Research Article Coexisting Late Cenozoic Potassic and Sodic Basalts in NE China: Role of Recycled Oceanic Components in Intraplate Magmatism and Mantle Heterogeneity

GeoScienceWorld Lithosphere Volume 2020, Article ID 8875012, 28 pages https://doi.org/10.2113/2020/8875012

1,2,3 1,2,3 1,2,3 1,2,3,4 1,2,3 Ming Lei, Zhengfu Guo , Wenbin Zhao, Maoliang Zhang, and Lin Ma

1Key Laboratory of Cenozoic Geology and Environment, Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing 100029, China 2CAS Center for Excellence in Life and Paleoenvironment, Beijing 100044, China 3University of Chinese Academy of Sciences, Beijing 100049, China 4Institute of Surface-Earth System Science, Tianjin University, Tianjin 300072, China

Correspondence should be addressed to Zhengfu Guo; [email protected]

Received 23 July 2019; Revised 28 May 2020; Accepted 24 June 2020; Published 1 September 2020

Academic Editor: Sarah M. Roeske

This study presents an integrated geochemical study of the Wudalianchi-Erkeshan potassic basalts and Halaha sodic basalts of NE China, and uses these data to further our understanding of the petrogenetic relationships between the coeval potassic and sodic basalts in this region. The potassic basalts with high concentrations of K2O have arc-like trace-element compositions and enriched Sr-Nd-Hf isotopic compositions with unradiogenic 206Pb/204Pb values (16.77–16.90). In contrast, the sodic basalts with high concentrations of Na2O have OIB-like trace-element compositions and depleted Sr-Nd-Hf isotopic compositions with radiogenic 206Pb/204Pb values (18.27–18.40). These data suggest that the potassic and sodic basalts were derived from mixed depleted mid-ocean-ridge basalt mantle (DMM) and enriched mantle source end-members, where the enriched end-members are ancient sediment for the potassic basalts and Paciﬁc oceanic crust for the sodic basalts. The combined geophysical and geochemical data indicate that these two enriched end-members are located in the mantle transition zone. We propose that partial melting of upwelling asthenospheric mantle comprising ambient DMM and recycled materials shifting from the ancient sediment to the Paciﬁc oceanic crust could have produced the coeval potassic and sodic basalts in NE China. The proposed mantle sources for the potassic and sodic basalts indicate that the upper mantle beneath NE China was highly heterogeneous during late Cenozoic.

1. Introduction [10]. According to Bonin [11, 12], potassic basalts are usually formed in postcollisional or postorogenic settings, whereas Continental alkali basalts including potassic basalts (K2O/ sodic basalts are normally formed within continental and Na2O>1) and sodic basalts (Na2O/K2O>1) are particularly oceanic lithosphere associated with rift systems, hot spots, important because they preserve geochemical features that or mantle plumes (e.g., [13]). likely reﬂect the nature of their mantle source (e.g., [1]). Pre- Intriguingly, coeval spatially and temporally related vious studies have suggested that potassic basalts are the potassic and sodic basalts are also reported in some places, result of the low degree of melting of phlogopite-bearing including the Basin-and-Range Province (e.g., the Rio peridotite (or pyroxenite) in the subcontinental lithospheric Grande Rift) [14–17], the East African Rift [18], and the mantle (SCLM) or asthenospheric mantle ([2–9], 2016), Hong’an-Dabie orogen, China [19–21]. Previous studies whereas sodic basalts are generally the result of decompres- have proposed two main models to explain the coeval potas- sion melting of asthenospheric mantle or mantle plumes sic and sodic basalts as follows:

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(1) In the lithospheric thinning or delamination model, relationship of these two suites of basalts, and (3) character- potassic basalts are formed by the partial melting of ize the upper mantle beneath NE China. a previously enriched lithospheric mantle, whereas sodic basalts are presumed to be formed by the 2. Geological Setting and Samples decompressional melting of sublithospheric material (asthenospheric mantle or mantle plume) when the The Xing’an-Mongolia Orogenic Belt is the eastern segment local lithospheric mantle is thinning [14, 15, 17, 18]. of the Central Asian Orogenic Belt, which lies between the Alternatively within this model, potassic basalts Siberia and Baltica cratons to the north and the Tarim and could be produced by the melting of a delaminated North China cratons to the south (e.g., [43]). NE China lies lithospheric mantle veined by a mica-bearing, Al- within the eastern portion of the Paleozoic Central Asian poor assemblage at high pressure (great depth), Orogenic Belt (Figure 1(a)). From Paleozoic to Mesozoic, whereas sodic basalts could be generated by the melt- NE China has experienced the amalgamation of several ing of a delaminated lithospheric mantle veined by an microcontinental blocks (e.g., Xing’an, Songliao, and Jamusi) aluminous amphibole-bearing assemblage at low along suture zones [44, 45]. Since the Late Jurassic, the tec- pressure (shallow depth) [16] tonic history of NE China has been dominated by the Paleo-Pacific plate, as evidenced by the Jurassic-Cretaceous – (2) In the recycled crustal material model [19 21], potas- accretionary complexes along the eastern Eurasian plate sic basalts are viewed as resulting from the partial melt- [46]. During the Cenozoic, NE China was in a continental ing of metasomatites that were produced by a reaction extension setting due to the Pacific slab rollback and trench between mantle-wedge peridotite and recycled conti- retreat [47], which probably resulted in asthenospheric nental crust, whereas sodic basalts are considered as upwelling and led to continental intraplate volcanism in NE resulting from the partial melting of metasomatites that China [48–50]. were produced by the reaction between mantle-wedge The Wudalianchi volcanic field and the adjacent Erke- peridotite and recycled oceanic crust shan volcanic field, which were located on the Northern margin of the Songliao Basin in the Xing’an-Mongolia Orogenic Late Cenozoic intraplate volcanic rocks are widely in and Belt (Figure 1(b)), are known for producing highly potassic around the Songliao Basin and occur along the Yilan-Yitong basalts (e.g., [51]). Previous studies indicated that the Wuda- and Fushun-Mishan faults, NE China (e.g., [22]). Coeval lianchi and Erkeshan volcanic activities mainly occurred in potassic and sodic basalts have also been extensively reported – – – the middle Pleistocene (0.56 0.13 Ma) and recent (1719 in NE China (e.g., [23 34]). However, the mantle sources of 1721 AD) periods (e.g., [22, 31]). these potassic and sodic basalts are still unresolved, with var- The Halaha volcanic field lies in the center of the Greater ious proposals for their sources including (1) SCLM metaso- Xing’An Mountains (Figure 1(b)). The magmatism of the matized by delaminated ancient lower continental crust or fi – Halaha volcanic eld was mainly distributed above the valley recycled ancient sediment [26, 27, 31, 33 35], (2) interaction of Halaha River, Chaoer River, Chai River, and Dele River between asthenospheric (or carbonated asthenospheric) forming a low lava platform [32]. Previous studies have mantle and enriched (or carbonated) lithospheric mantle shown that the volcanic activities of the Halaha volcanic field [28, 36], (3) asthenospheric mantle enriched by delaminated erupted over a short period from 2.30 to 0.16 Ma [23, 52]. ancient lower continental crust or recycled oceanic materials Sixteen basalts of the Wudalianchi-Erkeshan volcanic – (oceanic crust and/or sediment; [37 42]), (4) interaction fields and fourteen basalts of the Halaha volcanic field were between depleted lithospheric mantle and recycled ancient sampled in this study. The Wudalianchi-Erkeshan basalts subducted sediment [24, 25, 29], (5) depleted mid-ocean- have typical porphyritic texture and contain 10% pheno- ridge basalt (MORB) mantle (DMM) [23, 32], and (6) crysts, which are primarily olivine and clinopyroxene. The ancient primitive mantle with recycled oceanic materials matrix primarily comprises olivine, clinopyroxene, and some [30]. Recent studies have focused on the petrogenetic rela- plagioclase (Figures 2(a) and 2(b)). The Halaha basalts also tionship among these (ultra)potassic basalts and have pro- show typical porphyritic texture and contain 10%–20% phe- posed that the geochemical variations (e.g., K2O/Na2O and nocrysts, which are primarily olivine and minor clinopyrox- Rb/Nb ratios) of these potassic basalts might result from ene. The matrix primarily comprises olivine, clinopyroxene, melt-lithosphere interaction [24, 25]. However, another and minor oxide minerals (Figures 2(c) and 2(d)). The important issue is the petrogenetic relationship of the coeval descriptions of locations and ages for the studied samples potassic and sodic OIB basalts in NE China, which is still are summarized in Supporting Information Table S1. poorly constrained. For this study, we have conducted an integrated investi- 3. Analytical Methods gation of olivine, whole-rock major- and trace-element, and Sr-Nd-Pb-Hf radiogenic isotopic compositions of potassic Major-element analyses of olivine were performed using a basalts from the Wudalianchi-Erkeshan volcanic field and JEOL JXA-8230 electron microprobe. The precision of all ana- sodic basalts from the Halaha volcanic field of NE China. lyzed elements are better than 5%. Whole-rock major-element We combine our new data with previously published data contents were determined using a wavelength X-ray fluores- in these areas to (1) constrain the mantle source of the potas- cence (XRF) spectrometer. The analytical uncertainties on sic basalts and sodic basalts, (2) evaluate the petrogenetic major elements are generally better than 5%. Whole-rock

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(a) Russia 200 km N Figure 1(b)

Mongolia XMOB

Xiaogulihe Korea North China Craton Wudalianchi Jiagedaqi suture Keluo Russia East China South China Sea Block Nuominhe 0 300 km South China Sea Erkeshan Halaha

Mongololia

Songliao Mudanjiang basin

Jingpohu

Yitong-Yilan Fault

Abaga Longgang

Chifeng Mt. Changbai Sea of Japan (b) Fushum-Mishan Fault North Korea

Group 1 volcanic rocks Sample location Group 2 volcanic rocks Major fault Group 3 volcanic rocks

Figure 1: (a) Simplified geological map of eastern China, showing the spatial distribution of tectonic plates and late Cenozoic basalts. (b) Simplified map of sample locations in NE China (modified from [22, 25]). XMOB: Xing’an-Mongolia Orogenic Belt.

trace-element analyses were performed by ICP-MS using a during the analytical procedure are given in Supporting PerkinElmer Sciex ELAN 6000 instrument. For most of the Information Text 1 and Table S2, respectively. trace elements, analytical precision and accuracy are better than 5%. Whole-rock Sr-Nd-Pb-Hf isotope analyses were 4. Results performed with a Micromass Isoprobe MC-ICP-MS. The 87Sr/86Sr ratio obtained for the NBS SRM 987 standard 4.1. Whole-Rock Major, Trace Element, and Isotopic was 0:710288 ± 28 (2σ). The 143Nd/144Nd ratio obtained Geochemistry. The results of whole-rock major- and trace- for the Shin Etsu JNdi-1 standard was 0:512115 ± 7 (2σ). element concentrations and Sr-Nd-Pb-Hf isotopic composi- The 176Hf/177Hf ratio obtained for the JMC 475 standard tions for the studied samples are given in Tables 1 and 2, was 0:282224 ± 0:000019 (2σ). The measured Sr, Nd, and respectively. Olivine compositions are presented in Support- Hf isotope ratios were normalized to 86Sr/88Sr = 0:1194, ing Information Table S3. 146Nd/144Nd = 0:7219, and 179Hf/177Hf = 0:7325, respec- In the total alkali versus silica diagram (TAS), the tively. Measured Pb isotopic ratios were corrected for mass Wudalianchi-Erkeshan samples plot in the ﬁelds of basal- fractionation based on repeated analyses of international tic trachyandesite and phonotephrite to tephriphonolite, standard NBS981. The mean 206Pb/204Pb, 207Pb/204Pb, and whereas Halaha samples plot from the basalt to trachyba- 208 204 : σ n ﬁ Pb/ Pb ratios of NBS981 were 16 932 ± 6 (2 , =6), salt elds (Figure 3(a)). In the K2O versus Na2O diagram, 15:484 ± 6 (2σ, n =6), and 36:677 ± 18 (2σ, n =6), respec- the Wudalianchi-Erkeshan and Halaha basalts belong to tively. Detailed analytical methods and the isotopic ratios of potassic and sodic basalts, respectively (Figure 3(b)). The geological reference materials (BCR-2, BHVO-2) measured Wudalianchi-Erkeshan potassic basalts have lower MgO

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Potassic basalts OI Potassic basalts basalts lie above the North Hemisphere Reference Line ﬁ PI (NHRL) de ned by Hart [53], respectively. Cpx 4.2. Olivine Chemistry. In general, basaltic lavas contain two OI OI Cpx forms of olivine: (1) host magma-derived phenocrysts and (2) mantle-derived xenocrysts. The latter generally contain OI low concentrations of CaO (<0.1 wt.%), whereas olivine

100 �m 200 �m phenocrysts generally have high CaO contents (>0.1 wt.%; e.g., [54]). The majority of olivine xenocrysts are anhedral Sodic basalts Sodic basalts OI and may contain kink banding, whereas olivine phenocrysts are generally either euhedral or subhedral and are often free of kink banding (e.g., [55]; Kamenetsky et al., 2006). These OI PI Cpx criteria indicate that all of the olivine in the Wudalianchi- OI Erkeshan potassic basalts are phenocrysts, as they contain OI elevated concentrations of CaO (>0.1 wt.%) and possess either a euhedral or subhedral shape (Figure S1a). In comparison, the 500 �m 200 �m Halaha sodic basalts contain two groups of olivine. Group one olivines contain low concentrations of CaO (<0.1 wt.%) and Figure 2: Photomicrographs of the Wudalianchi-Erkeshan are angular with kink-banded extinction patterns, suggesting potassic basalts and Halaha sodic basalts. (a and b) Olivine and that they may be xenocrysts (Figures S1b and S1c). Group some clinopyroxene and plagioclase phenocrysts from the two olivines contain high concentrations of CaO (>0.1 wt.%) Wudalianchi-Erkeshan potassic basalts. (c and d) Olivine and and are euhedral, suggesting that they may be magmatic minor clinopyroxene phenocrysts from the Halaha sodic basalts. phenocrysts derived from the host magmas (Figure S1d). The olivine phenocrysts in the Wudalianchi-Erkeshan potassic basalts have a range of Fo (68.8–87.4), MnO (5.9–6.7 wt.%), Cr (140–240 ppm), and Ni (104–160 ppm) (0.14–0.49 wt.%), CaO (0.11–0.35 wt.%), and NiO (0.09– contents than those of Halaha sodic basalts, which are 0.39 wt.%) values. They have weak normal zoning that is characterized by higher MgO (9.8–11.9 wt.%), Cr (370– characterized by Fo values and NiO concentrations that 600 ppm), and Ni (231–433 ppm) contents. decrease, and they have CaO and MnO concentrations that In the chondrite-normalized REE diagrams (Figures 4(a) increase from core to rim (Figure S2). Group one olivine and 4(b)), the extent of fractionation between LREE and xenocrysts within the Halaha sodic basalts have high Fo HREE of the Wudalianchi-Erkeshan potassic basalts values (86.4–92.7) and contain low concentrations of CaO ð Þ : ‐ : ( La/Yb N =429 62 5) is higher than those of the Halaha (0.01–0.84 wt.%; Figure S2b). In comparison, group two ð Þ sodic basalts ( La/Yb N =10:3‐14:9). In the primitive- olivine phenocrysts within these basalts have a wider but mantle-normalized incompatible trace element spidergrams, slightly lower range of Fo values (72.0–89.6) and contain the Wudalianchi-Erkeshan potassic basalts are characterized variable MnO (0.11–0.46 wt.%), CaO (0.10–0.36 wt.%), by significantly negative high-field-strength element (HFSE) and NiO (0.11–0.40 wt.%) values. Group two olivine (e.g., Nb and Ta) anomalies and pronounced positive anom- phenocrysts are also weakly normally zoned with Fo values alies in the large ion lithophile elements (LILE) (e.g., Rb and and NiO concentrations decreasing and CaO and MnO Pb) (Figure 4(c)). In contrast, the Halaha sodic basalts show contents increasing from core to rim (Figure S2). Ba enrichment and positive Nb-Ta anomalies, resembling the typical OIBs (Figure 4(d)). 5. Discussion The Wudalianchi-Erkeshan potassic basalts have 87Sr/86Sr values from 0.705214 to 0.705630, 143Nd/144Nd 5.1. Role of Crustal Contamination and Fractional values from 0.512299 to 0.512321, and 176Hf/177Hf values Crystallization. In order to better constrain the nature of from 0.282513 to 0.282609 within the EM1 (enriched mantle the mantle source of the studied basalts, we first assess the 1) ranges in the Sr-Nd-Hf diagrams. The Halaha sodic basalts possible effects, if any, of low-pressure processes such as have less radiogenic Sr (87Sr/86Sr of 0.703613–0.704223) but crustal contamination and fractional crystallization on the more radiogenic Nd (143Nd/144Nd of 0.512894–0.512928) chemical compositions of these basalts. Based on the follow- and Hf (176Hf/177Hf of 0.282626–0.283100) isotopic ratios, ing lines of evidence, we suggest that the crustal contamina- comparable to OIBs (Figures 5(a)–5(c)). tion was not significant during their generation. Firstly, The Pb isotopic ratios of the Wudalianchi-Erkeshan both the potassic and sodic basalts display limited variations 206 204 207 204 87 86 potassic basalts ( Pb/ Pb = 16:77‐16:90, Pb/ Pb = in the ð Sr/ SrÞi and εNdðiÞ isotopic ratios with decreasing 15:43‐15:45, and 208Pb/204Pb = 36:76‐36:92) were less radio- MgO contents (Figures 6(a) and 6(b)). Secondly, the Nb/U genic than those of Halaha sodic basalts (206Pb/204Pb = ratios (40–64) of potassic and sodic basalts are similar to oce- 18:27‐18:40, 207Pb/204Pb = 15:52‐15:54, and 208Pb/204Pb = anic basalts (47 ± 10) (Figure 6(c), [56]) and higher than con- 38:20‐38:45). In the 207Pb/204Pb versus 206Pb/204Pb diagram tinental crust ratios (Nb/U = 6:2) [57], indicating that these (Figure 5(d)), the Wudalianchi-Erkeshan potassic basalts basalts did not suffer significant continental contamination. plot above the 4.55 Ga geochron line, while the Halaha sodic Thirdly, mantle xenoliths are present in both the potassic

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(a)

SiO2 52.3 52 52.7 51.1 53.5 53.9 52.7 54.3 51.3 52.2 54 52 52.3 52.3 TiO2 2.6 2.5 2.2 2.8 2.2 2.4 2.2 2.2 2.8 2.6 2.4 2.6 2.6 2.5 Al2O3 13.9 14 14.2 13.9 13.8 14.1 14.2 14.2 14 13.6 14 13.9 13.6 13.7 Fe2O3T 8.4 8.7 8.2 9.1 7.9 8.3 8.1 7.9 9.1 8.6 8.3 8.4 8.5 8.5 MnO 0.1 0.1 0.1 0.1 0.1 0.1 0.1 0.1 0.1 0.1 0.1 0.1 0.1 0.1 MgO 6.7 6.4 6.5 6.2 6.4 6.1 6.3 6.2 6.2 6.7 5.9 6.7 6.7 6.6 CaO 5.8 5.8 5.9 6.3 6.2 5.4 6 5.7 6.3 5.7 5.2 5.8 5.7 5.7

Na2O 3.6 4.1 3.7 3.5 3.5 3.8 3.6 3.4 3.6 3.8 3.8 3.7 3.7 3.7 K2O 5.8 5.1 4.6 5.7 4.8 5.5 4.8 5.2 5.6 5.6 5.5 5.8 5.7 5.8 P2O5 1.1 1.3 0.8 1.1 0.9 1 0.8 0.9 1.1 1.2 1 1.1 1.2 1.2 Mg# 0.65 0.63 0.65 0.61 0.65 0.63 0.64 0.64 0.61 0.64 0.62 0.65 0.65 0.65 LOI -0.2 0 0.5 0.1 0.3 -0.3 0.6 -0.1 0 0 0 -0.1 0 0 Total 100.2 101.2 99.5 99.9 99.7 100.3 99.4 100.1 100 99.1 99.2 100.1 99.1 100.4 (ppm) Sc 13.1 13.6 10.9 12.5 13.5 11.8 12.3 12.4 11.9 12.9 13.2 12.6 11.8 13.7 13.8 13.4 Cr 220 210 200 220 170 240 210 210 210 240 140 230 210 210 220 210 Ni 160 157 153.5 160.5 109 159 152.5 149.5 155.5 174 104 152.5 151.5 149.5 154.5 151.5 Ga 25.5 24.2 25.4 25.1 26.2 23.2 27 24.5 24.7 26.1 24 25.1 27.1 25.4 24.6 24.2 Rb 108 113.5 101 104 129 91.9 109.5 99.6 99.6 102.5 117.5 117 108 111.5 112.5 107 Sr 1720 1700 1950 1430 1500 1390 1490 1420 1450 1510 1450 1710 1570 1620 1620 1625 Y 22.5 21.7 21.8 18.6 19.8 16.9 22 18.1 18.3 21 18.7 22.2 22 22.4 22 21.9 Zr 494 486 381 406 409 345 526 399 375 444 384 493 533 493 487 487 Nb 65.1 64.3 69.2 54 61.7 45.2 69 53.1 49.7 63.9 57.6 65.3 67.8 65.4 64.5 65.1 Cs 0.94 0.86 0.93 0.91 1.04 0.8 0.86 0.81 0.68 0.84 0.95 0.81 0.86 0.8 0.82 0.77 Ba 2020 2000 2010 1675 2050 1720 1670 1695 1880 1680 2050 2090 1670 2030 2050 2040 La 101.5 98.8 104.5 71.1 85 68.1 90.8 71.2 73.9 81.7 80.3 102 91.5 100.5 100.5 99.5 Ce 195.5 195 202 139 163 133 173.5 140.5 144 158.5 156.5 196 177.5 194 195 191.5 Pr 21.8 22.2 22.9 16.15 18.2 15.45 19.05 15.8 16.15 17.9 17.15 21.8 19.65 21.5 21.6 20 Nd 78.7 74.7 86.1 57.8 67.5 58.3 71.4 60.2 59 63.5 65.7 78.6 72.3 77.5 78.1 76.4 Sm 12.8 13.15 13.95 10.45 11.3 9.9 11.5 10.15 10.3 11.2 10.75 12.75 12.1 12.6 12.85 11.7 Eu 3.48 3.39 3.78 2.84 3.21 2.84 3.19 2.96 2.76 3.04 3.15 3.47 3.26 3.4 3.42 3.21 5 on 29 September 2021 by guest Downloaded from http://pubs.geoscienceworld.org/gsa/lithosphere/article-pdf/doi/10.2113/2020/8875012/5293662/8875012.pdf 6 Table 1: Continued.

Wudalianchi-Erkeshan potassic basalts Sample 17EKS- 17EKS- 17WS- 17GLQ- 17LHS- 17WHS- 17LHS- 17GLQ- 17WHS- 17LHS- 17LHS- 17EKS- 17HSS- 17EKS- 17EKS- 17EKS- 04 01 01 02 01 02 02 01 01 06 03 02 03 06 03 05 Gd 9.18 8.35 9.24 7.43 8.26 6.83 8.44 7.38 7.29 7.71 7.97 9.09 8.03 8.56 8.56 8.39 Tb 1.09 1.02 1.14 0.94 1 0.91 1.06 0.91 0.87 0.97 0.97 1.11 1.04 1.05 1.09 1.07 Dy 5.41 5.2 5.52 4.42 5.12 4.18 5.28 4.63 4.36 5.04 4.46 5.43 5.23 5.31 5.31 5.04 Ho 0.91 0.83 0.87 0.71 0.8 0.68 0.88 0.71 0.69 0.8 0.73 0.88 0.87 0.85 0.87 0.83 Er 2.16 2.07 1.87 1.65 1.79 1.6 2.13 1.72 1.61 1.85 1.69 1.98 2.05 2.02 1.93 1.83 Tm 0.26 0.24 0.22 0.19 0.2 0.19 0.25 0.22 0.19 0.22 0.2 0.23 0.24 0.23 0.25 0.24 Yb 1.37 1.35 1.2 1.05 1.08 1.05 1.33 1.19 1.04 1.28 1.06 1.34 1.31 1.3 1.35 1.3 Lu 0.2 0.18 0.16 0.14 0.15 0.15 0.18 0.15 0.13 0.16 0.14 0.18 0.18 0.17 0.19 0.17 Hf 12.5 11.4 9 10 10.2 8.5 13.1 10.5 8.7 11 9.6 12.2 13.2 11.8 12.2 11.9 Ta 4.5 4 4 3 3.6 2.7 4.1 3.2 2.6 3.6 3.2 3.6 3.8 3.5 3.6 3.4 Pb 14.5 14.4 12.5 13 13.1 10.3 14 12.4 10.5 12.6 12.1 14.2 14.9 14.2 13.9 13.9 Th 7.08 6.52 7.31 6.23 6.96 5.35 7.6 6.38 5.34 7.33 6.49 6.99 7.6 6.77 6.9 6.96 U 1.3 1.29 1.37 1.33 1.32 1.06 1.58 1.09 0.9 1.51 1.19 1.44 1.65 1.4 1.31 1.34

(b)

Halaha sodic basalts Sample 17HLH-03 17CH-06 17CYH-05 17CH-02 17CH-01 17CH-04 17HLH-01 17CH-03 17HLH-04 17HLH-02 17HLH-05Q 17HLH-06Q 17CEH-04 17CERH-03 (wt.%)

SiO2 48.5 48.2 48 49.2 48.7 48 49.2 49 48.5 49 48.6 49.1 49 49 TiO2 2.2 2 2.1 2.1 2.1 2.1 2 2.1 2.1 2.2 2 2 2.1 2.1 Al2O3 12 12 12.2 12.4 12.4 13.2 12.2 12.6 12.3 12.4 11.9 12.1 12.8 12.7 Fe2O3T 12.1 12.3 12.2 11.9 12.2 12.1 12.5 11.8 12.4 11.9 12.5 12.4 11.6 11.7 MnO 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 MgO 10.9 11.9 11.1 10.3 10.2 9.8 10.3 10 9.8 11.2 10.8 10.3 9.9 9.9 CaO 9.2 8.9 9.6 9 9.2 9.7 8.9 9.4 9.8 9.3 8.9 8.8 9.4 9.6

Na2O 3 2.9 2.9 3.2 3.1 3 3 3.1 3 3.1 3.3 3.2 3 2.9 K2O 1.5 1.3 1.4 1.4 1.4 1.4 1.4 1.4 1.5 1.5 1.4 1.4 1.6 1.6 P2O5 0.4 0.4 0.4 0.4 0.4 0.5 0.4 0.4 0.4 0.4 0.4 0.4 0.5 0.4 Mg# 0.68 0.69 0.68 0.67 0.66 0.65 0.66 0.66 0.65 0.69 0.67 0.66 0.67 0.66 LOI 0 0 0 0 0 0 0 0 0 -0.6 0 0 0 0

Total 101 99.3 101.2 99.6 99.3 101 99.4 99.2 99.2 100.6 99.3 99.4 100.9 100.9 Lithosphere (ppm) Sc 20.9 19.7 20.5 19.3 20 20.4 18.8 21.5 21.1 20.8 20.5 20.6 22.6 21.1 on 29 September 2021 by guest Downloaded from http://pubs.geoscienceworld.org/gsa/lithosphere/article-pdf/doi/10.2113/2020/8875012/5293662/8875012.pdf Lithosphere

Table 1: Continued.

Halaha sodic basalts Sample 17HLH-03 17CH-06 17CYH-05 17CH-02 17CH-01 17CH-04 17HLH-01 17CH-03 17HLH-04 17HLH-02 17HLH-05Q 17HLH-06Q 17CEH-04 17CERH-03 Cr 430 600 530 500 410 390 450 480 380 520 470 450 370 420 Ni 270 433 335 325 319 234 353 263 231 370 380 366 271 265 Ga 20.9 19.4 20.4 20.2 19.4 20.4 19.8 20.8 22.2 19.5 19.2 19.4 18 20.9 Rb 31.6 27.2 32.7 30.5 27.3 22.7 30.8 27 36.2 31.5 31.8 31 28.3 26.7 Sr 509 464 553 538 567 683 491 537 639 515 481 494 670 660 Y 23.7 21.2 23.7 21.4 21.3 21.3 23.7 23.3 22.5 21.9 23.9 23.3 20.9 21.5 Zr 158 137 169 157 156 176 155 169 202 158 162 162 170 165 Nb 48.5 38.7 48.8 44.5 45.2 52.5 45 43.5 55.9 45.7 46.8 45.6 46.1 45.7 Cs 0.28 0.35 0.46 0.45 0.21 0.4 0.37 0.33 0.59 0.29 0.42 0.36 0.36 0.5 Ba 451 370 443 406 416 567 365 439 508 426 355 354 388 443 La 25.8 21.2 26.2 23.7 24.1 30.6 24.7 25.8 28.8 24.1 24.4 24.8 26.1 25.3 Ce 50.8 42.3 52.9 47.5 47.3 59.9 48.9 51 57.5 47.4 50.2 51.5 53.7 50.4 Pr 5.97 5.24 6.05 5.69 5.73 7.05 5.91 5.99 6.86 5.63 6.16 6.25 6.56 6 Nd 25.5 22.1 25.8 24.2 23.8 29 23.8 26.3 28.3 23.7 23.7 22.7 24.7 25.5 Sm 6.12 5.5 5.93 5.87 5.95 6.52 5.85 6.09 6.66 5.66 6.19 6.42 6.49 5.9 Eu 2.07 1.81 1.91 1.97 1.99 2.15 1.99 2.04 2.19 1.96 1.89 1.85 1.87 2 Gd 6.22 5.72 5.94 5.82 5.79 6.39 6.13 6.08 6.25 5.76 5.98 6.02 5.79 6 Tb 0.88 0.84 0.86 0.86 0.85 0.87 0.9 0.88 0.9 0.84 0.89 0.86 0.84 0.9 Dy 4.85 4.58 4.91 4.73 4.71 4.7 5.1 5.07 4.88 4.98 4.64 4.64 4.25 4.6 Ho 0.91 0.81 0.87 0.84 0.81 0.84 0.9 0.91 0.85 0.87 0.88 0.89 0.8 0.8 Er 2.15 2.11 2.33 2.08 2.03 2.13 2.3 2.32 2.19 2.03 2.27 2.29 2.08 2 Tm 0.27 0.26 0.29 0.27 0.24 0.26 0.29 0.29 0.27 0.26 0.28 0.29 0.26 0.3 Yb 1.62 1.47 1.64 1.48 1.47 1.47 1.61 1.73 1.53 1.58 1.52 1.59 1.56 1.6 Lu 0.22 0.21 0.21 0.2 0.21 0.22 0.22 0.24 0.21 0.21 0.21 0.22 0.21 0.2 Hf 4 3.6 4.2 4 4.1 4.4 4.1 4.6 4.9 4.2 3.8 3.8 4.1 4.4 Ta 2.3 2.8 3.1 2.9 2.9 3.2 2.9 2.7 3.3 2.9 2.8 2.7 2.9 2.6 Pb 2.1 2 2.1 2.5 2.2 3.3 2 2.3 3 2 2 2.1 2.9 2.7 Th 3.19 2.59 3.57 3.57 3.24 4.29 3.34 3.49 3.96 3.27 3.24 3.34 3.8 3.6 U 0.76 0.73 0.84 0.87 0.85 1.02 0.81 0.82 1 0.77 0.8 0.82 1 0.9 2+ ð 2+ 2+Þ 3+ ð 2+ 3+Þ : Note: total iron as Fe2O3T ; Mg# = 100 × Mg / Mg +Fe , assuming Fe / Fe +Fe =015. 7 on 29 September 2021 by guest Downloaded from http://pubs.geoscienceworld.org/gsa/lithosphere/article-pdf/doi/10.2113/2020/8875012/5293662/8875012.pdf 8 Table 2: Whole-rock Sr-Nd-Pb-Hf isotope for Wudalianchi-Erkeshan potassic basalts and Halaha sodic basalts.

(a)

Wudalianchi-Erkeshan potassic basalts Sample 17WS-01 17GLQ-02 17LHS-01 17WHS-02 17LHS-02 17GLQ-01 17LHS-06 17LHS-03 17EKS-02 17HSS-03 17EKS-06 17EKS-03 17EKS-05 87Sr/86Sr 0.705214 0.705266 0.705243 0.705489 0.705402 0.705299 0.705321 0.705259 0.705588 0.70542 0.705617 0.70563 0.705624 2σ 7 7 7 9 9 1 10 10 10 8 10 10 9 143 Nd/144 Nd 0.512362 0.512373 0.512384 0.512364 0.512374 0.512376 0.512399 0.51238 0.512324 0.512379 0.512323 0.512321 0.512322 2σ 64 4 5 6 4 5564655 εNd -5.4 -5.2 -4.9 -5.4 -5.1 -5.1 -4.7 -5 -6.1 -5.1 -6.1 -6.2 -6.2 176 Hf/177 Hf 0.282626 0.282586 0.282593 0.282592 0.282598 0.282592 0.282609 0.282514 0.282558 0.282522 0.282516 0.282513 2σ 1079 8 8 7575767 εHf -5.2 -6.6 -6.3 -6.4 -6.2 -6.4 -5.8 -9.1 -7.6 -8.8 -9.1 -9.2 206 Pb/204 Pb 16.86 16.86 16.84 16.77 16.83 16.86 16.9 16.84 16.79 16.83 16.79 16.79 16.79 2σ 66 5 7 5 6 6555545 207 Pb/204 Pb 15.44 15.45 15.44 15.43 15.44 15.45 15.44 15.44 15.43 15.44 15.43 15.43 15.43 2σ 56 5 6 5 6 6555544 208 Pb/204 Pb 36.92 36.88 36.85 36.78 36.81 36.88 36.92 36.85 36.76 36.80 36.77 36.76 36.76 2σ 14 15 13 15 12 14 15 13 11 12 12 9 11

(b)

Halaha sodic basalts Sample 17HLH-03 17CH-06 17CYH-05 17CH-02 17CH-01 17CH-04 17HLH-01 17CH-03 17HLH-04 17HLH-02 17HLH-06Q 17CEH-04 87Sr/86Sr 0.703672 0.703649 0.703936 0.703783 0.70371 0.703617 0.703652 0.70364 0.703617 0.703613 0.703653 0.704223 2σ 10 9 6 11 10 7 10 10 7 10 6 10 143 Nd/144 Nd 0.512905 0.512928 0.512915 0.512898 0.512898 0.512894 0.512894 0.512915 0.512898 0.512912 0.512906 0.512902 2σ 3553615445 4 6 3 εNd 5.2 5.7 5.4 5.1 5.1 5.1 5 5.4 5.1 5.3 5.2 5.1 176 Hf/177 Hf 0.2831 0.28308 0.283093 0.283068 0.28308 0.283065 0.283095 0.283096 0.283063 0.283082 0.283093 0.283061 2σ 8 15 13 14 14 8 11 14 8 9 6 13 εHf 11.6 10.9 11.4 10.5 10.9 10.4 11.4 11.5 10.3 11.0 11.4 10.2 206 Pb/204 Pb 18.39 18.36 18.4 18.38 18.31 18.2732 18.58 18.32 18.31 18.37 18.58 18.3523 2σ 766687784 7 7 9 207 Pb/204 Pb 15.52 15.52 15.52 15.53 15.52 15.5303 15.54 15.52 15.52 15.52 15.54 15.5315 2σ 666586674 6 6 8Lithosphere 208 Pb/204 Pb 38.28 38.24 38.29 38.3 38.24 38.2149 38.45 38.2 38.2 38.28 38.44 38.265 2σ 17 16 16 16 19 16 14 17 11 17 15 20 ε ð143 144 Þ : ε ð176 177 Þ : Note: Nd values were calculated using Nd/ Nd CHUR =0512638. Hf values were calculated using Hf/ Hf CHUR =0282772. Lithosphere 9

14 Ph

12 U3

T 10 U2 S3 8 O (wt.%)

2 S2

O+K 6 2 S1 Na

4 O2 Alkalic O1 Subalkalic 2 B

0 45 50 55 60 65

SiO2 (wt.%) (a) 12

K2O/Na2O = 3 10

K2O/Na2O = 2

8 Ultrapotassic rocks Potassic rocks 6 O (wt.%) 2 K2O/Na2O = 1 K

Sodic rocks 0 01234567

Na2O (wt.%)

Potassic basalts Sodic basalts Potassic basalts Sodic basalts (literature) (literature) (b) Figure 3: (a) Na2O+K2O (wt.%) versus SiO2 (wt.%) and (b) K2O (wt.%) versus Na2O (wt.%) plots for the Wudalianchi-Erkeshan potassic basalts and Halaha sodic basalts. All plotted data were recalculated to 100 wt.% on a volatile-free basis. The classiﬁcation boundaries are from Le Bas et al. [196]. Rock types: B—basalt; S1—trachybasalt; S2—basaltic trachyandesite; S3—trachyandesite; T—trachyte; U2— phonotephrite; U3—tephriphonolite; Ph—phonolite; O1—basaltic andesite; O2—andesite. The green squares and open squares represent data for the Wudalianchi-Erkeshan potassic basalts from this study and previously published data from Liu et al. [117], Zhang et al. [31], Hsu and Chen [197], Zou et al. [34], Chen et al. [93], Chu et al. [35], and Wang et al. [29], respectively. The red circles and open circles represent data for the Halaha sodic basalts from this study and previously published data from Zhao and Fan [32], Ho et al. [23], and Chen et al. [38], respectively.

and sodic basalts (e.g., [58, 59]), indicating that the host show that the potassic basalts have strong 230Th excesses. magmas ascended rapidly without significant interaction This observation also indicates that the potassic basalts can- with the continental crust. Lastly, U-Th disequilibrium data not suffer from significant crustal contamination. This is

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1000

100 100

100 100 Rock/chondrite Rock/chondrite

1 1

0.1 0.1 La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu (a) (b) 1000 0.1

100 100

Rock/primitive mantle Rock/primitive 1 mantle Rock/primitive 1

0.1 Rb T Nb La Pb Sr Zr Sm Gd Dy Ho Tm Lu Rb T Nb La Pb Sr Zr Sm Gd Dy Ho Tm Lu Ba U Ta Ce Pr Nd Hf Eu Tb Y Er Yb Ba U Ta Ce Pr Nd Hf Eu Tb Y Er Yb

Potassic basalts Sodic basalts Potassic basalts (literature) Sodic basalts (literature) (c) (d)

Figure 4: (a and b) Chondrite-normalized REE patterns and (c and d) primitive-mantle-normalized incompatible-element diagrams for the Wudalianchi-Erkeshan potassic basalts and Halaha sodic basalts. The trace-element compositions of chondrite and the primitive-mantle values are from Sun and McDonough [198]. The data sources are the same as those for Figure 3.

because assimilation of crustal rocks (230Th/238U=1:0) negative Eu and Sr anomalies in the REE patterns would reduce the extent of 230Th excesses of potassic basalts (Figures 5(a) and 5(c)). [34]. The Os isotopic data of the potassic basalts further indi- The Halaha sodic basalts in this study have relatively high cate that they might suffer relatively minor amounts (3.5%) MgO (9.8–11.9 wt.%) contents, suggesting insignificant crys- of lower crust contamination [35]. The sodic basalts display tal fractionation of the sodic basalts. The positive correlation positive Nb and Ta anomalies in the primitive-mantle- between Mg# and Ni values indicates that the parental normalized incompatible-element spidergrams (Figure 4(d)), magmas of sodic basalts underwent olivine fractionation also suggesting negligible contamination from the conti- (Figure 7(a)). The relatively constant concentrations of nental crust. CaO, CaO/Al2O3, and Al2O3 with a decreasing Mg# value The Wudalianchi-Erkeshan potassic basalts in this study indicate insignificant fractionation of clinopyroxene and pla- have low values of MgO (5.9–6.7 wt.%), indicating that their gioclase (Figures 7(b)–7(d)). parental magmas might have experienced a variable degree of differentiation. The positive correlations between Mg# ver- 5.2. Source Lithology. Primary magmas of basaltic lavas sus Ni, CaO, and CaO/Al2O3 suggest that they have experi- can be used as probes of their mantle sources (e.g., [60]). enced fractional crystallization of olivine and clinopyroxene Experimental studies have shown that basaltic melts can (Figures 7(a)–7(c)). Plagioclase fractionation is insignificant, be generated from partial melting of peridotite (e.g., [61, as demonstrated to some degree by no positive correlation of 62]), pyroxenite (e.g., [63, 64]) and carbonated peridotite Al2O3 with Mg# (Figure 7(d)) in concert with the absence of and/or pyroxenite [65, 66]. Here, the least-fractionated

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DMM DMM 0.2832 0.5130 Pitcairn EM1 OIB i i 0.2830 Mantle array Nd) Samoa EM2 Hf) 144 OIB 177

Hf/ 0.2828 Nd/ 0.5126 176

143 Samoa EM2 ( ( Pitcairn EM1 OIB OIB 0.2826

0.5122 0.2824 0.702 0.704 0.706 0.708 0.5122 0.5124 0.5126 0.5128 0.5130 0.5132 (87Sr/86Sr)i (143Nd/144Nd)i (a) (b)

DMM Southern Tibet 15.8 Western Australia 0.5130 Mediterranean

i Pitcairn EM1 OIB Gaussberg

i Geochron

Nd) Samoa EM2 15.6 Pb) 144 OIB Leucite Hills 204 Nd/

0.5126 Pb/ 143 ( 207 ( 15.4 NHRL DMM

0.5122 15.2 16 17 18 19 20 16 17 18 19 20

(206Pb/204Pb)i (206Pb/204Pb)i

Potassic basalts Sodic basalts Potassic basalts Sodic basalts (literature) (literature)

143 144 87 86 176 177 143 144 143 144 206 204 Figure 5: Plots of (a) ð Nd/ NdÞi versus ð Sr/ SrÞi, (b) ð Hf/ HfÞi versus ð Nd/ NdÞi, (c) ð Nd/ NdÞi versus ð Pb/ PbÞi, 207 204 206 204 and (d) ð Pb/ PbÞi versus ( Pb/ Pb) for the Wudalianchi-Erkeshan potassic basalts and Halaha sodic basalts. The data sources for EM1-OIB (Pitcairn islands) and EM2-type OIB (Samoa islands) are from http://georoc.mpch-mainz.gwdg.de/georoc/. The reference ﬁeld for DMM (Depleted MORB Mantle) is from Workman and Hart [199]. Data for (ultra)potassic igneous rocks in (b) are from Fraser et al. [148], Dudas et al. [147], O’Brien et al. [149], Murphy et al. [124], Prelević et al. [8, 9], Zhao et al. [141], and Guo et al. [6, 7]. The Northern Hemisphere Reference Line (NHRL) and Geochron are from Hart [53]. Other data sources are the same as those for Figure 3.

samples, which record only olivine fractionation, were used and sodic basalts may not have been derived from sources to calculate the primary-melt compositions of both the dominated by carbonated peridotite or pyroxenite material. Wudalianchi-Erkeshan potassic basalts and the Halaha sodic Previous researches have suggested that potassic and sodic basalts. The detailed methods and results are given in Sup- basalts within NE China were derived from peridotite- porting Information Text 2 and Table S4, respectively. dominated sources (e.g., [23, 26, 30, 32]). This conclusion is Partial melting of carbonated mantle (peridotite and/or consistent with the calculated primary magma compositions pyroxenite) commonly generates basaltic melts with high of the potassic and sodic basalts, which have the values of Zr/Hf ratios and large negative Zr and Hf anomalies in mul- FeOT ,Al2O3, and TiO2 similar to melts derived from partial tielement variation diagrams [67–71]. These characteristics melting of peridotite (Figures 8(a)–8(c)). However, the fol- are not present with either the Wudalianchi-Erkeshan potas- lowing lines of evidence argue that the mantle sources of sic basalts or the Halaha sodic basalts, which are character- the potassic and sodic basalts also contain pyroxenite: (1) ized by low Zr/Hf values (38–43 for both potassic and sodic Compared with basaltic magmas derived from pure perido- basalts; Table 1) and no negative Zr and Hf anomalies tite sources, both the potassic and sodic basalts have low (Figures 4(c) and 4(d)). This suggests that both the potassic CaO concentrations at a given MgO value (Figure 8(d);

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0.710 The olivine phenocrysts in the potassic and sodic basalts have higher Ni contents and Fe/Mn ratios, but lower Mn and Ca contents at a given Fo than those expected for olivine crystal- 0.708 lized from melting of pure peridotite (Figure 10; [72]). We

i therefore propose that the mantle lithologies of the potassic

Sr) and sodic basalts were mixed or came from hybrid sources 86 0.706 containing both peridotite and pyroxenite. Sr/ 87 ( 5.3. Mantle End-Members of the Potassic and Sodic Basalts. 0.704 Both the Wudalianchi-Erkeshan potassic basalts and the Halaha sodic basalts deﬁne mixing trends between depleted and enriched end-members within Sr-Nd-Pb-Hf isotopic 0.702 plots (Figure 5). The depleted end-member for the late Ceno- 481216 20 MgO (wt.%) zoic basalts in NE China is commonly thought to be DMM (e.g., [33]). However, studies indicate that a depleted compo- 8 nent may also be present within the deep mantle, which could contribute to the production of oceanic basalts (e.g., [76–79]). As all modern terrestrial lavas have 142Nd/144Nd 4 values that are about 18 ppm higher than those in ordinary chondrites (e.g., [80–82]), ancient primitive mantle is argued

( i) to have been both chondritic and nonchondritic [81, 83, 84]. 0

� Nd It has been further suggested that this ancient primitive mantle has superchondritic 142Nd/144Nd values and represents an –4 early precursor for all modern terrestrial mantle reservoirs (e.g., [85]). The so-called “FOZO,” which has also been defined as “PREMA” [86], “PHEM” [87], and “C” [88, 89], –8 is a less primitive but ubiquitous reservoir within the mantle 4 81216 20 that is thought to be a mixture of recycled components (e.g., MgO (wt.%) oceanic crust) and early isolated ancient primitive mantle [90]. Thus, it is highly likely that both ancient primitive man- 80 tle and FOZO could provide the depleted components for the production of basalts (e.g., [85, 90–92]). Based on radiogenic 60 isotopic data (e.g., Sr-Nd-Pb) from late Cenozoic basalts, previous studies have suggested that the depleted end-member in the mantle source of late Cenozoic basalts in NE China MORB & OIB 40 could be ancient primitive mantle material or FOZO [30, Nb/U 93]. However, it is not a simple task to discriminate between DMM, ancient primitive mantle, and FOZO reservoirs sim- 20 ply by using radiogenic isotopic values (e.g., Sr-Nd-Pb) alone (Figure S3). A more definitive discrimination requires the use of noble-gas isotopes. DMM-derived basalts (MORBs) 0 have nearly constant 3He/4He values (8 Ra, where Ra is the 020406080 atmospheric 3He/4He ratio; [94]), whereas basalts derived Nb (ppm) from relatively primordial ancient primitive mantle or 3 4 Sodic basalts FOZO reservoirs should have higher He/ He values Potassic basalts ć Sodic basalts (>30 Ra; [85, 91, 95]; Garapi et al., 2015). Potassic basalts 3 4 (literature) (literature) The low He/ He values (<8 Ra) of late Cenozoic basalts and associated mantle xenoliths within NE China ([93] and Figure ð87 86 Þ ε 6: (a) Sr/ Sr i versus MgO (wt.%), (b) NdðtÞ versus MgO references therein) suggest that these magmas were not (wt.%), and (c) Nb/U versus Nb (ppm) for the Wudalianchi- derived from a deep-seated mantle plume. This is consistent Erkeshan potassic basalts and Halaha sodic basalts. The data with a lack of geophysical evidence of a mantle plume in this sources are the same as those for Figure 3. region during the late Cenozoic (e.g., [96]). These observations suggest that the depleted component in the mantle [72]). (2) The potassic and sodic basalts have higher Fe/Mn source of the late Cenozoic basalts (e.g., the Wudalianchi- but lower Fe/Zn ratios than melts derived from the partial Erkeshan potassic basalts and the Halaha sodic basalts) is melting of normal mantle peridotite (Figure 9; e.g., [73, most likely DMM rather than ancient primitive lower mantle 74]). (3) As olivine is the first silicate mineral to crystallize or FOZO. from mantle-derived magmas, olivine geochemistry can also The nature of the enriched end-members in the mantle provide insights into the mantle source of basalts (e.g., [75]). source of these basalts remains contentious, with proposed

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600 12

9 400

6 Ni (ppm) Ni 200 CaO (wt.%) 3

0 0 60 65 70 60 65 70 Mg# Mg# (a) (b) 1.0 20

0.8 15 3

O 0.6 2 (wt.%)

3 10 O 0.4 2 CaO/AI AI

5 0.2

0.0 0 60 65 70 60 65 70 Mg# Mg#

Potassic basalts Sodic basalts Potassic basalts Sodic basalts (literature) (literature) (c) (d) Figure 7: Variations in (a) Ni (ppm) versus Mg#, (b) CaO (wt.%) versus Mg#, (c) CaO/Al2O3 versus Mg#, and (d) Al2O3 (wt.%) versus Mg# for the Wudalianchi-Erkeshan potassic basalts and Halaha sodic basalts, respectively. The data sources are the same as those for Figure 3.

sources including delaminated ancient lower crust [35, 39], is only ~0.61 wt.% [57]. Accordingly, it is diﬃcult to conceive recycled SCLM [31, 33, 34], and recycled oceanic materials that lower continental crust with such a low K2O content [24–27, 29, 30, 37, 38, 40, 41]. In the following section, we could modify the asthenospheric mantle and then produce focus mainly on the enriched end-members in the mantle the Wudalianchi-Erkeshan potassic basalts with high K2O sources of Wudalianchi-Erkeshan potassic basalts and contents (4.6–5.8 wt.%). Also, the mantle xenoliths hosted Halaha sodic basalts. in the volcanic rocks with Paleoproterozoic model ages argue against delamination of the lower crust having 5.4. Identiﬁcation of the Enriched Components in the occurred in this area during the Cenozoic [97]. Therefore, Mantle Source the EM1-like signature of the Wudalianchi-Erkeshan potassic basalts did not originate from the delaminated ancient 5.4.1. Recycled Ancient Sediment in the Mantle Source of the lower continental crust. Potassic Basalts. The Wudalianchi-Erkeshan potassic basalts The ancient metasomatized lithospheric mantle and have high Ba, Sr, and LREE contents as well as depletion in recycled ancient sediment residing in the mantle transition HFSEs and extremely unradiogenic Pb isotopic compositions zone (410–660 km depth) have been the two competing ori- (206Pb/204Pb = 16:77‐16:90), indicating that the enriched gins of the EM1-like signature of the Wudalianchi- component in the mantle source has a clear EM1-like signa- Erkeshan potassic basalts [26, 27, 29, 31, 33, 34, 41]. This is ture. Previous studies have proposed that this signature because both of them could account for the high K2O, Sr, originated mainly from the delaminated ancient lower conti- and Pb contents (Figure 4(b)), Ba/La (18–26) and Ba/Th nental crust of NE China [35]. However, it should be noted (220–352) values (Figure 11), and unradiogenic Pb isotopic that the average K2O content of the lower continental crust compositions of potassic basalts. Based on the following

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20 20

Pyroxenite+CO2 Quartz 15 eclogite Pyroxenite 16 Pyroxenite (wt.%) (wt.%) 10 Quartz 3

T Peridotite

eclogite O 2

FeO Peridotite+CO 2 AI 12 5 Peridotite

Pyroxenite+CO2 Peridotite +CO2 0 8 0102030 0102030 MgO (wt.%) MgO (wt.%)

(a) (b) 6 15

Pyroxenite+CO2 4 Peridotite-derived melts Quartz eclogite (wt.%) 10

2 Pyroxenite CaO (wt.%) TiO 2 Peridotite +CO Pyroxenite- 2 derived melts Peridotite 0 5 0102030 0102030 MgO (wt.%) MgO (wt.%) Primary magmas of potassic basalts Primary magmas of sodic basalts

(c) (d) Figure 8: (a) FeOT (wt.%) versus MgO (wt.%), (b) Al2O3 (wt.%) versus MgO (wt.%), (c) TiO2 (wt.%) versus MgO (wt.%), and (d) CaO (wt.%) versus MgO (wt.%) for the calculated primary magmas of the Wudalianchi-Erkeshan potassic basalts and Halaha sodic basalts, respectively. The ﬁelds of high-pressure experimental partial melts of various mantle lithologies in (a), (b), and (c) are modiﬁed according to the following literature: peridotite [61, 62, 200, 201], carbonated peridotite [65, 202], quartz eclogite [203, 204], garnet pyroxenite [64, 205, 206], and carbonated pyroxenite [207]. The red line in (d) separating melts formed from the melting of peridotite and pyroxenite is after Herzberg and Asimow [208].

two main observations, we propose that the EM1-like signa- these ancient mantle peridotites have been refertilized by ture of the Wudalianchi-Erkeshan potassic basalts is most asthenosphere-derived melts and their EM1 compositions likely derived from recycled ancient sediment residing in might have been diluted (e.g., Zhang et al., 2009, [114– the mantle transition zone: (1) Many mantle xenoliths from 116]). Besides, even if these ancient lithospheric mantle peri- NE China show that the lithospheric mantle had moderately dotites were characterized with an EM1 signature, it appears depleted Sr-Nd-Hf isotopic compositions [98–101], which to be volumetrically unrealistic that the small portion of could not have produced the EM1-type isotopic characteris- ancient lithospheric mantle beneath several local places could tics observed in the Wudalianchi-Erkeshan potassic basalts. be the source of EM1 basalts, which were widely distributed Actually, this observed EM1 signature is found not only in in NE China and NCC during the Cenozoic (e.g., [51, NE China but also in many other volcanic ﬁelds in the North 117]). (2) The low 206Pb/204Pb values (16.77–16.90) of the China Craton (e.g., [70, 102, 103]). Geochemical, geophysical Wudalianchi-Erkeshan potassic basalts indicate that their and petrological data have indicated that the lithospheric source should have very low 238U/204Pb values (as low as mantle beneath the present-day North China Craton has ~2), which would severely retard the subsequent production been mostly removed and replaced by a hot, thin, juvenile of radiogenic Pb isotopes in a prolonged (2–3 Gyr) period SCLM [104–111], which could not have provided the [118, 119]. The estimated high water contents (up to observed EM1 signature in the Cenozoic basalts of the North 4.5 wt.%) of the parental magmas of the Wudalianchi- China Craton. Although it has been discovered that there Erkeshan potassic basalts require that their mantle source might have been a small portion of Archean lithospheric should be highly hydrated [41, 120]. This above discussion mantle beneath NE China (e.g., Keluo, [97]) and NCC (e.g., implies that the mantle source of potassic basalts must be Hebi, Fanshi, [112, 113]), many studies have proven that hydrated and isolated for a long period (2–3 Gyr) from

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didate source of OIBs [127, 128, 131]. However, metasoma- 1250 tized minerals such as amphibole and phlogopite are not observed in the mantle peridotite xenoliths (including harz- 1050 MORB burgites and lherzolites) hosted in the Halaha sodic basalts [59]. In addition, if the high Nb-Ta contents were contrib- 850 uted by the Nb-rich minerals (e.g., rutile) in the mantle lith-

Fe/Zn osphere, they could also host Zr-Hf, thereby producing positive Zr-Hf anomalies (e.g., [42]), which are not observed 650 in the multielement variation diagram for the Halaha sodic basalts (Figure 4(d)). Therefore, the recycled lithospheric 450 mantle is unlikely to be the enriched component in the man- 50 60 70 80 90 100 tle source of the Halaha sodic basalts. Fe/Mn It is likely, therefore, that the Halaha sodic basalts originated from the asthenospheric mantle. However, these sodic Potassic basalts Sodic basalts basalts are enriched in LILEs and LREEs (Figures 4(c) and Potassic basalts Sodic basalts (literature) (literature) 4(d)) and have enriched Sr-Nd-Hf-Pb isotopes (Figure 5) compared to MORBs. These differences indicate that the nor- Figure 9: Relationship between the values of Fe/Mn and Fe/Zn for mal asthenospheric mantle cannot have served directly as the the Wudalianchi-Erkeshan potassic basalts and Halaha sodic source of these OIBs. Previous studies suggest that the basalts. The Fe/Mn values of mid-ocean-ridge basalt (MORB) are recycled oceanic crust is a common enriched component in from Humayun et al. [209] and Qin and Humayun [210], and the Fe/Zn values of MORB are from Le Roux et al. [73]. Other data the mantle sources of OIBs (e.g., [126, 129]). Based on the sources are the same as those for Figure 3. following lines of evidence, we favor the recycled oceanic crust as the most likely enriched component in the mantle source of the Halaha sodic basalts. As slab dehydration mantle convection. The Archean fluid-metasomatized SCLM occurred during the subduction of the oceanic crust in the could satisfy the long-term isolation of low-μ material that is rutile stability field, fluid-mobile elements (Th and U, as well required to generate an EM1-like signature (e.g., [31]). How- as Ba, Rb, Cs, and Sr) were transported to peridotite in the ever, because the addition of water into the SCLM would mantle wedge, while HFSEs (e.g., Nb, Ta, and Ti) remained have significantly decreased its viscosity [121, 122], the in the residual oceanic crust (e.g., [132]). Fluid-fluxed hydrated SCLM cannot remain isolated for a long period of mantle-wedge peridotites were generated above the subduct- time from the convective upper mantle [122]. In contrast, ing slab, and their partial melting produced oceanic arc the mantle transition zone is likely to be the slab “graveyard” basalts (OABs) that are enriched in fluid-mobile elements (e.g., [123]) and the recycled sediment can be isolated for a (LILE, LREE, and Th) but depleted in Nb, Ta, and Ti [133, long period of time (~2.0 Ga) in the mantle transition zone 134]. Compared with OABs, the residual oceanic crust after (e.g., [124]). In addition, as the mantle transition zone has dehydration is always characterized by high ðTa/UÞN , ð Þ a considerably high water content [125], the recycled Nb/Th N , Nb/U, and TiO2/Al2O3 ratios (e.g., [135, 136]). ancient sediment from the mantle transition zone could Thus, the Halaha sodic basalts with high ðTa/UÞN (>1), ð Þ – – add large amounts of water to the mantle source of potas- Nb/Th N (>1), Nb/U (46 64), and TiO2/Al2O3 (0.16 0.18) sic basalts. Therefore, we propose that the recycled ancient ratios were most likely derived from a mantle source that sediment from the mantle transition zone is the most likely contained a contribution from the recycled oceanic crust origin of the EM1 signature of the Wudalianchi-Erkeshan with the breakdown of rutile (Figure 12). In addition, the potassic basalts. high values of δ18O in the Halaha sodic basalts (cpx up to 8.57‰; [38]) also require the recycled oceanic crust and/or 5.4.2. Recycled Pacific Oceanic Crust in the Mantle Source sediment to be involved in their mantle source. This is of the Sodic Basalts. The Halaha sodic basalts have positive because the recycled oceanic crust and/or sediment could Nb and Ta anomalies and yield Ce/Pb and Nb/U ratios of have high δ18O values as a result of undergoing low- 18–25 and 46–64, respectively, resembling typical OIBs temperature (<350°C) water-rock interaction [137–139]. A (Figure 4(d); [56]). Previous studies indicate that the likely high-velocity representative of the stagnant segment of the mantle sources of OIBs are lithospheric mantle with subducted Pacific plate in the mantle transition zone beneath amphibole-bearing metasomatic veins, asthenospheric man- eastern China has been imaged by P and S wave tomography tle, or a mantle plume [126–130]. [96, 140, 141]. According to the geophysical data, the western As we argue in Section 5.3, there is no evidence that sup- edge of the stagnant Pacific slab has reached the mantle ports the presence of a deep mantle plume beneath NE China transition zone beneath the Daxing’Anling-Taihangshan during the late Cenozoic. Thus, the mantle plume model can- Gravity Lineament in eastern China, and the Halaha volca- not explain the mantle source of the Halaha sodic basalts. nic field is located close to the west of the Daxing’Anling- The model involving a recycled metasomatized lithospheric Taihangshan Gravity Lineament. Therefore, the subducted mantle proposes that the hornblendite veins that formed Pacific oceanic crust in the mantle transition zone most during the percolation and differentiation of volatile- likely provided the enriched component in the mantle bearing melts within the lithospheric mantle could be a can- source of the Halaha sodic basalts. Other volcanic fields,

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4000 5000 Olivine derivative Olivine magmas (8-20%) primary 4000 magmas Olivine 3000 (8-38%) primary Koolau magmas 3000 (8-38%) 2000 Ni (ppm) Ni Ca (ppm) 2000

1000 1000 Koolau Olivine derivative magmas (8-20%) 0 0 50 60 70 80 90 100 50 60 70 80 90 100 Fo Fo (a) (b) 5000 150

130 4000

Olivine derivative 110 Olivine 3000 magmas (8-20%) derivative magmas Koolau Olivine 90 (8-20%)

primary Fe/Mn

Mn (ppm) Mn 2000 magmas (8-38%) 70

1000 50 Koolau Olivine primary magmas (8-38%) 0 30 50 60 70 80 90 100 50 60 70 80 90 100 Fo Fo Olivine phenocrysts of potassic basalts Olivine phenocrysts of sodic basalts

Figure 10: Compositions of olivine phenocrysts in the Wudalianchi-Erkeshan potassic basalts and Halaha sodic basalts compared with calculated olivines from partial melts of peridotite and pyroxenite (the source for Koolau basalts) after Herzberg [72]. (a) Ca (ppm) versus Fo, (b) Ni (ppm) versus Fo, (c) Mn (ppm) versus Fo, and (d) Fe/Mn versus Fo.

including the Jining, Abaga, and Wulanhada basalts to the ducted slab, whereas the enriched component (Pacific oce- west of the Daxing’Anling-Taihangshan Gravity Lineament, anic crust) in the mantle source of the Halaha sodic basalts are also considered to be closely associated with the deep is likely linked to the stagnation of the recently subducted subduction of the Pacific oceanic plate [48–50, 142]. The Pacific oceanic slab. This conclusion is illustrated by the plots Halaha sodic basalts have high Ba/La (14–19) and Ba/Th of Ba/Th ratios versus 143Nd/144Nd and 206Pb/204Pb ratios (102–143) ratios, suggesting that their mantle source might (Figure 13), which also suggest that the enriched end- have a contribution from recycled sediment (Figure 8). members are ancient sediment for the potassic basalts and However, the low 143Nd/144Nd and 176Hf/177Hf ratios and Pacific oceanic crust for the sodic basalts. negative Nb and Ta anomalies of recycled subducted sediment do not match those of the Halaha sodic basalts (e.g., 5.5. Possible Genetic Relationship between the Potassic and [143, 144]), indicating that the contribution of subducted Sodic Basalts in NE China. In several areas in the Basin- sediment to the mantle source of the Halaha sodic basalts and-Range Province and the East African rift, late Ceno- is negligible. Therefore, we propose that the enriched com- zoic temporospatially related potassic and sodic basalts ponent in the mantle source of the Halaha sodic basalts is were generated from enriched lithosphere and sublitho- Pacific oceanic crust with negligible sediment, which also sphere (asthenospheric mantle or mantle plume), respec- resided in the mantle transition zone. tively [14, 15, 17, 18]. The transition from potassic to sodic In summary, the enriched component (ancient sediment) basalts in these areas was interpreted as a direct response to in the mantle source of the Wudalianchi-Erkeshan potassic lithospheric extension. In detail, initial extension triggered basalts is probably related to the stagnation of an ancient sub- melting of the enriched lithosphere to produce the potassic

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40 K-hollandite

30 Ba/La

0 0 100 200 300 400 500 600 700 Ba/T

Potassic basalts Sodic basalts Potassic basalts Sodic basalts (literature) (literature)

Figure 11: Ba/La versus Ba/Th values for the Wudalianchi-Erkeshan potassic basalts and Halaha sodic basalts. Data for K-hollandite are from Rapp et al. [119]. Other data sources are the same as those for Figure 3.

4 0.3 Oceanic crust-derived melts

3 Cenozoic basalts in eastern China 6 0.2 O N 2

2 /Al 2 Southern Tibetan (Ta/U)

TiO potassic mafc rocks Southern Tibetan potassic mafic rocks OIB 0.1 1 OAB

0 0 012 3 4 0 10 20 30 40 50 60 70

(Nb/T)N Nb/U

Sodic basalts Sodic basalts (literature) Figure ½ ½ ﬁ 12: Relationships between (a) Ta/U N and Nb/Th N and (b) TiO2/Al2O3 and Nb/U for the Halaha sodic basalts. The reference eld for the Cenozoic basalts of eastern China is from Guo et al. [49]. The data for OIB and OAB are from Niu and Batiza [135] and Kelemen et al. [133], and the data for southern Tibetan potassic maﬁc rocks are from Gao et al. [211], Zhao et al. [146], and Guo et al. [6]. Other data sources are the same as those for Figure 3.

basalts, which was followed by the decompressional melting the Wudalianchi-Erkeshan potassic basalts and Halaha sodic of upwelling sublithospheric mantle to produce the sodic basalts are suggested to be the asthenospheric mantle with basalts. Alternatively, both the potassic and sodic basalts recycled oceanic components without the involvement of were produced by partial melting of the delaminated the lithospheric mantle. There is no direct evidence of litho- enriched lithosphere [16]. The potassic basalts were devel- spheric mantle delamination having occurred in the study oped at higher pressures from deeper fragments of foun- area during the late Cenozoic. Thus, the late Cenozoic coeval dered lithosphere veined by a mica-bearing, Al-poor potassic and sodic basalts in NE China cannot have been assemblage, whereas the sodic rocks were generated at lower formed in the above way. pressures from shallower fragments of foundered litho- Coeval potassic and sodic basalts have also been reported sphere veined by an aluminous amphibole-bearing assem- in the Hong’an-Dabie orogen in eastern China. The change blage. As discussed in Section 5.4, the mantle sources for from potassic basalts (maﬁc intrusive rocks) to sodic basalts

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400 400

300 300 SS

200 200 Ba/T Ba/T

100 100 OC

0 0 0.5120 0.5124 0.5128 0.5132 16 17 18 19 20 143 144 206 204 ( Nd/ Nd)i ( Pb/ Pb)i

Potassic basalts Sodic basalts Potassic basalts Sodic basalts (literature) (literature) (a) (b)

143 144 206 204 Figure 13: (a) Ba/Th versus ð Nd/ NdÞi and (b) Ba/Th versus ð Pb/ PbÞi for the Wudalianchi-Erkeshan potassic basalts and Halaha sodic basalts. The Ba/Th ratios for DMM, Paciﬁc oceanic crust (OC), and recycled ancient subducted sediment (SS) are from Workman and Hart [199], Kelley et al. [212], and Plank and Langmuir [143], respectively. The 143Nd/144Nd and 206Pb/204Pb ratios of DMM, Paciﬁc oceanic crust (OC), and recycled ancient subducted sediment (SS) are from Workman and Hart [199], Mahoney et al. [213], and Stracke et al. [144], respectively. Other data sources are the same as those for Figure 3.

(mafic dikes) in the Hong’an-Dabie orogen has been attrib- been introduced to the deep mantle during an ancient sub- uted to mantle sources with distinct recycled crustal mate- duction event (i.e., ancient sediment). rials (oceanic crust versus continental crust) [19–21]. In the Because rutile is a key mineral for storing HFSEs, partial following discussion, we suggest that partial melting of the melting of the oceanic crust with the breakdown of rutile will mantle source with different recycled oceanic materials give rise to felsic melts in which Nb and Ta are enriched [150, (ancient sediment versus Pacific oceanic crust) could have 151]. Meanwhile, the oceanic crust could have high produced the coeval Wudalianchi-Erkeshan potassic basalts Na2O/K2O values and depleted the Sr-Nd-Hf radiogenic iso- and Halaha sodic basalts. topic compositions (e.g., [144, 152]). Thus, partial melting of Experimental studies have shown that partial melting of the mantle source with recycled oceanic crust with the break- fertile peridotite fluxed by hydrous sediment can generate down of rutile could generate sodic basalts with OIB-like (ultra)potassic magmas [145]. This hydrous sediment is gen- trace-element distribution patterns (i.e., enrichment of LILEs erally enriched in K2O, LILEs, and Sr-Nd-Hf radiogenic iso- and LREEs but with no depletion of HFSEs) and depleted topic compositions but depleted in HFSEs (e.g., [143, 144]). radiogenic Sr-Nd-Hf isotopic signatures. Experimental stud- The partial melting of a mantle source with recycled sedi- ies have further shown that partial melting of a mixed source ment would generate (ultra)potassic rocks with such features. of oceanic crust and fertile peridotite could generate sodic The Pb isotopic composition of (ultra)potassic rocks is basalts with OIB-like characteristics (e.g., [153, 154]). The strongly affected by the duration of isolation of the possible Pb isotopic system of sodic basalts with OIB-like characteris- sources, where short isolation causes samples to plot to the tics is sensitive to variations in the age of the recycled oceanic right of the Geochron (Figure 5(d)), and long isolation (i.e., crust and can be divided into basalts of typical HIMU islands from ancient subduction events) causes samples to plot to such as St. Helena, Tubuaii, and Mangaia (206Pb/204Pb = the left of the Geochron as a result of the significant retarda- 20:5‐22; [155, 156]) and basalts of young HIMU islands such tion of 206Pb/204Pb ratios [124]. For example, (ultra)potassic as La Palma and El Hierro (Canary Islands) (206Pb/204Pb = rocks from the western Mediterranean and southern Tibet 18:8‐20; Thirlwall et al., 1997; [157, 158]). The Pb isotopic are interpreted as having been derived from a mantle source difference between the typical and young HIMU island with recently recycled sediment and plot to the right of the sources depends on the age of the recycled materials and Geochron (Figure 5(d); [5–9, 146]). In contrast, the (ultra)- the presence of a small amount of sediment (e.g., [159]). potassic rocks from Western Australia, Leucite Hills, and The typical HIMU basalts with high 206Pb/204Pb values indi- Gaussberg plot to the left of the Geochron and are inter- cate that oceanic crust was recycled into their mantle source preted as having been derived from the mantle transition at least 2 Gyr ago (Hofmann, 1988; [160]). In contrast, the zone with ancient sediment that was isolated for more than young HIMU basalts with relatively low 206Pb/204Pb values ~2 Gyr (Figure 5(d); [124, 147–149]). The Wudalianchi- require recycled oceanic crust to have been incorporated into Erkeshan potassic basalts have 206Pb/204Pb ratios similar to their mantle more recently [159, 161, 162] because the those of the (ultra)potassic basalts from Western Australia. recently recycled oceanic crust in the mantle would have Thus, we interpret that this isotopic signature is likely to have had insufficient time to produce high Pb isotopic ratios. If a

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source contained oceanic crust without the long time- 7. Implications for Asthenospheric integrated ingrowth of Pb isotope systems, a resulting basal- Mantle Heterogeneity tic melt that is less enriched in radiogenic Pb isotopes is possible. The Halaha sodic basalts have radiogenic 206Pb/204Pb The asthenospheric component is commonly considered to (18.27–18.40) values that are slightly lower than those of have been depleted by previous melting events but subse- the young HIMU basalts (18.8–20.0), suggesting that the quently homogenized by convective stirring (e.g., [86]). recycled oceanic crust in their mantle source is related to a However, the deduced mantle sources (ambient DMM, recent subduction event (Pacific oceanic crust). two types of pyroxenite) for the potassic and sodic basalts We therefore propose that partial melting of the ambient indicate that the upper asthenospheric mantle beneath NE DMM with recycled ancient sediment would produce the China is highly heterogeneous. Recent studies of early Wudalianchi-Erkeshan potassic basalts, whereas partial Cenozoic basalts in the Songliao Basin have concluded that melting of the ambient DMM and recycled Pacific oceanic chemical heterogeneity was present in the asthenospheric crust would develop the Halaha sodic basalts. The transition mantle beneath this basin [37, 42]. These combined results from the potassic to the sodic basalts in NE China could be a show that the upper asthenospheric mantle beneath NE result of the difference in the recycled components incorpo- China may have been temporospatially heterogeneous dur- rated into their mantle sources, namely recycled ancient sed- ing the Cenozoic. iment and recent Pacific oceanic crust, respectively. Various lines of evidence suggest that the upper asthenospheric mantle is indeed incompletely homogenized on a 6. An Integrated Model for Late Cenozoic global scale. First, MORBs in the Indian and the southern Magmatism in NE China Atlantic oceans have distinctive isotopic compositions with relatively high 87Sr/86Sr and 208Pb/204Pb values for a given The deep-Earth cycling of fluids [125, 163, 164] due to the 206Pb/204Pb value, referred to as the Dupal anomaly [53, presence of water-enriched wadsleyite and ringwoodite in 175]. The Dupal anomaly was initially considered to imply the mantle transition zone [125, 165–167] may cause the existence of hemispheric-scale fertile geochemical hetero- Rayleigh-Taylor instabilities and generate wet plumes [168, geneity in the southern hemisphere upper asthenospheric 169]. Once wet plumes are generated, they could transport mantle. Subsequent studies established that the Dupal anom- oceanic materials (ancient sediment and recent Pacific crust) aly signature was also present along the mid-ocean ridges of from the mantle transition zone into the overlying upper the northern Atlantic [176, 177] and Arctic [178] oceans. asthenospheric mantle (Figure 14(a)). When these recycled The Dupal anomaly requires an enriched component to be oceanic materials were transported into the asthenospheric dispersed in the upper asthenospheric mantle. This enriched mantle, they could melt preferentially to the ambient perido- component has been suggested as being either delaminated titic mantle owing to the recycled oceanic components hav- recycled continental crust and/or ancient SCLM during the ing a lower solidus than peridotite [170, 171]. The recycled early rifting stages of Gondwana (e.g., [178–183]) or lower melt derived from oceanic components could react with continental crust and recycled pelagic sediment together with mantle peridotite and convert it to pyroxenite by forming altered oceanic crust from a deep mantle plume, possibly at orthopyroxene at the expense of olivine (e.g., [154, 172, the edge of a large low-shear-velocity province (e.g., [184– 173]). This is consistent with the mantle lithologies inferred 187]). Second, decoupling of Hf and Nd isotopes in some in this study for both potassic and sodic basalts in NE China, MORBs indicates that the asthenospheric mantle has a com- which have mixed sources of peridotite and pyroxenite. The ponent of ancient refractory domains, which were probably recycled ancient sediment would react with the astheno- characterized by an extremely enriched Hf isotopic composi- spheric mantle peridotite in generating the EM1-like pyroxe- tion (e.g., [188]). The observed very depleted 187Os/188Os nite, providing the enriched component for Wudalianchi- (<0.12) and εHf (up to 104) compositions found in some Erkeshan potassic basalts (Figure 14(b)), while the recycled abyssal peridotites [189–192] are considered as solid evi- Pacific oceanic crust would react with the asthenospheric dence for the presence of such ancient refractory mantle mantle peridotite to generate young HIMU-like pyroxenite, domains in the upper asthenospheric mantle. These ancient providing the enriched component for Halaha sodic basalts residual mantle domains in the upper asthenospheric mantle (Figure 14(b)). Therefore, the asthenospheric mantle beneath are argued to be either ancient residual oceanic lithosphere NE China was not homogeneous and these two types of (ReLish) or SCLM reservoirs that underwent previous deple- pyroxenite (EM1-like and young HIMU-like) may be dis- tion events followed by carbonatite-type metasomatism tributed as blobs, veinlets, or streaks within the upper [188, 193–195]. asthenospheric mantle, resembling a “plum-pudding” struc- The heterogeneity of the upper asthenospheric mantle ture (e.g., [174]). During the Cenozoic, NE China was in a can thus be attributed to at least three components: a nor- continental extensional setting due to the rollback of the mally depleted MORB mantle (DMM), an ancient residual Pacific slab and associated trench retreat [47]. In this exten- lithospheric mantle (ReLish or SCLM), and enriched recycled sional setting, partial melting of the upwelling heteroge- oceanic components as inferred in the present study neous asthenospheric mantle comprising ambient DMM (Figure 15). Therefore, the asthenospheric mantle is not a and the two types of pyroxenite produced the Wudalianchi- well-stirred and chemically homogenized mantle but could Erkeshan potassic basalts and Halaha sodic basalts, respec- be highly heterogeneous on both local (e.g., NE China) and tively (Figures 14(c) and 14(d)). global scales. As a result, using MORBs or abyssal peridotite

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Potassic basalts Sodic basalts (a) Sodic basalts Potassic basalts Figure 1(b) (c) 0 km (d) 0 km Japan Sea

Lithosphere Pyroxenite Lithosphere Lithosphere

Asthenosphere Wet plume

Subducted Pacifc Slab

410 km

Mantle transition zone Subducted Pacifc Slab Asthenosphere Asthenosphere 660 km 300 km 300 km

DMM (peridotite) DMM Ancient subducted sediment EM1-like pyroxenite Pacific oceanic crust Two types of pyroxenite Young HIMU-like pyroxenite

Figure 14: Petrogenetic model for the Wudalianchi-Erkeshan potassic basalts and the Halaha sodic basalts. (a) The subducted Paciﬁc slab stagnates in the mantle transition zone beneath NE China. (b) The ascent of wet plumes would transport the recycled oceanic components from the mantle transition zone into the above upper asthenosphere, which would react with mantle peridotite in producing two kinds of mantle pyroxenite. (c and d) Partial melting of the mantle source (ambient DMM and two kinds of mantle pyroxenite) would produce the Wudalianchi-Erkeshan potassic basalts and the Halaha sodic basalts during late Cenozoic, triggered by a rollback of the deeply subducted Paciﬁc slab.

Residual component

Lithosphere

Asthenosphere Enriched component

Figure 15: Schematic diagram of the upwelling asthenospheric mantle (modiﬁed from [191]). Both the enriched component and the ancient residual oceanic mantle component (ReLish or SCLM) are distributed among the “matrix” of normally depleted MORB mantle (DMM).

for estimating the average isotope compositions of the upper and 206Pb/204Pb values. We suggest that ancient sediment asthenospheric mantle needs to be undertaken with caution. and recent Paciﬁc oceanic crust in the mantle transition zone are the respective enriched end-members in the mantle 8. Conclusion sources of the potassic and sodic basalts. As wet plumes ascend through the upper mantle, they may bring up preex- The late Cenozoic Wudalianchi-Erkeshan potassic basalts isting recycled materials (ancient sediment and Paciﬁc oce- and Halaha sodic basalts were coeval in NE China. The anic crust) from the mantle transition zone into the above potassic and sodic basalts originated mainly from DMM asthenospheric mantle. These recycled materials could melt and an enriched end-member. The enriched end-member preferentially relative to the ambient peridotitic mantle to in the mantle source of the potassic basalts has an EM1-like produce silicic melts, which would react with mantle perido- signature with relatively low 143Nd/144Nd, 176Hf/177Hf, and tite to produce the two kinds of mantle pyroxenite (EM1-like 206Pb/204Pb contents and negative Nb and Ta anomalies but and young HIMU-like pyroxenite). high Ba/La and Ba/Th values, whereas the enriched end- The partial melting of the upper asthenospheric mantle member in the mantle source of the sodic basalts has high comprising the ambient DMM and these two kinds of pyrox- 143 144 176 177 ðTa/UÞN , ðNb/ThÞN , radiogenic Nd/ Nd, Hf/ Hf, enite produced the potassic and sodic basalts in NE China,

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