85.2 17.8 576
0.09 0.704881 0.70480
5.00 20.80 0.1460 0.512725
1.7 -0.26
2.2
Ishioka and Iizumi, 2003. Petrochemical and Sr-Nd isotope investigations of Cretaceous intrusive rocks and their enclaves in the TogouchiYoshiwa d istrict, northwest Hiroshima prefecture, SW Japan. Geochemical Journal, 37, 449-470
Togouchi granodiorite
TO01
85.6 88
243
1.05 0.707590 0.70631
—
—
—
—
—
TO02
85.6 76
223
0.99 0.707570 0.70637
—
—
—
—
—
TO10
85.6 106
182
1.70 0.708380 0.70632
3.70 23.90 0.0936 0.512421 -4.2 -0.52 -3.1
0.93 1.13
TO12
85.6 63
294
0.62 0.707010 0.70626
—
—
—
—
—
TO15
85.6 100
207
1.39 0.707990 0.70629
—
—
—
—
—
TO16
85.6 122
178
1.99 0.708650 0.70624
5.55 29.30 0.1145 0.512463 -3.4 -0.42 -2.5
1.06 1.09
TO23
85.6 105
198
1.53 0.708140 0.70628
4.64 25.80 0.1087 0.512466 -3.4 -0.45 -2.4
0.99 1.08
TO28
85.6 111
202
1.60 0.708220 0.70629
—
—
—
—
—
TO48
85.6 113
178
1.84 0.708770 0.70653
—
—
— 0.512506 -2.6
—
TO52
85.6 79
232
0.98 0.707720 0.70652
4.01 21.70 0.1117 0.512509 -2.5 -0.43 -1.6
0.96 1.02
TO02B
85.6 108
153
2.05 0.708800 0.70632
—
—
—
—
—
TO05B
85.6 115
107
3.09 0.710160 0.70638
—
—
—
—
—
TO09B
85.6 128
62
5.94 0.713520 0.70626
—
—
—
—
Togouchi phenocryst-free microdiorite enclaves (PFME)
TO12E
85.6 76
312
0.71 0.706590 0.70574
—
—
— 0.512517 -2.4
—
TO15E
85.6 53
283
0.54 0.706530 0.70587
4.02 19.60 0.1240 0.512520 -2.3 -0.37 -1.5
1.07 1.02
TO16AE
85.6 84
344
0.70 0.706760 0.70590
4.43 19.90 0.1346 0.512529 -2.1 -0.32 -1.4
1.20 1.02
TO16BE
85.6 109
258
1.23 0.707350 0.70587
4.20 22.30 0.1139 0.512455 -3.6 -0.42 -2.7
1.06 1.11
TO23AE
85.6 89
280
0.92 0.706890 0.70577
—
—
—
—
—
TO23BE
85.6 93
346
0.77 0.706800 0.70585
4.58 21.20 0.1306 0.512508 -2.5 -0.34 -1.8
1.18 1.04
TO28E
85.6 126
210
1.74 0.707830 0.70571 11.60 49.70 0.1411 0.512487
-2.9 -0.28 -2.3
1.39 1.09
Togouchi phenocryst-free microdiorite enclaves (PFME)
TO36AE
85.6 126
163
2.24 0.708610 0.70589 9.52 42.80 0.1345 0.512465
-3.4 -0.32 -2.7
1.32
1.12
TO36BE
85.6 180
151
3.45 0.709750 0.70555
—
—
— 0.512476
-3.2
—
TO52E
85.6 88
269
0.95 0.706830 0.70567
—
—
—
—
—
TO66AE
85.6 110
203
1.57 0.707860 0.70595
—
—
—
—
—
TO66BE
85.6 110
197
1.61 0.707850 0.70588 5.80 29.90 0.1173 0.512468
-3.3 -0.40 -2.4
1.08
1.09
Togouchi phenocryst-bearing microdiorite enclaves (PBME)
TO01E
97
236
1.19 0.707600 0.70615
—
—
—
—
—
TO30E
81
298
0.79 0.707200 0.70624
—
—
—
—
—
tapraid4/zqn-ajsc/zqn-ajsc/zqn01010/zqn2165d10a metzgerm S⫽18 3/11/11 16:52 Art:
Implications from a Sr-Nd isotopic study of the Phanerozoic granitoids
1237
Table A1
(continued)
Sample
No.
Age Rb
Sr
(Ma) (ppm) (ppm)
87
87
86
86
Rb
Sr
Sr
Sr
I (Sr)
Sm
Nd
(ppm) (ppm)
147
143
144
144
Sm
Nd
Nd
Nd
εNd(0) fSm/Nd εNd(T) TDM-1 TDM-2
(Ga) (Ga)
Ishioka and Iizumi, 2003. Petrochemical and Sr-Nd isotope investigations of Cretaceous intrusive rocks and their enclaves in the TogouchiYoshiwa d istrict, northwest Hiroshima prefecture, SW Japan. Geochemical Journal, 37, 449-470
Tateiwayama granite porphyry
TA71
77.4 143
151
2.74 0.709480 0.70647 4.53 25.90 0.1057 0.512441
-3.8 -0.46 -2.9
1.00
1.12
TA73A
77.4 149
73
5.88 0.712940 0.70644
—
—
— 0.512460
-3.5
—
TA73B
77.4 163
80
5.92 0.713080 0.70659
—
—
—
—
—
TA78
77.4 141
131
3.11 0.709970 0.70655
—
—
— 0.512447
-3.7
—
TA82
77.4 127
151
2.43 0.709220 0.70655
—
—
— 0.512418
-4.3
—
TA111
77.4 123
131
2.70 0.709570 0.70658
—
—
—
—
—
TA112
77.4 132
135
2.82 0.709550 0.70644 6.18 32.50 0.1150 0.512431
-4.0 -0.42 -3.2
1.11
1.15
Tateiwayama phenocryst-free microdiorite enclaves (PFME)
TA71E
77.4 174
277
1.82 0.707880 0.70588 5.28 26.40 0.1209 0.512489
-2.9 -0.39 -2.2
1.09
1.06
TA73E
77.4 170
239
2.06 0.708160 0.70589 5.34 25.20 0.1281 0.512462
-3.4 -0.35 -2.8
1.22
1.11
TA76E
77.4 68
387
0.51 0.706300 0.70574
—
—
— 0.512498
-2.7
—
Yoshiwa quartz diorite
YO74
161.6 13
502
0.08 0.706410 0.70625
—
—
—
—
—
YO81
161.6 77
311
0.72 0.707970 0.70632
—
—
— 0.512410
-4.4
—
YO86
161.6 113
269
1.22 0.709040 0.70624
—
—
— 0.512379
-5.1
—
YO93
161.6 38
514
0.22 0.706710 0.70623 3.41 16.40 0.1257 0.512448
-3.7 -0.36 -2.2
1.21
1.13
YO94
161.6 16
532
0.09 0.706550 0.70634
—
—
— 0.512496
-2.8
—
YO95
161.6 45
396
0.33 0.706820 0.70606 4.23 20.30 0.1260 0.512465
-3.4 -0.36 -1.9
1.19
1.11
YO96
161.6 31
329
0.27 0.706920 0.70630 4.68 22.90 0.1235 0.512425
-4.2 -0.37 -2.6
1.22
1.17
Kagami and others, 1992. Spatial variations of Sr and Nd isotope ratios of Cretaceous-Paleogene granitoid rocks, SW Japan Arc.
Contributions to Mineralogy and Petrology, 112, 165-177
1
65 113
271
1.20 0.705990 0.70488 4.34 22.10 0.1188 0.512618
-0.4 -0.40 0.3
0.85
0.85
2
65 125
135
2.68 0.707410 0.70494 4.08 19.90 0.1244 0.512636
0.0 -0.37 0.6
0.88
0.83
3
65 171
54.4
9.08 0.713190 0.70481
—
—
4
65 197
45
12.67 0.716620 0.70492
—
—
5
75
69.8 513
0.39 0.706000 0.70558
—
—
6
75
78.5 483
0.47 0.705930 0.70543 6.56 28.90 0.1371 0.512580
-1.1 -0.30 -0.6
1.13
0.94
7
75 159
194
2.38 0.708140 0.70561 6.21 29.70 0.1263 0.512526
-2.2 -0.36 -1.5
1.09
1.01
8
75 152
241
1.82 0.707390 0.70545
—
—
9
75
45.8 524
0.25 0.705850 0.70558
—
—
10
75 100
420
0.69 0.706290 0.70556
—
—
11
75 161
251
1.85 0.707570 0.70560
—
—
12
75 162
216
2.16 0.707720 0.70541
—
—
13
70 180
64.5
8.07 0.713640 0.70562 3.86 20.30 0.1150 0.512519
-2.3 -0.42 -1.6
0.97
1.01
14
70 166
75.3
6.39 0.711940 0.70559
—
—
15
70 158
61.2
7.46 0.712900 0.70549
—
—
16
72 162
83.9
5.57 0.712530 0.70683 7.87 36.20 0.1272 0.512492
-2.8 -0.35 -2.2
1.16
1.07
17
72 140
94.2
4.29 0.711210 0.70682 6.56 29.80 0.1332 0.512504
-2.6 -0.32 -2.0
1.22
1.05
18
39
68.8 238
0.83 0.705500 0.70504 4.11 19.70 0.1260 0.512683
0.9 -0.36 1.2
0.81
0.76
19
39
65.3 258
0.73 0.705630 0.70522
—
—
20
39
88.6 125
2.06 0.706210 0.70507 2.70 14.50 0.1126 0.512639
0.0 -0.43 0.4
0.77
0.81
21
39
78.9 144
1.59 0.705970 0.70509
—
—
22
39
86.7 165
1.52 0.705850 0.70501 2.31 12.30 0.1142 0.512649
0.2 -0.42 0.6
0.77
0.80
23
39
75.2 181
1.21 0.705820 0.70515
—
—
24
65
88.3 282
0.91 0.706680 0.70584 3.32 16.20 0.1244 0.512510
-2.5 -0.37 -1.9
1.09
1.03
25
65 100
217
1.33 0.707070 0.70584 3.54 19.80 0.1083 0.512497
-2.8 -0.45 -2.0
0.94
1.03
26
72
72
468
0.44 0.707880 0.70742 4.80 23.50 0.1235 0.512346
-5.7 -0.37 -5.0
1.36
1.29
27
72
62.8 330
0.55 0.707080 0.70652 3.56 18.00 0.1201 0.512403
-4.6 -0.39 -3.9
1.22
1.20
28
72
72.6 484
0.43 0.707260 0.70682 5.86 27.30 0.1298 0.512371
-5.2 -0.34 -4.6
1.41
1.26
29
72
93.9 257
1.06 0.707760 0.70668 3.79 19.60 0.1169 0.512425
-4.2 -0.41 -3.4
1.14
1.16
30
16
64.5 418
0.45 0.706300 0.70620 3.57 18.10 0.1197 0.512523
-2.2 -0.39 -2.1
1.02
1.01
31
75
60.3 319
0.55 0.705820 0.70524 2.83 22.70 0.0756 0.512515
-2.4 -0.62 -1.2
0.70
0.96
32
75 103
365
0.82 0.708680 0.70781 4.02 21.20 0.1145 0.512246
-7.6 -0.42 -6.9
1.39
1.44
33
84 169
175
2.80 0.711060 0.70772
—
—
34
84 177
180
2.86 0.711120 0.70771 7.12 32.00 0.1348 0.512367
-5.3 -0.31 -4.6
1.51
1.28
35
84 112
206
1.58 0.709230 0.70735 4.30 20.50 0.1269 0.512381
-5.0 -0.35 -4.3
1.35
1.24
36
84 171
109
4.54 0.712760 0.70734 5.37 22.30 0.1454 0.512391
-4.8 -0.26 -4.3
1.69
1.25
37
84 164
107
4.44 0.712520 0.70722 5.17 24.30 0.1285 0.512390
-4.8 -0.35 -4.1
1.36
1.23
38
84 124
130
2.76 0.710730 0.70743 4.12 20.00 0.1245 0.512307
-6.5 -0.37 -5.7
1.44
1.36
39
84
35.3 390
0.26 0.707760 0.70745 4.55 20.20 0.1367 0.512306
-6.5 -0.31 -5.8
1.67
1.38
tapraid4/zqn-ajsc/zqn-ajsc/zqn01010/zqn2165d10a metzgerm S⫽18 3/11/11 16:52 Art:
1238
Bor-Ming Jahn—Accretionary orogen and evolution of the Japanese Islands—
Table A1
(continued)
Sample
No.
Age Rb
Sr
(Ma) (ppm) (ppm)
87
87
86
86
Rb
Sr
Sr
Sr
I (Sr)
Sm
Nd
(ppm) (ppm)
147
143
144
144
Sm
Nd
Nd
Nd
εNd(0) fSm/Nd εNd(T) TDM-1 TDM-2
(Ga) (Ga)
Kagami and others, 1992. Spatial variations of Sr and Nd isotope ratios of Cretaceous-Paleogene granitoid rocks, SW Japan Arc.
Contributions to Mineralogy and Petrology, 112, 165-177
40
84
27.5 369
0.22 0.707480 0.70722 4.53 19.70 0.1389 0.512361 -5.4 -0.29 -4.8 1.60
1.29
41
84
206
35.2 17.00 0.727470 0.70718 4.22 17.20 0.1483 0.512388 -4.9 -0.25 -4.4 1.77
1.26
42
84
147
134
3.19 0.711120 0.70731 4.77 25.90 0.1115 0.512363 -5.4 -0.43 -4.5 1.17
1.25
43
84
228
17.1 38.76 0.754560 0.70830 4.69 15.40 0.1843 0.512415 -4.4 -0.06 -4.2 3.78
1.27
44
84
126
158
2.30 0.710040 0.70729 4.16 23.10 0.1089 0.512333 -5.9 -0.45 -5.0 1.19
1.30
45
82
107
312
0.99 0.708440 0.70729 5.79 36.80 0.0952 0.512369 -5.2 -0.52 -4.2 1.00
1.22
46
82
84.2 312
0.78 0.708220 0.70731 4.64 34.70 0.0810 0.512362 -5.4 -0.59 -4.2 0.91
1.21
47
93
118
270
1.27 0.709090 0.70741 3.62 20.20 0.1083 0.512377 -5.1 -0.45 -4.0 1.12
1.22
48
93
123
176
2.05 0.710330 0.70763
—
—
49
93
129
133
2.80 0.711010 0.70731
—
—
Kagami and others, 2000. Continental basalts in the accretionary complexes of the South-west Japan Arc: Constraints from geochemical and
Sr and Nd isotopic data of metadiabase.
The Island Arc, 9, 3-20
1
192
87.4 458
0.55 0.707588 0.70608 7.51 30.80 0.1475 0.512424 -4.2 -0.25 -3.0
2
192
56.7 438
0.37 0.709428 0.70841 6.90 32.50 0.1283 0.512252 -7.5 -0.35 -5.9
16
240
38.6 329
0.34 0.708269 0.70711 6.54 29.50 0.1341 0.512344 -5.7 -0.32 -3.8
17
240
46.7 371
0.36 0.708814 0.70757 7.68 35.80 0.1296 0.512275 -7.1 -0.34 -5.0
Morioka and others, 2000. Rb-Sr isochron age of the Cretaceous granitoids in the Ryoke belt, Kinki district, Southwest Japan. The Island
Arc, 9, 46-54.
Ya gyu granite
YGr-1
74.6 83
292
0.82 0.710190 0.70932
YGr-2
74.6 81
318
0.73 0.710100 0.70932
YGr-3
74.6 22
124
0.52 0.709820 0.70927
YGr-4
74.6 104
133
2.27 0.711810 0.70940
YGr-5
74.6 109
192
1.64 0.710920 0.70918
70301
74.6 71
301
0.69 0.710100 0.70937
70302
74.6 75
257
0.84 0.710370 0.70948
70303
74.6 56
282
0.57 0.710050 0.70944
70304
74.6 61
282
0.63 0.709920 0.70926
70305
74.6 67
295
0.66 0.710320 0.70962
70305Bio
74.6 378
23
48.00 0.758610 0.70774
70306Ef.
74.6 16
377
0.12 0.709760 0.70963
Narukawa granite
B83032803
79.5 198
183
3.13 0.712300 0.70876
B82032801
79.5 112
136
2.39 0.711180 0.70848
A820327-10
79.5 99
197
1.45 0.710210 0.70857
B83032803Bio 79.5 890
12
215.00 0.951870 0.70902
Takijiri adamellite
Y1601
78.3 204
103
5.74 0.713870 0.70748
Y1602
78.3 276
57
14.00 0.722970 0.70740
Y1603
78.3 226
57
11.50 0.720310 0.70752
Y1604
78.3 209
106
5.70 0.714280 0.70794
Y1605
78.3 220
63
10.10 0.714280 0.70304
Y1606
78.3 143
270
1.53 0.709400 0.70770
Y1607
78.3 183
296
1.79 0.709950 0.70796
Katsuragi quartz diorite
61901
85.1 38
481
0.23 0.707540 0.70727
61902
85.1 36
467
0.22 0.707580 0.70731
70402
85.1 19
640
0.09 0.707370 0.70727
70403
85.1 32
545
0.17 0.707500 0.70729
70405
85.1 49
458
0.31 0.707640 0.70727
61901Bio
85.1 189
9
63.60 0.774770 0.69787
61902Ef.
85.1
4
660
0.02 0.707250 0.70723
70405Bio
85.1 188
12
45.50 0.756960 0.70194
70405Ef.
85.1
6
599
0.03 0.707270 0.70723
Minamikawachi granite
50503
72.8 249
80
9.00 0.717980 0.70867
51407
72.8 279
36
22.70 0.732660 0.70918
51420
72.8 219
260
2.44 0.711610 0.70909
52205
72.8 145
246
1.71 0.710690 0.70892
52208
72.8 180
145 3.61
0.712560 0.70883
52209
72.8 191
134 4.13
0.713170 0.70890
Nakajima and others, 2004. Mafic rocks from the Ryoke Belt, Southwest Japan: implications for Cretaceous Ryoke/San-yo granitic magama
genesis. Transactions of the Royal Society of Edinburgh: Earth Sciences, 95, 249-263
95101702
258
125
0.70892
91030804
128
218
0.70813
99112902A
51
343
0.70807
99120101A
72
58
471
0.70734
tapraid4/zqn-ajsc/zqn-ajsc/zqn01010/zqn2165d10a metzgerm S⫽18 3/11/11 16:52 Art:
Implications from a Sr-Nd isotopic study of the Phanerozoic granitoids
1239
Table A1
(continued)
Sample
No.
Age Rb
Sr
(Ma) (ppm) (ppm)
87
87
86
86
Rb
Sr
Sr
Sr
I (Sr)
Sm
Nd
(ppm) (ppm)
147
143
144
144
Sm
Nd
Nd
Nd
εNd(0) fSm/Nd εNd(T) TDM-1 TDM-2
(Ga) (Ga)
Shinjoe H., 1997. Origin of the granodiorite in the forearc region of SW Japan: melting of the Shimanto accretionary prism. Chemical
Geology, 134, 237-255
Uwajima and Miuchi plutons
1302host
14
142
216
1.90
0.708047 0.70767 4.50 28.60 0.0951 0.512353 -5.6 -0.52 -5.4
1.02 1.24
1304A
14
159
209
2.20
0.708335 0.70790 4.40 27.30 0.0974 0.512344 -5.7 -0.50 -5.6
1.06 1.26
O202
14
167
182
2.65
0.707237 0.70671 4.50 29.40 0.0925 0.512426 -4.1 -0.53 -3.9
0.91 1.12
O613D
14
149
202
2.13
0.707351 0.70693 4.60 30.90 0.0900 0.512423 -4.2 -0.54 -4.0
0.90 1.13
2102
14
150
217
2.00
0.707126 0.70673 4.70 29.70 0.0957 0.512456 -3.6 -0.51 -3.4
0.90 1.08
2507
14
129
236
1.58
0.707004 0.70669 4.20 16.90 0.1502 0.512437 -3.9 -0.24 -3.8
1.71 1.19
2509
14
162
213
2.20
0.707123 0.70669 4.90 30.10 0.0984 0.512358 -5.5 -0.50 -5.3
1.05 1.24
1406
14
132
166
2.30
0.709281 0.70882 4.50 28.80 0.0945 0.512343 -5.8 -0.52 -5.6
1.03 1.26
1202
14
133
188
2.05
0.707339 0.70693 4.30 16.60 0.1566 0.512459 -3.5 -0.20 -3.4
1.84 1.16
1205
14
167
198
2.44
0.706855 0.70637 4.80 20.10 0.1444 0.512402 -4.6 -0.27 -4.5
1.64 1.23
1302SA
14
116
262
1.28
0.706013 0.70576 7.50 37.60 0.1206 0.512512 -2.5 -0.39 -2.3
1.04 1.02
1305B
14
69
264
0.76
0.706194 0.70604 4.80 28.90 0.1004 0.512499 -2.7 -0.49 -2.5
0.88 1.02
1401D
14
82
234
1.01
0.706133 0.70593 4.60 28.90 0.0962 0.512484 -3.0 -0.51 -2.8
0.86 1.04
1504A
14
130
236
1.59
0.706222 0.70591 4.90 22.30 0.1328 0.512465 -3.4 -0.32 -3.3
1.29 1.12
2105
14
160
252
1.84
0.705678 0.70531 10.50 43.00 0.1476 0.512550 -1.7 -0.25 -1.6
1.38 1.00
2405A
14
180
111
4.69
0.707878 0.70695 3.10 17.70 0.1059 0.512422 -4.2 -0.46 -4.1
1.03 1.15
Stein G and others, 1996. The Miocene Ashizuri complex (SW Japan): source and magma differentiation of an alkaline plutonic assemblage
in an island-arc environment. Bull Soc Geol France, 167, 125-139.
A17
13
281
124
0.705430 0.70413 11.78 62.28 0.1143 0.512651 0.3 -0.42 0.4
0.77 0.79
A13
13
283
30
0.709640 0.70421 11.65 61.17 0.1151 0.512731 1.8 -0.41 1.9
0.65 0.67
A1
13
312
43
0.708910 0.70469 6.19 32.83 0.1140 0.512600 -0.7 -0.42 -0.6
0.84 0.88
Other acid rocks from Outer Zone of SW Japan:
A6
13
101
192
0.707660 0.70736 5.19 24.13 0.1300 0.512440 -3.9 -0.34 -3.8
1.29 1.15
A7
13
186
96
0.708050 0.70894 5.20 17.10 0.1838 0.512406 -4.5 -0.07 -4.5
3.76 1.28
A9
13
134
205
0.708440 0.70806 5.22 27.27 0.1157 0.512368 -5.3 -0.41 -5.1
1.22 1.25
OS4
13
210
43
0.713240 0.71043 2.54 8.98 0.1710 0.512326 -6.1 -0.13 -6.0
2.92 1.39
OS9
13
125
165
0.710180 0.70972 6.86 35.15 0.1180 0.512365 -5.3 -0.40 -5.2
1.25 1.26
Takagi, T. and Kagami, H., 1995. Rb-Sr isochron ages and initial Sr isotope rarios of the Ukan granodiorite and Kayo granite central
Okayama prefecture, southwest Japan. Bulletin of the Geological Survey of Japan, v. 46, 219-224.
31106
92
96
234
1.19
0.708530 0.70691
12102
92
101
243
1.20
0.708530 0.70680
81011
92
108
242
1.29
0.708620 0.70664
80905
92
131
261
1.45
0.708810 0.70611
73108
92
127
218
1.69
0.709200 0.70616
73107
92
127
208
1.77
0.709280 0.70609
12105
92
141
205
1.99
0.709530 0.70554
80409
92
73
300
0.70
0.708020 0.70729
31108
92
70
268
0.76
0.708120 0.70737
62602
92
85
252
0.98
0.708270 0.70709
31102
92
106
220
1.39
0.708700 0.70660
31012
81
54
291
0.54
0.707410 0.70700
31607
81
68
308
0.64
0.707600 0.70698
30801
81
76
301
0.73
0.707740 0.70695
102301
81
99
191
1.50
0.708560 0.70645
31603
81
103
185
1.61
0.708680 0.70632
30803
81
103
168
1.77
0.708780 0.70618
12209
81
135
203
1.92
0.709170 0.70548
102108
81
114
144
2.29
0.709480 0.70577
Takagi T., 2004. Origin of magnetite- and ilmenite-series granitic rocks in the Japan Arc. American Journal of Science, 304, 169-202.
(compiled data, from 85 sources)
Kyushu district and SW islands
Ilmenite-series 143
0.70442
Ilmenite-series 164
0.70452
Ilmenite-series 102
0.70544
Ilmenite-series 117
0.70521
Ilmenite-series 101
0.70649
Ilmenite-series 118
0.70557
Ilmenite-series 121
0.70542
Ilmenite-series 117
0.70530
Ilmenite-series 14.6
0.70630
Ilmenite-series 13.8
0.70552
Ilmenite-series 143
0.70441
Ilmenite-series 70
0.70462
Ilmenite-series 61
0.70639
Ilmenite-series 69
0.70987
Ilmenite-series 41
0.70586
tapraid4/zqn-ajsc/zqn-ajsc/zqn01010/zqn2165d10a metzgerm S⫽18 3/11/11 16:52 Art:
1240
Bor-Ming Jahn—Accretionary orogen and evolution of the Japanese Islands—
Table A1
(continued)
Sample
No.
Age Rb
Sr
(Ma) (ppm) (ppm)
87
87
86
86
Rb
Sr
Sr
Sr
I (Sr)
Sm
Nd
(ppm) (ppm)
Nd εNd(0) fSm/Nd εNd(T) TDM-1 TDM-2
Nd
(Ga) (Ga)
147
143
144
144
Sm
Nd
Takagi T., 2004. Origin of magnetite- and ilmenite-series granitic rocks in the Japan Arc. American Journal of Science, 304, 169-202.
(compiled data, from 85 sources)
Kyushu district and SW islands
Magnetite-series
229
0.70678
Magnetite-series
116
0.70506
0.6
Ilmenite-series
114
0.70516
1.0
Magnetite-series
108
0.70517
-2.1
Magnetite-series
96
0.70635
-3.8
Ilmenite-series
88
0.70526
0.3
Magnetite-series
121
0.70493
Ilmenite-series
39
0.70478
Magnetite-series
210
2.8
Magnetite-series
115
0.6
Ilmenite-series
13.8
0.70537
-6.6
Ilmenite-series
16.2
0.70869
-5.8
Ilmenite-series
15
0.70643
-3.5
Chugoku and Shikoku districts
Ilmenite-series
78
0.70857
-4.2
Ilmenite-series
79
0.70650
Ilmenite-series
81
0.70596
-3.8
Ilmenite-series
84
0.70745
-4.7
Ilmenite-series
91
0.70770
Ilmenite-series
92
0.70696
Ilmenite-series
84
0.70568
Ilmenite-series
80
0.70595
Ilmenite-series
93
0.70627
Ilmenite-series
91
0.70631
Ilmenite-series
88
0.70678
Ilmenite-series
73
0.70733
Ilmenite-series
94
0.70660
Ilmenite-series
89
0.70749
Ilmenite-series
93
0.70662
Ilmenite-series
95
0.70740
Ilmenite-series
94
0.70750
Ilmenite-series
93
0.70510
Ilmenite-series
99
0.70616
Ilmenite-series
92
0.70727
Ilmenite-series
92
0.70734
Ilmenite-series
82
0.70731
-4.5
Ilmenite-series
91
0.70745
-4.1
Ilmenite-series
93
0.70769
Ilmenite-series
93
0.70752
Ilmenite-series
83
0.70803
-5.7
Ilmenite-series
95
0.70741
-5.6
Ilmenite-series
99
0.70734
-5.3
Ilmenite-series
84
0.70749
-5.5
Ilmenite-series
84
0.70791
-5.9
Ilmenite-series
76
0.70794
-5.5
Ilmenite-series
76
0.70774
-5.3
Ilmenite-series
16
0.70740
-5.2
Ilmenite-series
14
0.70676
Ilmenite-series
85
0.70526
0.2
Ilmenite-series
84
0.70583
Ilmenite-series
85
0.70635
Ilmenite-series
77
0.70653
Magnetite-series
60
0.70661
Magnetite-series
61
0.70558
Magnetite-series
60
0.70554
Magnetite-series
65
0.70475
-1.8
Magnetite-series
65
0.70550
0.5
Magnetite-series
73
0.70557
Magnetite-series
75
0.70553
Magnetite-series
70
0.70550
-1.7
Magnetite-series
72
0.70681
-2.1
Magnetite-series
128
0.70487
Magnetite-series
58
0.70617
Magnetite-series
29
0.70489
Magnetite-series
40
0.70730
Magnetite-series
44
0.70449
Magnetite-series
85
0.70730
Magnetite-series
69
0.70574
Magnetite-series
36
0.70532
tapraid4/zqn-ajsc/zqn-ajsc/zqn01010/zqn2165d10a metzgerm S⫽18 3/11/11 16:52 Art:
Implications from a Sr-Nd isotopic study of the Phanerozoic granitoids
1241
Table A1
(continued)
Sample
No.
Age Rb
Sr
(Ma) (ppm) (ppm)
87
87
86
86
Rb
Sr
Sr
Sr
I (Sr)
Sm
Nd
(ppm) (ppm)
Nd εNd(0) fSm/Nd εNd(T) TDM-1 TDM-2
Nd
(Ga) (Ga)
147
143
144
144
Sm
Nd
Takagi T., 2004. Origin of magnetite- and ilmenite-series granitic rocks in the Japan Arc. American Journal of Science, 304, 169-202.
(compiled data, from 85 sources)
Chugoku and Shikoku districts
Magnetite-series
85
0.70535
-0.2
Magnetite-series
39
0.70507
0.8
Magnetite-series
81
0.70684
Magnetite-series
81
0.70590
Magnetite-series
102
0.70570
Magnetite-series
82
0.70620
Magnetite-series
84
0.70639
Magnetite-series
87
0.70572
-0.1
Magnetite-series
61
0.70499
Ilmenite-series
83
0.70773
-3.9
Ilmenite-series
80
0.70521
Ilmenite-series
83
0.70581
Ilmenite-series
83
0.70595
Magnetite-series
62
0.70725
Magnetite-series
60
0.70769
Ilmenite-series
63
0.70793
Ilmenite-series
72
0.70740
Ilmenite-series
72
0.70840
Ilmenite-series
71
0.70760
Ilmenite-series
81
0.70766
Ilmenite-series
80
0.70796
Ilmenite-series
100
0.70790
Ilmenite-series
89
0.70730
Ilmenite-series
94
0.70790
Ilmenite-series
97
0.70607
-3.0
Magnetite-series
80
0.70519
Ilmenite-series
83
0.70775
Magnetite-series
64
0.70574
Ilm (S-type granite) 16
0.70913
-5.8
Ilm (S-type granite) 14
0.70747
-5.3
Ilmenite-series
66
0.70624
Kinki and Chubu districts
Ilmenite-series
161
0.70727
Ilmenite-series
121
0.70753
Ilmenite-series
121
0.70754
-5.7
Ilmenite-series
71
0.71243
-13.4
Ilmenite-series
99
0.71026
-9.8
Ilmenite-series
93
0.70910
-7.6
Ilmenite-series
82
0.70769
-5.3
Ilmenite-series
149
0.70605
Ilmenite-series
72
0.70711
Ilmenite-series
72
0.71060
Ilmenite-series
83
0.70960
Ilmenite-series
99
0.71010
Ilmenite-series
75
0.70938
Ilmenite-series
78
0.70764
Ilmenite-series
85
0.70728
Ilmenite-series
72
0.70895
Ilmenite-series
78
0.70914
Ilmenite-series
80
0.70951
Ilmenite-series
95
0.70989
Ilmenite-series
80
0.70984
Ilmenite-series
96
0.70687
Magnetite-series
69
0.70912
Magnetite-series
66
0.71000
Ilmenite-series
57
0.71179
Ilmenite-series
79
0.70831
-5.6
Ilmenite-series
85
0.70774
-5.8
Ilmenite-series
67
0.71247
Ilmenite-series
55
0.71052
Ilmenite-series
79
0.70719
Ilmenite-series
62
0.70740
Ilmenite-series
64
0.70803
Ilmenite-series
94
0.70740
Ilmenite-series
55
0.71073
Ilmenite-series
63
0.70778
tapraid4/zqn-ajsc/zqn-ajsc/zqn01010/zqn2165d10a metzgerm S⫽18 3/11/11 16:52 Art:
1242
Bor-Ming Jahn—Accretionary orogen and evolution of the Japanese Islands—
Table A1
(continued)
Sample
No.
Age Rb
Sr
(Ma) (ppm) (ppm)
87
87
86
86
Rb
Sr
Sr
Sr
I (Sr)
Sm
Nd
(ppm) (ppm)
Nd εNd(0) fSm/Nd εNd(T) TDM-1 TDM-2
Nd
(Ga) (Ga)
147
143
144
144
Sm
Nd
Takagi T., 2004. Origin of magnetite- and ilmenite-series granitic rocks in the Japan Arc. American Journal of Science, 304, 169-202.
(compiled data, from 85 sources)
Hida and Kanto districts
Ilmenite-series
62
0.71291
-10.3
Ilmenite-series
60
0.71138
Magnetite-series
183
0.70529
1.3
Magnetite-series
186
0.70487
Magnetite-series
193
0.70441
8.0
Magnetite-series
69
0.70800
Magnetite-series
201
0.70474
Magnetite-series
184
0.70485
Ilmenite-series
58
0.70969
Ilmenite-series
60
0.71320
Ilmenite-series
60
0.71063
Ilmenite-series
92
0.70817
-6.2
Magnetite-series
166
-5.2
Magnetite-series
183
0.70499
1.3
Magnetite-series
173
0.70681
-1.7
Magnetite-series
211
0.70617
Magnetite-series
7
0.70365
9.0
Tohoku district
Ilmenite-series
106
0.70518
0.0
Ilmenite-series
106
0.70553
Ilmenite-series
112
0.70645
Ilmenite-series
115
0.70521
Ilmenite-series
112
0.70493
Ilmenite-series
120
0.70518
Ilmenite-series
119
0.70489
Magnetite-series
107
0.70463
Magnetite-series
128
0.70392
Magnetite-series
157
0.70363
Magnetite-series
157
0.70415
Magnetite-series
124
0.70419
Magnetite-series
107
0.70445
Magnetite-series
132
0.70435
Magnetite-series
142
0.70420
Magnetite-series
138
0.70427
Magnetite-series
118
0.70390
Magnetite-series
135
0.70355
Ilmenite-series
90
0.70496
Ilmenite-series
100
0.70541
Hida and Kanto districts
Ilmenite-series
94
0.70537
-1.9
Ilmenite-series
97
0.70630
-5.7
Ilmenite-series
100
0.70492
-3.9
Ilmenite-series
71
0.70736
-4.8
Ilmenite-series
91
0.70564
-2.6
Ilmenite-series
74
0.70779
-4.7
Ilmenite-series
44
0.70935
-5.3
Magnetite-series
24
0.70528
0.6
Ilmenite-series
95
0.70535
0.5
Ilmenite-series
90
0.70528
0.5
Ilmenite-series
95
0.70521
-0.5
Magnetite-series
128
0.70377
2.7
Magnetite-series
107
0.70398
2.3
Magnetite-series
10
0.70439
4.6
Ilmenite-series
51
0.70452
Ilmenite-series
130
0.70487
Ilmenite-series
134
0.70500
Ilmenite-series
104
0.70536
Ilmenite-series
17.3
0.70460
tapraid4/zqn-ajsc/zqn-ajsc/zqn01010/zqn2165d10a metzgerm S⫽18 3/11/11 16:52 Art:
Implications from a Sr-Nd isotopic study of the Phanerozoic granitoids
1243
Table A1
(continued)
Sample
No.
Age Rb
(Ma) (ppm)
Sr
(ppm)
87
87
86
86
Rb
Sr
Sr
Sr
I (Sr)
Terakado and Nohda, 1993. Rb-Sr dating of acidic rocks from the middle part of the
Inner Zone of southwest Japan: tectonic implications for the migration of the
Cretaceous to Paleogene igneous activity. Chemical Geology, 109, issue 1-4, 69-87
MIYAZ U-IZUSHI area
KyMi-2
61.9 105
186
1.64
0.708731
0.70729
KyMi-10
60.4 145
154
2.71
0.710017
0.70769
KyMi-12
60.4 129
311
1.19
0.708638
0.70762
KyTa-4
60.4 140
199
2.04
0.710009
0.70826
HyIz-43
62.6 139
93.7
4.28
0.711676
0.70787
HyIz-46
62.6 142
119
3.45
0.710537
0.70747
MIYAZ U-IZUSHI area
HyIz-11
62.6
90.3
321
0.82
0.708332
0.70761
HyY-21
62.6 132
128
2.98
0.710682
0.70803
HyIz-21
62.6
62.9
325
0.56
0.708614
0.70812
HyIz-26
62.6
85.9
499
0.50
0.707608
0.70717
HyIz-42
62.6 159
53.2
8.64
0.715588
0.70790
ROKKO-HIRAKI area
ROK-1
72.1 124
81.9
4.37
0.711857
0.70738
ROK-8
71.9 168
63.5
7.67
0.716192
0.70836
ROK-10
71.2 228
18.4
36.00
0.743993
0.70758
ROK-3
71.2 226
21.8
30.10
0.739365
0.70892
ROK-6
71.2 194
65.8
8.56
0.716863
0.70820
ROK-9
71.2
86.7
190
1.32
0.708478
0.70714
ROK-11
71.2
85.3
219
1.13
0.708330
0.70719
ROK-15
71.2 168
45.1
10.80
0.719367
0.70844
NUN-1
70
83.4
249
0.97
0.708379
0.70741
NUN-4
70
72.1
262
0.80
0.708330
0.70754
HRK-1
70.1
92.8
325
0.83
0.708311
0.70749
HRK-2
70.1 163
35.1
13.50
0.720701
0.70726
HRK-4
70.1 139
91.7
4.40
0.711671
0.70729
HRK-13
70.1 122
87.8
4.02
0.711294
0.70729
HyK-1
70.1 127
217
1.69
0.709760
0.70808
HyK-2
70.1 103
191
1.56
0.708920
0.70737
HyTa-1
70.1 123
157
2.27
0.710795
0.70853
HyTa-5
70.1 108
129
2.42
0.710672
0.70826
HyTa-6
70.1 124
174
2.06
0.710277
0.70823
ROK-12
70.1 158
139
3.27
0.711223
0.70797
AWAJI area
AwOz-1
80.9 161
174
2.67
0.710746
0.70768
AwTu-5
80.4 102
189
1.56
0.709770
0.70799
AwNi-1
85.8 125
196
1.85
0.710342
0.70809
HyN-1
80
140
151
2.68
0.711460
0.70841
HyN-2
80
146
142
2.98
0.711820
0.70843
HyAi-17
78.4 120
190
1.83
0.709839
0.70780
HyAi-11
78.4 114
193
1.71
0.709721
0.70782
HyAi-1
78.4 163
121
3.90
0.712260
0.70792
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