accretionary orogen and evolution of the japanese islands—implications...

ACCRETIONARY OROGEN AND EVOLUTION OF THE JAPANESEISLANDS—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 subduction-related orogen developed along the western Pacific convergent margin, and mosttectonic units are composed of late Paleozoic to Cenozoic accretionary complexes andtheir high P/T metamorphic equivalents. The formation of the Japanese Islands hasbeen 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 thesubducting oceanic crust to the orogenic belt. Sengor and Natal’in (1996) named theorogenic complex the “Nipponides,” consisting predominantly of Permian to Recentsubduction-accretion complexes with very few fragments of older continental crust. Theseauthors pointed out the resemblance in orogenic style between Japan and the CentralAsian Orogenic Belt (CAOB). The present work uses new and published Sr-Nd isotopicdata from the literature to test the statements made by these authors. A largeproportion 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 instrong contrast with those of two celebrated accretionary orogens, the Central AsianOrogenic Belt and Arabian-Nubian Shield, but are quite comparable with thoseobserved in SE China and Taiwan, or in classical collisional orogens in the EuropeanHercynides and Caledonides. This raises questions about the bulk composition of thecontinental crust in SW Japan, or the type of material accreted in accretionarycomplexes, and negates the hypothesis that the “Nipponides” contains very fewfragments of older continental crust. The subduction-accretion complexes in Japan arecomposed mainly of recycled continental crust, probably of Proterozoic age. Thisstudy supports the idea that proto-Japan was initially developed along the southeasternmargin of the South China Block.

Key words: Accretionary orogen, accretionary complex, Japanese Islands, Sr-Ndisotope tracer, Mesozoic granitoids, Nipponides, crustal growth, juvenile/recycledcrust, Central Asian Orogenic Belt (CAOB), Arabian-Nubian Shield (ANS), SE China,Taiwan.

introductionAccretionary 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, Proterozoicorogens (for example, the Birimian of West Africa, Svecofennian of S. Finland,Cadomian of NW Europe, and the Arabian-Nubian Shield or ANS), Late Neoprotero-zoic to Mesozoic orogens of the Central Asian Orogenic Belt (CAOB), as well asPaleozoic to Recent orogens of the circum-Pacific, including the Canadian Cordillera,and the Caribbean. Accretionary orogens consist of accretionary wedges containingmaterial eroded from the upper plate and accreted from the downgoing plate, plusisland arcs, ophiolites, oceanic plateaux, old continental blocks, metamorphic rocksand syn- and post-orogenic granitoids (for example, Cawood and others, 2009; Isozakiand 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]

[American Journal of Science, Vol. 310, December, 2010, P. 1210–1249, DOI 10.2475/10.2010.02]

Fn*

1210

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Canadian Cordillera (Samson and others, 1989; Samson and Patchett, 1991), CAOB(Sengor and others, 1993; Sengor and Natal’in, 1996; Jahn, 2004; Kovalenko andothers, 2004) and ANS (Stern, 1994, 2002, 2008; Stein and Goldstein, 1996) haveconfirmed the massive generation of juvenile granitoid crust in the Neoproterozoicand Phanerozoic. This important period of crustal growth was seldom recognized ordown-graded in the classic models of continental growth (Armstrong, 1981; Reymerand Schubert, 1984; McCulloch and Bennett, 1994; Taylor and McLennan, 1995), butis 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-relatedorogen developed along the western Pacific convergent margin, and most tectonicunits are composed of late Paleozoic to Cenozoic accretionary complexes (AC) andtheir high P/T metamorphic equivalents (Isozaki, 1996; Isozaki and others, 2010).Japan appears to provide an ideal model of oceanward growth of an active continentalmargin by subduction-accretion processes. In fact, the formation of the JapaneseIslands has been taken as the classic model for accretionary orogeny and often serves asan example for understanding the crustal evolution of the CAOB and other accretion-ary orogens (Sengor and Natal’in, 1996; Condie, 2007; Cawood and others, 2009).According to Maruyama (1997), the most important cause of the orogeny is thesubduction of an oceanic ridge, by which the continental mass increases through thetransfer of granitic melt from the subducting oceanic crust and/or the mantle wedgeto an orogenic belt. Sengor and Natal’in (1996) named the Japanese orogeniccomplex the “Nipponides,” which consists predominantly of Permian to Recentsubduction-accretion complexes with very few fragments of older continental crust.These authors pointed out the resemblance in orogenic style between Japan and theCAOB, and further emphasized the large mass proportion of the accretionary complexrelative to older continental crust. By implication, the accretionary complex in Japanmust be quite “juvenile” as a whole, and consists mainly of mantle-derived crustalmaterials. In this scenario, voluminous granitic melts emplaced in SW Japan andelsewhere in the Japanese Islands would and should possess Sr-Nd isotopic signaturesindicative of juvenile crust, as observed in many parts of the CAOB or ANS. In the firstinstance, this appears to be in agreement with the absence of Precambrian rocks inJapan. However, the available Sr-Nd isotopic data from the literature and the newanalyses presented here of Cretaceous granites from the Sanyo Belt, Miocene granitesfrom the Shimanto Belt, and Quaternary granites from the Japan Alps, indicate thatthey are in strong contrast with those observed in the CAOB and ANS. In fact, theisotopic 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 rocksgenerated in the Japanese Islands from the Paleozoic to Recent, and argue that, inaddition to the accreted oceanic mafic rocks, the exposed continental crust in SWJapan was produced mainly by remelting or recycling of Proterozoic crust; whereasjuvenile crust of mantle-derivation constitutes only a small proportion. This is contraryto what was predicted by Sengor and Natal’in (1996) for the “Niponides” with respectto the importance of the lithological assemblages of an “ocean plate stratigraphy.” I willconclude that the subduction-accretion complexes in Japan are composed mainly ofrecycled continental crust, probably of Proterozoic age for the main part. On the otherhand, the isotopic data support the tectonic evolution model that proto-Japan wasdeveloped initially along SE China as a part of Cathaysia and shared the samegeochemical and isotopic characteristics as the South China Block (sensu lato; Isozakiand Maruyama, 1991; Maruyama and others, 1997; Isozaki and others, 2010). Themicrocontinent was later separated from SE China and drifted northeastward to formproto-Japan.

1211Bor-Ming Jahn 1211


methodology and source of dataIn 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 waycomparable to the genetic code (DNA) in biology. The continental crust comprises avariety of lithologic types; some of them represent “recycled” products of ancient crust,whereas others show “juvenile” character if they are produced by melting of mantleperidotites or remelting of mantle-derived rocks such as basalts or andesites. A terranecomposed only of island arc or ophiolite assemblages has clearly a juvenile nature, buta 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 tracertechnique is the most powerful tool in the determination of the proportion of themantle component in the making of a continent.

While basaltic rocks are the most commonly used material in studies of thecomposition and evolution of the upper mantle, the genesis and evolution of thecontinental crust must be understood through studies of granitoids because they aregenerally produced by melting of the middle to lower crust, and hence serve as anexcellent probe for the bulk of the continental crust. In the specific case of theJapanese Islands, only granitic rocks will be examined.

The source of data used in this paper is mainly from the literature (see Appendix1), supplemented by new analyses on fourteen Late Cretaceous granitoids from theSanyo Belt of SW Japan, two Miocene granitoids from the Shimanto belt of southernShikoku and two Pleistocene granodiorites (Takidani Pluton) from the Japan Alps innorth-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 dedicatedto the petrogenetic study (Jahn and others, in preparation). Only the Sr-Nd isotopicdata (Appendix 1) will be used in this paper for discussion and illustration.

general geological and tectonic setting of the japanese islandsThe Japanese Islands are composed mainly of subhorizontal nappe piles of an

accretionary complex (AC) and their metamorphic equivalents with late Paleozoic toCenozoic ages (Faure, 1985; Isozaki, 1996; Isozaki and Maruyama, 1991; Isozaki andothers, 2010). Japan is divided into several geologic units with broadly four periods ofaccretion: Permo-Triassic, Jurassic, Cretaceous and Tertiary (Faure and others, 1986;Taira and others, 1989; Ichikawa, 1990; Isozaki and Maruyama 1991). The accretednappe-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 crustalevolution of SW Japan.

According to Maruyama and others (1997), Japan originated from a riftedcontinental margin about 750 to 700 million years ago, when the South China Blockrifted apart from the Neoproterozoic supercontinent Rodinia to open the Paleo-Pacific Ocean (Hoffman, 1991; Dalziel, 1992; Powell and others, 1993; Park and others,1995). Since the tectonic inversion from a passive continental margin to an activeconvergent margin at ca. 450 Ma, proto-Japan has grown asymmetrically oceanward fornearly 400 km across-arc, through successive subduction of the “Pacific plate,” whichincluded the Farallon, Izanagi-Kula, Pacific and Philippine Sea plates. It was in theMiocene that proto-Japan converted to an island arc isolated from mainland Asiathrough 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 Japanand Hokkaido together belong to the North American plate. The Philippine Sea plateis subducting northwestwards at a rate of 4 cm/yr under SW Japan along the NankaiTrough and Ryukyu trench. The Pacific plate is subducting at a rate of 10 cm/yrbeneath NE Japan, with its leading slab reaching a depth of 660 km under Beijing,

1212 Bor-Ming Jahn—Accretionary orogen and evolution of the Japanese Islands—

T1b


China, as revealed by a tomographic study (Zhao and others, 2007; see also a review byIsozaki and others, 2010). Within the main island (Honshu), NE Japan collided againstSW Japan and formed a high mountain chain (elevation �2000 m) called the “JapanAlps.” The mountain chain extends across the Honshu arc and is uplifting very rapidlysince 2 Ma (based on our zircon U-Pb and fission track data; Jahn and others, inpreparation). Two of our analyzed granitoid samples reported herein were collectedfrom the Takidani pluton (or stock) of the Japan Alps (fig. 1).

The predominance of accretionary complexes and the association of detachedcontinental fragments in Japan suggest that the Japanese Islands have developedmainly through convergence between oceanic and continental plates along activemargins (Isozaki, 1997; Isozaki and others, 2010). Isozaki (1996) stated that severalmajor oceanic plates have subducted beneath the South China Block margin, leavingmore 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 andothers, 2010). All the AC belts occur as thin subhorizontal fault-bounded geologicbodies, that is, nappes, and show a clear downward and oceanward younging polarity(Isozaki and Itaya, 1991; Isozaki and Maruyama, 1991). Numerous oceanic fragmentsderived from subducted oceanic plates, including deep-sea sediments and seamountbasalts and reef limestone, were accreted to Japan.

In the tectonic evolution of the Japanese Islands, the Permo-Triassic tectonics isregarded as most important because the basic framework of the Japanese orogenicbelts was established and stabilized at that time (Isozaki, 1996). The occurrence ofPermo-Triassic tectonic units is well developed in SW Japan and the Ryukyu Islands. Bycontrast, 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 weregenerated by subduction of the Farallon plate, and (2) the continent-continentcollisional 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 toTaiwan, represents the southwestern extension of the Permo-Triassic accretionaryorogen in SW Japan.

The Median Tectonic Line (MTL) is a prominent strike-slip fault runningthrough most of SW Japan. It divides SW Japan into two zones: the “Inner Zone” on theback-arc side, and the “Outer Zone” on the fore-arc side (fig. 1). In the Outer Zone, thepost-Jurassic accretionary complexes are arranged to show oceanward younging fromthe Cretaceous to Miocene (Taira and others, 1988), and beyond to the presentaccretionary prism at the Nankai Trough. No collision-related Permo-Triassic unitshave been identified. The deep parts of the accretionary complexes are exposed as alow-pressure to high-pressure regional metamorphic belt, which includes the famousSanbagawa Belt. The Sanbagawa Belt is generally non-eclogitic and consists mainly ofmeta-sedimentary rocks and mafic schists. Most meta-sedimentary rocks are pelitic topsammistic schists and phylites, with rare metachert (quartz schist) and calcareousschists. However, several eclogite bodies occur in the Besshi and Kotsu areas onShikoku Island (Okamoto and others, 2000; Ota and others, 2004; Utsunomiya andothers, 2011). Conspicuous Miocene granitic rocks also occur on the Pacific side of SWJapan. These granitoids intrude into the Cretaceous and Tertiary accretionary com-plexes, and they were likely produced by remelting of the Shimanto accretionarycomplex (Stein and others, 1996; Shinjoe, 1997).

In the Inner Zone (fig. 1), Cretaceous to Paleogene granitoids are extensivelydistributed. Note that the majority of granitic intrusions were emplaced in theCretaceous, and they intruded into the pre-Cretaceous accretionary complexes whichinclude regional metamorphic rocks. The intrusive granitoids are associated with

1213Implications from a Sr-Nd isotopic study of the Phanerozoic granitoids

F1


Tab

le1

Sr-N

dis

otop

icda

taof

gran

itoid

san

dse

dim

ents

ofac

cret

iona

ryco

mpl

exes

from

SWJa

pan

Sa

mpl

e N

o.

Age

(M

a)

Loc

alit

y Pl

uton

nam

eor

for

mat

ion

Roc

k ty

pe

[Rb]

(p

pm)

[Sr]

(p

pm)

87R

b 86

Sr

87Sr

86

Sr

±2σ m

I(S

r)

TM

(M

a)

(I =

0.7

08)

TM

(M

a)

(I =

0.7

07)

[Sm

] (p

pm)

[Nd]

(p

pm)

147 Sm

14

4 Nd

143 N

d 14

4 Nd

±2σm

εNd(

0)ε N

d(T

)f

(Sm

/Nd)

TD

M-1

(Ma)

T

DM

-2(M

a)

70N

-508

72

Mat

suda

qua

rry,

Nae

gi

Nae

gi E

ast

co. b

iotit

e gr

anite

20

468

.58.

61

204

90.

7081

073

81

7.06

31.9

4 0.

1335

0.

5121

753

-9.0

-8

.5

-0.3

218

48

1581

6911

-213

64Iw

amot

o qu

arry

,H

iruk

awa

Nae

gi W

est

med

. bio

tite

gran

ite

335

12.6

77.4

33

520

0.

7081

164

65

7.10

23.0

9 0.

1858

0.

5122

204

-8.2

-8

.1

-0.0

650

14

1580

75T-

175A

64Sh

inde

n, H

iruk

awa

Nae

gi W

est

med

. bio

tite

gran

ite

338

14.6

67.5

33

88

0.70

853

65

667.

1823

.50

0.18

47

0.51

2198

7-8

.6

-8.5

-0

.06

4939

16

14

6911

-211

64K

anei

shi q

uarr

y,H

iruk

awa

Nae

gi W

est

biot

ite g

rani

te

346

5.40

18

8 34

6 7

0.70

757

6464

9.25

25.4

7 0.

2195

0.

5122

234

-8.1

-8.3

0.12

-2

6628

1621

TK

M 1

74

O

dou

rive

dam

-site

, O

htsu

T

anak

ami

med

. bio

tite

gran

ite

223

101.

56.

34

223

6 0.

7110

810

8 11

9 6.

21

24.2

3 0.

1548

0.

5120

845

-10.

8 -1

0.4

-0.2

1 27

43

1756

TK

M 2

74

M

isuj

i wat

er-f

all,

Oht

su

Tan

akam

ico

. bio

tite

gran

ite

340

4.80

209

340

10

0.69

855

71

717.

6021

.69

0.21

18

0.51

2257

5-7

.4

-7.6

0.

0858

909

1557

TK

M 3

74

M

iyam

achi

, Sh

igar

aki-

cho

Tan

akam

ico

. bio

tite

gran

ite

176

65.9

7.74

176

90.

7105

297

106

6.22

25.9

20.

1450

0.

5120

484

-11.

5-1

1.0

-0.2

624

33

1800

TK

M 4

74

K

ouga

Gol

f,

Koz

ai-c

ho

Tan

akam

ifi

ne b

iotit

egr

anite

26

034

.921

.6

260

26

0.70

737

72

755.

8422

.44

0.15

72

0.51

2145

6-9

.6

-9.2

-0

.20

2696

16

61

TK

M 5

67

K

ouga

Gol

f, s

outh

en

d T

anak

ami

fine

bio

tite

gran

ite

354

4.99

209

354

22

0.70

849

67

6812

.60

33.6

7 0.

2283

0.

5121

8514

-8

.8

-9.1

0.

16-1

0456

1694

TK

M 6

74

M

yoka

nji,

K

ozai

-cho

Tan

akam

ico

. bio

tite

gran

ite

307

18.8

42.3

30

716

0.

7133

783

85

6.90

22.2

9 0.

1871

0.

5121

476

-9.6

-9

.5

-0.0

556

60

1699

6910

-105

85Ta

kam

atsu

-cho

,O

kaya

ma

S O

kaya

ma

hb-b

io g

rani

te

148

163.

22.

62

148

11

0.70

671

50

77

4.75

21

.64

0.13

27

0.51

2400

5 -4

.6

-3.9

-0

.33

1409

12

20

6910

-157

A

85

Miy

oshi

min

e gu

lch,

Oka

yam

a S

Oka

yam

a fi

ne b

iotit

e le

ucog

rani

te

390

10.0

114

390

80.

7099

886

87

7.29

22.0

9 0.

1995

0.

5124

194

-4.3

-4

.3

0.01

7675

12

81

72T

O-2

87

85

Sosh

a, O

kaya

ma

S O

kaya

ma

fine

bio

tite

gran

ite

383

9.17

122

383

80.

7090

486

86

7.20

21.8

0 0.

1997

0.

5124

274

-4.1

-4

.1

0.02

7699

12

68

BJ0

3-2

85

Miy

oshi

min

e ar

ea

S O

kaya

ma

very

fin

e le

ucog

rani

te

458

7.63

177

458

90.

7070

885

857.

8722

.20

0.21

32

0.51

2446

5 -3

.7

-3.9

0.

08

1343

7312

56

R

1291

1 1.

9 H

otak

a D

ake

area

, Ja

pan

Alp

s Ta

kida

ni

hb-b

iogr

anod

iori

te

80.1

32

8.3

0.70

6 80

.1

13

0.70

748

4.03

19

.85

0.12

27

0.51

2462

6 -3

.4

-3.4

-0

.38

1152

11

08

R12

915

1.9

Hot

aka

Dak

e ar

ea,

Japa

n A

lps

Taki

dani

hb-b

iogr

anod

iori

te

107

295.

11.

05

107

11

0.70

732

6.07

29

.52

0.12

43

0.51

2469

14

-3.3

-3

.3

-0.3

7 11

60

1099

BJ0

6-20

1a

15K

ashi

waj

ima,

SW

Sh

ikok

u

bio

gran

ite

148

126.

23.

38

148

13

0.70

797

6.93

30

.83

0.13

59

0.51

2387

12

-4.9

-4

.8

-0.3

1 14

92

1245

BJ0

6-20

2b

15

Kas

hiw

ajim

a, S

W

Shik

oku

gt-b

io g

rani

te

141

126.

53.

21

141

12

0.70

797

7.13

32

.46

0.13

28

0.51

2393

8-4

.8

-4.7

-0

.32

1424

12

32

BJ0

6-20

4 60

Sh

iman

to B

elt,

S co

ast S

hiko

ku

mél

ange

bel

tm

udst

one

137

102.

93.

8713

712

0.71

242

4.72

25

.49

0.11

19

0.51

2329

6 -6

.0

-5.4

-0

.43

1229

13

06



Tab

le1

(con

tinue

d)Sa

mpl

e N

o.

Age

(M

a)

Loc

alit

y

Plut

on n

ame

or f

orm

atio

n R

ock

type

[R

b]

(ppm

)[S

r]

(ppm

)

87R

b 86

Sr

87Sr

86

Sr

±2σm

I(S

r)

TM

(M

a)

(I =

0.7

08)

TM

(M

a)

(I =

0.7

07)

[Sm

] (p

pm)

[Nd]

(p

pm)

147 Sm

14

4 Nd

143 N

d 14

4 Nd

±2σm

εNd(

0)ε N

d(T

)f

(Sm

/Nd)

TD

M-1

(Ma)

T

DM

-2(M

a)

BJ0

6-20

5 60

Sh

iman

to B

elt,

S co

ast S

hiko

ku

mél

ange

bel

t si

ltsto

ne

38.7

24

0.6

0.46

6 0.

7086

3211

0.

7082

3

2.

80

15.1

7 0.

1116

0.

5122

968

-6.7

-6

.0

-0.4

3 12

73

1358

BJ0

6-20

6 60

Sh

iman

to B

elt,

S co

ast S

hiko

ku

mél

ange

bel

t re

d ch

ert

161

73.1

6.

38

0.72

3833

11

0.71

839

4.79

23

.93

0.12

10

0.51

2229

6 -8

.0

-7.4

-0

.38

1512

14

78

BJ0

6-20

7a

60

Shim

anto

Bel

t, S

coas

t Shi

koku

m

élan

ge b

elt

silts

tone

22

.5

493.

50.

132

0.70

6805

110.

7066

95.

0521

.61

0.14

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coeval rhyolites and ignimbrites even though much of this cover series has beeneroded to expose the intrusive rocks. In addition, a few collisional belts, or non-accretionary units (Hida and Oki belts, fig. 1), occur in the northern part, and they arecomposed 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 oredeposits. He divided the Inner Zone into three metallogenic provinces, from south tonorth, a Barren, a Tungsten, and a Molybdenum Province (see also Ishihara andMurakami, 2006). The three provinces correspond to the Ryoke, Sanyo and Sanin Beltsas 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) classifiedthe Sanin Belt as belonging to the magnetite-series, whereas the two other belts belongto the ilmenite-series. The magnetite-series rocks contain higher Fe2O3/FeO ratiosthan the ilmenite-series rocks.

The lithological types in the Inner Zone are more extensive than granitoids andacid volcanic rocks alone. In fact, the Ryoke belt is a plutonic-metamorphic terranethat comprises unmetamorphosed pre-Cretaceous accretionary complexes with high-level granites, as well as high-grade, but low P/T, metasediments with migmatites and

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Fig. 1. General geologic map of SW Japan. The Median Tectonic Line (MTL) separates the granitoid-dominated terrane to the north from the Mesozoic-Cenozoic accretionary wedge to the south. The granitoidterrane is divided into three granitic belts (Ryoke, Sanyo and Sanin) based on the type of mineral depositsand 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 theJapan Alps. Their localities are given in table 1. The numerals in yellow circles correspond to the followingliterature data sources with the localities of study areas given in Appendix 1: (1) Arakawa (1990), Arakawaand 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 andothers (2000), (8) Morioka and others (2000), (9) Nakajima and others (2004), (10) Shinjoe (1997), (11)Takagi and Kagami (1995), (12) Terakado and Nohda (1993).


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gneissic granites. Granitic rocks are dominant over metamorphic rocks. Based on theapparent along-arc variation of isotopic ages, it has been suggested that the Ryoke andSanyo granitoids were produced by Cretaceous subduction of the Kula-Pacific ridgeand that the magmatism migrated eastward with passage of the ridge along the SWJapan margin (for example, Nakajima, 1994). However, such eastward migration ofmagmatic activities has not been verified.

Isozaki and others (2010) described that the continental side of the MTL (� InnerZone) is composed of a 15 km-thick lower crust of unknown composition, a 20km-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 subhorizontalstacks of multiple fault-bounded units, previously recognized as “nappes,” with a gentledip towards the Eurasian continent.

sample descriptionsIn this paper new Sr-Nd isotopic analyses (table 1) of samples, including grani-

toids, siltstones and cherts, are used in graphic representations. The collection of thesesamples was not systematic and different samples serve different purposes. The newdata only supplement the existing large dataset in the literature used in this paper (seeAppendix 1). The granitic rocks were collected by S. Ishihara from four plutons (NaegiEast, Naegi West, Tanakami, and S. Okayama) of the Sanyo Belt, SW Japan. The ageinformation was obtained from the literature. The Naegi granites were dated at 64 to72 Ma (K-Ar mineral ages) by Ishihara and others (1988). The Tanakami granites haveK-Ar biotite ages of 73.3 and 74.7 Ma for the central part, but 67.9 Ma for the easternpart of the pluton (Sawada and Itaya, 1993). For the granites of the Okayama area, amuscovite 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 wasobtained for the southern Okayama batholith (Kagami and others, 1988).

Two hornblende-biotite granodiorite samples from the Takidani pluton of theJapan Alps and two biotite granites from the Kashiwajima pluton of SW Shikoku werealso analyzed. The emplacement ages of these granitoids have been firmly establishedat 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 andK-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 accretionarycomplex (Inuyama area) were also included for analysis. This was to test the source ofthe sediments from the “ocean plate stratigraphy,” long considered to be the principalcomponent of the accretionary complexes of Japan.

sr-nd isotope dataFor 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 FinniganMAT-262 Thermal Ionization Mass Spectrometers (TIMS). Mass fractionation wascorrected against 86Sr/88Sr � 0.1194 and 146Nd/144Nd � 0.7219. All isotopic ratioswere finally adjusted against the standard salts of NBS-987 Sr � 0.710250 and La JollaNd � 0.511860. The in-run precisions as shown in the analytical tables are expressed as2 standard errors (2 sigma-mean), and they are approximately equal to 0.1 epsilonunit. However, the external precisions based on long-term duplicate analyses onstandard salts yielded about 0.4 epsilon unit.

All the new and literature Sr-Nd data used in the present paper are summarized inAppendix 1 and further illustrated in figures 2, 3, 4 and 5. Figure 2 shows a plot ofinitial 87Sr/86Sr ratios as a function of intrusive ages of granitoids and depositional agesof sedimentary rocks (siltstone and mudstone). The new data for granitoids are


F2


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 analysesof siltstones and cherts from the accretionary complex are shown with solid blue andgreen 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 250Ma, but the majority of them were emplaced in the Cretaceous (145-65 Ma); Triassicand Jurassic granites are relatively rare. (2) Most granitic rocks are characterized byinitial 87Sr/86Sr ratios higher than 0.705, which is a value typically observed forgranitoids of the Central Asian Orogenic Belt (for example, Jahn, 2004). (3) Grani-toids with initial 87Sr/86Sr ratios lower than 0.705 are mainly from the Jurassic HidaBelt (185-190 Ma), or were emplaced in the Early Cretaceous (140-100 Ma) andCenozoic (50-10 Ma). The low ratios suggest that these granitic rocks were likelyproduced by remelting of mantle-derived rocks (gabbros), or a lithological assemblagecontaining a large proportion of mantle component (accreted ocean plate stratigra-phy). (4) The high initial 87Sr/86Sr ratios (ISr value) indicate that the generation ofgranitic rocks must have involved a participation of much older rocks. That is, asignificant proportion of Precambrian crust is required in the source regions for thegeneration of these granites. Although no Precambrian rocks have been identified inJapan, the presence of protoliths with Precambrian heritage in the middle to lowercrust 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

Fig. 2. Initial Sr isotopic ratios (�ISr) of granitoids and sedimentary rocks of two accretionarycomplexes from SW Japan. A line at ISr � 0.705 is drawn for reference. Granitoids with ISr lower than this lineare considered “juvenile” and those with values higher than 0.710 are mainly “recycled.” The proportion ofthe recycled crustal component increases with increasing ISr values. Data sources: New data (table 1); Kagamiand 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 befound in table 1 and Appendix table.


F3

COLOR


(235) is reduced to about a half of the Sr isotope data. However, the distribution ofdata points, with respect to the reference line of εNd(T) � 0, form an impressive mirrorimage of the Sr isotope data (fig. 2). The majority of the data points show negativevalues. Granitic rocks with a large proportion of mantle component are expected tohave 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 figure3 indicates that most of the granitic rocks were derived by melting of protoliths with alarge proportion of recycled crust of Precambrian age.

εNd(T) and ISr values are commonly anti-correlated in most rocks. Figure 4 showsthat the majority of granitoids from SW Japan fall in the fourth quadrangle of theεNd(T) vs (87Sr/86Sr)o (�ISr) diagram, which is segmented by two reference lines—ahorizontal zero εNd(T) line (or CHUR, Chondritic Uniform Reservoir) and a verticalline of ISr � 0.7045 for Earth’s primitive mantle (PM). The data array is very similar tothat commonly observed for crustal rocks. Most mantle-derived mafic rocks and“juvenile” granitoids would reside in the second quadrangle, but only a few granitoidsof SW Japan are found there. Granitoids of the Hida Belt are distinguished from thebulk of the Japanese granitic rocks and have Sr-Nd isotope compositions close to thereference point of the primitive Earth (� intersection of the two reference lines).

The Sr-Nd isotopic characteristics of the Japanese granitoids indicate that theyhad a long crustal residence time. Figure 5 shows a plot of εNd(T) vs depleted-mantle-

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 negativevalues. 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).


F4

F5

COLOR


based single-stage and 2-stage model ages (TDM-1 and TDM-2). The reason for using the2-stage model age calculation is that some of the new analyses were obtained on highlydifferentiated granitic rocks with the lanthanide tetrad effect, which often leads toaberrant very large or negative model ages due to the increase of Sm/Nd ratios in thefinal stage of differentiation (Jahn and others, 2001). In figure 5, while the intrusiveages of the granitoids are younger than 250 Ma (shown by the yellow band), theirmodel ages are much older, from ca. 700 to over 2000 Ma. This suggests that theprotoliths of the granitoids contain a significant proportion of Precambrian crust. Thescenario is much the same as that for the Cenozoic sedimentary rocks of Taiwan, to beillustrated in a later section.

discussionTogether with the Japanese Islands, the Central Asian Orogenic Belt (CAOB) and

the Arabian-Nubian Shield (ANS) are three well-known “young” accretionary orogensformed in the Neoproterozoic or later. Therefore, a comparison between the threeaccretionary orogens in terms of their crustal development could be instructive.Numerous Sr-Nd isotopic analyses have confirmed that much of the crustal mass of theCAOB 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 crystalliza-tion of basaltic and andesitic magmas (for granitoids). Juvenile crust has substantiallycontributed 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; Kovalenkoand others, 2004; Eyal and others, 2010).

Fig. 4. εNd(T) vs (87Sr/86Sr)o plot for granitoids and sedimentary rocks from SW Japan. The majority ofgranitoid data points fall in the fourth quadrangle, suggesting their “recycled” nature. Data sources as infigure 3.


COLOR


Comparison with the CAOBThe 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. Itrepresents about 11 percent of Asia. NE China is also included even though most of ithas been named as the “Manchurides” by Sengor and Natal’in (1996). The Nd isotopiccharacteristics of granitoids from the different terranes of the CAOB are summarizedand illustrated in figure 6.

NE China and Inner Mongolia.—In NE China, more than 350 granitic bodies wereemplaced in the Great Xing’an (or Khinggan), Lesser Xing’an and ZhangguangcaiRanges, and mostly during Mesozoic times (Wu and others, 2011). The granites arecomposed mainly of I-type and subordinate A-type granites (Wu and others, 2000,2002, 2003a, 2003b). They are accompanied by extensive Mesozoic and Tertiary acidvolcanic rocks. Isotope tracer analysis and age determination of deep-drill cores fromthe Songliao Basin in central NE China revealed that the Basin is underlain by graniticrocks and deformed granitic gneisses of Phanerozoic age (Wu and others, 2001).Precambrian zircons have been identified, but they are substantially rarer (Wu andothers, 2011). Based on the time-space distribution of the granitic rocks, Wu and

Fig. 5. εNd(T) vs TDM (depleted-mantle-based model ages) plot for granitoids from SW Japan. Becausesome granites show the REE tetrad effect, which produced aberrant age values in the single-stage TDMcalculation, 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.


F6

COLOR


others (2011) suggested that the Jurassic granites in the Zhangguangcai Range wereprobably related to Paleo-Pacific plate subduction, whereas the Early Cretaceousgranites in the Great Xing’an Range resulted from delamination or extension of thepreviously thickened lithosphere.

In Inner Mongolia, several periods of granitic intrusion took place from Devonianto Jurassic times. The samples used in this study came from a Paleozoic anorogenicA-type suite (280 Ma; Hong and others, 1995, 1996), an arc-related calc-alkalinemagmatic belt composed of gabbroic diorite, quartz diorite, tonalite and granodiorite(SHRIMP zircon age � 309 � 8 Ma, Chen and others, 2000) and a Mesozoiccollision-type granitic suite comprising monzogranite (adamellite), granodiorite andleucogranite (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 PrecambrianJiamusi Massif (εNd(200 Ma) � �7 to �12). Such a close relationship between theisotopic compositions of granitoids and the ages and nature of their intruded “base-ment” rocks is also demonstrated by the granitoids from northern Xinjiang (Hu andothers, 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 crustalrocks in their magma genesis.

-25

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Intrusive Age (M a)

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Data: Kovalenko and others (1996)

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Intrusive Age (Ma)

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NE ChinaEast JunggarInner MongoliaTransbaikaliaW Altai-Sayan

Post-collisional granites (CAOB)

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C D

Intrusive Age (M a) Intrusive Age (M a)

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 (Heinhosrtand others, 2000; Kroner and others, 2008), Xinjiang—Altai Mountains (Zhao and others, 1993; Wang andothers, 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 (NEChina: 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).


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Xinjiang and Kazakhstan.—A variety of Phanerozoic granitoids occur throughoutnorthern Xinjiang. As for the case of NE China, the majority of granitoids have positiveεNd(T) values which suggest a dominance of the mantle component in the generationof these rocks (fig. 6B). This is particularly true for the granitoids from the E and WJunggar terranes (Zhao and others, 1993; Han and others, 1997; Chen and Jahn,2004). The Junggar Basin is covered by Cenozoic desert sands and thick continentalbasin sediments (�10 km) of Permian and younger ages. Drilling records indicatelittle deformation within the basin, suggesting stability of the basement at least sincethe Permian (Coleman, 1989). The nature of the Junggar basement has been muchdebated; some consider that it represents a micro-continent with Precambrian base-ment (Wu, 1987), whereas others regard it as trapped Paleozoic oceanic crust ofvarious origins (Feng and others, 1989; Hsu, 1989; Coleman, 1989; Carroll and others,1990). Surrounding the Junggar Basin are exposed numerous ophiolites in the Eastand West Junggar terranes, as well as in its southern margin. These terranes can beappropriately referred to as “island-arc assemblages,” and no rocks of Precambrian agehave been documented. Coleman (1989) considered these terranes as oceanic arcassemblages, and compared them with those in the present western Pacific. Based on atrace-element and Sr-Nd isotopic study, Chen and Jahn (2004) concluded that thebasement is most likely underlain by Early to Middle Paleozoic arc rocks and oceaniccrustal assemblages that were trapped during the Late Paleozoic tectonic consolidationof Central Asia. This is consistent with the very young model ages ranging from 400 to1000 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 compositeterrane show a wide range of isotopic composition and model ages (Hu and others,2000; Wang and others, 2009). A tight relationship between the isotopic compositionsof granitoids and the nature of their basement rocks can be established. The Sm-Ndisotope study by Hu and others (2000) revealed that the basement rocks of the Altaiand Tianshan were largely produced in the Proterozoic. The parallel manifestation ofisotopic compositions and model ages between basement rocks and intrusive granitesargues for the significant role of crustal “contamination” in the genesis of thePhanerozoic granitoids. An implication is that the presence of old Precambrianmicrocontinents is significant in the accretionary history of Central Asia (Kroner andothers, 2007). A more quantitative study on the proportion of the mantle componentin the crust of the Altai Mountains was presented by Wang and others (2009).

Heinhorst and others (2000) undertook a comprehensive study of mineralizationin association with a variety of magmatic rocks in east-central Kazakhstan. Although thetypes of mineralization (Au, Cu, rare-metal, or REE) may be related to a particularmagmatic suite or a lithological variety, most granitic rocks have positive εNd(T) valuesirrespective of their bulk compositions and types of mineralization (Heinhorst andothers, 2000). The granitoids were intruded in several episodes: 450 and 300 Ma formagmatic suites with gold mineralization, about 300 Ma for granitoids with rare-metalmineralization, and ca. 250 Ma for A-type granites with REE mineralization. There is aslight tendency for an increase of εNd(T) with younger ages of the rocks. Single-stagemodel ages for all cases are between 400 and 1500 Ma.

Mongolia and Transbaikalia.—Figure 6C shows the Nd-Sr isotopic compositions ofgranitoids from the northern belt of central Mongolia to Transbaikalia. This area hasbeen extensively studied by Kovalenko and others (1996, 2004). These authorsdelineated four isotope provinces (Precambrian, “Caledonian,” “Hercynian,” and“Indonesian”), which coincide with three tectonic zones of corresponding ages for thenorthern belt of the CAOB, and with one (Indonesian) in Inner Mongolia and NEChina (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



terrane is the only early Precambrian microcontinent containing granulitic andamphibolitic gneisses of Archean age. The Barguzin Belt and the Hangay-Hentey Basinare known to be “composite” terranes comprising Proterozoic and Phanerozoicformations. The Hangay-Hentey Basin is intruded by impressive amounts of EarlyPalaeozoic to Mesozoic granitoids. The granitoid belt extends to Transbaikalia andfurther 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 character-istics, whereas those intruded into the Baydrag and the composite terranes (Barguzinand Hangay-Hentay) show εNd(T) values from positive to negative, indicating variablecontributions of Precambrian crust in the generation of the granitic rocks. Note thatsome 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 mantlecomponent (�100% basaltic and/or andesitic source).

Most plutons and batholiths of the CAOB have calc-alkaline characteristics typicalof subduction zone magmatism, but the emplacement of voluminous granites of thealkaline and peralkaline series also deserves attention. Petrogenetically, these rocks areakin to the A-type granites, which are generally known to form in post-collisionalextensional environments (for example, Jahn and others, 2009). Figure 6D summa-rizes the isotopic characters of this kind of granite from the CAOB. The majority ofthese rocks possess positive εNd(T) values; only a few show negative values. All of themhave young model ages (TDM) from 500 to 1300 Ma. This indicates that the source ofpost-accretionary granitoids in the CAOB is dominated by the mantle-derived compo-nent.

Comparison with the ANSThe 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 juvenileformed 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 followedby continental collision at 640 to 650 Ma (Stern, 1994, 2002, and references therein).The Late Neoproterozoic post-collisional stage of tectonomagmatic evolution of theANS commenced at �640 Ma. Transition from collision to extension occurred at �600Ma (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 granitoidmagmatism, thought to be well correlated with the changing tectonic setting (Bentor,1985; Stern and Hedge, 1985; Bentor and Eyal, 1987; Kroner 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 magmatismincluding early medium-K calc-alkaline plutons (now gneisses) and metavolcanic rocksoccurred at �820 to 740 Ma; (2) late syn-collisional medium- to high-K calc-alkalinegranitoids and gabbro that bear evidence for penetrative deformation and low-grademetamorphism intruded at �670 to 635 Ma; (3) the most voluminous post-collisional(undeformed) high-K calk-alkaline gabbro-granodiorite-granite suite formed at �640to 610 Ma; and (4) within-plate alkaline and peralkaline granite suites preceded byintensive bimodal volcanism at �600 to 550 Ma.

Eyal and others (2010) recently conducted a petrological and geochemical studyof 27 calc-alkaline and alkaline plutons/complexes and one dike swarm from the SinaiPeninsula, in the northern part of the ANS. Granites of the alkaline suite were studiedin 16 plutons ranging in size from 1 to 400 km2, some of which are central plutons in



ring complexes. The most celebrated example is the Katherina ring complex (Katzirand others, 2007a), in which granite is intrusive into volcanic rocks and ring dikes andoften shows miarolitic texture, indicating crystallization at shallow depth. The majorityof alkaline plutons are composed of syenogranite, alkali feldspar granite and peralka-line 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 arecharacterized 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 fromca. 800 to 1100 Ma for the alkaline suite. Single-stage model ages are quite similar tothe two-stage model ages, suggesting that fSm/Nd values for most rocks are close to thatof the average continental crust (ca. �0.4). The Nd model ages suggest that littleArchean or early Proterozoic rocks exist in the lower to middle crust of the northernANS. This inference is supported by the U-Pb dating of individual zircon grains fromvarious plutonic rocks (Be’eri-Shlevin and others, 2009). The petrogenesis and se-quence of emplacement for the alkaline and post-collisional granitoids from the SinaiPeninsula have been discussed in detail by Eyal and others (2010).

Comparison Between Japan, CAOB and ANSThe 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 wereproduced by partial melting of mantle-derived protoliths with little contribution frommuch older rocks. More specifically, granitoids were generated by differentiation ofmantle-derived dioritic magma in the early stage of arc formation; by remelting ofmantle-derived arc rocks in later stages, with only very small amounts of Pre-Neoproterozoic crustal component; and by remelting of underplated basic rocks inpost-orogenic stages.

The dominance of positive εNd(T) values for the CAOB granitoids indicates thatmost granitoids are “relatively juvenile,” and that others have witnessed a greatercontribution from Archean to early Proterozoic micro-continents, hence producinggranitoids with negative εNd(T) values. By contrast, the granitoids from SW Japan havedominantly negative εNd(T) values and relatively high initial 87Sr/86Sr ratios (�0.707),suggesting involvement of a significant amount of recycled crustal rocks. Theirformation and emplacement in Japan do not imply a net growth of the continentalcrust. If the granitoids were derived by partial melting of accreted terranes, it suggeststhat the essential component of the accreted material is recycled crust of ultimatelyPrecambrian 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-Tanbaaccretionary complex (Shibata and Adachi, 1974). Maruyama (1997) hypothesizedthat the most important cause of the orogeny in SW Japan is the subduction of anoceanic ridge, by which the continental mass increases through the transfer of graniticmelt from the subducting oceanic crust to the orogenic belt. The present analysis ofSr-Nd isotopic data does not support such a hypothesis.

Comparison with SE China and TaiwanWhile the Nd isotopic characteristics of the Japanese accretionary orogen can be

distinguished from those of the CAOB and ANS, they are surprisingly comparable withthat of well-known “collisional orogens,” such as the Caledonides and Hercynides ofwestern Europe (Jahn and others, 2000a, 2000b; Jahn, 2004), the Paleozoic toMesozoic 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 Ndand 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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Granitoids & rhyolitesMafic dikes and trachydoleritesElat schists

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Southern Israel

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Monzogabbro, monzodiorite, Q monzodiorite

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Aqaba ComplexAraba Complex

Southwestern Jordan

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B

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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Granitoids of Katherina Complex

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Eastern DesertEgypt

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Fig. 7. (continued) (C) Sinai Peninsula (Katherina Complex: Stein and Goldstein, 1996; Katzir andothers, 2007a, 2007b; Eyal and others, 2010. Kid area, SE Sinai: Moghazi and others, 1998). (D) EasternDesert (Wadi El-Imra: Furnes and others, 1996; Gebel El-urf area: Moghazi, 1999). Data compilation by BorisLitvinovsky.


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Fig. 8. (A) εNd(T) vs. intrusive age plot of granitic rocks from the South China Block (Yangtze andCathaysia). Data sources: Chen and Jahn, 1998 and references therein; additional data from Hsieh andothers (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. Datasources as for (A).


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China: Dabie, Yangtze and Cathaysia. In the present compilation, literature datapublished since 1999 are included with the pre-1998 data. The combined data areillustrated in figure 8. Phanerozoic granitoids from SE China were emplaced fromabout 470 to 80 Ma, and are characterized by negative εNd(T) values from �17 to about0, with a few exceptions (fig. 8A). The granitoids have depleted-mantle-based modelages (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 tookplace in the Proterozoic, possibly with a very minor proportion produced in the LateArchean. I defend this statement even though an increasing number of Archean zircongrains have been identified in recent years in the Yangtze craton (for example, Zhengand others, 2006; Zheng and Zhang, 2007). In summary, the crustal evolution in SEChina, including the Yangtze Craton and Cathaysia, is distinctly different from theArchean-dominated North China Block (Chen and Jahn, 1998). Interestingly, theranges of εNd(T) and TDM are very similar to those of the Hercynian and Caledonianbelts in Europe (Jahn and others, 2000a, 2000b; Jahn, 2004).

The island of Taiwan is geologically young. The oldest rocks are the marblesequences from the Tanan’ao Complex in the east and from the “Peikang High” in thewest of the island, which were dated at about 250 Ma using their Sr isotopic composi-tions and the Pb-Pb isochron technique (Jahn and others, 1992). Granitic intrusionsare rare. A few small plutons of Cretaceous granitoids were emplaced in the Tanan’aoComplex, whereas a small Jurassic granite stock occurs within the schist belt of thesouthern Central Range (Yui and others, 2009). The mountain belts were formed bythe collision between the Eurasian and the Philippine Sea plates. A close geologicalcorrelation between Taiwan and SE China has long been established using geochrono-logical and geochemical data of the Mesozoic granitoids and the Late Permiancarbonates (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 granitoidsand metasedimentary rocks from Taiwan. The main figure is a plot of εNd(T) vsone-stage model age (TDM-1), whereas the inset is a plot of εNd(T) vs two-stage modelage (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 (Yuiand others, 2009). Single-stage model ages vary from 700 to 2000 Ma. This scenario issurprisingly similar to that of SW Japan (fig. 5). The Sm-Nd isotopic data of sedimen-tary 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 calculatedmodel ages (TDM). The model ages of sediments from Taiwan range from ca. 1200 to2300 Ma, whereas those from Japan show a wider range from 700 to 2600 Ma. Theyounger model ages of Japan indicate that these sedimentary rocks contain a higherproportion of the mafic component from the “ocean plate stratigraphy.” Nevertheless,the dominance of model ages between 1200 to 2500 Ma suggests that the sedimentaryrocks represent recycled Precambrian protoliths. Note that recent zircon geochronol-ogy of the Cenozoic sedimentary rocks in Taiwan has revealed many zircon grains ofArchean age (Shao and others, 2010). In fact, the Cenozoic accretionary wedge ofTaiwan is dominated by sediments of Cathaysian derivation.

tectonic implicationsSince the early Paleozoic, westward subduction of the Paleo-Pacific plate has

governed the tectonic evolution of the eastern Eurasian margin by building wide beltsof accretionary wedge along trench and plate-marginal volcanic-plutonic belts (Isozaki,1996, 1997; Kimura, 1997; Maruyama, 1997; Maruyama and others, 1997; Isozaki andothers, 2010). In the preceding sections, only SW Japan was discussed because thepattern of crustal growth of the Paleozoic to Mesozoic accretionary complexes is bestexemplified in SW Japan, due to the rapid Quaternary uplift and erosion of the


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Cenozoic cover. SW Japan is composed, from the continental side to ocean, of nineaccretionary complex units (Oeyama, Renge, Akiyoshi, Suo, Ultra-Tanba, Mino-Tanba-Chichibu, Sanbagawa, Northern Shimanto and Southern Shimanto belts (Isozaki andothers, 2010). The units have almost the same rock assemblages of the “ocean platestratigraphy,” including MORB-type basalt, chert, hemipelagic mudstone, limestone,turbidite or sandstone and conglomerate. The ocean plate stratigraphy records thehistory of sedimentation on the ocean floor as it travels from a ridge to a trench. In thescheme 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 theaccretionary complexes. However, it is not clearly shown whether the protoliths of thegranitoids were the accretionary complexes or the old Yangtze lower crust. The idea ofslab melting for the genesis of the vast amounts of granitic rocks (Maruyama, 1997) wasdeemed unlikely from the present analysis.

The revelation of the dominantly Precambrian heritage for granitoids of SWJapan is critical to the tectonic reconstruction of the Japanese Islands. An importantquestion is why, in terms of the Sr-Nd isotopic compositions, the Japanese accretionaryorogen is so different from other accretionary orogens, such as the CAOB and ANS. Bycontrast, the accretionary orogens of SW Japan are more comparable with the

Fig. 9. εNd(T) vs. model age plots of granitoids and metasedimentary rocks from Taiwan. (A) TDM-1 modelages are calculated with a single-stage model in which the Sm/Nd ratio of a rock is assumed to be identical to thatof its protolith. (B) TDM-2 model ages are obtained with a two-stage model in which the protolith of the first stageis assumed to have evolved as the average continental crust with 147Sm/144Nd � 0.12, or f(Sm/Nd) � �0.4 (seefootnote of table 1). Data sources: Chen and others (1990), Lan and others (2008). Because some granites showthe REE tetrad effect, which produced aberrant age values in the single-stage TDM calculation, the 2-stage modelages (TDM-2) values are also calculated for comparison (B).


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collisional orogens in SE China, Taiwan, and even the European Caledonides andHercynides. On the other hand, the similarity of isotopic signatures between Japan andSE China supports the models of tectonic evolution and paleogeographic position ofproto-Japan proposed by Maruyama and others (1997) and Sengor and Natal’in(1996). Both models proposed that the Pre-Cenozoic accreted terranes were devel-oped along the continental margin of SE China (fig. 11). According to Maruyama andothers (1997), the Ryoke low P/T and the Sanbagawa high P/T belts, as well as theShimanto accretionary complex, began to develop close to the present coast of SEChina 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) inthe Early Jurassic (ca. 160 Ma). By 145 Ma, at the Jurassic/Cretaceous boundary, theconstituent terranes of the microcontinent began to migrate northeastwards bytranspression. 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 rearrangedand formed the essential framework of the present Japanese Islands.

If the two models as described above are accepted, the similar Nd isotopicsignatures 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 continentalmargin of SE China. Since they are part of the South China Block, the granitoidformation and crustal evolution in SW Japan must have shared the same processes and

Fig. 10. Comparison of Sm-Nd isotopic compositions of sedimentary and metasedimentary rocks fromTaiwan 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 forTaiwan. The “young” sediments (500-1000 Ma) of Japan are likely to contain more materials from the oceanplate stratigraphy, such as siltstones from the early Tertiary accretionary complex of the Shimanto Belt insouthern Shikoku.


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conserved similar isotopic signatures. Using the age information, Sr-Nd isotopic signatureand geochemical data of the end-Permian marble sequence and Cretaceous granitoids ofthe Tanan’ao Complex, Jahn and others (1992) hypothesized that the paleogeographicposition of proto-Taiwan was situated to the south of Guangdong Province. This hypothesishas later been supported by an exhaustive monazite age study of the Tertiary sandstones ofTaiwan (Yokoyama and others, 2007), and a zircon age study of Early Tertiary andesite andrhyolite (Chen and others, 2010). Because the crustal and tectonic development of SWJapan and Taiwan took place in the proximal SE part of the South China Block, theirsharing of Sr-Nd isotopic characteristics is clearly explained.

conclusionsIn a recent review on accretionary orogens, Cawood and others (2009) stated that

accretionary orogens form at intraoceanic and active continental margin plate bound-aries. They include the supra-subduction zone forearc, magmatic arc and back-arccomponents. They further separated accretionary orogens into retreating and advanc-ing types. The case of Japan is of the retreating type. Similarly, in a discussion ontectonic models for accretion of the Central Asian Orogenic Belt, Windley and others

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 accretionarycomplex 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 theaccretionary complexes.


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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 microcontinentsin a manner comparable with that of circum-Pacific Mesozoic-Cenozoic accretionaryorogens. In both syntheses, accretionary orogens appear to consist dominantly of rocksof 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 distin-guished by the nature of the accreted lithological assemblages. Orogens with domi-nantly island arc assemblages would witness generation of granitoids with juvenilecharacters. This is best exemplified by the granitoids of the ANS and many parts of theCAOB. By contrast, orogens with accretionary complexes with a large proportion ofrecycled Precambrian crust relative to mantle-derived rocks would produce graniticrocks with a more crustal signature. This is represented by the Japanese Islands. TheSr-Nd isotopic compositions of Japanese granitoids shown in figures 2 to 5 indicate thatthe source regions varied from dominantly mantle-derived rocks to an assemblage witha large proportion of recycled Precambrian crust. This implies that the proportion oferoded Precambrian crust in the trench to the ocean plate stratigraphy was veryvariable 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 ofaccreted lithologic assemblages. The Arabian-Nubian Shield contains the highestproportion of mantle-derived rocks, or island arc suites, and juvenile granitoids. SEJapan shows the opposite scenario. Though the CAOB was mainly developed throughaccretion of island arcs, it also contains accreted Precambrian continental fragments.This is well demonstrated by the isotopic compositions of granitoids from west-centralMongolia (Jahn and others, 2004; Kovalenko and others, 2004) and the Chinese AltaiMountains (Hu and others, 2000; Wang and others, 2009). Finally, this study demon-strates that, despite the well-documented accretionary complexes (Isozaki and others,2010), the generation of extensive granitoids in SW Japan was probably dominated byremelting of Precambrian crustal sources underlying the “thin” roof-pendants ofaccretionary complexes (Isozaki and others, 2010). The oceanic component of the“ocean plate stratigraphy” has not participated to a significant amount in the produc-tion of the continental crust in SW Japan. On the other hand, the isotopic data supportthe idea that proto-Japan was initially developed along the southeastern part of theSouth China Block, as advocated by several authors (Isozaki, 1996, 1997; Sengor andNatal’in, 1996; Maruyama and others, 1997; Isozaki and others, 2010).

acknowledgmentsThis article is dedicated to Professor Alfred Kroner, a highly distinguished scholar

and long-time friend, in honor of his 70th birthday. The content of this paper was firstpresented in 2006 in the second ERAS International Workshop on “Accretionaryorogens and Continental Growth,” held at Kochi University, Japan, and convened byGaku Kimura and Yukio Isozaki. I benefited from discussions with many participantsduring the meeting. The company of Kazu Okamoto and Aoki-san during the samplecollection of Miocene granites at Kashiwajima, SW Shikoku, is highly appreciated.Shunso Ishihara provided a suite of granite samples from the Sanyo belt and theanalytical results are used in this paper. Nicole Morin (Rennes), Po-Hsuan Lin andMasako Usuki (Taipei) helped in the laboratory work. Kazu Okamoto taught me somegeology of Japan. The assistance of Atsushi Utsunomiya, Qingguo Zhai, and Po-HsuenLin in the preparation of this paper is deeply acknowledged. The paper was improvedby the comments and suggestions of Michel Faure, Fuyuan Wu and Simon Wilde. Thiswork is supported by NSC-Taiwan grant numbers 96-2116-M-001-004, 97-2752-M-002-003-PAE; 97-2116-M-001-011; 98-2116-M-001-009.



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 Age Rb Sr 87Rb 87Sr I (Sr) Sm Nd 147Sm 143Nd εNd(0) fSm/Nd εNd(T) TDM-1 TDM-2No. (Ma) (ppm) (ppm) 86Sr 86Sr (ppm) (ppm) 144Nd 144Nd (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 185 30.4 580 0.15 0.707290 0.70689 YT07 185 38.7 508 0.22 0.707440 0.70686 YT08 185 39.3 578 0.20 0.707370 0.70685 YT10 185 29.2 598 0.14 0.707410 0.70704 YT14 185 41.8 572 0.21 0.708520 0.70796 YT18 185 53.2 462 0.33 0.707600 0.70672 YT20 185 51.1 633 0.23 0.708040 0.70742 YT21 185 36.1 726 0.14 0.707430 0.70705 YT24 185 50.7 738 0.20 0.707010 0.70649 YT11 185 48.6 697.7 0.20 0.707350 0.70682 YT28 185 55.1 377 0.42 0.707830 0.70672 YT29 185 49.8 884 0.16 0.707130 0.70670 IN01 185 60.4 465 0.38 0.707730 0.70674 IN02 185 58 637 0.26 0.709050 0.70836 IN03 185 61.3 538.1 0.33 0.709300 0.70843 YT12 185 53.1 768 0.20 0.706480 0.70595 YT19 185 76 470.2 0.47 0.707260 0.70603 YT22 185 54 668 0.23 0.706820 0.70620 YT23 185 52.8 696 0.22 0.706690 0.70611 Hd03 185 47.8 777.1 0.18 0.706950 0.70648 Hd04 185 66.1 862.7 0.22 0.706270 0.70569 Hd06 185 59.1 605.5 0.28 0.707630 0.70689 Hd08 185 61.7 606.2 0.29 0.709290 0.70851 Hd09 185 42.2 1213 0.10 0.706200 0.70594 Hd13 185 34.1 1011.1 0.10 0.706680 0.70642 Hd18 185 172.6 205.6 2.43 0.716950 0.71055

Ng01 185 44.1 643.2 0.20 0.706720 0.70620 Ng02 185 56.6 625 0.26 0.706960 0.70627 Ng03 185 54.5 686.2 0.23 0.707580 0.70697 Ng08 185 82.6 683.2 0.35 0.709780 0.70886

Hs02 190 48.7 653.9 0.22 0.704980 0.70440 Hs03 190 46.4 678 0.20 0.704980 0.70444 Hs04 190 91.3 484.3 0.55 0.706160 0.70469 Hs05 190 89 481.7 0.53 0.705980 0.70454 Hs108 190 35.4 1147.1 0.09 0.704740 0.70450 Iori intrusion Ir01 190 80.3 510 0.46 0.707810 0.70658Ir02 190 73 527 0.40 0.707900 0.70682Ir03 190 46.3 1032 0.13 0.706770 0.70642Ir04 190 49.7 767 0.19 0.706870 0.70636Ir05 190 64.2 696 0.27 0.707400 0.70668Ir06 190 64.3 828 0.23 0.707220 0.70661III

r07 190 54.6 837 0.19 0.707290 0.70678r08 190 76.5 636 0.35 0.707890 0.70695r09 190 84.4 535 0.46 0.707550 0.70632



Table A1

(continued)Sample Age Rb Sr 87Rb 87Sr I (Sr) Sm Nd 147Sm 143Nd εNd(0) fSm/Nd εNd(T) TDM-1 TDM-2No. (Ma) (ppm) (ppm) 86Sr 86Sr (ppm) (ppm) 144Nd 144Nd (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 0.70487Kg03* 185.8 103.2 147.7 2.02 0.710310 0.70497Kg07* 185.8 134 226.5 1.71 0.709380 0.70485Kg09* 185.8 130.7 184 2.06 0.710290 0.70486 Okumayama intrusion Ok01 190 46.9 370 0.37 0.705750 0.70476Ok02 190 57 355 0.47 0.706270 0.70501Ok05 190 78.4 430 0.53 0.706460 0.70503 Komagatake intrusion Km03* 192.6 51.4 612 0.24 0.706090 0.70542Arakawa 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 0.95UB05 184 0.70539 2.85 12.53 0.1373 0.512570 -1.3 -0.30 0.1 1.16 0.95UB10 184 0.70521 3.82 28.08 0.0822 0.512591 -0.9 -0.58 1.8 0.65 0.85UB11 184 0.70536 3.33 19.83 0.1016 0.512633 -0.1 -0.48 2.1 0.70 0.81UB12 184 0.70539 3.23 19.74 0.0990 0.512635 -0.1 -0.50 2.2 0.69 0.80OK01 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 1.04OK25 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 1.73SN04 190 4.54 28.58 0.0961 0.512085 -10.8 -0.51 -8.3 1.38 1.67ON32 190 3.88 24.32 0.0963 0.512416 -4.3 -0.51 -1.9 0.95 1.15OM03 190 5.72 32.30 0.1071 0.512402 -4.6 -0.46 -2.4 1.07 1.18OM04 190 3.13 12.11 0.1562 0.512624 -0.3 -0.21 0.7 1.39 0.89OM05 190 3.47 14.88 0.1408 0.512406 -4.5 -0.28 -3.2 1.55 1.22YT06 190 4.67 19.49 0.1448 0.512459 -3.5 -0.26 -2.2 1.53 1.14YT22 190 10.05 24.40 0.2489 0.512674 0.7 0.27 -0.6 -2.08 0.94YT29 190 4.03 27.38 0.0890 0.512413 -4.4 -0.55 -1.8 0.90 1.14Hd03 190 7.41 47.47 0.0944 0.512402 -4.6 -0.52 -2.1 0.96 1.17Hd13 190 5.25 29.04 0.1393 0.512443 -3.8 -0.29 -2.4 1.45 1.16Hd18 190 2.57 13.50 0.1152 0.512012 -12.2 -0.41 -10.2 1.76 1.82GY2120 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 1.89GY1717 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 1.93GY2403 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 2.08Fujii 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 K95091204-3 161 20 468 0.13 0.707446 0.70716 1.95 8.74 0.1347 0.512358 -5.5 -0.32 -4.2 1.53 1.29K 94101010 161 33 532 0.18 0.707684 0.70727 3.53 17.20 0.1244 0.512355 -5.5 -0.37 -4.0 1.36 1.28K 96030105 161 40 430 0.27 0.707866 0.70725 5.55 24.60 0.1363 0.512304 -6.5 -0.31 -5.3 1.66 1.38K 96030101 161 85.9 434 0.57 0.708566 0.70726 4.01 17.90 0.1353 0.512362 -5.4 -0.31 -4.1 1.53 1.28K 96061902 161 47 455 0.30 0.707955 0.70727 5.76 21.50 0.1619 0.512338 -5.9 -0.18 -5.1 2.38 1.36K 96061903 161 49 427 0.33 0.708035 0.70728 5.60 21.20 0.1595 0.512312 -6.4 -0.19 -5.6 2.35 1.40K 96070302 161 24 453 0.16 0.707702 0.70734 4.40 17.10 0.1551 0.512394 -4.8 -0.21 -3.9 1.96 1.26K 96070303 161 30 486 0.18 0.707737 0.70732 5.40 20.10 0.1621 0.512315 -6.3 -0.18 -5.6 2.45 1.40K95091203-1 161 9 368 0.07 0.707424 0.70727 4.47 15.10 0.1792 0.512336 -5.9 -0.09 -5.5 3.57 1.39F 95072106 121 78 342 0.66 0.708615 0.70749 0.65 3.26 0.1202 0.512302 -6.6 -0.39 -5.4 1.38 1.36F 95072107 121 4.52 21.50 0.1270 0.512303 -6.5 -0.35 -5.5 1.49 1.37F 95072109 121 67 415 0.46 0.708335 0.70754 (Age 161 Ma) F 96022502-1 121 73 383 0.55 0.708480 0.70753 6.55 39.30 0.1280 0.512317 -6.3 -0.35 -5.2 1.48 1.35F95022502-2 121 78 383 0.59 0.708493 0.70748 5.21 16.70 0.1879 0.512315 -6.3 -0.04 -6.2 4.87 1.43F 96022503 121 79 388 0.59 0.708538 0.70752F 94103002 121 79 359 0.65 0.708727 0.70761 8.66 45.20 0.1159 0.512303 -6.5 -0.41 -5.3 1.32 1.35F 94103008 121 98 399 0.71 0.708752 0.70753FFF

96071904 121 76 406 0.54 0.708518 0.70759 7.92 29.80 0.1609 0.512336 -5.9 -0.18 -5.3 2.34 1.36 96071907-1 121 78 400 0.57 0.708502 0.70753 6.41 23.20 0.1667 0.512335 -5.9 -0.15 -5.4 2.63 1.37 94080404 121 69 417 0.48 0.708364 0.70754 6.38 24.50 0.1576 0.512340 -5.8 -0.20 -5.2 2.19 1.35



Table A1

(continued)Sample Age Rb Sr 87Rb 87Sr I (Sr) Sm Nd 147Sm 143Nd εNd(0) fSm/Nd εNd(T) TDM-1 TDM-2No. (Ma) (ppm) (ppm) 86Sr 86Sr (ppm) (ppm) 144Nd 144Nd (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 -3.94110206 82.9 98 225 1.26 0.708696 0.70710 5.45 26.50 0.1240 0.512394 -4.8 -0.37 -4.0AG005 82.9 79 313 0.73 0.706692 0.70580 3.92 19.20 0.1230 0.512596 -0.8 -0.37 0.0 correct950915 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 correctKO-005 82.9 129 324 1.15 0.706181 0.70470 5.25 28.60 0.1110 0.512664 0.5 -0.44 1.4TMS-01 82.9 31 399 0.23 0.706802 0.70650 4.68 25.20 0.1120 0.512571 -1.3 -0.43 -0.4TMO20 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 0.76010507 82.9 73 301 0.70 0.708388 0.70750 4.96 25.10 0.1190 0.512389 -4.9 -0.40 -4.0 correct6010505 82.9 94 268 1.02 0.708681 0.70740 5.34 27.80 0.1160 0.512390 -4.8 -0.41 -4.06010402 82.9 122 315 1.12 0.708782 0.70730 5.93 28.20 0.1270 0.512370 -5.2 -0.35 -4.56062205 82.9 66 277 0.69 0.707548 0.70670 5.52 27.70 0.1200 0.512408 -4.5 -0.39 -3.74103002 85.2 82 384 0.62 0.707138 0.70630 6.71 34.20 0.1190 0.512322 -6.2 -0.40 -5.3 correct5081901 85.2 51 386 0.38 0.707076 0.70660 6.18 29.80 0.1250 0.512431 -4.0 -0.36 -3.332219 85.2 41 491 0.24 0.706272 0.70600 3.84 18.60 0.1250 0.512421 -4.2 -0.36 -3.56062203 85.2 93 341 0.79 0.707419 0.70640 4.19 22.80 0.1110 0.512391 -4.8 -0.44 -3.96062204 85.2 91 348 0.76 0.707447 0.70650 4.07 22.10 0.1110 0.512378 -5.1 -0.44 -4.1 correct6062101 85.2 46 632 0.21 0.706685 0.70640 3.04 15.60 0.1180 0.512446 -3.7 -0.40 -2.97690503 85.2 17.8 576 0.09 0.704881 0.70480 5.00 20.80 0.1460 0.512725 1.7 -0.26 2.2Ishioka and Iizumi, 2003. Petrochemical and Sr-Nd isotope investigations of Cretaceous intrusive rocks and their enclaves in the Togouchi-Yoshiwa district, 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 1.13TO12 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 1.09TO23 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 1.08TO28 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 1.02TO02B 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 1.02TO16AE 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 1.02TO16BE 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 1.11TO23AE 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 1.04TO28E 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 1.12TO36BE 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 1.09Togouchi phenocryst-bearing microdiorite enclaves (PBME)

TO01E 97 236 1.19 0.707600 0.70615 — — — — — TO30E 81 298 0.79 0.707200 0.70624 — — — — —



Table A1

(continued)Sample Age Rb Sr 87Rb 87Sr I (Sr) Sm Nd 147Sm 143Nd εNd(0) fSm/Nd εNd(T) TDM-1 TDM-2No. (Ma) (ppm) (ppm) 86Sr 86Sr (ppm) (ppm) 144Nd 144Nd (Ga) (Ga)Ishioka and Iizumi, 2003. Petrochemical and Sr-Nd isotope investigations of Cretaceous intrusive rocks and their enclaves in the Togouchi-Yoshiwa district, 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 1.12TA73A 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 1.06TA73E 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 1.11TA76E 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 1.13YO94 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 1.11YO96 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 1.17Kagami 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 0.852 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 0.833 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 0.947 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 1.018 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 1.0114 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 1.0717 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 1.0518 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 0.7619 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 0.8121 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 0.8023 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 1.0325 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 1.0326 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 1.2927 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 1.2028 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 1.2629 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 1.1630 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 1.0131 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 0.9632 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 1.4433 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 1.2835 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 1.2436 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 1.2537 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 1.2338 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 1.3639 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



Table A1

(continued)Sample Age Rb Sr 87Rb 87Sr I (Sr) Sm Nd 147Sm 143Nd εNd(0) fSm/Nd εNd(T) TDM-1 TDM-2No. (Ma) (ppm) (ppm) 86Sr 86Sr (ppm) (ppm) 144Nd 144Nd (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 1.2941 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 1.2642 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 1.2543 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 1.2744 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 1.3045 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 1.2246 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 1.2147 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 1.2248 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 -3.02 192 56.7 438 0.37 0.709428 0.70841 6.90 32.50 0.1283 0.512252 -7.5 -0.35 -5.916 240 38.6 329 0.34 0.708269 0.70711 6.54 29.50 0.1341 0.512344 -5.7 -0.32 -3.817 240 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 0.7086751407 72.8 279 36 22.70 0.732660 0.7091851420 72.8 219 260 2.44 0.711610 0.7090952205 72.8 145 246 1.71 0.710690 0.7089252208 72.8 180 145 3.61 0.712560 0.7088352209 72.8 191 134 4.13 0.713170 0.70890Nakajima 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 0.7089291030804 128 218 0.7081399112902A 51 343 0.7080799120101A 72 58 471 0.70734



Table A1

(continued)Sample Age Rb Sr 87Rb 87Sr I (Sr) Sm Nd 147Sm 143Nd εNd(0) fSm/Nd εNd(T) TDM-1 TDM-2No. (Ma) (ppm) (ppm) 86Sr 86Sr (ppm) (ppm) 144Nd 144Nd (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 1.241304A 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 1.26O202 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 1.12O613D 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 1.132102 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 1.082507 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 1.192509 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 1.241406 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 1.261202 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 1.161205 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 1.231302SA 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 1.021305B 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 1.021401D 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 1.041504A 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 1.122105 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 1.002405A 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 1.15Stein 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 0.79A13 13 283 30 0.709640 0.70421 11.65 61.17 0.1151 0.512731 1.8 -0.41 1.9 0.65 0.67A1 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 1.15A7 13 186 96 0.708050 0.70894 5.20 17.10 0.1838 0.512406 -4.5 -0.07 -4.5 3.76 1.28A9 13 134 205 0.708440 0.70806 5.22 27.27 0.1157 0.512368 -5.3 -0.41 -5.1 1.22 1.25OS4 13 210 43 0.713240 0.71043 2.54 8.98 0.1710 0.512326 -6.1 -0.13 -6.0 2.92 1.39OS9 13 125 165 0.710180 0.70972 6.86 35.15 0.1180 0.512365 -5.3 -0.40 -5.2 1.25 1.26Takagi, T. and Kagami, H., 1995. Rb-Sr isochron ages and initial Sr isotope rarios of the Ukan granodiorite and Kayo granite centralOkayama prefecture, southwest Japan. Bulletin of the Geological Survey of Japan, v. 46, 219-224. 31106 92 96 234 1.19 0.708530 0.7069112102 92 101 243 1.20 0.708530 0.7068081011 92 108 242 1.29 0.708620 0.7066480905 92 131 261 1.45 0.708810 0.7061173108 92 127 218 1.69 0.709200 0.7061673107 92 127 208 1.77 0.709280 0.7060912105 92 141 205 1.99 0.709530 0.7055480409 92 73 300 0.70 0.708020 0.7072931108 92 70 268 0.76 0.708120 0.7073762602 92 85 252 0.98 0.708270 0.7070931102 92 106 220 1.39 0.708700 0.7066031012 81 54 291 0.54 0.707410 0.7070031607 81 68 308 0.64 0.707600 0.7069830801 81 76 301 0.73 0.707740 0.70695102301 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

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

Ilmenite-series 117



Table A1

(continued)Sample Age Rb Sr 87Rb 87Sr I (Sr) Sm Nd 147Sm 143Nd εNd(0) fSm/Nd εNd(T) TDM-1 TDM-2No. (Ma) (ppm) (ppm) 86Sr 86Sr (ppm) (ppm) 144Nd 144Nd (Ga) (Ga) 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



Table A1

(continued)Sample Age Rb Sr 87Rb 87Sr I (Sr) Sm Nd 147Sm 143Nd εNd(0) fSm/Nd εNd(T) TDM-1 TDM-2No. (Ma) (ppm) (ppm) 86Sr 86Sr (ppm) (ppm) 144Nd 144Nd (Ga) (Ga) 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



Table A1

(continued)Sample Age Rb Sr 87Rb 87Sr I (Sr) Sm Nd 147Sm 143Nd εNd(0) fSm/Nd εNd(T) TDM-1 TDM-2No. (Ma) (ppm) (ppm) 86Sr 86Sr (ppm) (ppm) 144Nd 144Nd (Ga) (Ga) 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



References

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Table A1

(continued)Sample Age Rb Sr 87Rb 87Sr I (Sr) No. (Ma) (ppm) (ppm) 86Sr 86SrTerakado 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 MIYAZU-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 MIYAZU-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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