# 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

Authors: Yoshimitsu Suda; Yasutaka Hayasaka; Kosuke Kimura
Journal: Journal of Geological Research
 (2014)

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## Abstract

The Yakuno ophiolite in southwest Japan is considered to have been obducted by the collision between an intra-oceanic island-arc-back-arc basin (intra-OIA-BAB) system and the East Asian continent during the late Paleozoic. New SIMS (SHRIMP) zircon U-Pb determinations for amphibolite and metagabbro of BAB origin within the Yakuno ophiolite yield ages of 293.4 ± 9.5 Ma and 288 ± 13 Ma, respectively. These ages are slightly older (however, overlapping within analytical errors) than the magmatic age of arc granitoids (ca. 285–282 Ma) that intruded into the mafic rocks of BAB origin. Results from geochronological and geochemical data of the Yakuno ophiolite give rise to the following tentative geotectonic model for the Paleozoic intra-OIA-BAB system: the initial stage of BAB rifting (ca. 293–288 Ma) formed the BAB crust with island-arc basalt (IAB) signatures, which was brought to the OIA setting, and generated the arc granitoids (ca. 285–282 Ma) by anatexis of the BAB crust. A later stage of BAB rifting (<ca. 285 Ma) formed the BAB crust with IAB to MORB signatures, on which the Permian sediments were conformably deposited. These components collided with the eastern margin of the East Asian continent during the early Mesozoic.


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## Body

## 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 ty3he 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].Figure 1
Distribution of the Maizuru Terrane in southwest Japan.The zircon U-Pb TIMS ages of 282 ± 2 Ma and 285 ± 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 (Figure1) 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)).Geological map (a) and schematic columnar section (b) of the Yakuno ophiolite and associated rocks in the Asago area [8].
(a)
(b)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 (Figure1) [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 (Pseudoalbaillellacf.fusiformis) are reported from the lower strata [16], and radiolarians of middle to late Permian age are reported from the middle to upper strata [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 (Figure1). 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.


## 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 (Figure1) 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)).Geological map (a) and schematic columnar section (b) of the Yakuno ophiolite and associated rocks in the Asago area [8].
(a)
(b)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 (Figure1) [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 (Pseudoalbaillellacf.fusiformis) are reported from the lower strata [16], and radiolarians of middle to late Permian age are reported from the middle to upper strata [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 (Figure1). 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 (Figure1). The outcrop from which sample Gb1 was taken is located at latitude 35.232209°N and longitude 134.709694°E and represents the structurally lowermost part of the ophiolite (Figure 2(b)). The outcrop for sample Am1 is located at latitude 35.234321°N and longitude 134.748472°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 ± 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 ± 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 <250μm 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 Fujii 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 (Figure3). 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 206Pb*/238U age of 293.4 ± 9.5 Ma (all errors give 2σ) is estimated (Figure 4(a)). The probability plot for these spot 206Pb*/238U 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).Table 1
Results of U-Pb analysis for zircons from metagabbro (Gb1) and amphibolite (Am1).
Sample grain spot
Point
U
Th/U
204Pb/206Pb
207Pb*/206Pb*
206Pb*/238U
206Pb*/238U
207Pb*/206Pb*
Disc.
(ppm)
age (Ma)
age (Ma)
(%)
Zircon from Gb1
Gb1-07
Core
407
0.338
−0.00008 ± 0.00007
0.0541 ± 0.0012
0.0494 ± 0.0011
311 ± 7
376 ± 50
17
Gb1-07-02
Mantle
130
0.221
0.00058 ± 0.00037
0.0525 ± 0.0062
0.0464 ± 0.0014
292 ± 9
307 ± 268
5
Gb1-08c
Core
121
0.373
0.00071 ± 0.00029
0.0455 ± 0.0049
0.0461 ± 0.0010
291 ± 6
−29 ± 262
1087
Gb1-19c
Core
417
0.237
−0.00006 ± 0.00005
0.0536 ± 0.0009
0.0482 ± 0.0010
304 ± 6
355 ± 38
14
Gb1-22r
Mantle
32
0.201
0.00274 ± 0.00105
0.0246 ± 0.0183
0.0449 ± 0.0014
283 ± 9
−1817 ± 2668
116
Gb1-24c
Core
195
0.239
0.00016 ± 0.00008
0.0540 ± 0.0017
0.0478 ± 0.0008
301 ± 5
372 ± 69
19
Gb1-24r
Mantle
61
0.191
0.00044 ± 0.00046
0.0559 ± 0.0076
0.0469 ± 0.0017
295 ± 11
447 ± 303
34
Gb1-50c
Mantle
633
0.373
0.00012 ± 0.00006
0.0509 ± 0.0011
0.0409 ± 0.0012
258 ± 7
238 ± 50
−9
Gb1-54c
Mantle
211
0.325
0.00027 ± 0.00014
0.0506 ± 0.0030
0.0445 ± 0.0010
281 ± 6
222 ± 139
−26
Gb1-58c
Mantle
92
0.320
0.00020 ± 0.00030
0.0553 ± 0.0049
0.0480 ± 0.0010
302 ± 6
426 ± 197
29
Gb1-32c
Mantle
122
0.303
−0.00098 ± 0.00189
0.0696 ± 0.0286
0.0466 ± 0.0019
294 ± 12
917 ± 845
68
Zircon from Am1
Am1-18
Core
577
0.633
0.00001 ± 0.00014
0.0552 ± 0.0025
0.0446 ± 0.0036
281 ± 22
420 ± 101
33
Am1-21c
Core
178
0.489
0.00046 ± 0.00018
0.0485 ± 0.0031
0.0453 ± 0.0012
286 ± 7
124 ± 152
−130
Am1-8
Mantle
139
1.155
0.00040 ± 0.00016
0.0531 ± 0.0028
0.0419 ± 0.0009
265 ± 6
334 ± 121
21
Am1-02
Mantle
167
0.397
−0.00080 ± 0.00092
0.0649 ± 0.0141
0.0487 ± 0.0012
306 ± 7
771 ± 458
60
Am1-15m
Mantle
339
1.066
0.00023 ± 0.00020
0.0511 ± 0.0034
0.0475 ± 0.0011
299 ± 7
246 ± 115
−22
Am1-05c
Mantle
125
0.930
0.00273 ± 0.00093
0.0417 ± 0.0161
0.0420 ± 0.0024
265 ± 15
−245 ± 978
208
Am1-10c
Core
343
0.562
0.00068 ± 0.00020
0.0487 ± 0.0035
0.0480 ± 0.0012
303 ± 7
132 ± 168
−130
Am1-12c
Mantle
65
0.840
0.00131 ± 0.00082
0.0496 ± 0.0139
0.0451 ± 0.0020
284 ± 12
174 ± 654
−63
Am1-09c
Mantle
714
0.588
0.00007 ± 0.00009
0.0514 ± 0.0017
0.0441 ± 0.0010
279 ± 6
260 ± 74
−7
Am1-2m
Mantle
195
0.506
0.00012 ± 0.00024
0.0512 ± 0.0044
0.0512 ± 0.0018
322 ± 11
248 ± 198
−30
Errors assigned to the isotopic ratios206Pb*/238U and 207Pb*/206Pb* ages are 2σ.
Discordancy (Disc. (%)) is defined as [1 − (206Pb*/238U age)/(207Pb*/206Pb* age)] × 100 (%).Figure 3
Cathodoluminescence image of representative zircons used for SHRIMP dating of the metagabbro (Gb1) and the amphibolite (Am1).(a) Tera and Wasserburg [24] U-Pb zircon diagrams for metagabbro (Gb1) and amphibolite (Am1). Error ellipses indicate 2σ. (b) Probability plot and histogram for the spot 206Pb*/238U ages and peak ages.
(a)
(b)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 (Figure3). The analyzed 10 spots lying on the concordia (Table 1) give a weighted mean concordant 206Pb*/238U age of 288 ± 13 Ma (Figure 4(a)). The probability plot for these spot 206Pb*/238U ages roughly shows 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 (Table1). This may be related to Th loss due to the granulite-facies metamorphism. In this case, the calculated 206Pb*/238U 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 206Pb*/238U ages from the Gb1 and Am1 are overlapping within 2σ error. From these results, we conclude that the 206Pb*/238U ages obtained from the Gb1 and Am1 zircons represent the age of magmatic crystallization of these mafic rocks.


## 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 (Figure1). The outcrop from which sample Gb1 was taken is located at latitude 35.232209°N and longitude 134.709694°E and represents the structurally lowermost part of the ophiolite (Figure 2(b)). The outcrop for sample Am1 is located at latitude 35.234321°N and longitude 134.748472°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 ± 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 ± 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 <250μm 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 Fujii 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 (Figure3). 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 206Pb*/238U age of 293.4 ± 9.5 Ma (all errors give 2σ) is estimated (Figure 4(a)). The probability plot for these spot 206Pb*/238U 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).Table 1
Results of U-Pb analysis for zircons from metagabbro (Gb1) and amphibolite (Am1).
Sample grain spot
Point
U
Th/U
204Pb/206Pb
207Pb*/206Pb*
206Pb*/238U
206Pb*/238U
207Pb*/206Pb*
Disc.
(ppm)
age (Ma)
age (Ma)
(%)
Zircon from Gb1
Gb1-07
Core
407
0.338
−0.00008 ± 0.00007
0.0541 ± 0.0012
0.0494 ± 0.0011
311 ± 7
376 ± 50
17
Gb1-07-02
Mantle
130
0.221
0.00058 ± 0.00037
0.0525 ± 0.0062
0.0464 ± 0.0014
292 ± 9
307 ± 268
5
Gb1-08c
Core
121
0.373
0.00071 ± 0.00029
0.0455 ± 0.0049
0.0461 ± 0.0010
291 ± 6
−29 ± 262
1087
Gb1-19c
Core
417
0.237
−0.00006 ± 0.00005
0.0536 ± 0.0009
0.0482 ± 0.0010
304 ± 6
355 ± 38
14
Gb1-22r
Mantle
32
0.201
0.00274 ± 0.00105
0.0246 ± 0.0183
0.0449 ± 0.0014
283 ± 9
−1817 ± 2668
116
Gb1-24c
Core
195
0.239
0.00016 ± 0.00008
0.0540 ± 0.0017
0.0478 ± 0.0008
301 ± 5
372 ± 69
19
Gb1-24r
Mantle
61
0.191
0.00044 ± 0.00046
0.0559 ± 0.0076
0.0469 ± 0.0017
295 ± 11
447 ± 303
34
Gb1-50c
Mantle
633
0.373
0.00012 ± 0.00006
0.0509 ± 0.0011
0.0409 ± 0.0012
258 ± 7
238 ± 50
−9
Gb1-54c
Mantle
211
0.325
0.00027 ± 0.00014
0.0506 ± 0.0030
0.0445 ± 0.0010
281 ± 6
222 ± 139
−26
Gb1-58c
Mantle
92
0.320
0.00020 ± 0.00030
0.0553 ± 0.0049
0.0480 ± 0.0010
302 ± 6
426 ± 197
29
Gb1-32c
Mantle
122
0.303
−0.00098 ± 0.00189
0.0696 ± 0.0286
0.0466 ± 0.0019
294 ± 12
917 ± 845
68
Zircon from Am1
Am1-18
Core
577
0.633
0.00001 ± 0.00014
0.0552 ± 0.0025
0.0446 ± 0.0036
281 ± 22
420 ± 101
33
Am1-21c
Core
178
0.489
0.00046 ± 0.00018
0.0485 ± 0.0031
0.0453 ± 0.0012
286 ± 7
124 ± 152
−130
Am1-8
Mantle
139
1.155
0.00040 ± 0.00016
0.0531 ± 0.0028
0.0419 ± 0.0009
265 ± 6
334 ± 121
21
Am1-02
Mantle
167
0.397
−0.00080 ± 0.00092
0.0649 ± 0.0141
0.0487 ± 0.0012
306 ± 7
771 ± 458
60
Am1-15m
Mantle
339
1.066
0.00023 ± 0.00020
0.0511 ± 0.0034
0.0475 ± 0.0011
299 ± 7
246 ± 115
−22
Am1-05c
Mantle
125
0.930
0.00273 ± 0.00093
0.0417 ± 0.0161
0.0420 ± 0.0024
265 ± 15
−245 ± 978
208
Am1-10c
Core
343
0.562
0.00068 ± 0.00020
0.0487 ± 0.0035
0.0480 ± 0.0012
303 ± 7
132 ± 168
−130
Am1-12c
Mantle
65
0.840
0.00131 ± 0.00082
0.0496 ± 0.0139
0.0451 ± 0.0020
284 ± 12
174 ± 654
−63
Am1-09c
Mantle
714
0.588
0.00007 ± 0.00009
0.0514 ± 0.0017
0.0441 ± 0.0010
279 ± 6
260 ± 74
−7
Am1-2m
Mantle
195
0.506
0.00012 ± 0.00024
0.0512 ± 0.0044
0.0512 ± 0.0018
322 ± 11
248 ± 198
−30
Errors assigned to the isotopic ratios206Pb*/238U and 207Pb*/206Pb* ages are 2σ.
Discordancy (Disc. (%)) is defined as [1 − (206Pb*/238U age)/(207Pb*/206Pb* age)] × 100 (%).Figure 3
Cathodoluminescence image of representative zircons used for SHRIMP dating of the metagabbro (Gb1) and the amphibolite (Am1).(a) Tera and Wasserburg [24] U-Pb zircon diagrams for metagabbro (Gb1) and amphibolite (Am1). Error ellipses indicate 2σ. (b) Probability plot and histogram for the spot 206Pb*/238U ages and peak ages.
(a)
(b)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 (Figure3). The analyzed 10 spots lying on the concordia (Table 1) give a weighted mean concordant 206Pb*/238U age of 288 ± 13 Ma (Figure 4(a)). The probability plot for these spot 206Pb*/238U ages roughly shows 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 (Table1). This may be related to Th loss due to the granulite-facies metamorphism. In this case, the calculated 206Pb*/238U 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 206Pb*/238U ages from the Gb1 and Am1 are overlapping within 2σ error. From these results, we conclude that the 206Pb*/238U 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)N ratio with respect to the (La/Y)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)N ratio >1.0, while the compositions of IAB [34–36] are plotted in the field of the (Nb/La)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.Figure 5
Variation diagram of N-MORB normalized La/Nb ratio versus La/Y ratio for the metabasalt in the Yakuno-cho area [11] and the noncumulitic metagabbro in the Asago area [7]. Also plotted for comparative purposes are the compositions of Cenozoic back-arc basin basalts (BABBs) in various areas [31], MORBs (N-MORB [34]; T- and E-MORBs [35]), and island-arc basalt (IAB) [36].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 Figure6. 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.Figure 6
Summary of isotopic ages for the Yakuno ophiolite and stratigraphic ages for the Permo-Triassic sediments in the Maizuru Terrane. Data sources for isotopic ages are (1) Sano [38]; (2) Koide et al. [14]; (3) Herzig et al. [9]; (4) Hayasaka et al. [6]; and (5) the present study.Koide et al. [37] reported an Rb-Sr whole-rock-mineral isochron age of 281 ± 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 ± 44 Ma and 412 ± 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 ± 62 Ma, 343 ± 34 Ma, and 385 ± 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; Figure7(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; Figure7(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; Figure7(c)).
(4)
These Paleozoic components collided and became accreted to the eastern margin of the East Asian continent during the early Mesozoic.Tentative geotectonic model and time scale for the Paleozoic intra-OIA-BAB system of the Yakuno ophiolite and associated rocks.
(a)
(b)
(c)The problems still remaining comprise the evidence of the subduction zone adjacent to the craton (Figure7(c)) and of how to survive the metagabbro of MORB origin from the Silurian period through the Permian period. The Sm-Nd 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.


## 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)N ratio with respect to the (La/Y)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)N ratio >1.0, while the compositions of IAB [34–36] are plotted in the field of the (Nb/La)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.Figure 5
Variation diagram of N-MORB normalized La/Nb ratio versus La/Y ratio for the metabasalt in the Yakuno-cho area [11] and the noncumulitic metagabbro in the Asago area [7]. Also plotted for comparative purposes are the compositions of Cenozoic back-arc basin basalts (BABBs) in various areas [31], MORBs (N-MORB [34]; T- and E-MORBs [35]), and island-arc basalt (IAB) [36].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 Figure6. 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.Figure 6
Summary of isotopic ages for the Yakuno ophiolite and stratigraphic ages for the Permo-Triassic sediments in the Maizuru Terrane. Data sources for isotopic ages are (1) Sano [38]; (2) Koide et al. [14]; (3) Herzig et al. [9]; (4) Hayasaka et al. [6]; and (5) the present study.Koide et al. [37] reported an Rb-Sr whole-rock-mineral isochron age of 281 ± 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 ± 44 Ma and 412 ± 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 ± 62 Ma, 343 ± 34 Ma, and 385 ± 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; Figure7(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; Figure7(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; Figure7(c)).
(4)
These Paleozoic components collided and became accreted to the eastern margin of the East Asian continent during the early Mesozoic.Tentative geotectonic model and time scale for the Paleozoic intra-OIA-BAB system of the Yakuno ophiolite and associated rocks.
(a)
(b)
(c)The problems still remaining comprise the evidence of the subduction zone adjacent to the craton (Figure7(c)) and of how to survive the metagabbro of MORB origin from the Silurian period through the Permian period. The Sm-Nd 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.



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*Source: 652484-2014-05-28.xml*