Chunxia Xu1,2
Chongyi E1,2,3*
Yunkun Shi1,2
Jing Zhang1,2
Manping Sun1,2
Zhaokang Zhang1,2
Yongxin Zeng1,2- 1Key Laboratory of Tibetan Plateau Land Surface Processes and Ecological Conservation (Ministry of Education), Qinghai Normal University, Xining, China
- 2Qinghai Province Key Laboratory of Physical Geography and Environmental Process, College of Geographical Science, Qinghai Normal University, Xining, China
- 3Academy of Plateau Science and Sustainability, People’s Government of Qinghai Province and Beijing Normal University, Xining, China
The Gonghe Basin (GHB) on the northeastern Qinghai-Tibet Plateau (NE-QTP) is sensitive to climatic change due to the interplay of the Asian summer monsoon and the westerlies. Extensive aeolian sediments in the basin represent important archives of regional environmental evolution. However, the paleosol development timing is still not clear because of limited number of optically stimulated luminescence (OSL) sampling and dating, which restricts our understanding of past aeolian activities during the Holocene in GHB. In this study, a loess-paleosol section, Najiao (NJ), from the southeastern margin of GHB was investigated. Eighteen OSL samples were obtained from the 400-cm section in order to construct a high-resolution chronological framework. Paleoenvironmental proxies including grain size distribution (GS), magnetic susceptibility (MS), total organic carbon (TOC), and geochemical elements were measured to reconstruct the Holocene aeolian activity. Results show a successive accumulation from Early to Middle Holocene at NJ section, but a c. 3 ka sedimentary hiatus is found between c. 5 and 1.5 ka. Paleosol ages are constrained by high-resolution OSL ages which are from c. 7–5 ka. Consistent with previous studies, strong aeolian activities occurred in GHB during the Early Holocene (c. 13–9 ka), indicating dry climate conditions. Initiation of pedogenesis was at c. 9 ka, and the intensified soil development and lowest aeolian activity were between c. 7 and 5 ka. The increased sand content after c. 1.5 ka indicates enhanced human activities in the interior of GHB in the Late Holocene.
Introduction
The arid/semi-arid northeastern Qinghai-Tibet Plateau (NE-QTP) is particularly sensitive to climatic change as it is under the interplay between the Asian summer monsoon and the westerlies (An et al., 2012; Chen et al., 2016). Sediments, tree rings, and ice cores are important archives of regional environmental and climatic change on the NE-QTP (An et al., 2012; Chen et al., 2016). Aeolian deposits are widespread on the arid NE-QTP, and taken as an important proxy for reconstructing paleoclimatic change, which is well-studied since the 1980s (Xu, 1987; Liu et al., 2012; Qiang et al., 2013; Sun et al., 2014; Hu et al., 2015; Qiang et al., 2016; Liu et al., 2017; Qin et al., 2017; Li et al., 2020). Generally, aeolian activity was stronger and accumulation rates were higher under the dry-cold climate during the Late Glacial to Early Holocene, while dune activity was weaker in the more humid Mid-Holocene, and intensified again in the Late Holocene (Stauch et al., 2016; Chen et al., 2020). It has been reported that natural factor was the dominant control on millennial-scale dust storm activity during most of the Holocene, but an upturn in dust storms since c. 2 cal ka BP has been linked with increasing human populations/intensifying human disturbance in dust source regions of northern China (Chen et al., 2021). Thus, aeolian activity is not only related to climate change, but also to human activity, on different timescales.
Aeolian deposits contain occasional paleosols that were formed when dunes were stabilized due to vegetation development. Published optically stimulated luminescence (OSL) ages for paleosol formation show great variation between basins, and even for different parts of the same basin, due to its limited occurrence (Chen et al., 2020) and moisture effects of local terrain (Qiang et al., 2013). However, few studies have considered the role of soil development mode on paleosol age, which limits understanding of paleoenvironments. The ideal soil development mode for reconstructing paleoenvironmental variations is “aeolian dust aggradation”, i.e., continuous accumulation of aeolian sand or dust over at least the millennial scale in either dry-cold or warm-wet periods. In such cases, paleosol development is simultaneous with dust input and paleosol OSL ages directly reflect the timing of humidity (Ee et al., 2018; Zhang et al., 2020). However, at the millennial scale, aeolian sedimentation on the NE-QTP is not continuous (Chongyi et al., 2018; Zhang et al., 2018; Chongyi et al., 2019; Yan et al., 2019; Zhang et al., 2020). During periods of warm and humid climate, dust input reduces and strong pedogenesis may occur; the mode of soil development comprises (in-situ) chemical weathering of aeolian—or other—parent material (E et al., 2018b; Zhang et al., 2020). Due to the predominately aeolian parent material, paleosol OSL ages indicate the timing of dust or sand deposition rather than soil formation. Thus, quartz OSL ages can be taken to indicate an upper limit to soil formation (Miao et al., 2016; Zhang et al., 2020), and the duration of mountain soil development can be effectively constrained by high-resolution OSL ages of deposits at different depths. In addition, high-resolution OSL sampling is an effective means of verifying the continuity of aeolian sedimentation and underpins millennial-scale paleoenvironmental reconstruction during the Holocene (Lu et al., 2006).
The Gonghe Basin (GHB) is the largest intramontane basin on the NE-QTP (Stauch et al., 2016) and its location in the arid/semi-arid transition zone makes it sensitive to climate change and environmental evolution. The prevailing westerly wind and high vegetation coverage of mountain areas in the southwestern basin provide suitable trapping and preservation conditions of dust and there are thick aeolian deposits. In this study, high-resolution OSL dating of a mountain sediment profile at Najiao (NJ) in the southwestern GHB, combined with analysis of grain size (GS), low frequency magnetic susceptibility (MS), total organic carbon (TOC), and geochemical elements, is used to constrain the timing of paleosol development and reconstruct Holocene aeolian activity. The findings are used to discuss the forcing mechanisms of aeolian activity in the context of regional ecological and climatic change.
Regional Setting
GHB (average elevation 3,000 m asl) is bounded by mountains, with Xiqing Mountain of the Qinling system to the east, the Heka, Ela, Wahong Mountains of the Kunlun system to the south and southeast, Qinghai South Mountain (and Qinghai Lake) to the north, and the Waligong, and Riyue Mountains to the northeast (Figure 1A) (Liu et al., 2013a; Liu et al., 2013b). The basin trends NW-SE, with an area of 13,800 km2, a width of 30–90 km, and a length of approximately 210 km (Liu et al., 2013a; Liu et al., 2013b). The region is characterized by a cold and dry alpine and arid/semi-arid climate, with an annual evaporation of 528–1937 mm, a temperature and precipitation of 1.0–5.2°C and 311.1–402.1 mm, with precipitation accounting for c. 80% in summer (Liu et al., 2020). The natural vegetation shows strong altitudinal zonation. Below 3,000 m, vegetation is mainly characterized by desert and desert steppe, with some mosaic meadows in lowland areas. Around 3,200 m, the vegetation consists of typical steppe adjacent to diluvial piedmont fans. Over 3,600 m, subalpine meadows dominate the community along the mountainside in the eastern GHB (Qiang et al., 2016). The main areas of desert comprise Muge Sands and Talatan Plain, with mobile, semi-fixed, and fixed sand dunes.
FIGURE 1. Location maps and site details of the study area. The sand field data set is provided by National Tibetan Plateau Data Center (http://data.tpdc.ac.cn). (A) Location of Gonghe Basin on the Northeast Qinghai-Tibet Plateau and location of the study section (NJ) in Gonghe Basin. (B) Photos of Stratigraphies, landforms for section NJ.
Materials and Methods
Lithology and Sample Collection
The NJ section (35°40′23.15″N, 101°5′49.04″E, 3,629 m altitude) (Figures 1A,B) is in the eastern Muge Sand, in the southwestern GHB. Surface vegetation is the subalpine meadow, with an outcrop thickness of 4 m. Based on lithology, the section can be divided into six layers: 0–35 cm, modern soil; 35–185 cm, weak paleosol, of which 10–60 cm contains white pseudomycelium; 185–235 cm, paleosol; 235–385 cm, loess; 385–395 cm, weak paleosol; 395–400 cm, loess. Total 18 OSL samples were collected at 10 cm intervals in/close to the paleosol layer and at 40 cm intervals elsewhere. Proxy samples—for GS, TOC, MS, and geochemical elements analysis—were collected continuously at 5 cm intervals, giving a total of 108 samples.
Proxy Analyses
A total of 108 samples have been used for measurements of GS, MS and TOC. Composition of geochemical elements was collected from 64 samples to calculate the rubidium/strontium ratio (Rb/Sr) that reflects the leaching degree of aeolian sediment in the process of weathering and pedogenesis (Nesbitt and Young, 1989; Chen et al., 1999). The GS distribution taken as an indicator of the intensity of aeolian activity was measured by a Malvern 2000 laser particle size analyzer, using the method described by Lu and An (1997). After removing carbonates, the TOC content indicating vegetation coverage and biomass was performed on an Elementar Vario TOC Cube analyzer (Gasse et al., 1991). Geochemical elements were carried out using the wavelength dispersion type of X-ray fluorescence spectrometer following a routine pretreatment protocol (Liu et al., 2013a). MS was measured by a Bartington MS2 meter after drying the samples below 40°C.
OSL Dating
The quartz fraction of 63–90 μm was extracted for equivalent dose (De) determination. Extracted quartz was checked for purity using infrared stimulated luminescence (IRSL) measurements (Duller, 2003). De was determined by the single aliquot regenerative (SAR) protocol on a Risø TL/OSL-DA-20-C/D reader (Murray and Wintle, 2000; Wintle and Murray, 2006). For De calculations, the signal was derived from the first 0.16 s of stimulation and an early background (0.16–0.32 s) to minimize the influence of slow and medium components (Cunningham and Wallinga, 2010). De rejection criteria were restricted by two test measurements (e.g., 0.9 < R5/R1 < 1.1, and R4/N < 5%). Average De was calculated based on the results of 16–18 aliquots.
The concentrations of uranium (U), thorium (Th) and potassium (K) were measured by inductively coupled plasma mass spectrometry for calculating the environmental dose rate. Then the concentrations of U, Th and K were converted into infinite matrix dry dose rates using the conversion factors of Guérin et al. (2012). The cosmic ray contribution was from Prescott and Hutton (1994). Due to the modern mountain climate is relatively humid, water content was estimated as 10 ± 5%. Detailed dating information including radionuclide concentrations, dose rates, equivalent doses and age results are summarized in Table 1.
TABLE 1. OSL dating results for section NJ, Gonghe Basin, NE-QTP.
Age-Depth Model
The age-depth relationship was established in section NJ using the Undatable model to construct the chronological framework and verify continuity of the aeolian sediment accumulation on millenial scale (Figure 2). Undatable model is a rapid, deterministic age-depth modeling routine for geological sequences, using Matlab software and programming practices (Lougheed and Obrochta, 2019). For the NJ section, model parameters xfactor = 0.1 and bootpc = 30 were used.
FIGURE 2. Age-depth relationship for the NJ section based on the Undatable model (Lougheed and Obrochta, 2019).
Results
Quartz Luminescence Characteristics
The quartz OSL signal of sample NJ-7 rapidly decreased to background in the first 2 s, indicating a fast component (Figure 3A). Preheat plateau tests were carried out on NJ-9 to select an appropriate preheating regime (Figure 3B). There is an apparent plateau between 180°C and 240°C. All of the recycling ratios are between 0.9 and 1.1 under different preheat temperature, and all recuperations are smaller than 5%. Consequently, a preheat temperature of 240°C and a cut-heat temperature of 200°C was selected to determine quartz De for all samples. Four randomly selected samples were chosen for dose recovery test, and all ratios lie within 10% of the slope of unity, indicating well dose recoveries (Figure 3C).
FIGURE 3. OSL characteristics for samples, NJ section. (A) Growth and decay (inset) curves for sample NJ-7. (B) Preheat plateau tests (De) at sample NJ-9 showing a plateau between 180 and 300°C. (C) Dose recovery test. Given doses versus measured doses for four randomly selected samples. The solid black line is the slope of unity, where the ratio is 100%, and the two red dashed lines indicate 10% above and below the line. Error bars represent one standard error.
Dating Results
Within one standard error, OSL ages are generally grown with the increase of sampling depth, except for one age inversions in upper weak paleosol with an age of 1.9 ± 0.1 ka at the depth of 1.5 m. The 2-m deep upper weak paleosol layer was deposited in the last c. 1.5 ka. The loess age is concentrated from 12.3 ± 0.9 ka to 9.5 ± 0.6 ka. The apparent paleosol age is from 9.4 ± 0.5 ka to 5.4 ± 0.3 ka.
The resulting age-depth curve (Figure 2) shows a continuous deposition from the Early to Middle Holocene and after 1.5 ka. A c. 3 ka hiatus in deposition took place in the Late Holocene (c. 5–1.5 ka). Similar millennial-scale hiatuses have been identified in other high-resolution OSL dated aeolian sections elsewhere on the NE-QTP (Zhang et al., 2018; E et al., 2019; Yan et al., 2019), indicating ubiquitous discontinuity in aeolian deposits over millennial-scale on the entire Qinghai-Tibet Plateau (QTP).
Proxy Results
The NJ section mainly comprises sand size sediment (>63 μm), ranging from 38.09 to 68.49% (average 51.31%) (Figure 4). Comparison of GS distributions between loess, weak paleosol, and paleosol samples (Figure 5) shows they are mostly unimodal grain size distribution with overlapping peaks, indicating they have a similar/single provenance and the material source has been stable over time. According to the prevailing wind direction in GHB is northwest, the desert in GHB should be the potential material source.
FIGURE 4. Ternary diagram showing grain size components for samples from the NJ section.
FIGURE 5. Grain size distribution curves for selected samples from the NJ section.
In the NJ section, MS varies from 23.4 to 65.8 × 10−8 m3/kg (average 35.7 × 10−8 m3/kg), with the highest value in paleosol and lowest in loess (Figure 6). But the MS in upper sandy weak paleosol is slightly higher than the lower loess. TOC varies from 1.05 to 4.5% (average 2.13%), with the highest proportion in modern soil with upper depth of 25 cm which is significantly affected by surface litter layer and root matter input (Figure 6). TOC in paleosol is much higher than loess and weak paleosol, but lowest in loess stratum. Rb/Sr ratio varies from 0.37 to 0.62, with an average of 0.5. Trend similar to TOC and MS is observed in the Rb/Sr ratio, which shows the highest value in paleosol and the lowest in loess (Figure 6).
FIGURE 6. Stratigraphic sequence of the NJ section showing OSL ages and variations in sediment size and various proxy indicators with depth.
Discussion
Timing of Paleosol Development in the GHB
As mentioned above, the accuracy of paleosol OSL ages depends on the soil development mode. The ideal soil development mode for OSL dating is “aeolian dust aggradation”, i.e., paleosol development is simultaneous with dust input (E et al., 2018b; Zhang et al., 2020). The high-resolution OSL dating of paleosol layer at NJ section indicates continuous dust deposition on the millennial scale. Thus, the paleosol OSL age falls well within the period of pedogenesis. According to the field observation (Figure 1B), the dark paleosol layer has a thickness of 50 cm (185–235 cm) dated from c. 9 ka to c.5 ka, indicating a very low dust accumulation rate during the pedogenic process. Then for obtaining a reliable paleosol age, the high-resolution OSL dating strategy is vital and necessary. The low-resolution OSL sampling strategy is difficult to differ the (in-situ) chemical weathering of previously deposited aeolian parent material or the “aeolian dust aggradation” at least on millennial scale. Therefore, it is not strange that the paleosol ages based on the low-resolution OSL sampling show great variations between basins, and even for different sites in the same basin.
Meanwhile, the environmental proxy indicator of paleoenvironment is equally important to verify the pedogenic intensity. In NJ, the highest MS, TOC, Rb/Sr and clay content indicate the strongest pedogenic process occurred during c. 7 to 5 ka in 185–200 cm (Figure 6). This result is consistent with the lake level highstands in Kuhai (Figure 7F) (Yan et al., 2018) and Qinghai Lake (Liu et al., 2015). Similarly, a high resolution OSL chronology at ND aeolian sand section (E et al., 2019) records the strongest pedogenesis from 6 to 4.5 ka in the neighboring Qinghai Lake area (Figure 7E). The tree ring (Yang et al., 2021) records a wet middle Holocene since 6.7 to 5 ka, and the precipitation decreased remarkably since 4 ka (Figure 7H). Although the deposition of 1.5–5 ka in NJ is absent, the strongest pedogenic period in GHB is clear in c. 7 to 5 ka.
FIGURE 7. Comparison of proxy indicators for the NJ section with published paleoclimate records for other sites on the Northeast Qinghai-Tibet Plateau (NE-QTP) (ages based on the Undatable model). (A) >63 μm content, NJ section. (B) Rb/Sr, NJ section. (C) Total organic carbon (TOC), NJ section. (D) Low frequency magnetic susceptibility (MS), NJ section. (E) Mean grain size (Mz), ND section, Qinghai Lake (E et al., 2019). (F) Lake level, core KH17, Kuhai Lake (Yan et al., 2018). (G) Salinity, Qinghai Lake (Zhang et al., 1989). (H) Precipitation, tree ring DLH, Qilian Mountains (Yang et al., 2021). (I) Stellera pollen, core GGHA, Gonghe Basin (Liu et al., 2016). (J) Brassicaceae pollen, core GGHA, Gonghe Basin (Huang et al., 2017).
History of Aeolian Activity in the GHB
The regional aeolian activity in GHB is reconstructed according to the records of different paleoclimate proxy indicators from neighboring sites on the NE-QTP in Figure 7. Three stages can be identified, designed I to Ⅲ.
Stage I. Late Glacial and Early Holocene (13–9 ka). NJ section lithostratigraphy is characterized by sandy loess with relatively high sand content, reflecting relatively strong and frequent wind. TOC and Rb/Sr are at their lowest in this period, indicating sparse vegetation, weak weathering, and dry climate conditions in general (Figures 7B,C). Aeolian sediment of ND in Qinghai Lake, high salinity of Qinghai Lake and low lake level from Kuhai Lake suggest a strengthened aeolian activity and dry climate condition in NE-QTP (Figures 7E–G) (Zhang et al., 1989; Yan et al., 2018; E et al., 2019). All these results are consistent with the climate change history in QTP (Chen et al., 2020). Overall, climatic conditions in GHB within NE-QTP show a consistent condition and reveal intensified aeolian activity during the early Holocene.
Stage II. Middle Holocene (9–5 ka). NJ section lithostratigraphy shifts to paleosol in this stage. The sand content decreased slightly, but the MS, TOC, clay content and Rb/Sr increased significantly. It could indicate increased precipitation, enhanced pedogenesis, high biomass and weakened aeolian activity under relatively stable warm and wet conditions (Figure 6). In the latter part of the period between c. 7–5 ka, sand content is at its lowest, TOC and Rb/Sr at highest (Figures 7B,C), indicating the strong pedogenesis. These findings are consistent with previous studies in GHB that show the highest moisture levels, and lowest aeolian activity in the Mid-Holocene (Stauch et al., 2016). Similar patterns are observed in other records in the NE-QTP including low mean grain size (Mz) at the ND section (Figure 7E); highest lake level in Kuhai Lake and lowest salinity in Qinghai Lake (Figures 7F,G); and maximal at Qilian Mountain (Yang et al., 2021) between c. 7.6–4 ka (Figure 7H). In general, the climatic optimum in the GHB between c. 7–5 ka corresponds with other parts of the NE-QTP that record their wettest conditions in the Middle Holocene.
Stage III. Late Holocene (after c. 1.5 ka). NJ section lithostratigraphy comprises weak paleosol. The sand content in this layer is much higher than the middle to early Holocene paleosol and sandy loess (Figures 6, 7A). It indicates aeolian activities after c. 1.5 ka have been enhanced and are even stronger than early Holocene. Contradictorily, the Rb/Sr and TOC are higher than the lower sandy loess, and the MS is slightly higher than the lower sandy loess (Figures 7B–D). All these imply a wetter and better climate condition in the late Holocene than early Holocene. The prevailing wind direction in GHB is northwest, and straight distance from the mountain of NJ section to the Muge sands is less than 10 km (Figure 1A). Undoubtedly, NJ section recorded enhanced aeolian activities in GHB. Consistently, the stronger aeolian activity after c. 1.5 ka BP was reported in NE-QTP by the summarization of 93 aeolian sand OSL ages from 39 sections (Chen et al., 2016).
However, there was no decreasing trend after 1.5 ka BP in the precipitation reconstruction based on tree rings from Qilian Mountain after 3.5 ka BP (Figure 7H) (Yang et al., 2021). It was inferred that the increased aeolian activity after c.1.5 ka BP is not related to climate change but a consequence of intensified human activity (Zhang et al., 1988; Chen et al., 2016). Pollen from Genggahai Lake in GHB suggests an intensification of human settlement and grazing activity after c. 1.4 ka by high percentages of Stellera and Brassicaceae pollen and Sporormiella spores (Liu et al., 2016; Huang et al., 2017, Huang et al., 2020) (Figures 7I,J). Repeated shifts between nomadic pasture and farmland in the Qinghai Lake area since the late Western Han Dynasty (2.0–1.8 ka, 1.9–1.5 ka) may promote aeolian activity (Sun et al., 2021; Wei et al., 2021). For broader northern China, increased dust storms since c. 2 ka BP were also closely linked to increasing human populations in the dust source regions of northern China (Chen et al., 2021). In the interior of GHB, the intensity of human activity is much stronger and the ecological resistance is much lower. With the enhancement of human activities in the interior of GHB, sand supply was increased to the mountain soils as parental material. Increased sand contents dilute clay contents and magnetic minerals that produced by pedogenesis, then the MS of weak plaeosol present a lower feature. Rb/Sr ratio is less affected by aeolian activity because it reflects the proportionality of the relative contents of two elements (Wang et al., 2020), so Rb/Sr ratio reflects pedogenesis more likely, similar with TOC.
Overall, strong aeolian activities in GHB since c. 1.5 ka BP is closely related to the enhanced human activities than natural variability of climate.
Conclusion
The duration of mountain soil development in GHB was effectively constrained by high-resolution OSL ages from c. 7–5 ka. The period of strong pedogenesis is consistent with the warm and wet climatic condition recorded with tree rings and high lake levels in NE-QTP. A successive accumulation at the NJ section was recorded over the millennial scale during the Early to Middle Holocene in GHB, but a c. 3 ka hiatus was found between c. 5 and 1.5 ka. The aeolian activities showed a strong aeolian activity in GHB during Early Holocene (13–9 ka), consistent with the paleoclimatic records on the NE-QTP. Pedogenesis began at c. 9 ka, with the most intensive paleosol development, and the lowest aeolian activity in c. 7–5 ka. Weak paleosol development after c. 1.5 ka, but increased sand content, imply that human activities were enhanced in the interior of GHB in the Late Holocene.
Data Availability Statement
The original contributions presented in the study are included in the article/Supplementary Material, further inquiries can be directed to the corresponding author.
Author Contributions
CX performed the OSL dating, proxy data measurement and analysis, and finished writing the manuscript. CE contributed to the conception of the study, organization of the manuscript and manuscript revision. YS, JZ, and MS contributed to the modifications and suggestions. ZZ contributed to the age-depth model. YZ helps in the experimental treatment of OSL dating and proxy analysis.
Funding
The research was funded by the National Natural Science Foundation of China (Grant Nos 42171011, 41761042), the Natural Science Foundation of Qinghai (Grant No. 2021-ZJ-918).
Conflicts of Interest
The authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.
Publisher’s Note
All claims expressed in this article are solely those of the authors and do not necessarily represent those of their affiliated organizations, or those of the publisher, the editors and the reviewers. Any product that may be evaluated in this article, or claim that may be made by its manufacturer, is not guaranteed or endorsed by the publisher.
Acknowledgments
We thank Ji Xianba, Qiang Peng, Liqian Xie, Fajun Su, Yang Li, Guochuan Xia for helps in the field and thank Barbara Rumsby for editing the manuscript. Special thanks to reviewers and editor Zhiwei Xu whose constructive suggestions and detailed comments helped to clarify and improve the paper.
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Keywords: aeolian activity, high resolution, OSL dating, holocene climate, human activities
Citation: Xu C, E C, Shi Y, Zhang J, Sun M, Zhang Z and Zeng Y (2022) Holocene Aeolian Activity Recorded by Mountain Paleosols, Gonghe Basin, Northeast Qinghai-Tibet Plateau. Front. Earth Sci. 10:832993. doi: 10.3389/feart.2022.832993
Received: 10 December 2021; Accepted: 17 January 2022;
Published: 10 February 2022.
Edited by:
Zhiwei Xu, Nanjing University, ChinaReviewed by:
Ruijie Lu, Beijing Normal University, ChinaBernd Wünnemann, Southwest Jiaotong University, China
Copyright © 2022 Xu, E, Shi, Zhang, Sun, Zhang and Zeng. This is an open-access article distributed under the terms of the Creative Commons Attribution License (CC BY). The use, distribution or reproduction in other forums is permitted, provided the original author(s) and the copyright owner(s) are credited and that the original publication in this journal is cited, in accordance with accepted academic practice. No use, distribution or reproduction is permitted which does not comply with these terms.
*Correspondence: Chongyi E, ZWNob25neWlAMTYzLmNvbQ==