Geochemical characteristics of Late Paleozoic–Early Mesozoic volcanic rocks in Heiyingshan, Beishan Orogenic Belt: evidence of the transition from subduction to collision of the Paleo-Asian Ocean
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摘要: 黑鹰山地区位于北山造山带北缘，是研究北山造山带古亚洲洋演化的关键地区。文章对黑鹰山地区出露的晚石炭世、晚三叠世火山凝灰岩进行了岩石地球化学研究。研究结果表明，晚石炭世火山凝灰岩属于过铝质钙碱性系列，富集大离子亲石元素（LILE）Rb、Ba、Th、U，亏损高场强元素Nb、Ta、Zr、Hf、Ti；稀土元素总量（ΣREE）为74.64×10−6～142.45×10−6，轻/重稀土分馏明显（LREE/HREE=5.14～7.49、（La/Yb）N=4.58～6.36），稀土元素配分模式呈右倾特征，具有弱的负Eu异常（δEu=0.35～0.66），表现出类I型花岗岩特征。晚三叠世火山凝灰岩属于弱过铝质高钾钙碱性系列，富硅、碱，贫铝、镁，具有强烈的Eu负异常（δEu=0.02～0.22）；稀土元素配分模式呈略微右倾的“海鸥型”，富集Rb、Th、U等大离子亲石元素，亏损Ba、Nb、Zr、Ti等不相容元素，具有类S型花岗岩的特征。黑鹰山地区晚石炭世和晚三叠世火山凝灰岩分别形成于北山地区古亚洲洋俯冲和碰撞的构造环境，岩浆来源主要为地壳熔融，指示晚石炭世至晚三叠世红石山—黑鹰山一带可能发生了构造环境的转变。Abstract:
Objective It is generally accepted that the Paleo-Asian Ocean in the northern part of the Beishan Orogenic Belt was in the stage of ocean–continent evolution during the Carboniferous–Permian. However, the timing of the closure of the Paleo-Asian Ocean remains controversial. The Heiyingshan area, located at the northern margin of the Beishan Orogenic Belt, is a key area for studying the evolution of the Paleo-Asian Ocean. This study analyzes the geochemical characteristics of tuffs in this area to reveal their tectonic setting and further constrain the evolution of the Paleo-Asian Ocean in the northern Beishan Orogenic Belt. Methods Late Carboniferous and Late Triassic volcanic tuffs exposed in the Heiyingshan area were analyzed using petrological and geochemical methods. Major, trace, and rare earth elements concentrations were determined to obtain the geochemical characteristics of the volcanic tuffs. Combined with published regional volcanic rock ages and geochemical data, the petrogenesis and tectonic setting of the volcanic tuff are discussed. Results The Late Carboniferous volcanic tuff belongs to the peraluminous calc-alkaline series; it is enriched in large ion lithophile elements (LILE; i.e., Rb, Ba, Th and U) and depleted in high field strength elements (HFSE; i.e., Nb, Ta, Zr, Hf and Ti). The total rare earth element content (ΣREE) ranges from 74.64×10−6 to 142.45×10−6, with significant fractionation between light and heavy REEs (LREE/HREE=5.14–7.49, (La/Yb)N=4.58–6.36). The chondrite-normalized REE distribution pattern is right-leaning, with a weak negative Eu anomaly (δEu=0.35–0.66). These characteristics are indicative of I-type granite. The Late Triassic volcanic tuff belongs to the peraluminous high-K calc-alkaline series. It is enriched in silicon and alkali but depleted in aluminum and magnesium. This tuff exhibits a strong negative Eu anomaly (δEu=0.02–0.22). Its chondrite-normalized REE distribution pattern is a slightly right-leaning ‘seagull type’. This tuff is enriched in LILE, (e.g., Rb, Th and U), depleted in incompatible elements (e.g., Ba, Nb, Zr and Ti), and depleted in HFSE, (e.g., Hf and Zr). These characteristics are typical of S-type granite. The Th content of the Late Carboniferous and Late Triassic rock samples in the Heiyingshan area ranges from 7.66 to 32.2μg/g, with an average of 19.24μg/g, which is much higher than the average mantle abundance and closer to the crust. The Nb/Ta ratios of the rock samples range from 8.01 to 12.78, with an average of 10.36, which is much lower than the mantle average of 60 and closer to the crust average of 11. In addition, the Ba/La ratios of the Late Carboniferous volcanic rocks range from 19.19 to 24.09, with an average of 21.64, slightly higher than the continental crust average of 15.63. Conclusion The Late Carboniferous and Late Triassic volcanic tuffs in the Heiyingshan area formed in the subduction and collision setting of the Paleo-Asian Ocean, respectively, indicating that the tectonic environment in the Hongshishan-Heiyingshan area transitioned from subduction to collision between the Late Carboniferous and the Late Triassic. The volcanic magma in this area was mainly derived from partial melting of the crust, with the Late Carboniferous volcanic rocks possibly mixed with a small amount of mantle-derived materials. [ Significance ] The geochemical characteristics of the Late Carboniferous and Late Triassic volcanic tuffs in the Heiyingshan area provide evidence for the subduction–collision processes of the Paleo-Asian Ocean in the Beishan Orogenic Belt. The results constrain the timing of the tectonic environment transformation in the Hongshishan–Heiyingshan area in the northern Beishan Orogenic Belt, which is of great significance for understanding the closure of the Paleo-Asian Ocean. -
图 1 北山地区地质图（据Zhang and Cunningham，2012修改）
Figure 1. Geological map of the Beishan area (modified after Zhang and Cunningham, 2012)
图 2 北山造山带北部黑鹰山地区地质图（底图据邵兆刚等，2024修改；年龄数据来源于邵兆刚等，2024）
Figure 2. Geological map of Heiyingshan area in the northern Beishan Orogenic Belt (modified after Shao et al., 2024; age data are cited from Shao et al., 2024)
图 3 北山北部黑鹰山地区构造解译图、野外及岩石显微照片
Pl—斜长石；Q—石英a—黑鹰山凝灰岩与上覆推覆体构造关系；b—凝灰岩露头照片；c—晚三叠世流纹质晶屑凝灰岩显微照片（样品号：HYS0919-4）；d—晚三叠世流纹质晶屑凝灰岩斑晶中的流体−熔体包裹体（样品号：HYS0919-5）；e—晚三叠世流纹质晶屑凝灰岩显微照片（样品号：HYS0919-6）；f—晚石炭世流纹质晶屑凝灰岩显微照片（样品号：HYS0919-1）；g—晚石炭世流纹质晶屑凝灰岩显微照片（样品号：HYS0919-3）
Figure 3. Google Earth satellite image, field photo, and rock micrographs of the Heiyingshan area in northern Beishan
(a) Structural relationship between the tuff and the overlying nappe in the Heiyingshan area; (b) Field photograph of a tuff outcrop; (c) Microphotograph of a Late Triassic rhyolitic crystal tuff (sample no.:HYS0919-4); (d) Fluid-melt inclusion in phenocrysts of a Late Triassic rhyolitic crystal tuff (sample no.: HYS0919-5); (e) Microphotograph of a Late Triassic rhyolitic crystal tuff (sample no.: HYS0919-6); (f) Microphotograph of a Late Carboniferous rhyolitic crystal tuff (sample no.: HYS0919-1); (g) Microphotograph of a Late Carboniferous rhyolitic crystal tuff (sample no.: HYS0919-3) Pl—plagioclase; Q—quartz
图 4 黑鹰山及邻区火山岩主量元素地球化学特征
邻区晚石炭世火山岩引自文献郝增元等，2020；李敏等，2018；徐旭明等，2018；朱炜等，2019；邻区晚三叠世火山岩数据引自黄增保等，2011；李敏等，2020；杨镇熙等，2021；图(a)中数字代表不同火山岩类型：1—玄武岩；2a—玄武安山岩；2b—低碱玄武岩；3—安山岩；4—英安岩；5—流纹岩；6—碱性流纹岩；7—粗面岩；8—粗面安山岩；9—碱性粗面安山岩；10—粗面英安岩；11—碱性粗面岩；12—响岩；13—碱性玄武岩；14—霞石粗面岩；15—霞石岩。Ir为Irvine分界线，用于区分碱性与亚碱性系列（据Bas et al., 1986）a—TAS图解（Bas et al.，1986）；b—A/CNK-A/NK图解（Maniar and Piccoli，1989）；c—K2O-SiO2图解（Peccerillo and Taylor，1976）；d—SiO2-AR图解（Wright，1969）
Figure 4. Major element geochemical characteristics of volcanic rocks in the Heiyingshan and adjacent areas
In panel (a), numbers correspond to different volcanic rock fields: 1—basalt; 2a—basaltic andesite; 2b—basaltic andesite (low-SiO2); 3—andesite; 4—dacite; 5—rhyolite; 6—alkaline rhyolite; 7—trachyte; 8—trachyandesite; 9—alkaline trachyandesite; 10—trachydacite; 11—alkaline trachyte; 12—phonolite; 13—tephrite/basanite; 14—phonotephrite; 15—foidite. Ir denotes the Irvine line separating alkaline and subalkaline series. after Le Bas et al. (1986)(a) TAS diagram of volcanic rocks (Bas et al., 1986); (b) A/CNK–A/NK diagram (Maniar and Piccoli, 1989); (c) K2O–SiO2 diagram (Peccerillo and Taylor, 1976); (d) SiO2–AR diagram (Wright, 1969)
图 5 黑鹰山及邻区火山岩微量元素地球化学特征
邻区晚石炭世火山岩引自文献郝增元等，2020；李敏等，2018；徐旭明等，2018；朱炜等，2019；邻区晚三叠世火山岩数据引自黄增保等，2011；李敏等，2020；杨镇熙等，2021；a—原始地幔标准化微量元素蛛网图；b—球粒陨石标准化稀土配分曲线（原始地幔值和球粒陨石据Sun and McDonough，1989）
Figure 5. Trace element geochemical characteristics of volcanic rocks in the Heiyingshan and adjacent areas
(a) Primitive mantle-normalized trace element spider diagram; (b) Chondrite-normalized REE patterns (chondrite and primitive mantle values are from Sun and McDonough, 1989)
图 6 黑鹰山及邻区火山岩成因类型图解（底图据Collins et al.，1982）
邻区晚石炭世火山岩引自文献郝增元等，2020；李敏等，2018；徐旭明等，2018；朱炜等，2019；邻区晚三叠世火山岩数据引自黄增保等，2011；李敏等，2020；杨镇熙等，2021
Figure 6. Genetic discrimination diagram of volcanic rocks in the Heiyingshan and adjacent areas (base map after Collins et al., 1982)
图 7 北山造山带北部岩浆岩分布图（卫彦升等，2020）
Figure 7. Simplified geological map showing the distribution of magmatic rocks in the northern Beishan Orogenic Belt (modified after Wei et al., 2020)
图 8 黑鹰山及邻区火山岩构造环境判别图
邻区晚石炭世火山岩引自文献郝增元等，2020；李敏等，2018；徐旭明等，2018；朱炜等，2019；邻区晚三叠世火山岩数据引自黄增保等，2011；李敏等，2020；杨镇熙等，2021WPG—板内环境；VAG—火山弧环境；syn-COLG—同碰撞环境；ORG—大洋中脊环境a—Rb-Nb+Y；b—Rb-Yb+Ta（底图据Pearce et al.，1984）
Figure 8. Tectonic discrimination diagrams for volcanic rocks in the Heiyingshan and adjacent areas
(a) Rb vs. Nb + Y; (b) Rb vs. Yb + Ta; (base map after Pearce et al., 1984) WPG—within-plate environment; VAG—volcanic arc environment; syn-ORG—syn-collisional environment; ORG—mid-ocean ridge environment
图 9 北山造山带北部构造演化模式图
a—晚石炭世古亚洲洋向南俯冲作用；b—晚三叠世碰撞作用
Figure 9. Schematic sketch of the tectonic evolution of the northern Beishan Orogenic Belt
(a) Late Carboniferous southward subduction of the Paleo-Asian Ocean; (b) Late Triassic collision
表 1 黑鹰山火山岩的主量元素（%）、微量元素（×10−6）和稀土元素（×10−6）分析结果
Table 1. Major (wt%) and trace and rare earth element (×10−6) compositions of volcanic rocks from the Heiyingshan area
样品号 HYS0919-1 HYS0919-3 HYS0919-4 HYS0919-5 HYS0919-6 HYS0914-3 SiO2 78.29 77.02 78.45 80.86 79.50 78.34 TiO2 0.20 0.07 0.03 0.05 0.05 0.04 Al2O3 11.49 12.00 9.82 9.26 9.57 12.39 Fe2O3T 1.52 1.37 0.89 0.76 0.66 0.56 MnO 0.06 0.03 0.01 0.01 0.01 0.02 MgO 0.38 0.07 0.15 0.43 0.17 0.13 CaO 0.81 0.65 0.56 0.43 0.71 0.18 Na2O 5.18 4.26 0.86 0.59 0.50 2.46 K2O 2.08 3.22 7.02 5.30 6.05 4.62 P2O5 0.04 0.01 <0.01 <0.01 <0.01 <0.01 烧失量 1.36 1.35 1.79 2.31 2.02 1.03 总量 100.18 100.05 99.58 100 99.24 99.77 Rb 25.0 78.7 228 276 388 105.5 Ba 284 641 385 151 367 480 Th 7.66 11.65 21.80 24.30 32.20 17.80 U 2.25 3.25 6.94 5.76 6.52 7.28 Ta 0.43 0.60 2.91 2.95 3.38 0.82 Nb 4.7 6.5 23.30 37.70 39.10 6.6 Sr 131.5 58.4 60.0 136.0 90.4 121.5 Zr 113 148 99 88 111 82 Hf 3.3 4.9 5.4 5.0 5.8 3.9 La 14.8 26.6 23.8 8.1 36.8 16.9 Ce 32.2 53.8 47.5 22.4 88.1 36.5 Pr 3.37 6.68 7.53 3.06 13.45 4.38 Nd 12.5 25.7 35.4 14.1 66.5 16.8 Sm 2.47 5.81 10.05 3.98 22.9 4.04 Eu 0.51 0.65 0.12 0.06 0.14 0.30 Gd 2.19 5.52 9.02 3.88 22.4 4.25 Tb 0.35 0.95 1.34 0.81 3.61 0.78 Dy 2.13 5.98 7.03 5.74 18.85 5.19 Ho 0.49 1.38 1.43 1.34 3.52 1.23 Er 1.44 3.93 3.70 4.13 10.25 3.72 Tm 0.24 0.62 0.56 0.70 1.57 0.62 Yb 1.67 4.17 3.69 5.03 10.50 4.19 Lu 0.28 0.66 0.56 0.78 1.72 0.66 Y 13.1 34.8 33.5 29.5 96.8 31.1 ΣREE 74.64 142.45 151.73 74.11 300.31 99.56 LREE/HREE 7.49 5.14 4.55 2.31 3.15 3.82 （La/Yb）N 6.36 4.58 4.63 1.16 2.51 2.89 δEu 0.66 0.35 0.04 0.05 0.02 0.22 注：δEu=Eu/(SmN×GdN)1/2（Taylor and McLennan，1985）；其中下标N为球粒陨石标准化值（Sun and McDonough，1989） 
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