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Crustal evolution of a paleozoic intra-oceanic island-arc-back-arc basin system constrained by the geochemistry and geochronology of the Yakuno ophiolite, Southwest Japan.

1. Introduction

Ophiolites are the rock assemblages of peridotite, gabbro, basalt, and associated pelagic sediment found at the orogenic belt of a convergent plate boundary. They are most commonly interpreted as the remnants of crustal components and the upper mantle beneath an ocean basin [1-3]. Therefore, ophiolites provide direct information about the deeper part of the crustal section without the need for deep drilling and are considered to be significant research target on the reconstruction of paleotectonic evolution of orogenic belts [1-4].

The Yakuno ophiolite in southwest Japan originated from the crustal sections of a Paleozoic intra-oceanic island-arc-back-arc basin (intra-OIA-BAB) system and formed through collision and accretion with the eastern margin of the East Asian continent during the early Mesozoic [5, 6]. The Yakuno ophiolite in the Asago area is composed of metagabbro and amphibolite of BAB origin (Figure 1) [7]. These mafic rocks are intruded by the granitoid of arc affinities. This field evidence suggests that the mafic rocks in this area originally formed as a BAB crust, which was subsequently brought to an OIA setting. In this regard, the Yakuno ophiolite in this area records various lines of evidence to help understand the tectonic evolution of an intra-OIA-BAB system [7, 8].

The zircon U-Pb TIMS ages of 282 [+ or -] 2 Ma and 285 [+ or -] 2 Ma were determined from the arc granitoid (i.e., tonalite and granodiorite) in the Asago area by Herzig et al. [9]. The ages were considered to be the period of the magmatic activity under the island-arc or intra-OIA setting. On the other hand, the magmatic age of the Yakuno ophiolite originated from the BAB crust has not yet been determined. The present study reports the SIMS (SHRIMP: sensitive high resolution ion microprobe) zircon U-Pb ages from the mafic rocks of BAB origin in the Asago area. On the basis of the compilation for the geological and geochronological data about the Yakuno ophiolite and associated rocks, we tentatively propose a geotectonic model and time scale for the Yakuno ophiolite in the context of the tectonic evolution of an intra-OIA-BAB system.

2. Yakuno Ophiolite in Maizuru Terrane

2.1. Geology. The Yakuno ophiolite is found in the upper Paleozoic to lower Mesozoic Maizuru Terrane in southwest Japan [5, 6]. The Maizuru Terrane is characterized by a distinct zonal structure with an extension of northeastern to southwestern direction and divided, based on lithology, into the Northern Zone, the Inner Zone, and the Southern Zone. The Maizuru Terrane comprises the following four major lithological units (Figure 1): (1) granitoid with a minor amount of pelitic gneiss and amphibolite in the Northern Zone, (2) Permian sediments of the Maizuru Group in the Inner Zone, (3) metamorphic peridotite, metagabbro, and amphibolite with minor amount of granitoid in the Southern Zone, and (4) Triassic sediments, which uncomfortably cover the rocks in Inner and Southern Zones.

The Yakuno ophiolite indicates the metamorphosed ultramafic to mafic rocks of peridotite, metagabbro, and amphibolite found in the Southern Zone. Previous works have reported that these rocks were originated from various kinds of upper mantle to crustal sections of ocean basin (OB) (i.e., MORB origin), intra-oceanic island-arc (intra-OIA), and back-arc basin (BAB) [5, 6].

2.2. Yakuno Ophiolite in Oshima Peninsula, Ayabe, and Yakuno-cho Areas. The Yakuno ophiolite in the Oshima peninsula and Ayabe areas (Figure 1) consists of ultramafic rock of upper mantle origin and mafic rocks of OIA and BAB origins. Ishiwatari [10] reported that harzburgite is observed predominantly in the Oshima peninsula area and originated from the upper mantle after the extraction of roughly 35% volume of basaltic magma. Ishiwatari [10] further indicated that the metabasalt and metagabbro in the Oshima peninsula and Ayabe areas possess geochemical affinities of MORB and are derived from a T-type MORB source.

Ichiyama and Ishiwatari [11] suggested that the Yakuno ophiolite in the Yakuno-cho area (Figure 1) originated from a BAB crust, consisting of metabasalt and metagabbro of BAB affinities and a minor amount of troctolite.

2.3. Yakuno Ophiolite and Associated Rocks in Asago Area. Hayasaka et al. [6] indicated that the Yakuno ophiolite in the Asago area (Figure 1) consists of the crustal components of three different tectonic settings: OB, intra-OIA, and BAB. Each of the components of different tectonic settings is bounded by a low-angle fault (Figure 2(a)).

Suda [8] and Suda and Hayasaka [7] suggested that the amphibolite and metagabbro in the Asago area possess geochemical affinities of BAB basalt (BABB), which are derived from a tholeiitic BABB source. These mafic rocks of BABB affinities are intruded by tonalite, quartz-diorite, and granodiorite of arc affinities. The presence of migmatites in the lower crustal level implies that the granitoid was formed by the lower crustal anatexis of the mafic rocks derived from BABB source. When combined, these findings indicate that the amphibolite and metagabbro in this area originally formed as a BAB crust, which was subsequently brought to an intra-OIA setting in which the granitoids of arc affinities were generated. Geological map and geologic columnar section indicating the relation between these components are shown in Figures 2(a) and 2(b), respectively. Localities of the samples for the SHRIMP zircon dating performed in the present study are also indicated in these figures.

Hayasaka [12] suggested that the cumulate metagabbro (pyroxenite, anorthosite, and eucrite) in the Asago area is rather similar in petrography and geochemistry to those in the Oshima peninsula and Ayabe areas (Figure 1), thus suggesting that this metagabbro originated from a lower crustal section of oceanic crust and was derived from the T-type MORB source (i.e., OB ophiolite) (Figure 2(a)).

Hayasaka et al. [6] indicated that metadolerites, metabasalts, and massive mudstone in the Asago area were derived from the upper crust in a BAB setting (i.e., BAB ophiolite) (Figure 2(a)). The intercalation of mudstone with the metabasalt implies that these rocks formed under an environment of simultaneous sedimentation and eruption of basalt, further supporting the interpretation of a BAB setting.

2.4. Yakuno Ophiolite and Associated Rocks in Ohara and Kamigori Areas. Ishiwatari et al. [5] and Ishiwatari [13] indicate that the Yakuno ophiolite in the Ohara and Kamigori areas, consisting of metagabbro and amphibolite of IAB affinities and a minor amount of shoshonitic metagabbro (Figure 1), originated from the lower crust in an OIA setting.

2.5. Yakuno Ophiolite and Associated Rocks in Ibara Area. The Yakuno ophiolite in the Ibara area was derived from the upper crust in a BAB setting (Figure 1) [14]. The Yakuno ophiolite in this area consists of metagabbro, metabasalt, and massive mudstone. The metabasalt is intercalated with the mudstone and possesses geochemical affinities of BABB, which supports the interpretation of a BAB setting.

2.6. Permian Maizuru Group. The Maizuru Group in the Inner Zone of the Maizuru Terrane is found alongside the exposure of the Yakuno ophiolite and consists of alternating metabasalt and mudstone in the lower strata, a massive mudstone in the middle strata, interbedded sandstone and mudstone in the upper strata, and sandstone and conglomerate in the uppermost strata [15]. Radiolarians of early to middle Permian age (Pseudoalbaillella cf. fusiformis) are reported from the lower strata [16], and radiolarians of middle to late Permianage are reported from the middle to upperstrata 17]. This stratigraphic sequence is characterized by an increase of terrigenous deposits with increasing structural level, and a marginal sea basin of relatively shallow depth is assumed as the sedimentary environment [15].

Ishiwatari [13] considered that the tectonic relationship between the Maizuru Group and the Yakuno ophiolite of BAB setting was originally conformable. The lower strata of the Maizuru Group are equivalent to the upper part of the Yakuno ophiolite and are characterized by the intercalation of mudstone with metabasalt.

2.7. Triassic Sediments. The Triassic sediments in the Maizuru Terrane consist of conglomerate, sandstone, and mudstone, which unconformably overlie the Yakuno ophiolite and the Maizuru Group (Figure 1). Early to late Triassic ammonoids and bivalves are reported from the Triassic sediments [18,19], which are assumed to have been deposited in beach, shore, and brackish water sedimentary environments.

2.8. Hinterland Models for the Permo-Triassic Sediments. Geochronological data from the detrital zircon and paleobiogeographical results from the Triassic sediments suggest that the East Asian continent was the hinterland for the Permo-Triassic sediments in the Maizuru Terrane, namely, the South China Craton [20], the North China Craton [21], and the Khanka Massif or the Northern Zone of the Maizuru Terrane [22]. The Yakuno ophiolite and Maizuru Group collided with the eastern margin of the East Asian continent during the beginning of the Mesozoic.

3. SHRIMP U-Pb Zircon Dating

3.1. Samples. We performed SHRIMP zircon U-Pb age dating at Hiroshima University, Japan, to clarify the magmatic or protolith age of the Yakuno ophiolite of BAB setting. The zircons used for the dating were separated from samples of metagabbro (Gb1) and amphibolite (Am1) in the Asago area (Figure 1). The outcrop from which sample Gb1 was taken is located at latitude 35.232209[degrees]N and longitude 134.709694[degrees]E and represents the structurally lowermost part of the ophiolite (Figure 2(b)). The outcrop for sample Am1 is located at latitude 35.234321[degrees]N and longitude 134.748472[degrees]E and represents the structurally upper part (Figure 2(b)).

Suda [8] indicates that both the metagabbro and amphibolite exhibit various degrees of deformation and metamorphic textures, such as gneissosity with a preferred orientation of minerals. Foliation and lineation are strongly developed in the amphibolite suite in particular. Gneissose metagabbro is gradually replaced by amphibolite in the upper part. In the lowermost part, the metagabbro contains hornblende + clinopyroxene + orthopyroxene + plagioclase [+ or -] quartz mineral assemblage indicating granulite-facies metamorphism. All the orthopyroxene crystals are replaced by bastite, and plagioclase is moderately saussuritized because of hydrothermal alteration. Pyroxene declines in abundance upwards, and the mineral paragenesis changes to hornblende + plagioclase [+ or -] clinopyroxene, indicating amphibolite-facies metamorphism. Apatite commonly occurs as an accessory mineral along with minor amounts of Fe-Ti oxides.

3.2. Method. Using a jaw crusher and stamp mill, chips of rock samples were crushed into powdered particles of <250 [micro]m in size. Heavy minerals were concentrated from the powdered sample by hydraulic elutriation and magnetic means. Zircon grains were handpicked, mounted in epoxy resin, and polished using diamond paste until they were reduced to approximately half their original thickness. Before isotopic analysis, in addition to microscopic observation, back-scattered electron (BSE) images and cathodoluminescence (CL) images were taken with an EPMA (electron probe micro-analyzer) to check for metamict regions, inclusions, and compositional zoning patterns. All the measured points for SHRIMP analysis were selected using the BSE and CL images. The isotopic analysis of zircon was performed using a SHRIMP-II machine at Hiroshima University. The procedures for U and Pb isotopic analysis and dating were the same as those used by Fuji et al. [22]. Isoplot/Ex 3.0 [23] was used for age calculations (Figures 4(a) and 4(b)).

3.3. Results and Interpretation. The zircon grains in the Gb1 (metagabbro) generally have round shape, in which oscillatory igneous zoning texture is blurred (Figure 3). Many lines visible in the CL images of Gb1 zircon show the cracks formed during sample preparation (Figure 3). On the Tera and Wasserburg [24] diagram, the analyzed 11 spots plot on the concordia (Table 1), from which a weighted mean concordant [sup.206][Pb.sup.*]/[sup.238]U age of 293.4 [+ or -] 9.5 Ma (all errors give 2a) is estimated (Figure 4(a)). The probability plot for these spot [sup.206][Pb.sup.*]/[sup.238]U ages shows a unimodal distribution ranging from 281 Ma to 308 Ma (Figure 4(b)). These spot ages show no correlation with Th/U ratios (Table 1).

The zircon grains in the Am1 (amphibolite) have prismatic euhedral shape and texture but the crystals are often broken, in which typical oscillatory igneous zoning texture is observed (Figure 3). The analyzed 10 spots lying on the concordia (Table 1) give a weighted mean concordant [sup.206][Pb.sup.*]/[sup.238]U age of 288 [+ or -] 13 Ma (Figure 4(a)). The probability plot for these spot [sup.206][Pb.sup.*]/[sup.238]U ages roughlyshows a unimodal distribution ranging from 264 Ma to 319 Ma (Figure 4(b)). There is no correlation with Th/U ratios (Table 1).

The Th/U ratios in the Gb1 zircon are relatively lower than those in the Am1 zircon (Table 1). This may be related to Th loss due to the granulite-facies metamorphism. In this case, the calculated [sup.206][Pb.sup.*]/[sup.238]U age would become slightly younger. However, the Th/U ratio in the Gb1 zircon is >0.2. This result strongly indicates that the Gb1 zircon has not crystallized during the granulite-facies metamorphism but has crystallized from magma (i.e., igneous origin). The Th/U ratio in metamorphic zircon is generally <0.07 (e.g., Rubatto [25]). Namely, the zoning texture in Gb1 zircon represents the blurred primary zoning. Furthermore, the results of [sup.206][Pb.sup.*]/[sup.238]U ages from the Gb1 and Am1 are overlapping within 2a error. From these results, we conclude that the [sup.206][Pb.sup.*]/[sup.238]U ages obtained from the Gb1 and Am1 zircons represent the age of magmatic crystallization of these mafic rocks.

4. Discussion

4.1. Overview of Intra-OIA-BAB System. An intra-OIA-BAB system is generally formed by the subduction of an oceanic plate at an oceanic-oceanic convergent plate boundary [26]. Previous studies of various intercontinental suture zones have proposed multiple lines of evidence for continental growth by accretion of intra-OIA-BAB systems [27,28]. In the Cenozoic intra-OIA-BAB system of the Izu-Bonin-Mariana (IBM) arc, the middle crust of the intra-OIA was emplaced within the Honshu arc in the Tanzawa Mountains of Japan due to the subduction of the Philippine Sea Plate beneath the Eurasian Plate [29, 30]. Thus, the tectonic history of an intra-OIA-BAB system will end during collision with and accretion to a continental margin, a process that may play a significant role in the growth and evolution of continental crust.

In an intra-OIA-BAB system, there are two sites of magmatic activity: (1) island-arc magmatism along the axis of the magmatic arc and (2) magmatism at the spreading center of the BAB. The BAB rifting will start in a region near to the axis of the magmatic arc and gradually move away from the subduction zone and the axis with the development of BAB spreading [31].

Under such tectonic scenarios, geochemical features of back-arc basin basalts (BABBs) will vary with the development of BAB spreading [31-33]. At the initial stage of BAB formation, BABBs possess geochemical signatures of island-arc basalt (IAB), whereas, at the late stage of BAB formation, the BABBs possess geochemical signatures of mid-ocean ridge basalt (MORB). Thus, geochemical signatures of BABBs will vary from IAB to MORB with the development of a BAB, with the signatures being controlled by the interaction between the mantle components and the subduction zone components. Consequently, BABBs with IAB signatures should be older than those with MORB signatures.

4.2. Geochemical Implications for the Evolution of BABB. The variation diagram of the [(Nb/La).sub.N] ratio with respect to the [(La/Y).sub.N] ratio (Figure 5) characterizes the geochemical signatures in the range between MORB and IAB [7]. Data source for the MORBs are excerpted after Pearce and Parkinson [34], and Kelemen et al. [35]. Those for the Cenozoic BABB and IAB are after Taylor and Martinez [31], and Tatsumi [36], respectively. The MORBs are plotted predominantly in the field of the [(Nb/La).sub.N] ratio >1.0, while the compositions of IAB [34-36] are plotted in the field of the [(Nb/La).sub.N] ratio <1.0. In the diagram, compositions of the Cenozoic BABB are generally plotted in the field between MORB and IAB and broadly include MORB and IAB compositions. Thus, the geochemical signatures of BABBs are characterized by the compositional trend connecting the fields between MORB and IAB.

Using this diagram, we evaluate the geochemical signatures of metabasalts and metagabbro in the Yakuno ophiolite. Data sources for the mafic rocks in Yakuno ophiolite are excerpted from Suda and Hayasaka [7] and Ichiyama and Ishiwatari [11]. The metagabbros in Yakuno ophiolite plotted in this diagram were evaluated to be the melt origin which do not possess the cumulite compositions by Suda and Hayasaka [7].

The results indicate that the mafic rocks in the Yakuno ophiolite have a clear BAB affinity. In particular, the metagabbros in the Asago area are plotted predominantly in the field around IAB, whereas the metabasalts in the Yakuno-cho area are plotted in the field between IAB and MORB. This may imply that the metagabbro in the Asago area formed during the initiation of BAB rifting near the axis of the magmatic arc. In contrast, the metabasalts in the Yakuno-cho area have an influence throughout the development of BAB crust.

4.3. Geotectonic Timescale Model for the Yakuno Intra-OIA-BAB System. Geochronological data for the Yakuno ophiolite and associated rocks after previous studies and the current investigation are compiled in Figure 6. Based on these data, we suggest that the metagabbro and amphibolite in the Asago area formed through igneous activity under the spreading center of BAB rifting at ca. 288-293 Ma (after the present study). The BAB rocks were intruded by the arc granitoid with a magmatic age of ca. 285-282 Ma (after U-Pb zircon TIMS ages [31]). These results suggest that the BAB crust was brought to the magmatic arc setting soon (within several million years) after its generation.

Koide et al. [37] reported an Rb-Sr whole-rock-mineral isochron age of 281 [+ or -] 8 Ma for the metagabbro and metabasalt of BABB origin in the Ibara area. This age is similar to the age of radiolarians from the lower strata of the Maizuru Group and may represent the magmatic age of the mafic rocks of BABB origin without the influence of arc magmatism.

Sano [38] reported Sm-Nd whole rock and mineral isochron ages of 409 [+ or -] 44 Ma and 412 [+ or -] 62 Ma, respectively, for the metagabbro of MORB origin in the Ayabe area (Figure 1). Hayasaka et al. [6] reported Sm-Nd whole rock and mineral isochron ages of 341 [+ or -] 62 Ma, 343 [+ or -] 34 Ma, and 385 [+ or -] 13 Ma for the metagabbro of MORB origin in the Oshima peninsula and the Asago area (Figure 1). These ages are clearly older than the ages of the magmatic events that produced the granitoid of intra-OIA setting (ca. 285-282 Ma) and BAB crust (ca. 288-293 Ma). Field observations further indicate that these rocks do not show any influence of arc magmatism. Taken together, these results suggest that these older metagabbros of MORB origin might have formed the basement of a forearc basin in the intra-OIA-BAB system.

Many K-Ar hornblende ages and K-Ar biotite ages of metagabbro and metabasalt have been reported for the Yakuno ophiolite in various areas [39-41]. These ages are concentrated over the interval extending from the middle Permian to the late Triassic, a time frame that may represent the cooling history after the magmatic event in the intra-OIA and BAB settings.

Based on the above discussion regarding the geology and geochronology of the Maizuru Terrane, we tentatively propose the following model of the geotectonic evolution and time scale for the Yakuno intra-OIA-BAB system.

(1) Initiation of BABB magmatism under the spreading center of the BAB rifting formed the BAB crust with IAB signatures (ca. 293-288 Ma; Figure 7(a)).

(2) The BAB crust gradually moved to the region near the axis of the magmatic arc because of BAB spreading and tectonic erosion of the forearc basin. Subsequently, the BAB crust was overlapped by the axis of the magmatic arc and formed the basement of the OIA (ca. 288-285 Ma; Figure 7(b)).

(3) The IAB magmatism led to the lower crustal anatexis of the OIA basement, consequently generating granitoids of arc affinities (ca. 285-282 Ma). Simultaneously, BABB magmatism under the spreading center of the BAB rifting formed the BAB crust with IAB to MORB signatures, on which terrigenous sediments derived from a nearby continent were deposited, forming the Permian Maizuru Group (<ca. 285 Ma; Figure 7(c)).

(4) These Paleozoic components collided and became accreted to the eastern margin of the East Asian continent during the early Mesozoic.

The problems still remaining comprise the evidence of the subduction zone adjacent to the craton (Figure 7(c)) and of how to survive the metagabbro of MORB origin from the Silurian period through the Permian period. The SmNd ages reported from studies on other ophiolites (e.g., in the Variscan Belt of Europe; Kryza and Pin [4]) appeared to be different from SIMS U-Pb zircon age data because of the parent-daughter disturbance and resetting due to the metasomatism and metamorphism. This suggests that the geochronological significance of the Sm-Nd isotopic ages can be problematic. More precise geochronological investigation on the Yakuno ophiolite of MORB origin in the Oshima peninsula and Ayabe area would be necessary.

Conflict of Interests

The authors declare that they have no conflict of interests.


The authors express their sincere thanks to Dr. T. Okudaira and Professor Dr. M. Satish-Kumar for their valuable comments and guidance. Earlier version of the paper was improved by Professor Dr. S. Arai and Professor Dr. Harald Furnes. Special thanks go to Professor Dr. R. Kryza for editing this paper. Funding was provided by a Grant-in-Aid for Scientific Research at the Center for Chronological Research at Nagoya University.


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Yoshimitsu Suda, (1,2) Yasutaka Hayasaka, (3) and Kosuke Kimura (3)

(1) Center for Obsidian and Lithic Studies, Meiji University, Nagano 386-0601, Japan

(2) Department of Geology, Faculty of Education, Nagasaki University, Nagasaki 825-8521, Japan

(3) Department of Earth and Planetary Systems Science, Hiroshima University, Higashihiroshima 739-8526, Japan

Correspondence should be addressed to Yoshimitsu Suda;

Received 9 December 2013; Revised 6 March 2014; Accepted 16 April 2014; Published 28 May 2014

Academic Editor: Ryszard Kryza

TABLE 1: Results of U-Pb analysis for zircons from metagabbro (Gbl)
and amphibolite (Ami).

Sample grain   Point    U (ppm)   Th/U     [sup.204]pb/[sup.206]pb

Zircon from Gbl

Gbl-07          Core      407     0.338   -0.00008 [+ or -] 0.00007
Gbl-07-02      Mantle     130     0.221   0.00058 [+ or -] 0.00037
Gbl-08c         Core      121     0.373   0.00071 [+ or -] 0.00029
Gbl-19c         Core      417     0.237   -0.00006 [+ or -] 0.00005
Gbl-22r        Mantle     32      0.201   0.00274 [+ or -] 0.00105
Gbl-24c         Core      195     0.239   0.00016 [+ or -] 0.00008
Gbl-24r        Mantle     61      0.191   0.00044 [+ or -] 0.00046
Gbl-50c        Mantle     633     0.373   0.00012 [+ or -] 0.00006
Gbl-54c        Mantle     211     0.325   0.00027 [+ or -] 0.00014
Gbl-58c        Mantle     92      0.320   0.00020 [+ or -] 0.00030
Gbl-32c        Mantle     122     0.303   -0.00098 [+ or -] 0.00189

Zircon from Ami

Aml-18          Core      577     0.633   0.00001 [+ or -] 0.00014
Aml-21c         Core      178     0.489   0.00046 [+ or -] 0.00018
Ami-8          Mantle     139     1.155   0.00040 [+ or -] 0.00016
Ami-02         Mantle     167     0.397   -0.00080 [+ or -] 0.00092
Aml-15m        Mantle     339     1.066   0.00023 [+ or -] 0.00020
Ami-05c        Mantle     125     0.930   0.00273 [+ or -] 0.00093
Aml-10c         Core      343     0.562   0.00068 [+ or -] 0.00020
Aml-12c        Mantle     65      0.840   0.00131 [+ or -] 0.00082
Aml-09c        Mantle     714     0.588   0.00007 [+ or -] 0.00009
Aml-2m         Mantle     195     0.506   0.00012 [+ or -] 0.00024

Sample grain   [sup.207][Pb.sup.*]/[sup.206][Pb.sup.*]

Zircon from Gbl

Gbl-07              0.0541 [+ or -] 0.0012
Gbl-07-02           0.0525 [+ or -] 0.0062
Gbl-08c             0.0455 [+ or -] 0.0049
Gbl-19c             0.0536 [+ or -] 0.0009
Gbl-22r             0.0246 [+ or -] 0.0183
Gbl-24c             0.0540 [+ or -] 0.0017
Gbl-24r             0.0559 [+ or -] 0.0076
Gbl-50c             0.0509 [+ or -] 0.0011
Gbl-54c             0.0506 [+ or -] 0.0030
Gbl-58c             0.0553 [+ or -] 0.0049
Gbl-32c             0.0696 [+ or -] 0.0286

Zircon from Ami

Aml-18              0.0552 [+ or -] 0.0025
Aml-21c             0.0485 [+ or -] 0.0031
Ami-8               0.0531 [+ or -] 0.0028
Ami-02              0.0649 [+ or -] 0.0141
Aml-15m             0.0511 [+ or -] 0.0034
Ami-05c             0.0417 [+ or -] 0.0161
Aml-10c             0.0487 [+ or -] 0.0035
Aml-12c             0.0496 [+ or -] 0.0139
Aml-09c             0.0514 [+ or -] 0.0017
Aml-2m              0.0512 [+ or -] 0.0044

Sample grain   [sup.206][Pb.sup.*]/[sup.208]pb

Zircon from Gbl

Gbl-07             0.0494 [+ or -] 0.0011
Gbl-07-02          0.0464 [+ or -] 0.0014
Gbl-08c            0.0461 [+ or -] 0.0010
Gbl-19c            0.0482 [+ or -] 0.0010
Gbl-22r            0.0449 [+ or -] 0.0014
Gbl-24c            0.0478 [+ or -] 0.0008
Gbl-24r            0.0469 [+ or -] 0.0017
Gbl-50c            0.0409 [+ or -] 0.0012
Gbl-54c            0.0445 [+ or -] 0.0010
Gbl-58c            0.0480 [+ or -] 0.0010
Gbl-32c            0.0466 [+ or -] 0.0019

Zircon from Ami

Aml-18             0.0446 [+ or -] 0.0036
Aml-21c            0.0453 [+ or -] 0.0012
Ami-8              0.0419 [+ or -] 0.0009
Ami-02             0.0487 [+ or -] 0.0012
Aml-15m            0.0475 [+ or -] 0.0011
Ami-05c            0.0420 [+ or -] 0.0024
Aml-10c            0.0480 [+ or -] 0.0012
Aml-12c            0.0451 [+ or -] 0.0020
Aml-09c            0.0441 [+ or -] 0.0010
Aml-2m             0.0512 [+ or -] 0.0018

Sample grain   [sup.206][Pb.sup.*]/[sup.208]pb
spot                      age (Ma)

Zircon from Gbl

Gbl-07                 311 [+ or -] 7
Gbl-07-02              292 [+ or -] 9
Gbl-08c                291 [+ or -] 6
Gbl-19c                304 [+ or -] 6
Gbl-22r                283 [+ or -] 9
Gbl-24c                301 [+ or -] 5
Gbl-24r                295 [+ or -] 11
Gbl-50c                258 [+ or -] 7
Gbl-54c                281 [+ or -] 6
Gbl-58c                302 [+ or -] 6
Gbl-32c                294 [+ or -] 12

Zircon from Ami

Aml-18                 281 [+ or -] 22
Aml-21c                286 [+ or -] 7
Ami-8                  265 [+ or -] 6
Ami-02                 306 [+ or -] 7
Aml-15m                299 [+ or -] 7
Ami-05c                265 [+ or -] 15
Aml-10c                303 [+ or -] 7
Aml-12c                284 [+ or -] 12
Aml-09c                279 [+ or -] 6
Aml-2m                 322 [+ or -] 11

Sample grain      [sup.207][Pb.sup.*]/     Disc.
spot               [sup.206][Pb.sup.*]      (%)
                         age (Ma)
Zircon from Gbl

Gbl-07               376 [+ or -] 50        17
Gbl-07-02           307 [+ or -] 268         5
Gbl-08c             -29 [+ or -] 262       1087
Gbl-19c              355 [+ or -] 38        14
Gbl-22r            -1817 [+ or -] 2668      116
Gbl-24c              372 [+ or -] 69        19
Gbl-24r             447 [+ or -] 303        34
Gbl-50c              238 [+ or -] 50        -9
Gbl-54c             222 [+ or -] 139        -26
Gbl-58c             426 [+ or -] 197        29
Gbl-32c             917 [+ or -] 845        68

Zircon from Ami

Aml-18              420 [+ or -] 101        33
Aml-21c             124 [+ or -] 152       -130
Ami-8               334 [+ or -] 121        21
Ami-02              771 [+ or -] 458        60
Aml-15m             246 [+ or -] 155        -22
Ami-05c             -245 [+ or -] 978       208
Aml-10c             132 [+ or -] 168       -130
Aml-12c             174 [+ or -] 654        -63
Aml-09c              260 [+ or -] 74        -7
Aml-2m              248 [+ or -] 198        -30

Errors assigned to the isotopic ratios [sup.206][Pb.sup.*]/
[sup.238]U and [sup.207]Pb/[sup.206][Pb.sup.*] ages are 2a.

Discordancy (Disc. (%)) is defined as [1 - ([sup.206][Pb.sup.*]/
[sup.238]U age)/([sup.207][Pb.sup.*]/[sup.206][Pb.sup.*] age)]
x 100 (%).
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Title Annotation:Research Article
Author:Suda, Yoshimitsu; Hayasaka, Yasutaka; Kimura, Kosuke
Publication:Journal of Geological Research
Article Type:Report
Date:Jan 1, 2014
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