| Citation: | Fangpeng Du, Furong Tan, Shiming Liu, Xiaochen Zhao, Yingtao Chen, Junwei Qiao. First Discovery of Late Triassic Tuffs in the South Qilian Basin: Geochemical Characteristics, Zircon LA-ICP-MS U-Pb Ages and Potential Source Regions. Journal of Earth Science, 2023, 34(6): 1692-1703. doi: 10.1007/s12583-021-1446-7
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This investigation reports the first discovery of more than 70 tuff intervals in the Upper Triassic, South Qilian Basin. Petrographic and geochemical analyses were carried out on ten tuff samples and zircon U-Pb dating were on three. Thin section and X-ray diffraction (XRD) results indicate that the tuffs were composed of crystal shards and altered glass shards; crystal shards include plagioclase and quartz. Most of the tuffs had been transformed into illite/smectite mixed-layers (I/S). In addition, calcite, pyrite, dolomite and siderite were also identified in some of the tuff samples. Analysis of major elements suggests that the tuffs are peraluminous high-K calcalkaline series. Trace elements indicate that the tuffs are enriched in high field strength elements (HFSE), including Th, U, Ta, Zr and Hf. Geochemical characteristics suggest that the tuffs originated from comendite pantellerite and rhyolite from within plate setting. Zircon U-Pb dating (236.0 ± 1.7, 231.4 ± 1.6, and 223.1 ± 3.9 Ma) indicate that the tuffs were erupted in the Late Triassic. Comparative chronology and geochemical analyses suggest that the West Qinling belt and the East Kunlun belt are the potential source regions of these tuffs, and they originated from the within plate magma during a post-collisional period.
Significant temporal and material composition information on volcanic activity are recorded in tuffs; magmatic and tectonic setting information of source volcanoes can also be inferred from these deposits (Mai et al., 2021; Ellis et al., 2019; MacDonald et al., 2019; Mahar et al., 2019; Yang et al., 2019; Jin et al., 2018; Grevenitz, et al., 2003). Due to their isochronism and widespread distribution, tuff intervals are critical basis for stratigraphic correlation and for defining stratigraphic ages (Astini et al., 2007; Min et al., 2001). In addition, tuffs are also important for hydrocarbon source rocks in many sedimentary basins (Parrish, 2013; Lin et al., 2011; Gaibor et al., 2008; Su et al., 2003; Dawson, 2000). Therefore, analysis of material composition and isotopic chronology of tuffs have provided important geological information.
The South Qilian Basin located at the Central Orogenic Belt of China, and the belt completed its collision and amalgamation in the Late Triassic (Peng et al., 2023; Wang et al., 2021; Kong et al., 2020; Zhao et al., 2018; Dong et al., 2016). At the same time, the sedimentary environment in the basin was transformed from marine-coastal to continental lake (Fu and Zhou, 1998). As the occurrence of the environmental shift lacks precise time constraints, the discovery of tuff intervals in the Late Triassic may provide a constraint for the conversion age. Over 70 tuff intervals were discovered in the Galedesi Formation, Upper Triassic, from a core (ZK6-6) extracted in Muli sag, South Qilian Basin. To date, no volcanic activity had been reported at the Upper Triassic in the South Qilian Basin. Formation age of the tuff intervals using zircon U-Pb isotopic chronology provides important information regarding formation time, so that the tuffs are significant for time constraint of the Triassic successions and the conversion time node in the South Qilian Basin. In addition, tuffs are the links between original regions and the sedimentary basin which can help to build coupling relationships. However, determination of potential source regions is the basis for relationship building, and petrographic and geochemical characteristics of tuffs are significant to determine source regions.
The Galedesi Formation, a potential hydrocarbon source rock with black shale (Mao et al., 2022; Tan et al., 2017), has been documented to contain several tuff intervals. Previous studies have suggested that enriched transition metal elements and radioactive elements are responsible for tuffs promoting the formation of high-quality hydrocarbon source rocks (Wang et al., 2018; Mao et al., 2012). Therefore, elemental composition analysis and U-Pb isotopic dating of tuff intervals in the Upper Triassic of South Qilian are significant for studies on basin evolution and the genesis of high-quality hydrocarbon source rocks in the Upper Triassic.
The Qilian tectonic belt is part of the Central Orogenic Belt in China, located at the border of the Paleo-Tethys tectonic domain and the Paleo-Asian tectonic domain. The Central Orogenic Belt was amalgamated in the Late Triassic and converted via intracontinental tectonic activity (Kong et al., 2020; Zhao et al., 2018). Correspondingly, volcanic rocks and tuffs are widely distributed in the Upper Triassic in the Central Orogenic Belt and its adjacent tectonic units, including West Qinling, East Kunlun, Qiangtang, Songpan-Ganzi, North Qinling and the southern Ordos Basin (Liu et al., 2019; Peng et al., 2019; Yang et al., 2018; Hu et al., 2016; Qiu et al, 2014; Fu et al., 2010).
Collision and amalgamation of the Central Orogenic Belt occurred during the Indosinian period, having a significant influence on regional geological evolution (Guo et al., 2009). Well ZK6-6 from Muli sag is located in the middle part of the Qilian tectonic belt, being part of the South Qilian Basin in the Triassic. The South Qilian Basin is bounded by the Qilian fold belt in the northeast, the Zongwulong structural belt in the southwest, and connected with the West Qinling in the southeast (Fig. 1). This belt was controlled and influenced by several tectonic units in different periods, such as North China, Qilian, Qaidam, East Kunlun, West Qinling, Songpan-Ganzi and Yangtze cratons (Xie et al., 2011; Pan et al., 2009).
The South Qilian Basin was a marine and coastal sedimentary basin from the Carboniferous to the Middle Triassic, which was sedimented on the folded basement of the Early Paleozoic (Yao et al., 2019). During the Late Triassic, it transformed into a continental basin as a result of collision and amalgamation to the south of the basin. The Atasi Formation, the first sedimentary strata in Late Triassic with thick sandstone, is overlain by the Galedesi Formation, having semi-deep lacustrine shale (Yao et al., 2019) and sandstone (Fig. 1b). The Galedesi Formation provides an insight into the evolution of the continental South Qilian Basin.
Samples were collected from well ZK6-6, with a 910 m long core (Fig. 1c), collected by the Qinghai Bureau of Coal Geology, China National Administration of Coal Geology. Ten tuffs were sampled for analysis from the 70 tuff intervals identified between 153–318 m in this core (Fig. 2). As the well was located on a thrust nappe, the sequence in the well may be partially reversed.
Mineralogical analyses were undertaken using thin sections and XRD analysis. Tuff samples were made into slices before being examined under a petrographic microscope to determine mineral composition and morphology. Mineral composition of the samples was determined by X-ray powder diffraction (XRD) using a D8 Discover with a stepwise scanning of 0.02°. The scanning range of the whole rock was 5° to 45° 2θ, and the clay was scanned three times with the scanning ranges of 2.5–15°, 2.5–30° and 3–15° 2θ, respectively.
Tuff samples were crushed to powder and passed through a 200 mesh prior to chemical analyses. Major element concentrations were measured by XRF (Rikagu RIX 2100), with an error of < 5% indicated by the international standards (BHVO-2 and AGV-2). Trace element concentrations were determined by ICP-MS (Agilent 7500a) after the sample powders were digested with HNO3/HF + H3BO3. The error for most trace elements was < 5%.
Three samples (T-01, T-05 and T-07) were selected for zircon U-Pb dating, and twenty-four zircons were selected from each tuff sample. A petrographic microscope was used to separate zircons from the samples. After sample preparation, zircons were analyzed using transmitted and reflected light and cathodoluminescence (CL) imaging. Laser ablation multi-collector inductively coupled plasma mass spectrometer (LA-ICP-MS) zircon U-Pb isotopic dating was performed in the State Key Laboratory of Continental Dynamic, Northwest University, using an Agilent 7500a quadruple (Q)-ICPMS instrument. The operation conditions and calculation methods followed those reported in Liu et al. (2010). The 206Pb/238U ages were calibrated using zircon 91500 as an external standard (Yuan et al., 2003).
Tuff intervals were prominent in the black mudstone of the Galedesi Formation, with greyish-buff and brownish red colors in the cores of the well ZK6-6 (Fig. 3). Tuff thickness varied from 0.3 to 65 cm, and the gross thickness of all identified tuff intervals was over 4.5 m. Under a petrographic microscope, clay minerals were found to be the most dominant composition in the tuffs, and various crystal shards were observed dominated by angular quartz and plagioclase. Calcite was also observed in several tuff intervals, mainly appearing as cement without fixed shapes (Fig. 4). Heavy minerals were also present, including pyrite and zircon.
The XRD mineral composition results (Table 1) and XRD diagrams for whole rock and clay separation (Fig. 5) indicate that tuffs in ZK6-6 were mainly composed of clay minerals, plagioclase, quartz, calcite, pyrite, dolomite and siderite were also identified in some of the tuff intervals. Specifically, tuffs were dominated by clay minerals (58.2%–92.9%), in which the illite/smectite (I/S) mix layer accounted for 96%–99%; kaolinite and chlorite accounted for the remainder. Quartz and plagioclase accounted for 2.0%–5.9% and 4.2%–35.8%, respectively. Calcite was detected in samples T-01, T-02, T-03 and T-06, with amounts varying from 1.0% to 8.4%. Pyrite amounts varied from 0.2% to 4.4% in samples T-03, T-04, T-05, T-06 and T-10. Dolomite was only detected in sample T-09 (1.2%) and siderite was only detected in sample T-08 (3.9%).
| Sample | Relative content of clay minerals (%) | Whole rock quantitative analysis (%) | ||||||||||
| Kaolinite | Chlorite | I/S | %S | Total clay | Quartz | Plagioclase | Calcite | Dolomite | Pyrite | Siderite | ||
| T-01 | 1 | 1 | 98 | 25 | 85.3 | 2.1 | 4.2 | 8.4 | ||||
| T-02 | 2 | 1 | 97 | 25 | 86.9 | 5.9 | 4.4 | 2.8 | ||||
| T-03 | 1 | 1 | 98 | 25 | 58.2 | 4.7 | 35.8 | 1.3 | ||||
| T-04 | 2 | 1 | 97 | 25 | 89.9 | 4.8 | 4.3 | 1 | ||||
| T-05 | 3 | 1 | 96 | 25 | 62 | 5 | 21.8 | 6.8 | 4.4 | |||
| T-06 | 1 | 2 | 97 | 25 | 88.4 | 2 | 9.6 | |||||
| T-07 | 1 | 99 | 25 | 87.3 | 3.5 | 8 | 1 | 0.2 | ||||
| T-08 | 1 | 2 | 97 | 25 | 84.1 | 4.4 | 7.6 | 3.9 | ||||
| T-09 | 1 | 1 | 98 | 25 | 90.3 | 3.4 | 5.1 | 1.2 | ||||
| T-10 | 2 | 1 | 97 | 25 | 92.9 | 2.9 | 3.9 | 0.3 | ||||
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Mineral composition suggests that devitrification altered most glasses to clay minerals in the tuffs, and the high content of I/S in the samples indicates middle to late stages of normal diagenetic alteration (Qiu et al., 2014).
Analysis of major elements (Table S1) recorded SiO2 and Al2O3 to account for about 80 wt.% of the total major element content, with concentrations ranging from 49.27 wt.% to 54.19 wt.% (51.72% average) and 22.71 wt.% to 29.51 wt.% (27.03 wt.% average), respectively. Fe, Mg, CaO, Na, Mn, Ti and P oxides had low contents whilst K2O was high, ranging from 3.17 wt.% to 7.03 wt.%, with an average of 5.95 wt.%. However, results from Spears and Rice (1973) suggest that the percentages of Al2O3, CaO, P2O5 and total Fe were enriched during the diagenetic alteration of volcanic ash; SiO2, Na2O and K2O were commonly depleted. The primitive volcanic ashes were therefore more acidic than the data indicate, with K2O contents being higher and Al2O3 contents being lower.
Results for trace element concentrations in the tuff samples (Table S1) indicate total rare earth element (∑REE) concentrations range from 58.78 μg/g to 250.85 μg/g, with an average of 149.34 μg/g. The ratios of light rare earth elements (LREE) to heavy rare earth elements (HREE) vary from 3.21 to 13.70, with a mean of 6.39. Although no anomalies were recorded for Ce in all of the samples, chondrite-normalized REE patterns (Fig. 6a) could be divided into two types by Eu: four tuff samples (T-06, T-08, T-09 and T-10) have a positive Eu anomaly with δEu, varying from 1.34 to 1.84, and six tuff samples (T-01, T-02, T-03, T-04, T-05 and T-07) have a negative Eu anomaly with δEu, ranging from 0.66 to 0.98.
Primitive mantle-normalized spider diagrams (Fig. 6b) generally show strong positive anomalies in high field strength elements (HFSE), including Th, U, Ta, Zr and Hf, and negative anomalies in large ion lithophile elements, including Rb, Ba, Nb and Sr. The ratio of Zr/Hf varies from 29.97 to 43.92, with an average of 36.38, and the ratio of Nb/Ta ranged from 5.16 to 13.87, with an average of 9.34.
Zircon grains within the three tuff intervals are euhedral or sub euhedral, with clear oscillating growth rings in cathodeluminescence images (Fig.7). Grains generally ranged from 60 to 150 μm in length, and the length/width ratios ranged from 1 to 3. In addition, zircon Th/U ratios were 0.84 on average (Table S2). These characteristics indicate that zircon grains have a magmatic origin (Koschek, 1993; Le Bas et al., 1986; Pupin, 1980). Samples T-01, T-05 and T-07 were selected for U-Pb isotope aging, and results of U-Pb isotopic age analyses are listed in Table S2 together with errors (1σ) and concordances (≥95%).
Twenty-four zircon grains from each sample were selected for U-Pb isotope dating. Zircons that did not demonstrate concordant ages were deemed to be unreliable because their closed isotope system had been destroyed, therefore being excluded from U-Pb aging processes (Yin et al., 2019). The Results indicate that 206Pb/238U ages of the three tuff samples occurred within restricted fields on the concordia lines, respectively (Fig. 7). Sixteen analyzed spots on 16 zircon grains separated from sample T-01 were analyzed, yielding a weighted mean 206Pb/238U age of 231.4 ± 1.6 Ma (MSWD = 1.17). Eleven analyzed spots on 11 zircon grains from sample T-05 yielded a weighted mean 206Pb/238U age of 236.0 ± 1.7 Ma (MSWD = 1.2). Fifteen analyzed spots on 15 zircon grains from sample T-07 yielded a weighted mean 206Pb/238U age of 223.1 ± 3.9 Ma (MSWD = 4.4).
Fossil evidence dates sedimentation in the Galedesi Formation, South Qilian Basin, to have occurred during the Late Triassic (Norian to Rhaetian Age) (Yang, 1983). Although U-Pb isotope records from tuff intervals in this formation also indicate Late Triassic deposition, deposition is dated as being Carnian and Norian Age, thus being earlier than previous reports. This finding raises the question of whether the Atasi Formation, which underlies the Galedesi Formation, was also formed during the Late Triassic during past stratigraphic division. Although this formation is generally considered to be part of the Upper Triassic, Sun (1997) suggested this formation to be a time-transgressive formation of the Middle and Upper Triassic; a deficiency of fossils in the sandstone dominant strata of the Atasi Formation made it hard to fully distinguish a time period for this formation. The oldest tuff interval in the Galedesi Formation (T-05) was recorded to have a U-Pb isotope age of 236.0 ± 1.4 Ma, being approximately equal to the boundary age of the Middle and Late Triassic; there was limited time for hundreds of meters of sediments in the Atasi Formation to be deposited in a down-warped basin in the Late Triassic. Thus, the sedimentary period of the Atasi Formation is more questionable according to the time limitation of tuffs in the Galedesi Formation, and the precise transition time of the sedimentary environment from marine-coastal to continental lake in the South Qilian Basin in the Triassic is also an important research area that requires further investigation.
Quartz and plagioclase compositions identified in the tuff samples suggest an intermediate-to-felsic series magma of parental magma prior to eruption. The immobile elements, including TiO2, high field strength (HFS) elements (Zr, Nb, Hf, Ta) and REEs have been previously used to provide useful information on parental magmas and tectonic settings of volcanic ash (Astini et al., 2007). The Zr/TiO2-Nb/Y magmatic discrimination diagram (Fig. 8) shows that the majority of tuff samples from the Galedesi Formation occurred around the comendite pantellerite and rhyolite boundary, with one sample occurring in the rhyodacite dacite section. A high K2O content in the tuffs indicates that these are classified as a high-K calcalkaline series.
By plotting tuff data on bivariate plots of Nb versus Y, Rb versus Y + Nb, and TiO2 versus Zr, and a ternary plot of Rb/10-Hf-Ta × 3, we were able to determine the possible tectonic setting of the volcanoes responsible for the tuffs in the Galedesi Formation (Fig. 9). The Nb versus Y and Rb versus Y + Nb plots were used to determine the tectonic setting of granitic rocks (Pearce et al., 1984; Pearce, 1982), and the majority of tuff data fell within plate granite (WPG) and volcanic arc granite (VAG). T-03, T-05, T-06 and T-10 samples were located in the "VAG + syn COLG" area (Fig. 9a) and T-03, T-05, T-06 and T-09 occurred in the VAG area (Fig. 9b). However, the tuffs were derived from within plate lavas when results occurred within the plate area in TiO2 versus Zr and Rb/10-Hf-Ta × 3 (Figs. 9c, 9d).
Different tectonic background results (Figs. 9a–9d) may be caused by crustal contamination, which can produce geochemical characteristics (the negative anomaly of Nb) similar to AVG (Dang et al., 2013), resulting in a shift from the "WPG" area to the "VAG" area in Figs. 9a and 9b.
As volcanic ash can be transported long distances in the atmosphere, potential tuff source regions are not limited to the sedimentary basin or the adjacent belts of the basin (Huff et al., 1992). However, identification of material sources is important for the tectonic significance of the tuff (Yang et al., 2019). Late Triassic volcanic rocks are widely distributed to the south of the Qilian tectonic belt, including the East Kunlun belt, the West Qinling belt, the Songpan-Ganzi belt, and the Qiangtang Block (Fig. 1b), which were the major potential material source regions of tuffs in the Galedesi Formation.
Eruption age, geochemical characteristics and tectonic settings of the examined tuffs are important for the identification of their source regions. Volcanic rocks in the Qiangtang Block are divided into two types; basalt distributed in the central uplift of the Qiangtang Block are rift related, erupting around 205–225 Ma (Fu et al., 2010; Wang et al., 2007). Basalt deposits had low levels of K2O whereas rhyolite had high K2O levels; Th and U were normal in both deposits. Ta and Nb were depleted in the primitive mantle-normalized spider diagrams. Dacites distributed in the northern and eastern margins of the Qiangtang Block and the Songpan-Ganzi belt are arc related, erupting around 213–231 Ma (Liu Y et al., 2019; Liu B et al., 2016; Zhao et al., 2015; Wang B Q et al., 2013; Yang et al., 2012; Wang Q et al., 2008). These formations are characterized by moderate K2O contents and low Al2O3 contents; negative anomalies of Nb and Ta in the primitive mantle-normalized spider diagrams are notably different from the geochemical characteristics of tuffs in the Galedesi Formation. Differences in geochemical characteristics and forming tectonics between tuffs in the South Qilian Basin and volcanic rocks in the Qiangtang Block and the Songpan-Ganzi belt suggest that these areas were unlikely to be source regions for tuffs examined in this investigation.
Felsic volcanic rocks distributed in the East Kunlun belt and the West Qinling belt erupted around 214–234 and 216–232 Ma, respectively (Table 2). The geochemical characteristics of Late Triassic volcanic rocks in the East Kunlun belt and West Qinling are highly similar, having a peraluminous high-K calc-alkaline series, with a K2O content around 5.0% (Chen et al., 2020; Hu et al., 2016), consistent with tuff characteristics in this study. In addition, rhyolite in both the East Kunlun belt and the West Qinling belt is characterized by Rb, Th and U enrichment and a relative depletion in Ti and P, which are consistent with those in this study. High Nb-Ta rhyolite recorded in the East Kunlun belt is very similar to the tuffs in this study. The East Kunlun belt and the West Qinling belt were adjacent to the South Qilian Basin, being the nearest regions to where Late Triassic volcanic rocks were distributed; eruption ages and geochemical characteristics of the volcanic rocks are also consistent with tuffs in this study. The East Kunlun belt and the West Qinling belt are therefore the most likely source regions of tuffs sedimented in the Galedesi Formation. However, Late Triassic volcanic rocks with positive Eu anomalies or high Zr concentrations were not found. These differences suggest more detailed investigations are needed to accurately distinguish potential source regions of the tuffs.
| Region | Location | Sample | Age (Ma) | Method | References |
| South Qilian | Muli | Rhyolitic tuff | 223.1 ± 3.9 | LA-ICP-MS Zircon U-Pb | This study |
| Muli | Rhyolitic tuff | 231.4 ± 1.6 | LA-ICP-MS Zircon U-Pb | This study | |
| Muli | Rhyolitic tuff | 236.0 ± 1.7 | LA-ICP-MS Zircon U-Pb | This study | |
| Western Qinling | Dangchang | Rhyolite | 229 ± 2 | LA-ICP-MS Zircon U-Pb | Huang et al. (2013) |
| Tianshui | Rhyolite | 216± 2 | LA-ICP-MS Zircon U-Pb | Qiu et al. (2014) | |
| Hezuo | Andesite | 232± 2 | LA-ICP-MS Zircon U-Pb | Li et al. (2019) | |
| Eastern Kunlun | Dulan | Rhyolite | 214 ± 1 | LA-ICP-MS Zircon U-Pb | Ding et al. (2011) |
| Dulan | Rhyolite | 228 ± 2 | LA-ICP-MS Zircon U-Pb | Hu et al. (2016) | |
| Tufangzi | Rhyolitic tuff | 220 ± 2 | LA-ICP-MS Zircon U-Pb | Hu et al. (2016) | |
| Boluositai | Dacite | 234 ± 1.5 | LA-ICP-MS Zircon U-Pb | Feng et al. (2022) | |
| Songpan-Ganzi | Tuotuohe | Nb-enriched basalts | 229 ± 7 | LA-ICP-MS Zircon U-Pb | Wang et al. (2008) |
| Yushu | Dacite | 230 ± 2 | LA-ICP-MS Zircon U-Pb | Liu et al. (2016) | |
| Xiangcheng | Dacite | 228 ± 2 | LA-ICP-MS Zircon U-Pb | Wang et al. (2013) | |
| Gacun | Dacite | 231 ± 1 | LA-ICP-MS Zircon U-Pb | Wang et al. (2013) | |
| Qiangtang | Geladaidong | Basalt | 220 ± 2 | SHRIMP Zircon U-Pb | Fu et al. (2010) |
| Geladaidong | Rhyolite | 210 ± 2 | SHRIMP Zircon U-Pb | Wang et al. (2007) | |
| Duocai | Dacite | 221 ± 1 | LA-ICP-MS Zircon U-Pb | Zhao et al. (2015) | |
| Duorirong | Dacite | 228 ± 1 | LA-ICP-MS Zircon U-Pb | Liu et al. (2019) | |
| Longmogou | Dacite | 227 ± 2 | LA-ICP-MS Zircon U-Pb | Liu et al. (2019) |
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(1) More than 70 tuff intervals were recorded in cores of well ZK6-6, located in Muli, South Qilian Basin. The majority of tuffs transformed into I/S, and the crystal shards in the tuffs were plagioclase and quartz; calcite, pyrite, dolomite and siderite were also identified. The tuffs are a peraluminous high-K calcalkaline series that were enriched in high field strength elements (HFSE), including Th, U, Ta, Zr and Hf; both positive and negative Eu anomalies in REEs were identified in the samples.
(2) The majority of tuffs occurred in the shale sedimentary section of the Galedesi Formation, Upper Triassic. LA-ICP-MS U-Pb ages of three tuff samples (236.0 ± 1.7, 231.4 ± 1.6, and 223.1 ± 3.9 Ma) indicated that tuffs in the Galedesi Formation erupted in the Carnian and Norian age, Late Triassic.
(3) The tuffs originated from comendite pantellerite and rhyolite from within plate settings. The West Qinling belt and the East Kunlun belt are the potential source regions of these tuffs, and they originated from within plate magma in the post-collisional period of the belts.
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Figures(9) / Tables(2)
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Fangpeng Du, Furong Tan, Shiming Liu, Xiaochen Zhao, Yingtao Chen, Junwei Qiao. First Discovery of Late Triassic Tuffs in the South Qilian Basin: Geochemical Characteristics, Zircon LA-ICP-MS U-Pb Ages and Potential Source Regions. Journal of Earth Science, 2023, 34(6): 1692-1703. doi: 10.1007/s12583-021-1446-7
| Sample | Relative content of clay minerals (%) | Whole rock quantitative analysis (%) | ||||||||||
| Kaolinite | Chlorite | I/S | %S | Total clay | Quartz | Plagioclase | Calcite | Dolomite | Pyrite | Siderite | ||
| T-01 | 1 | 1 | 98 | 25 | 85.3 | 2.1 | 4.2 | 8.4 | ||||
| T-02 | 2 | 1 | 97 | 25 | 86.9 | 5.9 | 4.4 | 2.8 | ||||
| T-03 | 1 | 1 | 98 | 25 | 58.2 | 4.7 | 35.8 | 1.3 | ||||
| T-04 | 2 | 1 | 97 | 25 | 89.9 | 4.8 | 4.3 | 1 | ||||
| T-05 | 3 | 1 | 96 | 25 | 62 | 5 | 21.8 | 6.8 | 4.4 | |||
| T-06 | 1 | 2 | 97 | 25 | 88.4 | 2 | 9.6 | |||||
| T-07 | 1 | 99 | 25 | 87.3 | 3.5 | 8 | 1 | 0.2 | ||||
| T-08 | 1 | 2 | 97 | 25 | 84.1 | 4.4 | 7.6 | 3.9 | ||||
| T-09 | 1 | 1 | 98 | 25 | 90.3 | 3.4 | 5.1 | 1.2 | ||||
| T-10 | 2 | 1 | 97 | 25 | 92.9 | 2.9 | 3.9 | 0.3 | ||||
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CSV
| Region | Location | Sample | Age (Ma) | Method | References |
| South Qilian | Muli | Rhyolitic tuff | 223.1 ± 3.9 | LA-ICP-MS Zircon U-Pb | This study |
| Muli | Rhyolitic tuff | 231.4 ± 1.6 | LA-ICP-MS Zircon U-Pb | This study | |
| Muli | Rhyolitic tuff | 236.0 ± 1.7 | LA-ICP-MS Zircon U-Pb | This study | |
| Western Qinling | Dangchang | Rhyolite | 229 ± 2 | LA-ICP-MS Zircon U-Pb | Huang et al. (2013) |
| Tianshui | Rhyolite | 216± 2 | LA-ICP-MS Zircon U-Pb | Qiu et al. (2014) | |
| Hezuo | Andesite | 232± 2 | LA-ICP-MS Zircon U-Pb | Li et al. (2019) | |
| Eastern Kunlun | Dulan | Rhyolite | 214 ± 1 | LA-ICP-MS Zircon U-Pb | Ding et al. (2011) |
| Dulan | Rhyolite | 228 ± 2 | LA-ICP-MS Zircon U-Pb | Hu et al. (2016) | |
| Tufangzi | Rhyolitic tuff | 220 ± 2 | LA-ICP-MS Zircon U-Pb | Hu et al. (2016) | |
| Boluositai | Dacite | 234 ± 1.5 | LA-ICP-MS Zircon U-Pb | Feng et al. (2022) | |
| Songpan-Ganzi | Tuotuohe | Nb-enriched basalts | 229 ± 7 | LA-ICP-MS Zircon U-Pb | Wang et al. (2008) |
| Yushu | Dacite | 230 ± 2 | LA-ICP-MS Zircon U-Pb | Liu et al. (2016) | |
| Xiangcheng | Dacite | 228 ± 2 | LA-ICP-MS Zircon U-Pb | Wang et al. (2013) | |
| Gacun | Dacite | 231 ± 1 | LA-ICP-MS Zircon U-Pb | Wang et al. (2013) | |
| Qiangtang | Geladaidong | Basalt | 220 ± 2 | SHRIMP Zircon U-Pb | Fu et al. (2010) |
| Geladaidong | Rhyolite | 210 ± 2 | SHRIMP Zircon U-Pb | Wang et al. (2007) | |
| Duocai | Dacite | 221 ± 1 | LA-ICP-MS Zircon U-Pb | Zhao et al. (2015) | |
| Duorirong | Dacite | 228 ± 1 | LA-ICP-MS Zircon U-Pb | Liu et al. (2019) | |
| Longmogou | Dacite | 227 ± 2 | LA-ICP-MS Zircon U-Pb | Liu et al. (2019) |
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CSV
| Sample | Relative content of clay minerals (%) | Whole rock quantitative analysis (%) | ||||||||||
| Kaolinite | Chlorite | I/S | %S | Total clay | Quartz | Plagioclase | Calcite | Dolomite | Pyrite | Siderite | ||
| T-01 | 1 | 1 | 98 | 25 | 85.3 | 2.1 | 4.2 | 8.4 | ||||
| T-02 | 2 | 1 | 97 | 25 | 86.9 | 5.9 | 4.4 | 2.8 | ||||
| T-03 | 1 | 1 | 98 | 25 | 58.2 | 4.7 | 35.8 | 1.3 | ||||
| T-04 | 2 | 1 | 97 | 25 | 89.9 | 4.8 | 4.3 | 1 | ||||
| T-05 | 3 | 1 | 96 | 25 | 62 | 5 | 21.8 | 6.8 | 4.4 | |||
| T-06 | 1 | 2 | 97 | 25 | 88.4 | 2 | 9.6 | |||||
| T-07 | 1 | 99 | 25 | 87.3 | 3.5 | 8 | 1 | 0.2 | ||||
| T-08 | 1 | 2 | 97 | 25 | 84.1 | 4.4 | 7.6 | 3.9 | ||||
| T-09 | 1 | 1 | 98 | 25 | 90.3 | 3.4 | 5.1 | 1.2 | ||||
| T-10 | 2 | 1 | 97 | 25 | 92.9 | 2.9 | 3.9 | 0.3 | ||||
| Region | Location | Sample | Age (Ma) | Method | References |
| South Qilian | Muli | Rhyolitic tuff | 223.1 ± 3.9 | LA-ICP-MS Zircon U-Pb | This study |
| Muli | Rhyolitic tuff | 231.4 ± 1.6 | LA-ICP-MS Zircon U-Pb | This study | |
| Muli | Rhyolitic tuff | 236.0 ± 1.7 | LA-ICP-MS Zircon U-Pb | This study | |
| Western Qinling | Dangchang | Rhyolite | 229 ± 2 | LA-ICP-MS Zircon U-Pb | Huang et al. (2013) |
| Tianshui | Rhyolite | 216± 2 | LA-ICP-MS Zircon U-Pb | Qiu et al. (2014) | |
| Hezuo | Andesite | 232± 2 | LA-ICP-MS Zircon U-Pb | Li et al. (2019) | |
| Eastern Kunlun | Dulan | Rhyolite | 214 ± 1 | LA-ICP-MS Zircon U-Pb | Ding et al. (2011) |
| Dulan | Rhyolite | 228 ± 2 | LA-ICP-MS Zircon U-Pb | Hu et al. (2016) | |
| Tufangzi | Rhyolitic tuff | 220 ± 2 | LA-ICP-MS Zircon U-Pb | Hu et al. (2016) | |
| Boluositai | Dacite | 234 ± 1.5 | LA-ICP-MS Zircon U-Pb | Feng et al. (2022) | |
| Songpan-Ganzi | Tuotuohe | Nb-enriched basalts | 229 ± 7 | LA-ICP-MS Zircon U-Pb | Wang et al. (2008) |
| Yushu | Dacite | 230 ± 2 | LA-ICP-MS Zircon U-Pb | Liu et al. (2016) | |
| Xiangcheng | Dacite | 228 ± 2 | LA-ICP-MS Zircon U-Pb | Wang et al. (2013) | |
| Gacun | Dacite | 231 ± 1 | LA-ICP-MS Zircon U-Pb | Wang et al. (2013) | |
| Qiangtang | Geladaidong | Basalt | 220 ± 2 | SHRIMP Zircon U-Pb | Fu et al. (2010) |
| Geladaidong | Rhyolite | 210 ± 2 | SHRIMP Zircon U-Pb | Wang et al. (2007) | |
| Duocai | Dacite | 221 ± 1 | LA-ICP-MS Zircon U-Pb | Zhao et al. (2015) | |
| Duorirong | Dacite | 228 ± 1 | LA-ICP-MS Zircon U-Pb | Liu et al. (2019) | |
| Longmogou | Dacite | 227 ± 2 | LA-ICP-MS Zircon U-Pb | Liu et al. (2019) |
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