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Article

Geochemical Characteristics of the Hida Granitoids in the Unazuki and Katakaigawa Areas, Central Japan

by
Kazuki Oishi
,
Rui Kuwahara
,
Kazuya Shimooka
* and
Motohiro Tsuboi
Department of Applied Chemistry for Environment, School of Biological and Environmental Sciences, Kwansei Gakuin University, 1 Gakuen Uegahara, Sanda 669-1330, Japan
*
Author to whom correspondence should be addressed.
Geosciences 2025, 15(8), 285; https://doi.org/10.3390/geosciences15080285
Submission received: 31 March 2025 / Revised: 26 July 2025 / Accepted: 28 July 2025 / Published: 29 July 2025
(This article belongs to the Section Geochemistry)
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Abstract

The Hida Belt in central Japan is a key geological unit for understanding the crustal growth of the Eurasian continent in the Mesozoic. However, while previous studies have focused primarily on geochronology, the geochemical characteristics of its rocks and minerals remain largely unexplored. This study investigates the geochemical characteristics and magmatic processes of the Hida granitoids, including adakitic rocks, distributed in the Unazuki and Katakaigawa areas. Whole-rock major oxides and trace elements, as well as Rb-Sr isotopes, were analyzed. Based on Rb–Sr isotopic compositions, the Hida granitoids are classified into two types. The younger and older granitoids in the Unazuki area, categorized as Type I, exhibit a narrow range of isotopic ratios, whereas the older granitoids in the Katakaigawa area, classified as Type II, display significantly higher values than those of Type I. The geochemical data suggest that the adakitic rocks in the older granitoids originated from interaction with alkali-rich melts or fluids, while those in the younger granitoids were derived from hydrous felsic magmas sourced from subducted oceanic crust. These findings provide new insights into the formation and evolution of granitic magmatism in the Hida Belt.

1. Introduction

The Hida Belt, located on the back-arc side of central Japan (Figure 1a), is regarded as a fragmented portion of geological terranes that collided and amalgamated during the Middle Triassic (~230 Ma), including the North China Craton [1,2] and the South China Craton [3].
Debates have continued regarding whether the Japanese archipelago, including the Hida Belt, is affiliated with the North China Block or the South China Block. For example, zircon U-Pb dating of gneisses distributed in the Tetori Group of the Hida Belt has suggested a correlation with the North China Block [4,5,6,7]. Additionally, the Hida Belt has been compared to complex gneisses from the Busan region of the Korean Peninsula, which belong to the North China Block [8]. Furthermore, the discovery of staurolite in the 240–220 Ma Unazuki Metamorphic Rocks of the Unazuki area has led to their characterization as part of a collision-type orogen [9]. Thus, the Hida Belt is crucial for elucidating crustal growth processes along the eastern margin of the Eurasian continent. The Early Mesozoic plutonic rocks of the Hida Belt (Figure 1b), collectively referred to as the ‘Hida Granites’ by Kano (1990) [10,11], have been subject to various classification schemes. For example, Arakawa (1988; 1990) [12,13] and Arakawa and Shinmura (1995) [14] categorized the Hida granitoids as Type I or II plutons according to their isotopic signatures. Type I plutons are predominantly exposed in the eastern part of the Hida Belt, whereas Type II plutons are mainly found in the western part. Geochemically, Type I plutons are characterized by low initial 87Sr/86Sr ratios (0.7044–0.7054) and high εNd values (−0.8 to +5.5). In contrast, Type II plutons exhibit high initial 87Sr/86Sr ratios (0.7055–0.7105) and low εNd values (−10.3 to +0.7). The latter also typically contain abundant gneiss xenoliths (Arakawa and Shinmura, 1995) [14]. Takahashi et al. (2010) [15] and Takahashi et al. (2018) [16] divided the Hida granitoids into two groups: ‘Hida older granites’ (ca. 235–250 Ma) and ‘Hida younger granites’ (ca. 190–200 Ma) based on the lithologies and age data. According to their interpretation, the Hida younger granites correspond to Type I plutons, while the Hida older granites correspond to Type II plutons. However, previous discussions have mainly focused on geochronology, while the geochemical characteristics of rocks and minerals in this area have received less attention. Furthermore, the formation and geochemical characteristics of the Hida granitoids in the Unazuki area remain largely unknown.
Adakitic granitic magmas are considered primary continental crustal components responsible for substantial continental growth [17]. These rocks provide crucial evidence for crust–mantle material recycling [18,19,20]. In recent years, various genetic models for adakitic rocks have been proposed, including partial melting of lower crustal basalt that has undergone eclogite–facies metamorphism [21], partial melting of subducted oceanic crust [19], and mixing of adakitic magmas derived from oceanic crust with mantle peridotite [22,23]. However, many aspects of their genesis and ascent mechanisms remain unresolved. Despite the reported presence of some adakitic rocks in the Hida granitoids [24], limited studies of magmatic processes based on their geochemistry have been carried out. Therefore, this study aims to characterize the geochemical features of the Hida granitoids (including adakitic rocks) distributed in the Unazuki and Katakaigawa areas, through whole-rock major oxide and trace element analyses, as well as Rb–Sr isotopic analyses. Based on the chemical composition of the adakitic rocks, we further aim to elucidate the magmatic processes involved in their formation.
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Figure 1. (a) Location map of the Hida belt (modified from Takeuchi et al., 2023 [25]). (b) Simplified geological map of Hida belt (modified from Yamada et al. (2021) [24]). The exposed areas of gray granites are from Kano (1990) [11], and the zircon U-Pb ages are from Takeuchi et al. (2019) [26]. (c) Distribution of the Hida granitoids in Unazuki and Katakaigawa areas (modified after Takahashi et al., 2010 [15]).
Figure 1. (a) Location map of the Hida belt (modified from Takeuchi et al., 2023 [25]). (b) Simplified geological map of Hida belt (modified from Yamada et al. (2021) [24]). The exposed areas of gray granites are from Kano (1990) [11], and the zircon U-Pb ages are from Takeuchi et al. (2019) [26]. (c) Distribution of the Hida granitoids in Unazuki and Katakaigawa areas (modified after Takahashi et al., 2010 [15]).
Geosciences 15 00285 g001
It is worth noting that various terminologies, such as ‘Hida Granites,’ have been historically used to refer to the plutonic rocks of the Hida Belt. In this study, we adopt the terms ‘Hida granitoids,’ ‘older granitoids,’ and ‘younger granitoids’ to describe these plutonic bodies, which include relatively mafic lithologies, to distinguish them from the more narrowly defined term ‘granite’. The division into younger and older phases is based on Takahashi et al. (2010) [15].

2. Geological Background

2.1. Basement Rocks

In the Hida belt, the Unazuki metamorphic rocks and the Hida gneiss are exposed as basement rocks (Figure 1b,c). The Unazuki metamorphic rocks are mainly exposed in the eastern part of the Hida belt and are interpreted to have formed through medium P/T metamorphism around 250 Ma, affecting Carboniferous sedimentary rocks, limestones, and volcanic rocks [27,28]. The Hida gneiss shows extensive exposure in the southern part of the Hida belt, with minor outcrops in the eastern area. It is considered to have formed from shelf sedimentary rocks that underwent metamorphism ranging from amphibolite facies under medium P/T conditions to granulite facies under low P/T conditions around 235–250 Ma [16]. In the southern Hida Belt, where the Hida gneiss is widely exposed, gray to white granitic rocks are frequently found within the gneiss. These granitic rocks, referred to as “gray granites” [11], are interpreted to have formed by processes such as partial melting [29], and zircon U–Pb ages of 230–240 Ma have been reported [26].

2.2. Hida Granitoids

Various types of plutonic rocks are exposed in the Hida Belt (Figure 1b,c). These are classified into two groups, the Hida older granitoids (ca. 235–250 Ma) and the Hida younger granitoids (ca. 190–200 Ma), based on zircon U-Pb ages and petrography [15,16]. In addition, Hida granitoids are classified into Type I and Type II based on Sr and Nd isotopic compositions [14]. Type I and Type II plutons correspond to the younger and older granitoids, respectively. Type I plutons, found in the southern and eastern Hida Belt, exhibit a narrow isotopic range, whereas Type II plutons in the northwestern region show a wider variation, likely due to interaction with gray granites (Figure 1b). Ishihara (2005) [30] suggested that Type II plutons originated from adakitic magma, either by assimilation of felsic crustal sediments or through reduction during solidification. However, the origin of Type I plutons has not been discussed. The Unazuki and Katakaigawa areas are composed of the Unazuki metamorphic rocks, Hida older granitoids, and Hida younger granitoids [31]. The Hida older granitoids consist of the Unazuki Granite (UG), Hayatsukigawa Granite (HG), Augen Granite Mylonite (AGM), Otodani Gabbro (OG), Funakawa Granite (FG), and Oitsurushiyama Granite [32,33,34,35,36]. The Hida younger granitoids comprise the Yatazodani Quartz Diorite (YQD), Yatazodani Hornblende Quartz Diorite (YHQD), and Kegachidake granite [21,34,36]. The petrographic characteristics and zircon U-Pb age of each plutonic body except for the Oitsurushiyama Granite, are summarized in Table 1.

3. Analytical Methods

A total of 35 rock samples were collected from the Hida granitoids in the Unazuki and Katakaigawa areas, Toyama Prefecture (Figure 1b,c). Of the Hida granitoid samples, 12 correspond to the Hida younger granitoids, while 23 correspond to the Hida older granitoids.

3.1. Whole-Rock Chemical Analysis

The major oxide and trace element compositions were measured using wavelength dispersive X-ray fluorescence spectrometry (WD-XRF). Rock fragments obtained by avoiding altered parts of the collected rock samples were crushed to prepare powder samples. Powdered samples were mixed with a flux (Lithium Tetraborate, type II, Fujifilm Wako Pure Chemical Corporation, Osaka, Japan) and fused at 1000 °C. The weight proportion of the sample to flux was 0.7:6 for major element analysis and 2:3 for trace element analysis. The resulting glass disks were analyzed using WD-XRF (Shimadzu XRF-1800, Kyoto, Japan) at Kwansei Gakuin University. The analytical procedure was based on Nakazaki et al. (2004) [38] and Koga and Tsuboi (2021) [39]. The accuracy of the analysis was assessed using standard rock samples (JR-2, JGb-1, and JG-3) released by the Geological Survey of Japan. The relative deviations of the measured values from the reference values [40] were less than 1%. The composition of REEs in 14 samples (3 younger and 11 older granitoids), including some adakitic rocks, was determined using inductively coupled plasma mass spectrometry (ICP-MS). The glass disks used for the trace element measurements were powdered using an iron mortar and alumina mortar and acid-decomposed using hydrochloric acid. The resulting solution was used to remove Li added during glass disk preparation using a cation exchange resin (AG 50W-X8, Bio-Rad, Hercules, CA, USA), and the REEs were extracted by column separation. The concentration of REEs in the solution was measured using an ICP-MS (Agilent Technologies ICP-MS 7700, Tokyo, Japan) at Kwansei Gakuin University. Detailed sample preparation methods for REEs are described in Koga and Tsuboi (2021) [39]. It should be noted that REE data for the younger granitoids are limited to only three samples. Therefore, this study refrains from discussing igneous processes based primarily on REE compositions. Data for the whole-rock analysis are presented in Table 2.

3.2. Rb-Sr Isotope Analysis

Seven samples from the Unazuki area and four samples from the Katakaigawa area of the Hida plutonic rocks were analyzed using thermal ionization mass spectrometry (TIMS). Sr was extracted from powdered samples by acid decomposition using hydrofluoric acid, nitric acid, and hydrochloric acid, and column separation using a cation exchange resin (AG 50W-X8, Bio-Rad). The Sr obtained was applied to Ta filaments and the Sr isotopes ratio were measured using TIMS (Thermo Fisher Scientific Finnigan MAT262, Bremen, Germany) at Kwansei Gakuin University. Detailed analytical methods are described in Xue et al. (2024) [41]. Repeated analyses of NIST SRM 987 during this study yielded 87Sr/86Sr ratios of 0.710234 ± 0.000030 (2SD, n = 8). The Rb and Sr contents were analyzed by XRF (Table 2). The initial Sr isotope ratios (SrI) were calculated using the decay constants λ87Rb = 1.42 × 10−11/year (Steiger and Jäger, 1977) [42], using the zircon U-Pb ages reported from each rock body (Table 1). Data for the Rb-Sr analysis are presented in Table 3.

4. Results

4.1. Whole-Rock Chemical Analysis

Variation diagrams of major oxide and trace element vs. SiO2 are shown in Figure 2. K2O vs. SiO2, alumina saturation index (ASI: Al2O3/(CaO + K2O + Na2O) (mole ratio)) vs. SiO2, Sr/Y vs. Y, and (Eu/Eu*)N vs. SiO2 are shown in Figure 3. The Hida granitoids possess a wide compositional range of 48.7 to 75.5 wt.% SiO2 since these intrusions include a variety of lithologies from gabbro to granite. The older granitoids range from 48.7 to 75.5 wt.% SiO2, while the younger granitoids range from 50.3 to 75.4 wt.% SiO2. Most samples of the older granitoids plot in the high-SiO2 domain, whereas many of the younger granitoid samples fall within the low-SiO2 range. The variation diagrams show that major oxides such as TiO2, Fe2O3, MnO, MgO, CaO, and P2O5 decrease with increasing SiO2 content in both granitoid suites, while K2O shows an increasing trend. Among the trace elements, V, Cr, Co, Ni, Cu, and Zn decrease with increasing SiO2 content, while Rb, Ba and Pb increase. Classification based on the ASI values reveals that granitoid samples with high SiO2 contents are peraluminous, while those with lower SiO2 contents are metaluminous in both the older and younger granitoids (Figure 3b).
Trace element compositions were further analyzed using the Sr/Y vs. Y diagram for separation of adakitic rocks from arc related rocks [43] (Figure 3c). In this study, 35 samples were analyzed, of which 13 were classified as adakitic rocks. The remaining 22 samples plot within the arc-related rocks field. Samples belonging to both the older and younger granitoids plot both in the adakitic and non-adakitic fields. The granitoids classified into these adakitic fields exhibit characteristic chemical compositions of adakites, such as high Al2O3 contents, high Sr/Y, low Y contents, and low HREE concentrations (as discussed later). However, since some of their chemical characteristics differ from those of typical adakites—such as MgO < 3 wt%, Cr = 5–14 ppm, and Ni = 2–9 ppm [43]—this study refers to them as “adakitic rocks”.
Table 2. Whole-rock chemical composition of the Hida granitoids.
Table 2. Whole-rock chemical composition of the Hida granitoids.
Rock SuiteHida Younger Granitoids
Igneous BodiesKG YQDYHQD
SampleUNA3UNA5UNA6UNA9UNA27UNA2UNA4UNA7UNA8UNA18UNA19UNA28
Major oxides (wt%)
SiO272.4964.1375.3865.6174.6451.4453.97 57.07 58.99 50.51 50.25 53.21
TiO20.250.620.210.650.240.970.97 1.07 1.23 1.26 1.20 0.64
Al2O315.0615.8512.7118.4314.0714.7715.45 16.50 16.86 20.06 18.57 16.09
Fe2O31.615.511.202.181.6710.559.17 8.22 6.52 7.19 8.97 6.88
MnO0.040.110.020.080.040.170.16 0.14 0.10 0.14 0.16 0.15
MgO0.431.180.610.450.277.266.15 3.94 2.31 4.13 3.16 2.34
CaO1.172.531.573.391.048.937.58 6.51 3.34 9.21 9.60 5.86
Na2O4.173.903.494.122.663.053.29 3.81 4.18 4.12 3.59 3.60
K2O3.952.054.142.304.721.901.65 1.91 3.40 1.28 1.91 2.44
P2O50.080.260.050.170.050.320.29 0.34 0.54 0.41 0.34 0.15
Total99.2596.1599.3997.3799.4199.3798.68 99.50 97.47 98.30 97.75 91.35
Trace elements (ppm)
V24.3 27.5 27.4 35.8 17.5 242.9 205.8 172.8 82.1 162.3 212.6 50.4
Cr0.9 0.3 0.3 13.0 2.1 177.8 205.8 35.9 2.6 12.6 1.1 133.9
Co3.1 17.7 3.1 5.0 5.2 57.3 38.4 34.3 24.9 25.6 31.3 28.9
Ni3.2 4.1 10.2 4.4 4.2 65.3 42.9 28.5 0.7 14.6 2.4 4.1
Cu0.8 32.4 21.6 8.9 4.2 87.3 42.0 42.6 29.4 36.8 25.4 12.8
Zn39.0 83.8 12.4 34.1 38.2 93.8 62.0 79.5 77.9 63.7 78.1 108.8
Rb68.4 72.2 79.4 83.7 145.9 53.4 43.7 50.2 112.3 37.6 48.7 103.1
Sr460.8 196.9 192.4 289.9 147.5 1066.1 764.7 694.8 869.0 1158.2 980.9 380.5
Y13.5 26.8 21.1 22.2 26.6 16.7 17.3 22.2 19.9 25.3 23.6 19.3
Zr145.2 327.2 138.4 174.2 163.9 93.5 124.2 80.5 76.8 140.3 168.8 150.2
Nb2.6 5.6 3.9 7.5 4.1 1.0 1.6 4.6 4.8 3.5 1.5 4.1
Ba1314.7 664.1 718.4 593.7 742.5 409.6 447.2 468.5 780.6 358.3 743.5 533.6
Pb16.5 9.6 9.5 14.2 29.3 10.0 5.0 6.7 9.6 8.7 15.8 19.9
Th11.5 5.2 13.7 11.5 11.9 11.8 3.3 7.2 5.7 0.3 0.1 4.1
Rare-earth elements (ppm)
La29.25 22.46 16.50
Ce38.87 47.16 33.40
Pr4.71 6.09 4.41
Nd15.49 25.97 19.23
Sm2.04 5.16 4.07
Eu0.48 1.44 1.13
Gd1.20 4.58 3.72
Tb0.14 0.61 0.50
Dy0.79 3.82 3.10
Ho0.14 0.73 0.57
Er0.39 2.06 1.63
Tm0.05 0.29 0.22
Yb0.49 2.06 1.56
Lu0.07 0.28 0.22
ASI1.131.200.971.191.240.630.74 0.82 1.01 0.81 0.73 0.84
Mg#18.815.630.515.112.237.236.6 29.2 23.4 33.1 23.3 22.7
Sr/Y34.2 7.3 9.1 13.1 5.5 63.7 44.1 31.3 43.6 45.8 41.6 19.7
(Eu/Eu*)N0.94 0.91 0.89
Rock suiteHida Older granitoids
Igneous bodiesUG FG
SampleUNA11UNA12UNA13UNA17UNA22UNA23aUNA26UNA1UNA10UNA15UNA16aUNA16b
Major oxides (wt%)
SiO272.01 74.66 72.70 74.58 74.48 75.53 70.62 64.13 60.72 70.27 65.74 65.92
TiO20.24 0.23 0.24 0.20 0.22 0.14 0.35 0.33 0.80 0.42 0.26 0.21
Al2O314.01 13.80 14.37 13.74 14.13 13.39 15.18 17.99 19.54 16.09 16.94 17.26
Fe2O32.51 3.23 2.22 1.24 1.48 1.13 2.14 5.91 4.48 2.32 3.99 3.75
MnO0.01 0.01 0.01 0.04 0.04 0.01 0.05 0.12 0.08 0.05 0.07 0.08
MgO0.40 0.41 0.42 0.17 0.22 0.16 0.13 0.51 1.23 0.54 0.42 0.42
CaO1.23 1.10 1.30 0.67 0.58 0.42 0.68 2.66 2.59 1.77 1.65 1.85
Na2O2.52 2.45 2.72 3.97 3.73 3.21 4.71 5.97 6.18 5.39 6.11 6.77
K2O4.72 4.72 4.70 4.25 4.85 5.16 4.43 1.81 3.12 2.44 2.93 2.43
P2O50.05 0.05 0.02 0.05 0.05 0.02 0.09 0.07 0.24 0.15 0.08 0.07
Total97.70 100.66 98.69 98.89 99.79 99.18 98.37 99.50 98.98 99.44 98.19 98.78
Trace elements (ppm)
V23.9 22.3 25.4 16.7 17.3 19.0 21.5 6.1 33.0 29.4 6.7 11.2
Cr1.3 7.1 0.5 1.9 2.1 2.2 3.3 2.4 1.9 1.6 1.2 3.1
Co6.7 9.5 6.3 2.9 3.1 3.1 4.3 15.7 10.0 3.9 10.8 10.8
Ni2.8 2.6 3.6 4.6 3.3 3.7 5.2 2.2 2.8 4.4 2.9 3.8
Cu10.6 1.3 6.7 1.1 0.4 0.4 1.2 2.3 4.3 14.7 8.2 25.9
Zn38.6 35.4 35.5 41.8 48.9 53.3 24.8 108.6 47.8 72.0 43.5 40.7
Rb146.1 150.5 144.8 95.3 68.5 56.4 161.6 52.6 44.5 42.9 93.4 90.6
Sr148.6 140.1 162.1 189.1 669.0 663.7 172.2 407.2 680.3 700.4 385.8 305.1
Y29.6 25.1 28.4 14.0 14.7 14.7 26.3 19.7 15.3 12.1 23.7 21.8
Zr166.8 161.0 161.6 120.3 175.1 203.2 152.9 479.7 619.9 174.5 418.9 310.5
Nb1.9 3.0 3.3 1.6 0.9 0.2 4.5 2.6 0.7 0.4 1.6 0.3
Ba875.9 798.1 805.2 582.2 1668.6 1484.5 693.4 694.8 1657.8 784.6 806.0 613.7
Pb24.1 19.2 17.7 25.4 19.1 15.8 18.6 13.1 11.5 26.2 11.5 11.7
Th9.8 10.4 11.4 13.5 3.2 3.0 21.4 35.5 1.6 2.8 29.8 23.8
Rare-earth elements (ppm)
La 20.28 18.90 21.21
Ce 36.36 38.76 41.36
Pr 4.16 4.39 4.69
Nd 17.49 17.21 18.01
Sm 3.19 2.84 2.83
Eu 1.97 0.58 0.67
Gd 2.70 1.55 1.58
Tb 0.30 0.18 0.16
Dy 1.67 0.91 0.84
Ho 0.33 0.15 0.13
Er 0.97 0.38 0.32
Tm 0.14 0.05 0.04
Yb 1.09 0.38 0.32
Lu 0.18 0.05 0.04
ASI1.22 1.24 1.21 1.11 1.13 1.15 1.10 1.08 1.07 1.09 1.04 1.00
Mg#12.2 9.9 14.2 10.6 11.5 11.2 4.9 6.9 19.2 16.8 8.4 8.8
Sr/Y5.0 5.6 5.7 13.5 45.7 45.3 6.5 20.7 44.4 57.7 16.3 14.0
(Eu/Eu*)N 2.05 0.85 0.97
Rock suiteHida older granitoids
Igneous bodiesFG HG AGMOG
SampleUNA16cUNA16dUNA20UNA21UNA29UNA31UNA30UNA14UNA23bUNA24UNA25
Major oxides (wt%)
SiO268.95 67.30 70.92 69.56 69.49 69.36 70.60 48.70 49.37 51.00 53.09
TiO20.43 0.53 0.17 0.21 0.21 0.16 0.17 0.74 1.33 1.34 0.91
Al2O316.04 13.51 16.65 17.18 16.98 16.77 16.58 11.62 16.54 18.33 15.84
Fe2O32.18 4.46 1.63 1.61 1.71 1.28 1.51 10.21 10.79 10.31 7.89
MnO0.04 0.18 0.04 0.03 0.04 0.03 0.04 0.20 0.16 0.19 0.17
MgO0.57 2.34 0.29 0.26 0.15 0.14 0.29 12.27 6.21 4.67 5.71
CaO2.17 4.39 1.52 1.68 1.92 1.50 0.46 12.56 8.20 5.13 7.90
Na2O5.09 3.74 5.27 5.69 5.42 5.38 5.55 1.19 3.70 4.18 3.42
K2O3.23 3.58 3.59 3.20 3.26 3.42 3.77 0.82 1.27 1.84 2.37
P2O50.15 0.15 0.03 0.04 0.04 0.03 0.03 0.12 0.37 0.37 0.27
Total98.85 100.18 100.12 99.48 99.23 98.07 99.01 98.44 97.95 97.36 97.58
Trace elements (ppm)
V32.3 73.7 14.3 20.5 15.1 16.8 16.4 197.6 252.2 171.4 168.7
Cr0.6 4.6 5.3 2.9 1.1 1.7 1.0 674.6 138.4 22.0 64.2
Co4.4 14.1 4.2 4.8 3.3 3.1 2.6 47.3 59.6 51.8 39.2
Ni4.0 3.5 4.6 4.0 2.5 3.6 2.4 123.2 50.8 28.4 45.2
Cu3.6 7.0 0.1 1.8 0.9 1.5 1.5 32.9 23.3 46.3 43.3
Zn89.9 98.6 8.2 23.9 47.9 46.4 36.4 118.1 94.5 141.7 90.4
Rb49.7 94.3 178.4 96.3 48.5 84.3 60.1 20.9 41.2 55.4 87.7
Sr1084.6 340.5 120.5 224.3 709.5 681.8 564.1 430.3 740.5 793.7 734.7
Y11.4 22.4 23.1 28.8 13.9 14.5 14.0 14.8 18.3 17.5 18.1
Zr183.5 207.7 113.0 296.1 195.1 152.4 171.2 55.9 98.9 81.2 128.7
Nb0.7 3.3 3.3 6.3 0.9 1.6 0.3 0.5 0.8 3.4 1.3
Ba1088.2 879.7 590.0 835.9 1503.2 1636.3 1481.8 177.1 324.3 1073.9 312.7
Pb35.4 13.8 16.6 15.8 16.5 20.5 16.7 12.4 6.5 11.7 11.1
Th3.9 7.3 27.4 15.8 0.8 0.1 1.5 4.8 0.8 4.1 2.6
Rare-earth elements (ppm)
La 15.35 21.94 13.43 16.17 11.45 13.43 15.73 14.69
Ce 24.07 33.94 29.18 27.34 20.14 29.18 34.11 29.96
Pr 2.71 3.52 3.89 2.85 2.22 3.89 4.19 3.72
Nd 9.44 11.83 17.46 9.75 8.02 17.46 17.61 16.20
Sm 1.43 1.66 3.82 1.48 1.36 3.82 3.68 3.51
Eu 0.34 0.42 1.14 0.34 0.29 1.14 1.11 0.96
Gd 1.07 1.18 3.57 1.05 1.04 3.57 3.86 3.28
Tb 0.14 0.16 0.48 0.14 0.14 0.48 0.44 0.46
Dy 0.89 0.96 2.90 0.88 0.87 2.90 2.66 2.93
Ho 0.17 0.18 0.54 0.18 0.16 0.54 0.50 0.55
Er 0.51 0.55 1.51 0.51 0.46 1.51 1.45 1.60
Tm 0.08 0.08 0.21 0.08 0.06 0.21 0.20 0.22
Yb 0.62 0.64 1.39 0.60 0.55 1.39 1.35 1.58
Lu 0.090.090.180.090.07 0.180.180.22
ASI1.01 0.75 1.08 1.08 1.06 1.10 1.18 0.45 0.74 1.01 0.70
Mg#18.4 31.1 13.3 12.3 7.2 8.5 14.2 50.9 33.2 28.1 38.4
Sr/Y95.0 15.2 5.2 7.8 50.9 47.1 40.4 29.0 40.5 45.3 40.6
(Eu/Eu*)N 0.84 0.92 0.94 0.83 0.75 0.94 0.90 0.86
Total Fe as Fe2O3. Alumina saturation index (ASI): molar Al2O3/(Na2O + K2O + CaO). Mg#: Mg/(Mg + Fe). Eu*: (Sm × Gd)0.5. CI chondrite composition from Sun and McDonough (1989) [44] were used. Abbreviations for names of igneous bodies are given in Table 1.
Table 3. Sr isotopic compositions of the Hida granitoids.
Table 3. Sr isotopic compositions of the Hida granitoids.
AreaIgneous
Suite		Igneous
Bodies		Sample87Rb/86Sr87Sr/86SrSrI
UnazukiHida younger granitoidsYQDUNA20.1449 0.70485 0.70446
YHQDUNA40.1651 0.70493 0.70447
Hida older granitoidsFGUNA100.1892 0.70511 0.70447
UNA150.1770 0.70528 0.70468
UNA16c0.1325 0.70516 0.70471
OGUNA240.2018 0.70540 0.70469
UNA250.3451 0.70551 0.70455
KatakaigawaHida older granitoidsHGUNA200.2960 0.70740 0.70645
UNA210.2457 0.70717 0.70639
UNA290.1979 0.70700 0.70637
AGMUNA300.3575 0.70758 0.70633
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Figure 3. Variation diagrams of Hida granitoids. (a) K2O vs. SiO2. Shoshonite, high-K, medium-K, and low-K fields are after Peccerillo and Taylor (1976) [45], (b) ASI vs. SiO2. Metaluminous, and peraluminous fields are after Shand (1943) [46], (c) Sr/Y vs. Y as discrimination [43] of adakitic rocks, (d) (Eu/Eu*)N vs. SiO2 of the 11 adakitic rock samples and three non-adakitic rocks (UNA20, 21, and 23b) analyzed for REE. Normalized values of CI chondrite are after Sun and McDonough (1989) [44].
Figure 3. Variation diagrams of Hida granitoids. (a) K2O vs. SiO2. Shoshonite, high-K, medium-K, and low-K fields are after Peccerillo and Taylor (1976) [45], (b) ASI vs. SiO2. Metaluminous, and peraluminous fields are after Shand (1943) [46], (c) Sr/Y vs. Y as discrimination [43] of adakitic rocks, (d) (Eu/Eu*)N vs. SiO2 of the 11 adakitic rock samples and three non-adakitic rocks (UNA20, 21, and 23b) analyzed for REE. Normalized values of CI chondrite are after Sun and McDonough (1989) [44].
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In Figure 4, variation diagrams depict the Ba, Cr and Ni contents of the 13 adakitic rock samples. There are six samples of the older granitoids with Ba > 1400 in this diagram. Furthermore, two samples of the younger granitoid samples display high concentrations of Cr (>170 ppm) and Ni (>40 ppm). Based on these characteristics, two distinct types of adakitic rocks are identified: (1) high Ba contents in younger and older granitoid samples and (2) high Cr and Ni contents in younger samples.
The chondrite-normalized REE patterns of the 14 samples of Hida granitoids analyzed for REE are shown in Figure 5. All samples show depletion in heavy rare earth elements. Two of the three younger granitoid samples analyzed for REE fall in the high HREE category together with five older granitoid samples, while one young sample falls into the low HREE category together with six older granitoid samples.
Most of the analyzed samples show weak negative Eu anomalies on the variation diagram of (Eu/Eu*)N vs. SiO2, with no differences between older granitoids and younger granitoids, but one older granitoid sample shows a significant positive Eu anomaly of 2.05 (Figure 3d).

4.2. Rb-Sr Isotope Analysis

SrI of all analyzed samples exceed 0.7040. In the Unazuki area, SrI ranges from 0.70446 to 0.70471, with both the younger and older granitoids exhibiting similar values within this range. In contrast, the older granitoids from Katakaigawa area display significantly higher SrI, ranging from 0.70633 to 0.70645.

5. Discussion

Arakawa and Shinmura (1995) [14] classified the Hida granitoids into two groups based on SrI: Type I plutons with low SrI (0.7044–0.7054), and Type II plutons with higher SrI (0.7055–0.7105). While the genesis of Type I plutons was not discussed in their study, Type II plutons were interpreted to have formed through mixing of material from the gray granites. The results of the present study show that the older granitoids from the Katakaigawa area (SrI = 0.70633–0.70645) fall within the range of Type II, whereas both the older (SrI = 0.70447–0.70471) and younger granitoids (SrI = 0.70446–0.70447) from the Unazuki area plot within the Type I field (Figure 6a). According to Sr-Nd isotopic data from Arakawa and Shinmura (1995) [14], Type II plutons exhibit isotopic variation extending to the isotopic range of the gray granites (Figure 6b), without evidence of localized isotopic modification due to post-solidification alteration. The Hida granitoids analyzed in this study similarly exhibit Sr isotopic characteristics consistent with those reported by Arakawa and Shinmura (1995) [14], supporting the interpretation that their isotopic compositions reflect pre-solidification magmatic processes within the crust rather than secondary alteration. The older granitoids from the Katakaigawa area show compositional ranges similar to Hida gneisses (SrI = 0.70588–0.72006) and gray granites (SrI = 0.70954–0.71273), suggesting, as noted in previous studies, that these granitoids may have assimilated crustal materials during magma evolution. In contrast, the older granitoids from the Unazuki area exhibit low SrI independent of SiO2 content (Figure 6a), indicating minimal assimilation of crustal components during magma genesis. Furthermore, the classification of the older granitoids in the Unazuki area as Type I contradicts the geochronological data-based model proposed by Takahashi et al. (2010) [15], which associates Type I with younger granitoids and Type II with older granitoids. Given the absence of exposed gray granites near the Unazuki region and their presence in the southwestern part of the Katakaigawa area (Figure 1b), it is plausible that the magmatic processes of the Hida granitoids were controlled more by regional and stratigraphic variability in the crustal composition at the time of magma emplacement, rather than by temporal factors alone.
Adakitic rocks identified in this study were observed in all analyzed plutonic bodies. These rocks occur consistently from early to late crystallization stages in both the Hida older and younger granitoids (Figure 7a), suggesting that adakitic magma generation did not occur as a widespread event during pluton formation. In addition, the observed depletion of HREEs in these granitoids suggests the presence of residual phases containing minerals with high partition coefficients, such as garnet and amphibole, during partial melting of the source material. Non-adakitic rocks show a decreasing trend in Sr/Y ratios with increasing SiO2 (Figure 7b), indicative of plagioclase fractionation within individual magma chambers. This trend is absent in adakitic rocks (Figure 7b). Based on their geochemical characteristics, the adakitic rocks in this area can be further divided into two subtypes: those in the younger granitoids are characterized by high Cr and Ni concentrations in low-SiO2 samples (Figure 4b,c), whereas those in the older granitoids are distinguished by elevated Ba contents (Figure 4a). Those found in the younger granitoids exhibit high Cr and Ni contents. Typical adakites are characterized by MgO < 3 wt%, Cr = 5–14 ppm, and Ni = 2–9 ppm [43], which is inconsistent with the characteristics of the adakitic rocks in the younger granitoids of this study. Instead, their geochemical features suggest a magma process involving mantle-derived material. However, their whole-rock Mg# values are <40, significantly lower than the equilibrium range for mantle-derived melts (Mg# < 64), ruling out direct partial melting of the mantle as the source. This chemical composition and the relatively low SrI (~0.7045) indicate that these adakitic rocks were generated from hydrous felsic magmas derived from the partial melting of subducted oceanic crust. These ascending magmas provided heat and water to the mantle material, leading to partial melting and subsequent magma mixing. The geochemical characteristics and formation mechanisms of these rocks align with those of volcanic rocks distributed east of Wajima on the Noto Peninsula [22] and volcanic rocks in the Miocene Iwane Formation of southern Toyama Prefecture [47]. In contrast, adakitic rocks in the older granitoids are often characterized by high Ba content. Given that LIL elements such as Ba are typically enriched in the melt during magmatic differentiation, an increase in Ba concentration in granitoid samples with high SiO2 content can be anticipated to a certain extent. However, Ba concentrations exceeding 1400 ppm cannot be explained solely by fractional crystallization. Among the mineral phases in granitic rocks, the partition coefficient of Ba between alkali feldspar and melt is significantly higher than that between plagioclase and melt or amphibole and melt [48,49]. Thus, the high Ba content in the older granitoid samples is attributed to the abundance of alkali feldspar. This Ba enrichment, coupled with a strong positive Eu anomaly in one of the older granitoid samples, suggests that the adakitic magmas in the older granitoids interacted with alkali-rich melts or fluids during their ascent from the partially melted mafic lower crust.

6. Conclusions

  • This study revealed the geochemical characteristics of the Hida granitoids in the Unazuki and Katakaigawa areas. Trace element data identified 13 adakitic rocks among 35 samples. These were found in both older and younger granitoids, suggesting adakitic features are not time-restricted.
  • SrI distinguished regional differences: Katakaigawa older granitoids match Type II signatures, implying crustal assimilation, while both older and younger granitoids in Unazuki show low SrI, fitting Type I characteristics. These results suggest crustal composition, rather than age, played a key role in magma evolution.
  • Adakitic rocks fall into two subtypes: high Cr–Ni types in younger granitoids indicate interaction with mantle material, while Ba-rich types in older granitoids suggest alkali-rich melt involvement. These differences imply varied magma genesis and ascent processes.

Author Contributions

Investigation, K.O., R.K., K.S. and M.T.; Discussion, K.O., R.K., K.S. and M.T.; Project administration, K.S. and M.T.; Supervision, K.S. and M.T.; Writing—original draft, K.O.; Writing—review and editing, K.S. and M.T. All authors have read and agreed to the published version of the manuscript.

Funding

This research was funded by JSPS KAKENHI, grant number JP 23K04797 to M.T.

Data Availability Statement

Data are available on request.

Conflicts of Interest

The authors declare no conflicts of interest.

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Figure 2. Selected major oxide and trace element variation diagrams relative to SiO2 for the Hida granitoids.
Figure 2. Selected major oxide and trace element variation diagrams relative to SiO2 for the Hida granitoids.
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Figure 4. Selected trace element variation diagrams of adakitic rocks of the Hida granitoids. (a) Ba vs. SiO2. (b) Cr vs. SiO2. (c) Ni vs. SiO2. The symbols are the same as in Figure 2.
Figure 4. Selected trace element variation diagrams of adakitic rocks of the Hida granitoids. (a) Ba vs. SiO2. (b) Cr vs. SiO2. (c) Ni vs. SiO2. The symbols are the same as in Figure 2.
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Figure 5. CI Chondrite [44]-normalized REE patterns of the Hida granitoids.
Figure 5. CI Chondrite [44]-normalized REE patterns of the Hida granitoids.
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Figure 6. (a) SrI vs. SiO2 diagram. The range of SrI values for Hida gneisses and gray granites indicated by arrows and the classification boundaries are after Arakawa and Shinmura (1995) [14]. (b) εNd vs. εSr diagram. The epsilon values of Sr in this study are shown at the top of the figure. The symbols are the same as in (a). The composition range of gray granites is based on Arakawa and Shinmura (1995) [14].
Figure 6. (a) SrI vs. SiO2 diagram. The range of SrI values for Hida gneisses and gray granites indicated by arrows and the classification boundaries are after Arakawa and Shinmura (1995) [14]. (b) εNd vs. εSr diagram. The epsilon values of Sr in this study are shown at the top of the figure. The symbols are the same as in (a). The composition range of gray granites is based on Arakawa and Shinmura (1995) [14].
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Figure 7. Variation diagrams of Hida granitoids containing adakitic rocks. (a) Sr/Y vs. SiO2. (b) Zircon U-Pb age vs. SiO2. See Table 1 for the U-Pb data referenced. The symbol colors are the same as in Figure 2.
Figure 7. Variation diagrams of Hida granitoids containing adakitic rocks. (a) Sr/Y vs. SiO2. (b) Zircon U-Pb age vs. SiO2. See Table 1 for the U-Pb data referenced. The symbol colors are the same as in Figure 2.
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Table 1. Summary of petrographic features and zircon U-Pb age of plutonic rocks from the Unazuki and Katakaigawa areas.
Table 1. Summary of petrographic features and zircon U-Pb age of plutonic rocks from the Unazuki and Katakaigawa areas.
Igneous BodiesRock TypeZircon U-Pb Age (Ma)
Hida younger Kekachidake granite (KG)Biotite granite to quartz diorite192.0 ± 2.4 a
granitoidsYatazodani quartz diorite (YQD)Quartz diorite191.1 ± 0.3 b
Yatazodani hornblende-quartz diorite (YHQD)Hornblende quartz diorite195.6 ± 2.0 a
Hida older Unazuki granite (UG)Biotite granite, slightly mylonaitized 236.5 ± 3.1 a
granitoidsFunakawa granite (FG)Biotite granite, slightly mylonaitized240.7 ± 4.1 a
Hayatsukigawa granite (HG)Biotite granite to granodiorite224.8 ± 1.7 a
Augen granite mylonite (AGM)Granitic mylonite245 ± 2 c
Otodani gabbro (OG)Hornblende gabbro, slightly mylonaitized 247.7 ± 3.7 a
a Takeuchi et al. (2021) [31], b Horie et al. (2013) [37], c Zhao et al. (2013) [35].
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Oishi, K.; Kuwahara, R.; Shimooka, K.; Tsuboi, M. Geochemical Characteristics of the Hida Granitoids in the Unazuki and Katakaigawa Areas, Central Japan. Geosciences 2025, 15, 285. https://doi.org/10.3390/geosciences15080285

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Oishi K, Kuwahara R, Shimooka K, Tsuboi M. Geochemical Characteristics of the Hida Granitoids in the Unazuki and Katakaigawa Areas, Central Japan. Geosciences. 2025; 15(8):285. https://doi.org/10.3390/geosciences15080285

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Oishi, Kazuki, Rui Kuwahara, Kazuya Shimooka, and Motohiro Tsuboi. 2025. "Geochemical Characteristics of the Hida Granitoids in the Unazuki and Katakaigawa Areas, Central Japan" Geosciences 15, no. 8: 285. https://doi.org/10.3390/geosciences15080285

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Oishi, K., Kuwahara, R., Shimooka, K., & Tsuboi, M. (2025). Geochemical Characteristics of the Hida Granitoids in the Unazuki and Katakaigawa Areas, Central Japan. Geosciences, 15(8), 285. https://doi.org/10.3390/geosciences15080285

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