Figure
1.
Simplified regional geological map of the Emeishan large igneous province (modified from Shellnutt and Pham, 2018). Sample locations are identified.
| Citation: | Dong Yi, Jing Zhao, Chunhui Li, Xiuhong Peng. Crustal Contaminations Responsible for the Petrogenesis of Basalts from the Emeishan Large Igneous Province, NW China: New Evidence from Ba Isotopes. Journal of Earth Science, 2022, 33(1): 109-120. doi: 10.1007/s12583-021-1513-0
|
Emeishan large igneous province (ELIP) is widely distributed in three provinces of Sichuan, Yunnan, and Guizhou in southwestern China, with its erupted area exceeding 2.5 × 105 km2 (Fig. 1, Chung and Jahn, 1995). In the ELIP, the continental flood basalts are the dominant volcanic rocks, even though a few picrites, rhyolites, basaltic andesites and pyroclastics are locally exposed. In the past decades, involving geochemistry, isotopic compositions (e.g., Sr-Nd-Pb-Os-Lu-O-Mg) and zircon U-Pb dating of these basalts, have been reported (Fu et al., 2021; Ji et al., 2021; Tian et al., 2017; Zhong et al., 2014; Lai et al., 2012; Shellnutt and Jahn, 2011; Yan et al., 2010; Fan et al., 2008; Li et al., 2008; Qi et al., 2008; Xu Y G et al., 2008, 2001; Xu J F et al., 2007; Zhou et al., 2006, 2002; Xiao et al., 2004; Song et al., 2001). Xu et al. (2001) and He et al. (2010) divided the basalts from the ELIP into high-Ti and low-Ti basalts in terms of their bulk TiO2 contents, Ti/Y ratios and a linear relationship (TiO2 = -0.08MgO + 2.91). Except for Ti, both of them also display distinct geochemical and Sr-Nd-Pb isotopic compositions. For instance, the high-Ti basalts have lower Mg#, (87Sr/86Sr)i, CaO, MgO, and higher Sm/Yb ratios, εNd(t), and Total FeO, K2O, Na2O contents relative to those in low-Ti basalts (Liu et al., 2020; Tian et al., 2017; Jiang et al., 2009; Xiao et al., 2004; Song et al., 2001; Xu et al., 2001). These compositional variations suggest that they might be affected by different magmatic processes. Xu et al. (2001) proposed that the geochemical heterogeneity in both low-Ti and high-Ti basalts might be derived from the same mantle plume, possibly accompanied by variable extents of contamination. Xu et al. (2007) further advocated that some subcontinental lithospheric mantle (SCLM) materials have greatly contributed to the formation of the high-Ti basalts during the magma ascent. In a study of the basalts from the Panzhihua area, partial melting and crustal contamination appeared to be two major processes that controlled the compositional diversity of the high-Ti and low-Ti basaltic magmas (Shellnutt and Jahn, 2011). Nevertheless, Lai et al. (2012) believed that the basalts with high Ti/Y ratios from the Yunnan and Guizhou provinces probably originated from the SCLM of the Yangtze Block with minor contamination of crustal materials or metasomatic veins of the lithosphere heated by the plume. Recently, Li et al. (2016) also claimed that crustal contamination exerted a limited effect on the genesis of the Permian basalts in the Sichuan Province on the basis of their geochemical and Sr-Nd isotopic features. Therefore, the role of crustal contamination, needs to be re-appraised in order to promote a better understanding of the genesis of the ELIP.
As an incompatible element, Ba is readily incorporated into magma during the partial melting of the mantle. Compared to the mantle, crustal rocks are usually abundant in Ba. The average Ba content in the primitive mantle (PM) is about 6.9 ppm (Palme and O'Neill, 2014; McDonough and Sun, 1995), which is obviously lower than that in continental crusts. The latter is as high as 456 ppm, as reported by Rudnick and Gao (2014). Furthermore, it is generally believed that both low-temperature (e.g., mineral precipitation and adsorption) and high-temperature (e.g., crystal-melt separation) processes can lead to Ba isotopic fractionation (Deng et al., 2021; Gou et al., 2020; Gong et al., 2019; Böttcher et al., 2012; von Allmen et al., 2010). The δ138/134Ba values in the PM are homogeneous; however, crustal materials have a wide range from -0.63‰ to 0.47‰ (An et al., 2020; Li et al., 2020; Nan et al., 2018; Nielsen et al., 2018). Accordingly, the Ba isotopic system is expected to be a sensitive tracer of crust recycling and crust-mantle interactions (Li et al., 2020). Furthermore, Nielsen et al. (2018) reported that the Ba isotopic discrepancy in global mid-ocean ridge basalts (MORB) could probably be attributed to the variable input of sedimentary materials into the mantle, making it a reliable tool for tracking the genesis of basaltic rocks.
In this study, based on the whole-rock geochemical compositions, we present new Ba isotopic evidence of the low-Ti and high-Ti continental flood basalts from the Lijiang, Miyi and Emeishan regions in order to discuss their petrogenesis. This study further provides isotopic constraints on the role of crustal contamination in the magmatic evolution of basaltic melts from the mantle.
The ELIP is extensively distributed along the western margin of the Yangtze Block, SW China, with significant variations in the thickness of volcanic sequences (several hundred meters in the east and nearly 5 km in the west) (Xiao et al., 2004; Song et al., 2001; Xu et al., 2001; Chung and Jahn, 1995). The detailed geology of the ELIP has been described in previous studies (Xu et al., 2013, 2004, 2001; Ali et al., 2010, 2005; Fan et al., 2008; Wang et al., 2007; He at al., 2006, 2003; Song et al., 2006; Zhang et al., 2006, 2004; Zhou et al., 2006). Here, we offer a brief description as follows: the ELIP comprises abundant continental flood basalts, minor picrites, basaltic andesites, rhyolites, trachytes, as well as associated mafic-ultramafic and syenitic intrusions (Fig. 1, Xu et al., 2001; Chung and Jahn, 1995). The continental flood basalts are exposed in a large area of over 2.5 × 105 km2 (Fig. 1, Chung and Jahn, 1995). The mineral assemblage includes plagioclase, clinopyroxene, olivine, basaltic glass, and minor amounts of magnetite, and ilmenite. In particular, the aphyric, porphyritic, and amygdaloidal basalts dominate in the ELIP (Fu et al., 2021; Tian et al., 2017; Jiang et al., 2007; Wang et al., 2007; Xu et al., 2001). According to their bulk TiO2 contents and Ti/Y ratios, the continental flood basalts from the ELIP can be classified into two groups: high-Ti basalts (TiO2 > 2.5, Ti/Y > 500) and low-Ti basalts (TiO2 < 2.5, Ti/Y < 500). These two groups show distinct petrologic and geochemical characteristics (Tian et al., 2017; You and Liu, 2014; Xu Y G et al., 2013, 2001; Xu J F et al., 2007). The low-Ti basalts contain more clinopyroxenes and less magnetites, whereas the high-Ti basalts are dominated by plagioclases with minor amounts of clinopyroxene phenocrysts; the high-Ti basalts have lower Mg# (0.32-0.61) and (87Sr/86Sr)i (0.704 9-0.706 4), but higher Sm/Yb ratio, εNd(t) (-0.71-1.5) and γOS(t) (-1.4- -0.8) compared to the low-Ti basalts (Mg# = 0.52-0.64, (87Sr/86Sr)i = 0.706 3-0.707 8, εNd(t) = (-6.74- -0.3), γOS(t) = 6.5). Regarding spatial distribution, the inner zone, comprises low-Ti and high-Ti basalts, however, the outer zone, is merely confined to high-Ti basalts (Tian et al., 2017). As shown above, the geology, geophysics, stratigraphy, sedimentology, petrology, geochemistry and Sr-Nb-Pb isotope signatures of the ELIP supported that a mantle plume potentially made a great contribution to the generation of the Emeishan volcanism (He et al., 2006, 2003; Zhang et al., 2006, 2004; Xu et al., 2004, 2001).
Eighteen continental flood basaltswere collected from Lijiang, Miyi and Emeishan in the ELIP for detailed analyses (Fig. 1). Based on petrographic observations, the basalts mainly comprised plagioclases, clinopyroxenes, olivines and a few opaque minerals (e.g., magnetite). Most of the basaltic samples are relatively fresh with a little secondary alteration. In terms of their bulk TiO2 contents and Ti/Y ratios, high-Ti basalts were only observed in Miyi and Emeishan, whereas low-Ti basalts dominantly distributed in Lijiang (Section 3.1). The basalts are mostly cryptocrystalline, and some high-Ti samples typically exhibit porphyritic textures in the presence of plagioclase phenocrysts (Fig. 2).
The whole-rock major oxides (e.g., MgO, SiO2, TiO2, Al2O3, K2O, etc.) of the studied basalts (wt.%) were measured by gravimetry (wet chemistry) and X-ray fluorescence (XRF) at University of Science and Technology of China, Hefei (USTC). The concentrations of trace elements (including rare earth elements, REE) were analyzed by inductively coupled plasma mass spectrometer (ICP-MS) at Key Laboratory of Crust-Mantle Materials and Environments, Chinese Academy of Sciences (CAS), Hefei. Two standard materials (BCR-2 and BHVO-2) were used for quality monitoring. The uncertainties are better than 1.0% for major elements and 5.0% for trace elements.
Barium isotopic compositions of the basalts were performed at CAS Key Laboratory of Crust-Mantle Materials and Environments, University of Science and Technology of China. More details about the procedure of sample digestion, chemical separation and purification have been already published by Nan et al.(2018, 2015) and An et al. (2020). During dissolution and purification processes, the basalt powders were dissolved in double-distilled high purity acids (HF, HNO3 and HCl) in Teflon screw-top beakers with 18.2 MΩ/cm ultra-pure water. After that, barium was purified from the matrix by cation exchange column with AG50W-X12 resin (200-400 mesh, Bio-Rad, USA). The twice purification process is performed twice, firstly using a column with 2 mL resin followed by the second column with a 0.5 mL resin. The 3 mol/L HCl was utilized to elute matrix elements, and then 3 mol/L HNO3 was added to collect barium. The procedural blank was 4.2 ng, which is negligible (< 1‰) compared with the amount of Ba analyzed from the samples (1-5 μg).
Barium isotopic compositions were conducted using a Neptune Plus multi-collector inductively coupled plasma mass spectrometer (MC-ICP-MS). 135Ba-136Ba double-spike method with anoptimal ratio of 1.72 (m/m; Rudge et al., 2009) was utilized to correct for instrumental mass discrimination. Signals of 131Xe, 134Ba, 135Ba, 136Ba, 137Ba, and 140Ce were collected simultaneously by L4, L2, L1, C, H1, and H3 Faraday cups, respectively. The background signals of 137Ba (< 0.005 V) were negligible relative to the sample signals (approximately 7 V). Relative to NIST Standard Reference Material (SRM) 3104a, Ba isotopic composition is defined as
|
δ138/134Ba=[(138Ba/134Ba)sample /(138Ba/134Ba)sRM3104a −1]×1000 |
For comparison, all published δ137/134Ba values have been recalculated to δ138/134Ba values by multiplying the measured δ137/134Ba by a factor of 1.33 (Pretet et al., 2015). The three-isotope plot is shown in Fig. 3. The average δ138/134Ba values of reference materials (BCR-2 and BHVO-2) in this study are consistent with the uncertainty reported in previous studies (Table 1, An et al., 2020; Li et al., 2020; Bullen and Chadwich, 2016; Nan et al., 2015).
| Standard | Description | δ138/134Ba (‰) | 2SD | References |
| BCR-2 | Basalt, Columbia River, USA | 0.05 | 0.04 | Li et al. (2020) |
| 0.06 | 0.04 | An et al. (2020) | ||
| 0.06 | 0.03 | Nan et al. (2015) | ||
| 0.07 | 0.02 | This study | ||
| BHVO-2 | Basalt, Hawaii, USA | 0.06 | 0.03 | Nan et al. (2015) |
| 0.06 | 0.03 | Bullen and Chadwich (2016) | ||
| 0.05 | 0.03 | This study |
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Except for only one sample (EM001-1), most of the studied basalts have relatively low LOI (loss on ignition) contents varying from 1.42 wt.% to 3.67 wt.%. According to the bulk TiO2 contents and Ti/Y ratios (Xiao et al., 2004; Xu et al., 2001, Fig. 4), basalts from the Lijiang region had low TiO2 contents (1.24-1.85) with Ti/Y ratios of 269-429, whereas the Miyi and Emeishan basalts had higher TiO2contents and Ti/Y ratios (TiO2 = 3.33-4.87, Ti/Y = 519-897). Moreover, the high-Ti basalts display larger compositional variations of SiO2 (42.64 wt.%-54.00 wt.%) and MgO (3.73 wt.%-7.49 wt.%), relative to low-Ti basalts (SiO2 = 49.55 wt.%-51.92 wt.%, MgO = 4.60 wt.%-6.12 wt.%, Fig. 5). The former does not show any linear correlations between MgO and other major oxides (e.g., Na2O, SiO2, TiO2, total Fe2O3, Fig. 5, Table S1).
As shown in the primitive mantle-normalized spider diagrams (Figs. 6a-6b), the basalts generally show negative Nb and Sr anomalies, even though they are variably enriched in Ta with respect to neighboring elements. The high-Ti samples contain high Sm/Yb ratios (3.62-4.98) and Nb/U (20.23-31.32) ratios (Figs. 4b and 7a). Furthermore, almost all samples have LREE-enriched chondrite-normalized REE patterns comparable to the average ocean-island basalts (OIB) with obviously negative Eu anomalies (Figs. 6c-6d). In addition, the high-Ti basalts contain higher total REE contents (∑REE = 222 ppm -420 ppm) and stronger LREE/HREE differentiation ((La/Yb)N = 8.5-17.9) than that of the low-Ti basalts (∑REE = 112 ppm -202 ppm, (La/Yb)N = 4.4-8.2). Both high-Ti and low-Ti basalts were commonly enriched in large ion lithophile elements (LILEs, e.g., Ba, Th and U).
Generally, the δ138/134Ba values of the basalts are highly heterogeneous, ranging from -0.38‰ to 0.38‰ with a mean of 0.026‰ ± 0.38‰ (2SD, n = 16, Table 2). The two samples had the lowest δ138/134Ba values of -0.38‰ and -0.33‰, respectively. As for the low-Ti basalts, their δ138/134Ba values vary from -0.33‰ to +0.23‰ with an average of -0.02‰ ± 0.40‰ (2SD, n = 4). The high-Ti samples show a similar range of Ba isotopic compositions from -0.38‰ to +0.38‰ with their average value of 0.038‰ ± 0.36‰.
| Locality | Types | Sample | Ba (ppm) | δ137/134Ba (‰) | 2SD | δ138/134Ba (‰) | 2SD |
| Lijiang | Low-Ti | WKB7 | 711 | 0.02 | 0.05 | 0.01 | 0.04 |
| WKB9 | 396 | 0.19 | 0.00 | 0.23 | 0.02 | ||
| PCB1 | 384 | -0.26 | 0.01 | -0.33 | 0.01 | ||
| PCB2 | 170 | -0.03 | 0.03 | -0.04 | 0.02 | ||
| Replicate | -0.03 | 0.03 | -0.03 | 0.03 | |||
| Miyi | High-Ti | MY1 | 402 | 0.29 | 0.00 | 0.38 | 0.01 |
| MY2 | 1 028 | -0.28 | 0.02 | -0.38 | 0.03 | ||
| MY4 | 619 | 0.09 | 0.00 | 0.13 | 0.02 | ||
| MY5 | 468 | 0.14 | 0.01 | 0.18 | 0.03 | ||
| MY6 | 527 | 0.05 | 0.02 | 0.06 | 0.03 | ||
| MY7 | 365 | 0.19 | 0.00 | 0.26 | 0.04 | ||
| Emeishan | High-Ti | EM001-1 | 272 | 0.03 | 0.04 | 0.04 | 0.05 |
| EM001-2 | 250 | 0.03 | 0.00 | 0.04 | 0.01 | ||
| EM002-1 | 523 | 0.08 | 0.02 | 0.11 | 0.01 | ||
| EM002-2 | 564 | 0.05 | 0.02 | 0.07 | 0.05 | ||
| EM002-3 | 495 | 0.15 | 0.01 | 0.19 | 0.01 | ||
| EM004-2 | 517 | 0.01 | 0.02 | 0.01 | 0.02 | ||
| EMSB001 | 479 | -0.02 | 0.01 | -0.03 | 0.01 |
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The geochemical and isotopic compositions of basalts can be strongly influenced by partial melting, fractional crystallization, weathering alterations and crustal contaminations (Gong et al., 2019; You and Liu, 2014; Zhu et al., 2013; Hou et al., 2011; Jiang et al., 2007; Xu et al., 2007). In this study, the Ba isotopic compositions of the flood basalts were highly heterogeneous (-0.38‰ to 0.38‰, Figs. 8 and 9), indicating that petrogenesis is more complex than previous thoughts.
Except for only one sample (EM001-1), all analyzed basalts contain relatively low LOI contents (1.42 wt.%-3.67 wt.%), reflecting that weathering alterations pose a limited impact on their geochemical components. Sample EM001-1 has the highest LOI (7.13 wt.%) and median δ138/134Ba value (0.038‰). Because of its highly fluid-mobile ability, barium preferentially enters into low-temperature fluids during weathering processes, such as serpentinization. However, it is uncertain that whether the weathering process could cause Ba isotopic fractionation within basalts. Thus, the sample EM001-1 is not considered in the following discussion.
Owing to a highly incompatible coefficient (Dsolid/melt) of 0.000 12 during mantle melting (Workman and Hart, 2005), a large proportion of Ba (99%) is preferentially incorporated into melts despite 1% partial melting (Nan et al., 2018; Nielsen et al., 2018). Xu et al. (2001) proposed that the high-Ti basalts were formed via a partial melting of 1.5% within the garnet stability field, whereas the low-Ti magmas were generated by a greater extent of melting (16%). Accordingly, almost all Ba were separated from the mantle and entered into the basaltic magmas after partial melting. Therefore, this process, does not result in significant Ba isotopic fractionation, i.e., the δ138/134Ba values of the primitive basaltic melts were likely dependent on those in the mantle source.
Previous studies have demonstrated that the high-Ti and low-Ti basalts underwent fractional crystallization during basaltic magma ascent, supporting the abundance of plagioclase or clinopyroxene phenocrysts as well as other geochemical fingerprints (Cheng et al., 2019; Yang et al., 2018; Tian et al., 2017; Song et al., 2008; Hao et al., 2004). The continental flood basalts, especially high-Ti samples, are no exception. The high-Ti basalts contain numerous plagioclase phenocrysts (Fig. 2), supporting the possibility that they might have experienced significant fractionation of plagioclases. The negative Eu and Sr anomalies are also considered to be a consequence of plagioclase fractional crystallization (Fig. 6, Huang et al., 2014). Even so, the geochemical proxies of fractional crystallization (e.g., solidification index, SI = 100 × MgO/(MgO + FeO + Fe2O3 + Na2O + K2O), Liu et al., 2020 and references therein) did not coincide with the measured δ138/134Ba values (Fig. 10a), suggesting that the variations in Ba isotopic compositions of the basalts are independent of plagioclase fractionation crystallization due to an elevated degree of fractionation corresponding to a decreased SI value (Liu et al., 2020, and references therein). Similarly, the lack of linear correlations between SI and Eu or Sr further provides additional evidence for this possibility (Fig. 10b).
The high-Ti and low-Ti basalts collected from the Emei-shan, Miyi and Lijiang regions have wider ranges of δ138/134Ba values (-0.38‰- +0.38‰) relative to the typical ones of the typical ocean island basalts (-0.11‰- +0.20‰, Nan, 2017) and PM (0.05‰ ± 0.06‰, Li et al., 2020, Fig. 8). In view of a fact that Ba isotope is indeed homogeneous in the upper mantle (Li et al., 2020), such isotopic diversity suggests probable contamination of some crustal materials either in magmatic sources through lithosphere-plume interactions (e.g., He et al., 2010; Fan et al., 2008), or during the basaltic magmas en route to the surface. If the contamination process took place in their magmatic chambers via crust-mantle interaction, both the high-Ti and low-Ti basalts possibly originated from the same sources because of their similar δ138/134Ba values. This possibility can be ruled out owing to their distinct Ce/Y, Sm/Y (Fig. 11b), Th/Nb as well as Zr/Nb ratios (e.g., Li et al., 2016). Also, Gd/Yb ratio can be utilized to estimate the depth of partial melting (e.g., He et al., 2010). The Gd/Yb ratios of the high-Ti basalts (3.57-4.94) are obviously greater than the low-Ti basalts (2.06-2.33), reflecting a larger melting depth of the high-Ti basalts. In addition, two different mantle sources responsible for these two types of basalts have been well demonstrated in previous studies (e.g., Xu J F et al., 2007; Yan et al., 2007; Xu Y G et al., 2001; Xiao et al., 2004).
The ratios of incompatible elements of basalts, such as Nb/U, Th/Ta, Nb/La, Th/Nb, Ce/Y, and Sm/Y, is indicative of crustal contamination (e.g., Fu et al., 2021; Liang et al., 2021; Tan et al., 2019; Li H B et al., 2017; Lai et al., 2012; Li C S et al., 2012; Zi et al., 2011; He et al., 2010; Jiang et al., 2009, 2007), in that these ratios are not easily affected by fractional crystallization (Song et al., 2006). In practice, crustal contamination commonly results in low Nb/La, Nb/U and high Th/Ta, Th/Nb, Th/Yb (e.g., Fu et al., 2021; Li et al., 2017; Qi and Zhou, 2008; Wang et al., 2007; Song et al., 2006). The studied basalts exhibit a similar compositional feature (Table 3), which proves crustal contamination played a significant role in the petrogenesis of the basalts. Another evidence comes from the (Th/Yb)PM versus (Nb/Th)PM diagram (Fig. 11c), in which all samples are plotted along the trend line of crustal contamination. Crustal contamination also accounts for the negative Nb anomalies shown in the PM-normalized spider diagrams of trace elements (Figs. 6a-6b) and Ba isotopic deviation from the PM (Fig. 9). What is peculiar to note that their Th/Nb (0.13-0.60), Nb/La (0.56-1.29), Nb/U (6.58-31.32), La/Sm (3.09-5.21) and Th/Yb (1.10-5.76) ratios are between those of PM (McDonough and Sun, 1995) and continental crust (Rudnick and Gao, 2014, Table 3). This strongly indicates that the overlying continental crusts might be the most potential source of contamination materials. More importantly, these low-Ti basalts have lower Nb/U, Sm/Y, Nb/Y ratios as well as Nb and Ta abundances with respect to the high-Ti basalts (Fig. 11). Thus, the low-Ti basalts had undergone higher degrees of crustal contamination. Figure 7 further illustrates that the basalts containing more amounts of contaminated materials (e.g., low-Ti basalts) seem to display a nearly linear correlation between their δ138/134Ba values and geochemical proxies of crustal contamination (e.g., Th/Ta, Th/Yb, Nb/U and Th/Nb).
| Magma types | High-Ti basalts | Low-Ti basalts | PMc | OIBd | UCCe | ||||
| Ranges | Rangesa | Rangesb | Ranges | Rangesa | Rangesb | ||||
| Ti/Y | 519-897 | 449-979 | 528-682 | 351-531 | 149-531 | 269-430 | 813 | 593 | 182 |
| Nb/La | 0.76-1.06 | 0.78-1.16 | 0.62-1.07 | 0.56-1.29 | 0.81-0.99 | 0.61-1.81 | 1.04 | 1.30 | 0.39 |
| Th/Yb | 1.84-3.75 | 0.11-0.15 | 0.31-3.22 | 1.10-2.95 | 1.35-1.52 | 0.45-2.88 | 0.17 | 1.85 | 5.36 |
| Nb/U | 20.23-31.32 | 28.75-38.00 | 20.67-46 | 6.58-21.96 | 19.8-23.3 | 8.00-50.00 | 33.95 | 47.05 | 4.44 |
| Th/Nb | 0.13-0.21 | 0.11-0.15 | 0.07-0.24 | 0.14-0.60 | 0.17-0.18 | 0.06-0.4 | 0.12 | 0.08 | 0.88 |
| La/Sm | 3.09-5.00 | 2.78-4.55 | 3.32-4.72 | 3.35-5.21 | 3.28-4.04 | 2.43-4.23 | 1.55 | 3.70 | 6.60 |
| Th/Ta | 1.10-2.84 | 1.56-2.07 | 1.23-3.35 | 1.73-5.76 | 2.41-2.55 | 1.67-6.55 | 2.07 | 1.48 | 11.67 |
| a Data from He et al. (2010); b data from Xu et al. (2001); c PM. primitive mantle; d OIB. ocean-island basalts, OIB and PM data are from McDonough and Sun (1995); e UCC. upper continental crust, the upper continental crust data are from Rudnick and Gao (2014). | |||||||||
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In conclusion, crustal contamination is the most likely interpretation for the Ba isotopic variation in basalts, rather than partial melting, fractional crystallization and weathering alteration.
It is generally believed that the mantle plume-derived melts played a decisive role in the genesis of the ELIP during the Late Permian-Early Triassic (Fu et al., 2021; Liu et al., 2020; Shellnutt and Pham, 2018; Li H B et al., 2016; Deng et al., 2014; Li C S et al., 2012; Ali et al., 2010, 2005; He Q et al., 2010; He B et al., 2006, 2003; Zhang et al., 2006; Chung and Jahn, 1995, and references therein), even though a few scholars still insisted a non-mantle plume model for the genesis of the ELIP (e.g., Liu et al., 2015; Thompson et al., 2001; Huang et al., 1992). Regardless of whether ELIP has a genetic affinity with a plume, the wider ranges of Ba isotopic compositions of the Emeishan basalts (-0.38‰- +0.38‰) in contrast to that of the PM prove that they have been variably contaminated by crustal materials. As corroborated by their geochemical and Ba isotopic features, the basaltic magma was initially generated via partial melting of the mantle, and subsequently overprinted by crustal contamination of the overlying continental materials during the ascent. Evidence from studies on their Sr-Nd-Pb-Hf and Re-Os isotopes also confirms this process (e.g., Fu et al., 2021; Zhang, 2019; Shellnutt and Jahn, 2011; He et al., 2010; Xu J F et al., 2007; Xiao et al., 2003; Xu Y G et al., 2001). More importantly, the low-Ti basalts had undergone a higher degree of crustal contamination relative to the high-Ti basalts. It is well consistent with their spatial distributions that the high-Ti basalts are located in the periphery of the ELIP and the low-Ti basalts are within the center (Tian et al., 2017). Due to their higher mantle potential temperature (T > 1 550 ℃), the hotter, low-Ti basaltic magmas from the plume center could assimilate more crustal materials easily than those cooler, high-Ti basalts (T < 1 500 ℃) during eruption (Liang et al., 2021; Xu et al., 2001). This is also reinforced by additional elemental data of the basalts from Lijiang, Dongchuan, Binchuan, and Miyi of the ELIP (Table 3, He et al., 2010; Xu et al., 2001).
(1) The δ138/134Ba values of the Emeishan continental flood basalts are highly heterogeneous, ranging from -0.38‰ to 0.38‰, which reflects significant contributions from variable contamination of crustal materials rather than other geological processes, such as partial melting, fractionation crystallization and weathering alteration.
(2) The elemental ratios of incompatible element simply that the low-Ti basalts from Lijiang experienced higher degrees of crustal contamination than the high-Ti basalts from Miyi and Emeishan during the ascent of basaltic magmas to the surface.
ACKNOWLEDGMENTS: This work was financially supported by the Program of Co-construction and Development of Universities (No. 80000-19z050201). The authors thank the editors, two anonymous reviewers and Prof. Zaicong Wang for their constructive suggestions. We gratefully acknowledge the Chinese Academy of Sciences (CAS) Key Laboratory of Crust-Mantle Materials and Environments at University of Science and Technology of China for help during geochemical and Ba isotope analyses. We are grateful to Prof. Yuanfu Xiao from Chengdu University of Technology for sharing the samples from the Lijiang region.The final publication is available at Springer via https://doi.org/10.1007/s12583-021-1513-0.| Ali, J. R., Fitton, J. G., Herzberg, C., 2010. Emeishan Large Igneous Province (SW China) and the Mantle-Plume Up-Doming Hypothesis. Journal of the Geological Society, 167(5): 953-959. https://doi.org/10.1144/0016-76492009-129 |
| Ali, J. R., Thompson, G. M., Zhou, M. F., et al., 2005. Emeishan Large Igneous Province, SW China. Lithos, 79(3/4): 475-489. https://doi.org/10.1016/j.lithos.2004.09.013 |
| An, Y. J., Li, X., Zhang, Z. F., 2020. Barium Isotopic Compositions in Thirty-Four Geological Reference Materials Analysed by MC-ICP-MS. Geostandards and Geoanalytical Research, 44(1): 183-199. https://doi.org/10.1111/ggr.12299 |
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Dong Yi, Jing Zhao, Chunhui Li, Xiuhong Peng. Crustal Contaminations Responsible for the Petrogenesis of Basalts from the Emeishan Large Igneous Province, NW China: New Evidence from Ba Isotopes. Journal of Earth Science, 2022, 33(1): 109-120. doi: 10.1007/s12583-021-1513-0
| Standard | Description | δ138/134Ba (‰) | 2SD | References |
| BCR-2 | Basalt, Columbia River, USA | 0.05 | 0.04 | Li et al. (2020) |
| 0.06 | 0.04 | An et al. (2020) | ||
| 0.06 | 0.03 | Nan et al. (2015) | ||
| 0.07 | 0.02 | This study | ||
| BHVO-2 | Basalt, Hawaii, USA | 0.06 | 0.03 | Nan et al. (2015) |
| 0.06 | 0.03 | Bullen and Chadwich (2016) | ||
| 0.05 | 0.03 | This study |
DownLoad:
CSV
| Locality | Types | Sample | Ba (ppm) | δ137/134Ba (‰) | 2SD | δ138/134Ba (‰) | 2SD |
| Lijiang | Low-Ti | WKB7 | 711 | 0.02 | 0.05 | 0.01 | 0.04 |
| WKB9 | 396 | 0.19 | 0.00 | 0.23 | 0.02 | ||
| PCB1 | 384 | -0.26 | 0.01 | -0.33 | 0.01 | ||
| PCB2 | 170 | -0.03 | 0.03 | -0.04 | 0.02 | ||
| Replicate | -0.03 | 0.03 | -0.03 | 0.03 | |||
| Miyi | High-Ti | MY1 | 402 | 0.29 | 0.00 | 0.38 | 0.01 |
| MY2 | 1 028 | -0.28 | 0.02 | -0.38 | 0.03 | ||
| MY4 | 619 | 0.09 | 0.00 | 0.13 | 0.02 | ||
| MY5 | 468 | 0.14 | 0.01 | 0.18 | 0.03 | ||
| MY6 | 527 | 0.05 | 0.02 | 0.06 | 0.03 | ||
| MY7 | 365 | 0.19 | 0.00 | 0.26 | 0.04 | ||
| Emeishan | High-Ti | EM001-1 | 272 | 0.03 | 0.04 | 0.04 | 0.05 |
| EM001-2 | 250 | 0.03 | 0.00 | 0.04 | 0.01 | ||
| EM002-1 | 523 | 0.08 | 0.02 | 0.11 | 0.01 | ||
| EM002-2 | 564 | 0.05 | 0.02 | 0.07 | 0.05 | ||
| EM002-3 | 495 | 0.15 | 0.01 | 0.19 | 0.01 | ||
| EM004-2 | 517 | 0.01 | 0.02 | 0.01 | 0.02 | ||
| EMSB001 | 479 | -0.02 | 0.01 | -0.03 | 0.01 |
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CSV
| Magma types | High-Ti basalts | Low-Ti basalts | PMc | OIBd | UCCe | ||||
| Ranges | Rangesa | Rangesb | Ranges | Rangesa | Rangesb | ||||
| Ti/Y | 519-897 | 449-979 | 528-682 | 351-531 | 149-531 | 269-430 | 813 | 593 | 182 |
| Nb/La | 0.76-1.06 | 0.78-1.16 | 0.62-1.07 | 0.56-1.29 | 0.81-0.99 | 0.61-1.81 | 1.04 | 1.30 | 0.39 |
| Th/Yb | 1.84-3.75 | 0.11-0.15 | 0.31-3.22 | 1.10-2.95 | 1.35-1.52 | 0.45-2.88 | 0.17 | 1.85 | 5.36 |
| Nb/U | 20.23-31.32 | 28.75-38.00 | 20.67-46 | 6.58-21.96 | 19.8-23.3 | 8.00-50.00 | 33.95 | 47.05 | 4.44 |
| Th/Nb | 0.13-0.21 | 0.11-0.15 | 0.07-0.24 | 0.14-0.60 | 0.17-0.18 | 0.06-0.4 | 0.12 | 0.08 | 0.88 |
| La/Sm | 3.09-5.00 | 2.78-4.55 | 3.32-4.72 | 3.35-5.21 | 3.28-4.04 | 2.43-4.23 | 1.55 | 3.70 | 6.60 |
| Th/Ta | 1.10-2.84 | 1.56-2.07 | 1.23-3.35 | 1.73-5.76 | 2.41-2.55 | 1.67-6.55 | 2.07 | 1.48 | 11.67 |
| a Data from He et al. (2010); b data from Xu et al. (2001); c PM. primitive mantle; d OIB. ocean-island basalts, OIB and PM data are from McDonough and Sun (1995); e UCC. upper continental crust, the upper continental crust data are from Rudnick and Gao (2014). | |||||||||
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CSV
| Standard | Description | δ138/134Ba (‰) | 2SD | References |
| BCR-2 | Basalt, Columbia River, USA | 0.05 | 0.04 | Li et al. (2020) |
| 0.06 | 0.04 | An et al. (2020) | ||
| 0.06 | 0.03 | Nan et al. (2015) | ||
| 0.07 | 0.02 | This study | ||
| BHVO-2 | Basalt, Hawaii, USA | 0.06 | 0.03 | Nan et al. (2015) |
| 0.06 | 0.03 | Bullen and Chadwich (2016) | ||
| 0.05 | 0.03 | This study |
| Locality | Types | Sample | Ba (ppm) | δ137/134Ba (‰) | 2SD | δ138/134Ba (‰) | 2SD |
| Lijiang | Low-Ti | WKB7 | 711 | 0.02 | 0.05 | 0.01 | 0.04 |
| WKB9 | 396 | 0.19 | 0.00 | 0.23 | 0.02 | ||
| PCB1 | 384 | -0.26 | 0.01 | -0.33 | 0.01 | ||
| PCB2 | 170 | -0.03 | 0.03 | -0.04 | 0.02 | ||
| Replicate | -0.03 | 0.03 | -0.03 | 0.03 | |||
| Miyi | High-Ti | MY1 | 402 | 0.29 | 0.00 | 0.38 | 0.01 |
| MY2 | 1 028 | -0.28 | 0.02 | -0.38 | 0.03 | ||
| MY4 | 619 | 0.09 | 0.00 | 0.13 | 0.02 | ||
| MY5 | 468 | 0.14 | 0.01 | 0.18 | 0.03 | ||
| MY6 | 527 | 0.05 | 0.02 | 0.06 | 0.03 | ||
| MY7 | 365 | 0.19 | 0.00 | 0.26 | 0.04 | ||
| Emeishan | High-Ti | EM001-1 | 272 | 0.03 | 0.04 | 0.04 | 0.05 |
| EM001-2 | 250 | 0.03 | 0.00 | 0.04 | 0.01 | ||
| EM002-1 | 523 | 0.08 | 0.02 | 0.11 | 0.01 | ||
| EM002-2 | 564 | 0.05 | 0.02 | 0.07 | 0.05 | ||
| EM002-3 | 495 | 0.15 | 0.01 | 0.19 | 0.01 | ||
| EM004-2 | 517 | 0.01 | 0.02 | 0.01 | 0.02 | ||
| EMSB001 | 479 | -0.02 | 0.01 | -0.03 | 0.01 |
| Magma types | High-Ti basalts | Low-Ti basalts | PMc | OIBd | UCCe | ||||
| Ranges | Rangesa | Rangesb | Ranges | Rangesa | Rangesb | ||||
| Ti/Y | 519-897 | 449-979 | 528-682 | 351-531 | 149-531 | 269-430 | 813 | 593 | 182 |
| Nb/La | 0.76-1.06 | 0.78-1.16 | 0.62-1.07 | 0.56-1.29 | 0.81-0.99 | 0.61-1.81 | 1.04 | 1.30 | 0.39 |
| Th/Yb | 1.84-3.75 | 0.11-0.15 | 0.31-3.22 | 1.10-2.95 | 1.35-1.52 | 0.45-2.88 | 0.17 | 1.85 | 5.36 |
| Nb/U | 20.23-31.32 | 28.75-38.00 | 20.67-46 | 6.58-21.96 | 19.8-23.3 | 8.00-50.00 | 33.95 | 47.05 | 4.44 |
| Th/Nb | 0.13-0.21 | 0.11-0.15 | 0.07-0.24 | 0.14-0.60 | 0.17-0.18 | 0.06-0.4 | 0.12 | 0.08 | 0.88 |
| La/Sm | 3.09-5.00 | 2.78-4.55 | 3.32-4.72 | 3.35-5.21 | 3.28-4.04 | 2.43-4.23 | 1.55 | 3.70 | 6.60 |
| Th/Ta | 1.10-2.84 | 1.56-2.07 | 1.23-3.35 | 1.73-5.76 | 2.41-2.55 | 1.67-6.55 | 2.07 | 1.48 | 11.67 |
| a Data from He et al. (2010); b data from Xu et al. (2001); c PM. primitive mantle; d OIB. ocean-island basalts, OIB and PM data are from McDonough and Sun (1995); e UCC. upper continental crust, the upper continental crust data are from Rudnick and Gao (2014). | |||||||||
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