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Detrital zircon trace elements from the Mesozoic Jiyuan Basin, central China and its implication on tectonic transition of the Qinling Orogenic Belt

  • Min Wang , Wenfei Guo and Wentao Yang EMAIL logo
Published/Copyright: April 1, 2019
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From the journal Open Geosciences Volume 11 Issue 1

Abstract

The Qinling Orogen and the Jiyuan Basin constitute a basin-mountain system during the Early Mesozoic. Therefore, sediments from the Jiyuan Basin can be used to deduce the orogenic process of the Qinling Orogen. This paper attempts to use detrital zircon trace elements with ages ranging from the Late Carboniferous to the Middle Triassic that were obtained from the Jiyuan Basin to discuss the tectonic evolution of Qinling Orogen. On the tectonic setting discriminating diagrams, most grains are concentrated in convergent continental margins/orogenic settings,whereas the remaining samples (268 Ma, 265Ma, 264 Ma and 254Ma) are plotted in anorogenic field. Compared to the Early Paleozoic (400-500Ma) zircons, 306Ma and 281Ma grains represent higher Th/ Nb ratios, which might be related to the Mianlve oceanic crust subduction. The lower Th/Nb ratios containing 268 Ma, 265Ma, 264 Ma and 254Ma grains might indicate lithospheric extension subsequently. The final continent-continent collision between South China and North China blocks took place after the Middle Triassic (242Ma).

Keywords: Zircon; Basin-mountain interaction; Subduction-collision transition; Mianlve Ocean

1 Introduction

Zircon has strong resistance to weathering and/or alteration during sedimentation, magmatism, and metamorphism. Therefore, zircon U-Pb ages, along with Hf and O isotopes, are widely used in earth science researches [1, 2, 3, 4]. The trace element composition of magmatic zircon is strongly controlled by the composition of parental melts [5, 6]. Although some challenges exist like the complicated trace element distribution in zircons, it can also be an indispensable tool that should be developed for application in discriminating the host rock types [5, 6, 7, 8, 9], magmatic evolution and metamorphism [10, 11], crustal evolution [12], reconstructing mountain-basin interaction [14, 15].

Many investigations, concerning detrital zircon chronology, have been successfully performed in the surrounding basins of the Qinling Orogen [4, 16, 17, 18, 19, 20, 21, 22, 23, 24, 25,]. The Qinling Orogen emerged as the closure of the Mianlve Ocean, which resulted in the final amalgamation of the South China Block and the North China Block [26, 27]. But the Mianlve suture is now largely buried by later long-distance overthrusting [28, 29]. Therefore, to investigate the tectonic evolution of the Mianlve Ocean seems difficult. However, the Late Paleozoic detrital zircons largely persevered in the surrounding basins of the Qinling Orogen are suggested to be related to the Mianlve suture zone [18]. These zircons can be a good object to collect some important information about the development of the Mianlve Ocean. In addition, provenance analysis of the Late Paleozoic sediments on the southern North China Block reveals that the tectonic uplift of the Qinling Orogen retreated during the Permian [20, 30, 31, 32, 33]. However, there is a lack of data describing the Permian tectonic transition of the Qinling Orogen.

There are some important achievements regarding interactions between Jiyuan Basin and Qinling Orogen during Middle Triassic to Middle Jurassic. These works mainly focus on the filling feature of sediments [34, 35], geochemistry of mudstones [36, 37], detrital zircon geochronology and Hf isotopes [24, 33, 38], and suggest that the Late Triassic was the critical period to the formation of the Jiyuan Basin controlled by the Qinling orogenesis. This paper focuses on the detrital zircons from the Middle Triassic-Middle Jurassic Jiyuan Basin and integrated zircon geochronology with geochemistry, to unravel the evolutional process of the Mianlve Ocean during the Late Paleozoic to the Middle Triassic.

2 Geological setting

The Qinling Orogen is expressed as the South China, Qinling, and North China blocks converged along the Shangdan and Mianlve suture zones [26, 27]. These two sutures, integrated with the Luanchuan fault, separate the Qinling Orogen into the North Qinling and the South Qinling belts (Figure 1-a, b).

Figure 1 (a) the location of the Qinling Orogen and the Jiyuan Basin in China. (b) schematic tectonic map of the Qinling Orogen and the surrounding basins. (c) geological sketch map of the Jiyuan Basin defined by the Mesozoic strata, and showing the sampled location.
Figure 1

(a) the location of the Qinling Orogen and the Jiyuan Basin in China. (b) schematic tectonic map of the Qinling Orogen and the surrounding basins. (c) geological sketch map of the Jiyuan Basin defined by the Mesozoic strata, and showing the sampled location.

The Shangdan Ocean is considered to be formed at least before the Cambrian [26]. The northward subduction of the Shangdan Ocean plate didn’t happen until the early time of Cambrian [39, 40, 41]. A large number of subduction-related intrusions, mainly concentrated at 514-420 Ma, are found in the North Qinling Belt [27, 42]. The closure of the Shangdan Ocean, constrained by the detrital zircons from the Liuling Group [43], is considered to have occurred in the Early Devonian. Thereafter the North Qinling Belt was exhumed and denudated [44], however the deposition continued on the South Qinling Belt. A continent-continent subduction model, expressed as the subduction of the South Qinling Belt underneath the North Qinling Belt, is proposed to visualize the tectonic evolution along the Shangdan suture during the Late Paleozoic [26, 27].

The Mianlve Ocean might be formed at the Devonian and constrained from expanding before the Carboniferous [27, 40]. The island-arc volcanics from the Permian to Early Triassic indicate the subduction of the Mianlve Ocean along the southern margin of the South Qinling Belt [45, 46]. The Mianlve Ocean closed at the Late Triassic, which resulted in the Triassic orogeny between the South China Block and the North China Block [47]. The syncollisional granites with the ages of 220-210 Ma are largely distributed in the South Qinling Belt [48], and the post-collision process occurred subsequently during ca. 210-200 Ma.

The Jiyuan Basin is located to the north of Qinling Orogen, and adjacent to the Taihang Mountains (Figure 1-b, c). During the Early to Middle Triassic, the Jiyuan Basin was an intracratonic terrestrial depression in the south margin of the North China Block and developed a suit of red beds with stable distribution [35, 49, 50]. The Liujiagou Formation in the low part of the Early Triassic strata mainly represents several layers of light red conglomerates intercalated in purple red thick-bed middle-fine grained sandstones and thin-bed mudstones. The Heshanggou Formation in the upper part of the Lower Triassic strata is composed of bright red siltstones and mudstones with incidental fine grain conglomerates. The Middle Triassic strata can be divided into two formations by the occurrence of green mudstones. The lower part named Ermaying Formation is characterized by grayish yellow sandstones interbedded with purple red siltstones and mudstones, whereas the upper part named Youfangzhuang Formation contains yellow green fine grained sandstones interbedded with purple red and green siltstones, muddy sandstones and sandy mudstones. As the South China Block collided with the North China Block in the Late Triassic, the eastern part of North China Block was extensively uplifted, whereas the western part underwent tectonic subsidence [34, 35, 51]. Continuous deposition occurred in the Jiyuan Basin forming the Chunshuyao and Tanzhuang formations in ascending order. Both of the formations represent gray yellow fine-grained sandstones, siltstones, sandy mudstones and mudstones, but the Tanzhuang Formation contains 9-10 layers of black oil shales. Great changes took place in the depositional environment, sedimentary sequence and petrographic features, which indicated the tectonic attribute of Jiyuan Basin alternated from a part of intracraton to a foreland basin [34, 35, 51]. The lithofacies evolved into thick conglomerates and coal beds in the southern part of the Basin and lacustrine turbidites in the northern part of the Basin were controlled by the intense thrusting of Qinling Orogen during the Early Jurassic [52, 53]. This unit named the Anyao Formation mainly consists of gray yellow thick layered fine-grained sandstones, gray green mudstones, muddy sandstones and siltstones. The Middle Jurassic Yangshuzhuang Formation records a sequence of a shore-shallow lacustrine sedimentary system, with gray yellow and gray green mudstones, intercalated with yellow muddy sandstones, siltstones and fine-grained sandstones. The Jiyuan foreland basin was closed in the late Middle Jurassic as the Taihang Mountains uplift. The Maao Formation, unconformable to the underlying Yangshuzhuang Formation,was formed during this period, and represented a series of coarse quartz sandstones in the lower part and green mudstones in the upper part.

3 Zircon geochronology

The sedimentary evolution history suggests that the Jiyuan foreland basin developed from the Late Triassic to the Early Jurassic [35, 37], which should theoretically preserve sediments derived from the Qinling Orogen. Therefore, detrital zircon samples mainly concentrated on this period, but two samples are collected from the Middle Triassic Youfangzhuang Formation and Middle Jurassic Maao Formation respectively to have a comparison between each stage of the basin-mountain interaction (Figure 2). Samples from the Youfangzhuang and Chunshuyao formations are medium-grain sandstones, but fine-grain sandstones from the Tanzhuang, Anyao and Yangshuzhuang formations, whereas a sample from the Maao Formation represents coarse-grain sandstone.

Figure 2 Measured section from the Middle Triassic to Middle Jurassic Youfangzhuang, Chunshuyao, Tanzhuang, Anyao, Yangshuzhuang and Maao formations.
Figure 2

Measured section from the Middle Triassic to Middle Jurassic Youfangzhuang, Chunshuyao, Tanzhuang, Anyao, Yangshuzhuang and Maao formations.

Sample preparation and test procedure were given by Yang et al. [24]. Off-line conversion of signals into isotope ratios, ages, and geochemical data were conducted by software ICPMSDataCal [54, 55]. Concordia diagrams and weighted mean age calculations were generated by using the Isoplot 3.0 software [56]. Six detrital zircon samples yielded a total of 444 available ages (more than 90% concordance, discordance was defined as 100% ×abs [1(206Pb/238U age)/(207Pb/235U age)], Figure 3). They are plotted on a probability density diagram and can be characterized by the age peaks at: 2.5 Ga, 1.9Ga, 840 Ma, 439 Ma, and 261 Ma, respectively (Figure 4-a). 2.5 Ga and 1.9 Ga represent the tectonic-magmatic events during the Late Neoarchean in North China Block [57, 58] and the development of Paleoproterozoic Trans-North China Orogen [59, 60, 61, 62], respectively (Figure 4-f). 840 Maand 439 Maare associated with the Qinling Orogenic Belt (Figure 4-h). They represent the Neoproterozoic collisional event on the south margin of North China Block [48, 63] and the subduction-collision of Qinling Block with the North China Block along the Shangdan zone [64, 65], respectively.

Figure 3 The relative probability density diagrams of detrital zircon U-Pb ages for the analyzed samples [24]. (a) detrital zircon U-Pb ages from the Middle Triassic Youfangzhuang Formation; (b) detrital zircon U-Pb ages from the Late Triassic Chunshuyao Formation; (c) detrital zircon U-Pb ages from the Late Triassic Tanzhuang Formation; (d) detrital zircon U-Pb ages from the Early Jurassic Anyao Formation; (e) detrital zircon U-Pb ages from the Middle Jurassic Yangshuzhuang Formation; (f) detrital zircon U-Pb ages from the Middle Jurassic Maao Formation.
Figure 3

The relative probability density diagrams of detrital zircon U-Pb ages for the analyzed samples [24]. (a) detrital zircon U-Pb ages from the Middle Triassic Youfangzhuang Formation; (b) detrital zircon U-Pb ages from the Late Triassic Chunshuyao Formation; (c) detrital zircon U-Pb ages from the Late Triassic Tanzhuang Formation; (d) detrital zircon U-Pb ages from the Early Jurassic Anyao Formation; (e) detrital zircon U-Pb ages from the Middle Jurassic Yangshuzhuang Formation; (f) detrital zircon U-Pb ages from the Middle Jurassic Maao Formation.

Figure 4 Relative probability of detrital zircon U-Pb ages from the surrounding basins of Qinling Orogen. (a) Middle Triassic-Middle Jurassic sediments from Jiyuan Basin [24]; (b) Late Triassic sediments from Erdos Basin [4, 23]; (c) Jurassic sediments from Hefei Basin [66]; (d) Late Triassic sediments from Songpan-ganzi Basin [22]; (e) Middle-Late Triassic sediments from Sichuan Basin [19]; (g) Jurassic sediments from Huangshi basin [67]; (f), (h) referenced from Yang et al. [24].
Figure 4

Relative probability of detrital zircon U-Pb ages from the surrounding basins of Qinling Orogen. (a) Middle Triassic-Middle Jurassic sediments from Jiyuan Basin [24]; (b) Late Triassic sediments from Erdos Basin [4, 23]; (c) Jurassic sediments from Hefei Basin [66]; (d) Late Triassic sediments from Songpan-ganzi Basin [22]; (e) Middle-Late Triassic sediments from Sichuan Basin [19]; (g) Jurassic sediments from Huangshi basin [67]; (f), (h) referenced from Yang et al. [24].

Additionally, we suggest that the Late Paleozoic- Middle Triassic zircons with age peaks at 261 Ma are also related to the Qinling Orogen. The following arguments are considered: (1) although most opinions suggested that the Late Paleozoic detrital zircons delivered from the Inner Mongolia Palaeo-Uplift (the northern margin of North China Block) [30, 31, 38], the age peak of these zircons (290-300Ma) is different with the samples from Jiyuan Basin. (2) 400-500Ma detrital zircons not only exist largely in the Carboniferous Benxi Formation in the North China Block [32], but also in the overlying strata Taiyuan Formation with the extra 900-1000 Ma detrital zircons [38]. These dates suggest that the North Qinling was a highland during the Late Carboniferous and Early Permian. Although provenance analysis of Early-Middle Permian strata revealed that the source area was converted to the north margin of the North China Block [38], the detrital composition statistics from the Upper Permian sandstones represented high quartz and feldspar content, indicating arc orogen sources [34]. This fact confirmed that the Qinling was uplifted in the Late Permian (253 Ma), which was in accordance with the progradational delta deposit system developing on the south margin of North China Block [34]. As the Qinling Orogen continuously uplifted in the Triassic [35], a large amount of sediment sourced from the Qinling Orogen is preserved in the Early Triassic strata [33]. Therefore, the Qinling Orogen was certainly an important source to the Jiyuan Basin as the mountain building after the Middle Triassic. (3) The Late Paleozoic materials were found in the surrounding basins of Qinling Orogen, such as the Ordos Basin [4, 23] (Figure 4-b), Hefei Basin [66] (Figure 4-c), Songpan-Ganzi Basin [22] (Figure 4-d), Sichuan Basin [18, 19] (Figure 4-e), Huangshi Basin [67] (Figure 4-g), and also the internal basin of the Qinling orogen [68]. Qian et al. [18] suggested that these zircons might derive from the Mianlve suture zone, which were now largely buried by later long-distance overthrusting [28, 29].

4 Zircon trace elements

62 Late Paleozoic-Middle Triassic detrital zircons were compared with 36 Early Paleozoic (500-400Ma) zircons to evaluate the tectonic significances, because the Early Paleozoic zircons might provide valuable information in subduction and collision [46]. However, many restrictive factors, such as apatite and monazite inclusions, metamorphism, secondary alteration, and metamictization, make the difficulties for zircon trace elements interpretation [10, 11, 69]. Therefore, it is important to distinguish magmatic zircons from LREE overabundance zircons, metamorphic zircons, and hydrothermal zircons.

Metamorphic zircon experiences a complex elementary process of solution and reprecipitation, substitution, and diffusion [5, 70, 71]. Therefore, magmatism signatures are hardly deciphered by metamorphic zircon trace elements. Metamorphic zircons usually show considerably lower Th/U, which can be a criterion to distinguish magmatic zircon from metamorphic zircon [11, 72, 73]. Figure 5-a shows the selected zircons with Th/U > 0.1.

Figure 5 Magmatic genesis zircons discriminating diagrams. (a) zircon age and Th/U relationship diagram; (b) The overabundance of the LREE discriminating diagram. Igneous zircon fields data are from [5]; (c), (d) magmatic zircon and hydrothermal zircon discriminating diagrams. Color-shaded fields of “magmatic” and “hydrothermal” are from Hoskin [77].
Figure 5

Magmatic genesis zircons discriminating diagrams. (a) zircon age and Th/U relationship diagram; (b) The overabundance of the LREE discriminating diagram. Igneous zircon fields data are from [5]; (c), (d) magmatic zircon and hydrothermal zircon discriminating diagrams. Color-shaded fields of “magmatic” and “hydrothermal” are from Hoskin [77].

REE pattern of zircons is distinctly influenced by the existence of garnet, monazite and feldspar under various metamorphic conditions [74, 75, 76]. Therefore, abnormal REE patterns of zircons, such as LREE-overabundance or HREE-depleted, should be removed. In addition, LREE-overabundance is not always displayed on the chondrite-normalized REE distribution diagram. LaN and ΣLREE (La, Ce, and Pr) values are suggested to illustrate whether the LREE is over enriched (Figure 5-b).

Various trace element compositions of hydrothermal zircon can be formed in similar geological and geophysical conditions, which cause considerable difficulties for the trace elements interpretation [5]. (Sm/La)N-La and PrN-LaN diagrams can be used to distinguish hydrothermal zircon from magmatic zircon [77] (Figure 5-c, d).

On the basis of the foregoing works, the remaining zircons contain 27 grains with ages ranging from the Late Carboniferous to the Middle Triassic and 23 Early Paleozoic grains. LA-ICP-MS trace element data for these zircons are listed in Table 1. They possess steep chondrite-normalized REE patterns with positive Ce and negative Eu anomalies (Figure 6), and high Th/U (Th/U = 0.28-2.35), which are indicative of derivation from an igneous source [5, 78].

Figure 6 Rare earth element (REE) concentrations normalized to chondrite [98] for magmatic genesis zircons.
Figure 6

Rare earth element (REE) concentrations normalized to chondrite [98] for magmatic genesis zircons.

5 Discussion

5.1 Provenance signatures of zircons

Grimes et al. [13, 79] suggested Hf and Y versus U/Yb diagrams to discriminate zircons crystallized in oceanic crust from continental zircon. Further contribution had been done to introduce various tectonic settings to these diagrams [14], which was beneficial to detrital zircon provenance analysis. Figure 7-a and b show that most of the zircon samples are plotted in convergent continental margins. Little of them are present in the mixed field of convergent continental margins and post-collision extensional settings. Yang et al. [15] proposed two discriminating diagrams, Th/U versus Nb/Hf and Th/Nb versus Hf/Th, to understand the tectonic settings (Figure 7-c, d). The results show that most of zircon samples are plotted in an arc/orogenic-related field, while 264Ma sample indicates a within-plate/anorogenic setting. There are also several grains, including 268 Ma, 265 Ma and 254 Ma samples, falling in the mixed field.

Figure 7 The possible tectonic settings of magmatic genesis zircons. Zircon Hf and Y vs. U/Yb diagrams from Grimes et al. [13] and Gao et al. [14]; Zircon Th/U vs. Nb/Hf and Th/Nb vs. Hf/Th diagrams from Yang et al. [15].
Figure 7

The possible tectonic settings of magmatic genesis zircons. Zircon Hf and Y vs. U/Yb diagrams from Grimes et al. [13] and Gao et al. [14]; Zircon Th/U vs. Nb/Hf and Th/Nb vs. Hf/Th diagrams from Yang et al. [15].

Barth et al. [80] suggested that the Th/Nb ratio could be used to discriminate zircons crystallized from arc-related magmas, MORB (mid ocean ridge basalt), and OIB (oceanic island basalt) lavas. Compared to the Early Paleozoic (400-500Ma) zircons mainly formed under the subduction-collision setting [41, 46], 306Ma and 281Ma grains with higher Th/Nb ratios may reflect arc-related magmas with more differentiated materials. Grains of 268 Ma, 265 Ma, 264 Ma and 254 Ma with lower Th/Nb ratios indicate the enhanced involvement of mantle materials (Figure 8).

Tab.1

LA-ICP-MS analytical results (ppm) of magmatic origin zircon trace elements with the ages ranging from the Late Carboniferous to the Middle Triassic from the Jiyuan basin, China.

Sample206PB/238U
No.Age(Ma)lσPbThUPTiYNbLaCePrNdSmEuGdTbDyHoErTmYbLuHf
J-m-5-822258.9902031106.91970.730.04218.10.060.551.030.294.31.4166297721612408
T-c-5-8242228.1440565873.16351.100.22731.60.282.443.671.6213.94.4491990212305611393
J-m-12-224345.610311419615.83631.000.01125.20.061.432.420.7811.63.535125010982010150
T-y-6-7249319.14053482254.811052.020.08551.80.386.318.793.0331.59.09935157353507211459
J-m-11-225446.31001242342.311356.360.18024.20.151.495.050.0426.49.410942174353166010292
J-m-1-7255316.12043171344.77810.560.04812.60.152.304.661.2618.96.26925115262555510720
T-c-6-9255223.933647440812.918603.930.06430.00.244.277.162.3638.812.916364288625801118713
J-m-10-125937.935178431.61160.180.0021.10.000.180.310.081.60.573185571410953
J-m-10-6259314.22682643748.318273.230.04719.20.335.148.721.5743.013.216564287595431107991
J-m-7-626348.813617225813.08030.990.01613.60.061.403.010.5917.55.77026119252354811242
J-m-8-326439.51191883557.37851.360.00712.90.040.491.870.3313.65.06226123272575212331
J-m-6-4264318.12253603132.6247811.760.04244.90.184.2810.800.4869.824.127899400725741018146
J-m-2-6264325.1188513891.93890.630.0708.70.040.780.650.234.41.7241161161924613814
T-y-2-826548.117913232411.211621.690.03628.40.192.355.961.5128.69.410839179383627210247
J-m-1-5265313.41932491922.615306.360.01424.10.121.975.800.0335.212.71525724248415789735
J-a-10-42662613.12712233045.711371.620.07029.90.233.576.111.9225.37.99637175414259010778
T-t-7-8268224.62264985911.018368.090.00220.50.051.234.280.1430.711.6151633006969413711864
T-y-3-3272410.91691932336.67502.890.00955.60.121.873.651.2218.45.56725117262505210174
J-m-1-1275317.82203932242.58921.820.03914.60.070.912.460.4514.05.36828140333267010738
J-m-4-8277317.32043253536.412690.900.19812.50.223.144.751.3026.18.510442196444389010861
T-t-3-3280417.61823352735.28101.100.0209.80.071.302.670.4913.24.66326126292835911413
J-m-7-1281341.09526252491.413750.120.10910.10.345.667.594.3632.110.31174320045461964863
T-y-6-8284339.35586683101.923463.300.07133.80.458.3213.132.8760.919.1216793587874014710671
J-m-6-2306411.81991811115.23820.170.0244.80.091.191.821.408.42.632126014158369160
T-c-6-8307327.31714952264.112744.450.04427.20.080.942.661.5717.66.586382015156112811463
T-t-11-7312417.74832054784.222964.340.19873.01.0613.8720.818.7386.424.225184336675821089544
T-c-6-6334339.45615392576.916837.070.18479.80.527.7412.033.1945.214.215856244514779010129
T-t-1-6359412.81011862025.214621.100.0134.80.174.158.910.8740.213.014653221433817310130
T-t-3-5361416.824121432613.112611.810.11427.90.303.426.120.8631.29.511142183373376511948
J-y-3-2374339.12985322123.58594.610.00844.40.030.601.940.4712.14.86427137323387311479
T-t-2-6383515.32291773914.215052.070.01430.30.386.079.613.7043.312.313950222484649910694
J-a-4-6384413.21401651705.85302.220.03227.00.050.191.870.429.73.4411782202074210688
J-y-7-4388330.52643864674.812882.230.00638.00.071.964.421.2723.98.210342202454469510441
J-m-5-4393550.43256742894.811303.050.18316.20.947.337.682.4226.99.110237168373407011293
J-y-9-6406361.84767583126.69847.590.05254.50.232.753.130.6516.46.37732153363557211881
J-y-1-342168.97210420412.83980.900.00514.40.040.651.320.357.82.83413601413127Hill
J-y-9-2421530.925736927110.07781.480.01021.20.101.633.140.9215.75.36124118282755910484
J-y-2-5421511.613412232010.26600.660.00228.90.121.884.291.2717.95.2592195201964110352
J-y-11-2421521.931721622114.08800.900.04929.70.6710.7613.555.1740.110.0943011423207408473
J-y-16-1423450.73416311152.16151.470.04230.20.091.732.761.3313.03.8461888212295211101
J-y-3-4429421.218823421010.811720.750.0029.40.233.565.860.6725.08.610140178373356810809
J-y-8-3432610.612111126218.812580.770.03716.90.405.768.921.8835.210.611943180363316610000
J-y-12-1436511.11071191696.17920.850.04419.10.273.965.342.2523.56.66925114252525510190
J-y-6-2436610.38011523610.35371.530.00215.80.040.471.250.308.53.3431783191873911572
J-y-5-443869.77410734310.05790.370.01016.90.050.961.960.6311.33.9461886191944210980
J-a-3-2440453.42446411950.58332.080.0457.90.040.931.730.2311.24.46026136333427312360
J-y-7-1446546.42845382556.06871.990.22615.10.483.693.411.1011.73.94920108272977110991
J-a-2-4459455.0181635198910.631963.030.1224.60.142.106.940.1751.221.4283114525111100218213212
J-y-2-4463532.333230941517.68211.300.05030.70.335.045.591.9021.16.1692712326254549801
J-y-17-247468.149881706.73620.950.0067.00.010.380.930.435.21.825115915175439945
J-y-4-1511616.515914018219.93922.220.00628.40.142.314.180.6515.14.341145410901610667
Figure 8 Th/Nb against the detrital zircon ages diagram.
Figure 8

Th/Nb against the detrital zircon ages diagram.

The Late Carboniferous - Middle Triassic zircons were largely persevered in the Late Paleozoic - Middle Triassic strata in the North China Basin [24, 30, 32, 33, 38]. Some authors argued that these zircons were sourced from the Inner Mongolia Palaeo-Uplift in the north margin of the North China Block. The Inner Mongolia Palaeo-Uplift experienced crustal contraction related to the collision of the North China Block and the Mongolia terrane during the Middle Permian, and crustal extension caused by upwelling of calc-alkali magma at the end of the Permian [81]. Another controversial source area is the Xingmeng Orogen (the south margin of the Central Asian Orogenic Belt) along the north margin of the North China Block. Two main arguments had been proposed to explain the tectonic evolution of the Xingmeng Orogen: (1) the north margin of North China Block was an Andean-style continental margin at the Late Carboniferous, which represented the subduction of the paleo-Asian oceanic plate beneath the North China Block. Postcollisional/postorogenic lithospheric extension occurred after the final collision between the Mongolian arc terranes with the North China Block during the Late Permian-Middle Triassic [82, 83, 84]. (2) The Xingmeng Orogen was generated at the Middle Devonian, and then stepped into the post-collision at the Late Devonian-Early Carboniferous [85, 86, 87]. These tectonic evolutional models are not consistent with the result of the zircon trace element analyses in this paper, which indicates that the Late Carboniferous - Middle Triassic zircons mainly crystallized from the subduction-collision/orogenic setting, only a few of them (zircon ages of 268 Ma, 265 Ma, 264 Ma and 254 Ma) displayed an extensional/anorogenic environment. For these perspectives, the Late Carboniferous - Middle Triassic detrital zircons are most likely derived from the Qinling Orogen along the south margin of the North China Block, which is consistent with the detrital zircon age analyses as discussed above.

5.2 Development of the Mianlve Ocean

The Mianlve Ocean is interpreted as a remnant branch of the Palaeo-Tethys Ocean that rifted from the north margin of the South China Block. Most scholars believed that the Mianlve Ocean developed from the Late Paleozoic to Middle Triassic [26, 27]. Therefore, the most probably source of the Late Carboniferous - Middle Triassic detrital zircons are related to the Mianlve suture zone [18], which in turn can be used to decipher the tectonic evolution of the Mianlve Ocean.

According to the zircon trace element analyses, continent-continent subduction between the South Qinling Belt and the North Qinling Belt could generate more differentiated materials before the Early Permian (281Ma). After that, the subduction of the Mianlve Ocean was formed, which could weaken the continent-continent subduction [26, 27]. Then afterwards, some mantle materials could intrude into the upper crust at the Middle Permian (268Ma),which could result in extension of the lithosphere restrictedly. This tectonic regime may be lasting to the Early Triassic (254Ma). The final continent-continent collision between South China and North China blocks took place after the Middle Triassic (242Ma) (the formation of mostly granites occurred in subduction zones and post-collision extensional settings, [46]), then the Qinling Orogen stepped into mountain buliding. This evolution process can be responded by the Late Paleozoic paleogeography of the southern North China Block. Provenance analyses indicated that the Qinling Orogen was a highland during the Late Carboniferous to Early Permian [31, 32]. This topographic feature constrained transgression had to take place from the northeast of the North China Block at the Late Carboniferous. However, topographic conversion occurred at the Middle Permian, which could be certified by the transgression originated from the southeast of the North China Block and the fluvial delta extended from north to south [88, 89]. We attributed the subsidence of southeastern edge of the North China Block (including the Qinling Orogen) to the extension occurred in the Qinling Orogen. Marine deposits ending at the Early Triassic might be related to the continuous subduction of the Mianlve Oceanic plate. In addition, Wang et al. [20] reported detrital zircon U-Pb ages from the Middle - Late Permian sediments in the southern North China Block. Their data suggests that the south margin of the North China Block and the Qinling Orogen subsided during the Middle Permian, and subsequently uplifted during the late Late Permian. This conclusion supports the viewpoint from the zircon trace elements in this paper.

Many other geologic records have also been listed to demonstrate the Late Paleozoic oceanic subduction in the Qinling Orogen, such as subduction-related deformation [90], zircon trace elements and types of mineral inclusions [91, 92], Permian-Triassic HP metamorphic terrane in the Tongbai Orogen [93], muscovite 40Ar/39Ar ages obtained from the Nanwan flysch (262 ± 2 Ma) and the Foziling Group (271 - 261 Ma) [62, 94], and the island-arc volcanics from the Permian to Early Triassic along the south margin of the South Qinling Belt [45, 95, 96]. In addition, the Late Paleozoic-Early Triassic trough in the Qinling Orogen might be the response to the extension [96, 97].

In summary, the Qinling Orogen was a highland during the Late Carboniferous, which should be related to the Early Paleozoic tectonic framework or the initial subduction of the Mianlve Ocean (Figure 9-a). The lithospheric extension could be understood as back-arc spreading, which made the Qinling Orogen and the south margin of North China Block subsided (Figure 9-b). However, the continuous subduction of the Mianlve Ocean was existence and caused the strong uplift of the Mianlve suture zone (Figure 9-c). The lithospheric extension disappeared in the Middle Triassic, and then the continent-continent collision occurred in the Qinling Orogen (Figure 9-d).

Figure 9 Possible supplement of the sediments to the interior of the North China Block, and showing the tectonic uplift model of the Qinling Orogen. (Revised after Zhu et al. [31]). IMPU: Inner Mongolia Palaeo-Uplift; MO: Mianlve Ocean; NCB: North China Block; NQ: North Qinling Belt; SQ: South Qinling Belt; YZB: South China Block.
Figure 9

Possible supplement of the sediments to the interior of the North China Block, and showing the tectonic uplift model of the Qinling Orogen. (Revised after Zhu et al. [31]). IMPU: Inner Mongolia Palaeo-Uplift; MO: Mianlve Ocean; NCB: North China Block; NQ: North Qinling Belt; SQ: South Qinling Belt; YZB: South China Block.

6 Conclusion

  1. According to the analyses of magmatic zircon trace elements, most Late Carboniferous - Middle Triassic grains crystallized from convergent/orogenic tectonic settings. Only a small number of grains indicate extensional/anorogenic tectonic environments. The process of magmatism and tectonic evolution, proposed by the zircon trace elements, is different with that of the north margin of North China Block but similar to the Qinling Orogen. Integrated with detrital zircon age analyses, it is convincing that the Late Carboniferous - Middle Triassic detrital zircons are related to the Qinling Orogen rather than the north margin of the North China Block.

  2. The subduction of Mianlve Ocean was already formed before the Early Permian (281Ma), which induced the limited lithospheric extension subsequently. The final continent-continent collision between South China and North China blocks took place after the Middle Triassic (242Ma).

Acknowledgement

The present research was supported by the National Natural Science Foundation of China (Grant Nos. 41440016). We thank two anonymous reviewers for their critical comments. We also want to thank the editors for their help on the manuscript.

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Received: 2018-04-26
Accepted: 2018-11-17
Published Online: 2019-04-01

© 2019 W. Yang and M. Wang, published by De Gruyter

This work is licensed under the Creative Commons Attribution 4.0 Public License.

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https://doi.org/10.1515/geo-2019-0011
Keywords for this article
Zircon; Basin-mountain interaction; Subduction-collision transition; Mianlve Ocean
Creative Commons
BY 4.0

Articles in the same Issue

  1. Regular Articles
  2. 2D Seismic Interpretation of the Meyal Area, Northern Potwar Deform Zone, Potwar Basin, Pakistan
  3. A new method of lithologic identification and distribution characteristics of fine - grained sediments: A case study in southwest of Ordos Basin, China
  4. Modified Gompertz sigmoidal model removing fine-ending of grain-size distribution
  5. Diagenesis and its influence on reservoir quality and oil-water relative permeability: A case study in the Yanchang Formation Chang 8 tight sandstone oil reservoir, Ordos Basin, China
  6. Evaluation of AHRS algorithms for Foot-Mounted Inertial-based Indoor Navigation Systems
  7. Identification and evaluation of land use vulnerability in a coal mining area under the coupled human-environment
  8. Hydrocarbon Generation Potential of Chia Gara Formation in Three Selected Wells, Northern Iraq
  9. Source Analysis of Silicon and Uranium in uranium-rich shale in the Xiuwu Basin, Southern China
  10. Lithologic heterogeneity of lacustrine shale and its geological significance for shale hydrocarbon-a case study of Zhangjiatan Shale
  11. Characterization of soil permeability in the former Lake Texcoco, Mexico
  12. Detrital zircon trace elements from the Mesozoic Jiyuan Basin, central China and its implication on tectonic transition of the Qinling Orogenic Belt
  13. Turkey OpenStreetMap Dataset - Spatial Analysis of Development and Growth Proxies
  14. Morphological Changes of the Lower Ping and Chao Phraya Rivers, North and Central Thailand: Flood and Coastal Equilibrium Analyses
  15. Landscape Transformations in Rapidly Developing Peri-urban Areas of Accra, Ghana: Results of 30 years
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  18. Selected components of geological structures and numerical modelling of slope stability
  19. Spatial data quality and uncertainty publication patterns and trends by bibliometric analysis
  20. Application of microstructure classification for the assessment of the variability of geological-engineering and pore space properties in clay soils
  21. Shear failure modes and AE characteristics of sandstone and marble fractures
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  26. Petrographical and geophysical investigation of the Ecca Group between Fort Beaufort and Grahamstown, in the Eastern Cape Province, South Africa
  27. Ecological risk assessment of geohazards in Natural World Heritage Sites: an empirical analysis of Bogda, Tianshan
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  29. Go social for your own safety! Review of social networks use on natural disasters – case studies from worldwide
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  32. Using Monarch Butterfly Optimization to Solve the Emergency Vehicle Routing Problem with Relief Materials in Sudden Disasters
  33. Potential influence of meteorological variables on forest fire risk in Serbia during the period 2000-2017
  34. Controlling factors on the geochemistry of Al-Shuaiba and Al-Mejarma coastal lagoons, Red Sea, Saudi Arabia
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  37. The Mechanism and Control Technology of Strong Strata Behavior in Extra-Thick Coal Seam Mining Influenced by Overlying Coal Pillar
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  42. Remediation of Copper and Zinc from wastewater by modified clay in Asir region southwest of Saudi Arabia
  43. Sedimentary facies of Paleogene lacustrine dolomicrite and implications for petroleum reservoirs in the southern Qianjiang Depression, China
  44. Correlation between ore particle flow pattern and velocity field through multiple drawpoints under the influence of a flexible barrier
  45. Atmospheric refractivity estimation from AIS signal power using the quantum-behaved particle swarm optimization algorithm
  46. A geophysical and hydro physico-chemical study of the contaminant impact of a solid waste landfill (swl) in King Williams’ Town, Eastern Cape, South Africa
  47. Landscape characterization using photographs from crowdsourced platforms: content analysis of social media photographs
  48. A Study on Transient Electromagnetic Interpretation Method Based on the Seismic Wave Impedance Inversion Model
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  50. Variable secondary porosity modeling of carbonate rocks based on μ-CT images
  51. Traditional versus modern settlement on torrential alluvial fans considering the danger of debris flows: a case study of the Upper Sava Valley (NW Slovenia)
  52. The Influence of Gangue Particle size and Gangue Feeding Rate on Safety and Service Life of the Suspended Buffer’s Spring
  53. Research on the Transition Section Length of the Mixed Workface Using Gangue Backfilling Method and Caving Method
  54. Rainfall erosivity and extreme precipitation in the Pannonian basin
  55. Structure of the Sediment and Crust in the Northeast North China Craton from Improved Sequential H-k Stacking Method
  56. Planning Activities Improvements Responding Local Interests Change through Participatory Approach
  57. GIS-based landslide susceptibility mapping using bivariate statistical methods in North-western Tunisia
  58. Uncertainty based multi-step seismic analysis for near-surface imaging
  59. Deformation monitoring and prediction for residential areas in the Panji mining area based on an InSAR time series analysis and the GM-SVR model
  60. Statistical and expert-based landslide susceptibility modeling on a national scale applied to North Macedonia
  61. Natural hazards and their impact on rural settlements in NE Romania – A cartographical approach
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  63. Influence of Rapid Transit on Accessibility Pattern and Economic Linkage at Urban Agglomeration Scale in China
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  66. Unification of data from various seismic catalogues to study seismic activity in the Carpathians Mountain arc
  67. Quality assessment of DEM derived from topographic maps for geomorphometric purposes
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  69. Utilizing Maximum Entropy Spectral Analysis (MESA) to identify Milankovitch cycles in Lower Member of Miocene Zhujiang Formation in north slope of Baiyun Sag, Pearl River Mouth Basin, South China Sea
  70. Stability Analysis of a Slurry Trench in Cohesive-Frictional Soils
  71. Integrating Landsat 7 and 8 data to improve basalt formation classification: A case study at Buon Ma Thuot region, Central Highland, Vietnam
  72. Assessment of the hydrocarbon potentiality of the Late Jurassic formations of NW Iraq: A case study based on TOC and Rock-Eval pyrolysis in selected oil-wells
  73. Rare earth element geochemistry of sediments from the southern Okinawa Trough since 3 ka: Implications for river-sea processes and sediment source
  74. Effect of gas adsorption-induced pore radius and effective stress on shale gas permeability in slip flow: New Insights
  75. Development of the Narva-Jõesuu beach, mineral composition of beach deposits and destruction of the pier, southeastern coast of the Gulf of Finland
  76. Selecting fracturing interval for the exploitation of tight oil reservoirs from logs: a case study
  77. A comprehensive scheme for lithological mapping using Sentinel-2A and ASTER GDEM in weathered and vegetated coastal zone, Southern China
  78. Sedimentary model of K-Successions Sandstones in H21 Area of Huizhou Depression, Pearl River Mouth Basin, South China Sea
  79. A non-uniform dip slip formula to calculate the coseismic deformation: Case study of Tohoku Mw9.0 Earthquake
  80. Decision trees in environmental justice research — a case study on the floods of 2001 and 2010 in Hungary
  81. The Impacts of Climate Change on Maximum Daily Discharge in the Payab Jamash Watershed, Iran
  82. Mass tourism in protected areas – underestimated threat? Polish National Parks case study
  83. Decadal variations of total organic carbon production in the inner-shelf of the South China Sea and East China Sea
  84. Hydrogeothermal potentials of Rogozna mountain and possibility of their valorization
  85. Postglacial talus slope development imaged by the ERT method: comparison of slopes from SW Spitsbergen, Norway and Tatra Mountains, Poland
  86. Seismotectonics of Malatya Fault, Eastern Turkey
  87. Investigating of soil features and landslide risk in Western-Atakent (İstanbul) using resistivity, MASW, Microtremor and boreholes methods
  88. Assessment of Aquifer Vulnerability Using Integrated Geophysical Approach in Weathered Terrains of South China
  89. An integrated analysis of mineralogical and microstructural characteristics and petrophysical properties of carbonate rocks in the lower Indus Basin, Pakistan
  90. Applicability of Hydrological Models for Flash Flood Simulation in Small Catchments of Hilly Area in China
  91. Heterogeneity analysis of shale reservoir based on multi-stage pumping data
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