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Article

U-Pb Ages and Hf Isotopes of Detrital Zircon Grains from the Mesoproterozoic Chuanlinggou Formation in North China Craton: Implications for the Geochronology of Sedimentary Iron Deposits and Crustal Evolution

by
Chao Duan
1,*,
Yanhe Li
1,*,
Yun Yang
2,
Yongsheng Liang
2,
Minghui Wei
2 and
Kejun Hou
1
1
Ministry of Natural Resources Key Laboratory of Metallogeny and Mineral Assessment, Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing 100037, China
2
No. 3 Geological Brigade, Hebei Geological and Mineral Exploration Bureau, Zhangjiakou 075000, China
*
Authors to whom correspondence should be addressed.
Minerals 2018, 8(12), 547; https://doi.org/10.3390/min8120547
Submission received: 6 September 2018 / Revised: 20 November 2018 / Accepted: 21 November 2018 / Published: 26 November 2018
(This article belongs to the Section Mineral Geochemistry and Geochronology)
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Abstract

:
The Chuanlinggou Formation is the lower formation of the Changchengian System, and hosts sedimentary iron deposits (marine oolitic ironstones) of the North China Craton (NCC). To determine the age of the iron deposits, and provide insight into the crustal growth of the craton, laser ablation multiple collector inductively coupled plasma mass spectrometry (LA-MC-ICP-MS)U-Pb and in situ Hf isotope analysis were performed on detrital zircon grains. Samples were taken from the roof sand-shale of the sedimentary iron deposits at Jiangjiazhai and Pangjiapbu. Overall, 186 detrital zircon grain U-Pb ages yield three major age populations, with weighted average ages of 2450 Ma, 1848 Ma, and 1765 Ma, respectively. Four younger ages from magmatic zircon grains were obtained, ranging from 1694 to 1657 Ma. Combined with observations from published studies, the results define the lower limit for the age of the Chuanlinggou Formation, and constrain the age of the sedimentary iron deposits (marine oolitic ironstone) close to 1650 Ma. The peak ages of 1848 Ma and 2450 Ma define the major collisional events of the NCC. The age of 1765 Ma can be linked to the age range of the widespread mafic dyke swarms that represent the rifting of the NCC within the Columbia supercontinent. Detrital zircon grains from the Chuanlinggou Formation form two obvious groups, with different εHf (t) values ranging from −1 to −8 and from +1 to +8, which correspond to the U-Pb age ranges of 1.7–1.9 Ga and 2.3–2.6 Ga, respectively. They have a similar two-stage Hf model age peak at 2.65–2.85 Ga, suggesting that the source rocks for each of these events were derived from the recycling of ancient crust. The source rocks of the older group of zircon grains might be derived from juvenile crust with a short reworking period. The critical crust–mantle differentiation event might happen during the period of 2.65–2.85 Ga, marking the most significant stage of the crustal growth in the NCC.

1. Introduction

The North China Craton (NCC) covers an area of about 1.5 million km2 and is one of the oldest cratons, with age components as old as ~3.8 Ga [1,2,3]. The craton is bounded by the early Palaeozoic Qilianshan Orogen and late Palaeozoic Central Asian Orogenic Belt to the west and north, and the Mesozoic Qinling–Dabie and Su–Lu ultrahigh-pressure metamorphic belts to the south and east, respectively (Figure 1). From the Archean, the craton experienced a geological history containing many recorded tectonic and metamorphic events [2,4,5,6,7,8,9,10,11,12]. Three main models for the formation of the NCC have been proposed using stratigraphic, structural, metamorphic, geochemical, and geochronological studies. (1) The NCC was originally divided into several micro-blocks (Jiaoliao, Qianhuai, Fuping, Jining, Xuchang, and Alashan), which formed the final craton during the late Neoarchean (~2.5 Ga) [3,6,13,14,15,16,17]; (2) Zhao et al. (2001, 2005, 2012) [1,2,7] suggested a model for the evolution of the NCC, which divided the NCC into three parts: the Western Block, Eastern Block, and Trans-North China Orogeny (TNCO) (Figure 1). Prior to the collision of the Western and Eastern blocks along the TNCO at ~1.85 Ga, the Western Block was formed by the amalgamation of the Ordos Block in the south and the Yinshan Block in the north, along the east–west-trending Khondalite Belt, and the Eastern Block underwent a Paleoproterozoic rifting event along its eastern continental margin in the period 2.2–1.9 Ga, forming the Jiao-Liao-Ji Belt [18,19,20,21,22,23,24]; (3) Another model suggests that the Eastern and Western blocks were amalgamated at ca. 2.5 Ga, and that at ca. 1.85 Ga the Central Orogenic Belt experienced a metamorphic reworking/overprinting by the collision of the northern margin of the NCC with another continental block in the Columbia (Nuna) Supercontinent [25,26,27,28].
The North China Craton is rich in mineral resources; the Precambrian is one of the critical mineralization periods, which is marked by the appearances of large iron, rare earth elements, lead–zinc, and magnetite deposits [29,30]. Precambrian iron deposits are the most important mineral resource in the North China Craton, of which the banded iron formation (BIF) type is predominant, accounting for ~80% of metamorphosed sedimentary iron ores in China, with a peak formation age of 2.5–2.6 Ga [31,32,33,34,35,36,37]. Marine oolitic ironstone is another type of sedimentary hosted iron ore in the NCC, referred to as the Xuanlong type deposit in the Chinese literatures. The oolitic iron deposit is a distinctive subset of iron deposits, characterized by spherical grains composed of concentric layers containing hematite and goethite. Different to BIF, most deposits of this type have a biogenic origin. As a result of its special genesis environment, oolitic iron ores also provide much significant information about the evolution of palaeogeographic facies and marine chemical conditions [38,39,40]. Oolitic iron ores (ironstones) occur worldwide and were formed throughout the geological time from the Proterozoic Eon to the Cenozoic Era. In the NCC, it is considered to have occurred in the Mesoproterozoic, hosted in the Chuanlinggou Formation. However, the geochronology of the Chuanlinggou Formation with the oolitic iron deposit is still poorly understood.
In this study, we present U-Pb ages and Hf isotope data from detrital zircon grains from sand-shale samples collected from the roof of the sedimentary iron ores at Jiangjiazhai and Pangjiabu (Figure 1), in order to determine the chronology of the iron deposition, supplying a piece of the picture of the time frame of the distribution of oolitic iron deposits in the global context, and provide further information on the crustal growth and evolution of the NCC.

2. Geological Setting

2.1. Regional Geology

In the NCC, the marine oolitic ironstones are located in the Trans-North China Orogeny (TNCO), which was defined by Zhao et al. (2001, 2005) [1,2], with boundaries of the Xinyang–Kaifeng–Shijiazhaung–Jianping fault zone and the Huashan–Lishi–Datong–Duolun fault zone. During the late Archean to early Paleoproterozoic, the western margin of the Eastern Block faced a major ocean, and east-dipping subduction beneath the western margin of the Eastern Block led to the formation of magmatic arcs that were subsequently incorporated into the TNCO [7]. Continued subduction resulted in a major continental–continental collision, leading to extensive thrusting and high-pressure metamorphism. During the period 2.56–1.85 Ga, the Huai’an, Hengshan, Wutai, Fuping, Zanhuang, Lvliang, Zhongtiao, Dengfeng, Taihua, and other metamorphic complexes formed in the TNCO [41,42], providing records of the tectonic activity. The available age data for metamorphism and deformation in the Trans-North China Orogen indicate that this collisional event occurred at about 1.85 Ga ago, resulting in the formation of the TNCO and final amalgamation of the North China Craton [7,43]. After 1.80 Ga, the NCC experienced extensional tectonism, marked by the development of large mafic and alkaline intrusions [9,16,44]. The North China Craton experienced large-scale sedimentation in the Mesoproterozoic, forming the Changchengian System and the Jixianian System. The Changchengian System (~3000 m thick) contains four units from its base to top; the Changzhougou Formation (~860 m thick), Chuanlinggou Formation (~890 m thick), Tuanshanzi Formation (~520 m thick) and Dahongyu Formation (~480 m thick) (Zhang et al., 2015 [45] and references therein).

2.2. Chuanlinggou Formation

The Chuanlinggou Formation is widely distributed in North China and can be divided into three depositional regions. The eastern area, including Jixian, Zunhua, Xinglong, and Kuancheng, is characterized by the development of thick black shale. The middle area is located in the northern part of Miyun–Huairou and comprises lacustrine dolomite and lagoon facies depositions. The western area is located in the Xuanhua–Zhangjiakou area, where the thickness of the formation is significantly thinner, and is characterized by the development of the sedimentary iron rocks. Xuanlong type iron deposits occurred in this typical area.
The type profile of the Chuanlinggou Formation is divided into three members [46] (Figure 2a). Member one contains yellowish brown sandy shale with yellow-green siltstone and iron-rich sandstone. Clay minerals are mainly illite. Sandstone, siltstone, and shale exhibit obvious rhythmic sedimentary characteristics, with horizontal bedding and microwave bedding, mud cracks, and ripple level structures. The maximum thickness of one single rhythm is 127 mm; member two is mainly composed of black and dark grey silty shale, locally intercalated with thin silty bars and dolomite, with horizontal bedding. The silty shale is the basic rhythmic layer and is less than 1 cm thick; and member three is composed of black silty shale and greyish white thin siltstone, with 2–3 layers of lightly colored microcrystalline carbonaceous dolomite at the top, with wavy and horizontal bedding. Some bedding planes show mud cracks and underwater sliding load curling structures.
The Chuanlinggou Formation contains three ironstone layers: the lower one is a stromatolite hematite, the middle is a pisolitic and oolitic hematite, and the upper part is an oolitic hematite (Figure 2b). Between the layers is a sandy shale unit. There are commonly siderite intercalations or thin lenses in the transitional parts of the shale and hematite layers. The stromatolite hematite is purplish red, usually upright without bending, developing a single tubular or bell-shaped aggregate structure. Quartz grains are deposited among the stromatolite hematite and are cemented by siderite or hematite. The pillar shaped stromatolite hematite has a diameter of 0.5–2 cm and a height of about 5 cm. The columnar bedding is fine and regular and has good symmetry. Oolitic hematite is dark red, of which 50–70% is oolitic. Ooids vary in size, have a particle size of 0.5–3 mm, and are mostly spherical or sub-spherical. Most of the terrigenous clastic material, primarily quartz, is deposited between the oolitic grains. Most of the oolitic cores are single or clustered quartz grains, and sometimes they are also composed of iron debris and clay mineral mixtures, feldspar clasts and apatite fragments. The ooid shells have a transparent–translucent concentric ring structure and are composed mainly of hematite and siderite (Figure 3).
The sedimentary iron deposits are mainly distributed in the Zhangjiakou area, the western part of the Yanshan, in the south of Huai’an–Chicheng and north of Huaxiaoying–Xiahuayuan–Xinglinbao. This covers an area of 3900 km2, with a length of 130 km oriented east-west and a width of 154 km running north-south. There are 23 Xuanlong type iron deposits in the belt, containing 304 million metric tons (Mt) of iron [49]. In this study, the samples analyzed were collected from the roof sand-shale (Figure 2b and Figure 3d) overlying the first hematite layer of the Chuanlinggou Formation in representative iron deposits at Jiangjiazhai (JJZ12-08, E 115°34′55″ N 40°42′25″) and Pangjiabu (PJB12-11, E 115°27′31″ N 40°37′39″) (Figure 1).

3. Analytical Methods

3.1. Zircon LA-MC-ICP-MS U-Pb Dating

The samples were crushed and individual zircon grains were separated using conventional heavy liquid and magnetic techniques. Grains were handpicked under a binocular microscope, mounted in epoxy resin discs, and then polished. Zircon grains were examined under transmitted and reflected light, and then imaged by cathodoluminescence (CL) using a HITACHI S3000-N microprobe in the Institute of Mineral Resources, Geology Chinese Academy of Geological Sciences. The zircon grains, which were euhedral or subhedral, with a striped cathodoluminescence pattern and oscillatory zoning rims, were selected for U-Pb and Hf isotope dating.
U-Pb dating analyses were conducted by laser ablation multiple collector inductively coupled plasma mass spectrometry (LA-MC-ICP-MS) at the Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing. Detailed operating conditions for the laser ablation system and the MC-ICP-MS instrument and data reduction are the same as described by Hou et al. (2009) [50] and Liu et al. (2010) [51]. Laser sampling was performed using a New Wave UP 213 laser ablation system, with a beam diameter of 25 μm. A Thermo Finnigan Neptune MC-ICP-MS instrument was used to acquire ion-signal intensities. The array of four multi-ion-counters and three Faraday cups allows for the simultaneous detection of 202Hg (on IC5), 204Hg, 204Pb (on IC4), 206Pb (on IC3), 207Pb (on IC2), 208Pb (on L4), 232Th (on H2), and 238U (on H4) ion signals. Helium was used as a carrier gas. Argon was used as the make-up gas and mixed with the carrier gas via a T-connector before entering the ICP. Each analysis incorporated a background acquisition of approximately 20–30 s (gas blank) followed by 30 s of data acquisition from the sample. Off-line raw data selection and the integration of background and analyzed signals, as well as time-drift correction and quantitative calibration for U-Pb dating, were performed by ICPMSDataCal program [51]. Zircon GJ-1 was used as a reference material for U-Pb normalization, and was analyzed twice every 5–10 analyses. Time-dependent drifts of U-Th-Pb isotopic ratios were corrected using a linear interpolation (with time) for every 5–10 analyses according to the variations of GJ-1 (i.e., 2 GJ-1 zircon grains + 5–10 samples + 2 GJ-1 zircon grains) [51]. The preferred U-Th-Pb isotopic ratios used for GJ-1 are from Jackson et al. (2004) [52]. Uncertainty of preferred values for the external standard GJ-1 was propagated to the ultimate results of the samples. In all analyzed zircon grains, the common Pb correction has not been made due to the low signal of common 204Pb and high 206Pb/204Pb. U, Th, and Pb concentrations were calibrated by zircon GJ-1 (with U:315 ppm and Th: 9.33 ppm; Liu et al., 2010 [51]). Concordia diagrams and weighted mean calculations were made using Isoplot 3.0 [53]. The reference zircon Plešovice was treated as an unknown and yielded the weighted mean 206Pb/238U age of 336.6 ± 2.5 Ma (2σ, n = 20), which is in good agreement with the recommended 206Pb/238U age of 337.13 ± 0.37 Ma (2σ) [54].

3.2. In Situ Zircon Lu-Hf Isotope Analyses

The zircon Hf analyses of two samples were performed on the same grains as used for U-Pb dating. Zircon Hf isotope analysis was carried out in situ using a New Wave UP 213 laser-ablation microprobe attached to a Neptune multi-collector ICP-MS at the Key Laboratory of Metallogeny and Mineral Assessment, Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing. The same positions of zircon grains were used for the present analyses, with a beam diameter of 55 μm. Helium was used as the carrier gas to transport the ablated sample from the laser-ablation cell to the ICP-MS torch, via a mixing chamber where it was mixed with argon. To correct the isobaric interferences of 176Lu and 176Yb on 176Hf, the 176Lu/175Lu and 176Yb/173Yb values were determined (0.02658 and 0.796218, respectively) [55]. For instrumental mass bias correction, Yb and Hf isotope ratios were normalized to 1.35274 for 172Yb/173Yb [55] and to 0.7325 for 179Hf/177Hf using an exponential law. The mass bias behavior of Lu was assumed to follow that of Yb. The mass bias correction protocols details are described in Wu et al. (2006) [56] and Hou et al. (2007) [57]. Zircon GJ-1 was used as the reference standards during our routine analyses, with a weighted mean 176Hf/177Hf value of 0.282017 ± 0.000021 (2σ, n = 13). This is not distinguishable from the weighted mean 176Hf/177Hf value of 0.282000 ± 0.000005 (2σ) using a solution analysis method by Morel et al. (2008) [58]. Also, a Temora zircon standard was measured daily, giving a mean 176Hf/177Hf value of 0.282681 ± 33 (2σ, n =4), which is in good agreement with the recommended mean 176Hf/177Hf value of 0.282680 ± 31 [56].
εHf, T, and f are defined in this study as follows:
εHf(0) = [(176Hf/177Hf)S/(176Hf/177Hf)CHUR,0 − 1] × 10,000,
εHf(t) = [(176Hf/177Hf)S − (176Lu/177Hf)S × (eλt − 1)]/[(176Hf/177Hf)CHUR,0 − (176Lu/177Hf)CHUR × (eλt − 1)) −1] × 10,000,
TDM1 = 1/λ × ln{1 + [(176Hf/177Hf)S − (176Hf/177Hf)DM]/[(176Lu177Hf)S − (176Lu/177Hf)DM]},
TDM2 = TDM1 − (TDM1 − t) × [(fCC − fS)/(fCC − fDM)],
fS = (176Lu/177Hf)S/(176Lu/177Hf)CHUR − 1,
fCC = (176Lu/177Hf)C/(176Lu/177Hf)CHUR − 1, and
fDM = (176Lu/177Hf)DM/(176Lu/177Hf)CHUR − 1
where (176Lu/177Hf)S and (176Hf/177Hf)S are the sample measured values, (176Lu/177Hf)CHUR = 0.0332, (176Hf/177Hf)CHUR,0 = 0.282772, (176Lu/177Hf)DM = 0.0384, (176Hf177Hf)DM = 0.28325 [59], (176Lu/177Hf)C = 0.015 [60], t is the formation time of the sample, and λLu = 1.867 × 10−11 yr−1 [61]. TDM1 and TDM2 are the single-stage Hf model and two-stage Hf model ages, respectively. fCC, fS, and fDM are the fLu/Hf values of the crustal source, sample, and depleted mantle, respectively.

4. Analytical Results

The 200 detrital zircon grains have been subjected to U-Pb age dating, and the most concordant (>95%) results are listed in Table 1. The 186 concordant (>5%) detrital zircon grains have been analyzed for Hf isotopic data. The Lu-Hf isotope data are listed in Table 2. Representative zircon grain CL images and Th/U values are shown in Figure 4 and Figure 5. The results are presented as a series of concordia diagrams (Figure 6). The probability density maps of ages are given in Figure 7. Hf isotope characteristics and U-Pb ages of detrital zircon grains are shown in Figure 8 and Figure 9.

4.1. Sample JJZ12-08

The zircon grains collected from sample JJZ12-08 were mostly well rounded to short columnar in shape, with grain sizes ranging from 100 μm to 500 μm (Figure 4). One hundred zircon grain U-Pb ages were obtained, and 6 more discordant (>5%) zircon grains were discarded. Uranium concentrations ranged from 8 to 220 ppm, and thorium from 5 to 561 ppm. The Th/U values are mostly greater than 0.4 and are clustered at 0.6 to 1.5 (Figure 5), which, combined with the oscillatory growth zoning in CL images, indicates their magmatic origin [62,63,64,65]. The 94 grains yield three age populations: 1739–1799 Ma, with a weighted average age of 1774 ± 8 Ma (n = 22, MSWD = 0.73); 1839–1857 Ma, with a weighted average age of 1849 ± 8 Ma (n = 22, MSWD = 0.08); and 2436–2465 Ma with a weighted average age of 2453 ± 8 Ma (n = 10, MSWD = 0.71) (Figure 6 and Figure 7). There are two smaller populations with ages in the ranges of 1872–1907 Ma and 1945–2000 Ma, and a few ages are plotted in the ranges 2068–2394 Ma and 2526–2611 Ma. Four younger magmatic detrital zircon ages are obtained; the youngest is 1657 ± 17 Ma (JJZ12-08-2).
Lu-Hf isotopic analyses were performed on the 94 grains already used for zircon U-Pb age dating. εHf (t) values from these zircon grains cluster into two main populations of −1 to −8 and +1 to +8, corresponding to age ranges of 1.7–1.9 Ga and 2.3–2.6 Ga, respectively (Figure 8). The zircon population with an age of 1739–1799 Ma has one zircon grain with a positive εHf (t) value of 2.38, whereas the other grains have negative εHf (t) values from −0.08 to −9.20, 176Hf/177Hf values of 0.281420 to 0.281678, and two-stage Hf model ages (TDM2) of 2429–2993 Ma. The zircon population with age of 1839–1857 Ma has five zircon grains with positive εHf (t) values of 0.80 to 5.08, whereas the other grains have negative εHf (t) values from −1.20 to −8.07, 176Hf/177Hf values of 0.281409 to 0.281605, and TDM2 of 2579–2998 Ma. The zircon population with an age of 2436–2465 Ma has one zircon grain with a high positive εHf (t) value of 14.05, whereas the other grains have positive εHf (t) values from 1.11 to 5.13, 176Hf/177Hf values of 0.281288 to 0.281432, and TDM2 of 2657–2894 Ma.

4.2. Sample PJB12-11

The zircon grains collected from sample PJB12-11 were mostly well rounded to short columnar in shape, with grain sizes ranging from 100 μm to 500 μm (Figure 4). One hundred zircon grain U-Pb ages were obtained and eight more discordant zircon grains were ignored. Uranium concentrations range from 10 to 510 ppm, and thorium from 6 to 374 ppm. The Th/U values are mostly greater than 0.4 and are clustered at 0.6 to 1.5 (Figure 5), which, combined with the oscillatory growth zoning in the CL images, indicates their magmatic origin [62,63,64,65]. The 92 grains yield three age populations: 1743–1766 Ma, with a weighted average age of 1752 ± 9 Ma (n = 14, MSWD = 0.17); 1831–1863 Ma, with a weighted average age of 1844 ± 11 Ma (n = 13, MSWD=0.28); and 2435–2476 Ma with a weighted average age of 2449 ± 6 Ma (n = 15, MSWD = 0.70) (Figure 6 and Figure 7). In addition, there are two smaller population ages: 2381 ± 6 Ma (n = 11, MSWD = 1.8, ranging from 2347–2394 Ma) and 2551 ± 10 Ma (n = 10, MSWD = 0.50, ranging from 2528–2561 Ma). Furthermore, there are a few ages which are plotted between 1883–2315 Ma. There are also two older ages (3038 Ma and 3109 Ma), and one younger metamorphic age (1391 Ma with the Th/U value of 0.07).
Lu-Hf isotopic analyses were performed on the 92 samples already used for zircon U-Pb age dating. εHf (t) values from these zircon grains cluster into two main populations of −0.5 to −9 and 1 to 8, corresponding to age ranges of 1.7 Ga to 1.9 Ga and 2.3 Ga to 2.6 Ga, similar to sample JZZ12-08 (Figure 8). The zircon grain population with an age range of 1743–1766 Ma has zircon grains with negative εHf (t) values from −4.46 to −11.16, 176Hf/177Hf values of 0.281367 to 0.281566, and two-stage Hf model ages (TDM2) of 2694–3113 Ma. The zircon grain population with an age of 1831–1863 Ma has zircon grains with negative εHf (t) values from −0.52 to −9.37, 176Hf/177Hf values of 0.281364 to 0.281627, and two-stage Hf model ages (TDM2) of 2536–3072 Ma. The zircon population with an age of 2435–2476 Ma has two zircon grains with negative εHf (t) values of −8.92 and −4.28, whereas the other grains have εHf (t) values from 0.23 to 5.24, with 176Hf/177Hf values of 0.281247 to 0.281388 and TDM2 of 2638–2951 Ma.

5. Discussion

5.1. Geochronology of the Sedimentary Iron Deposit

During the Mesoproterozoic, the North China Craton underwent a long period of sedimentation. In the geological time scale of China (GTSC), the lower to upper Mesoproterozoic consists of the Changchengian and Jixianian systems. Within the older Changchengian System, the lowermost Changzhougou and Chuanlinggou Formations (Figure 2) unconformably overlie the Archean to Paleoproterozoic crystalline basement sequence. Gao et al. (2009) [66] obtained an emplacement age of 1638 ± 14 Ma by SHRIMP U-Pb dating method for a diabase dike crosscutting the Chuanlinggou Formation at Jixian. Zhang et al. (2013) [67] obtained an emplacement age of 1634 ± 9 Ma by LA-ICP-MS U-Pb dating method for a dioritic porphyrite dyke emplaced into the Chuanlinggou Formation at Jixian. Sun et al. (2013) [68] obtained an age for the tuff from the upper most part of the Chuanlinggou Formation of 1621 ± 12 Ma by SHRIMP U-Pb dating method, which is within the error range of the intrusion ages in this formation. These geochronological ages constrain the Chuanlinggou Formation deposition age to be not later than 1638 Ma. He et al. (2011) [69] obtained paleo-weathered mantle clastic rock detrital zircon U-Pb ages of 1682 ± 20 Ma and 1708 ± 6 Ma by SHRIMP and LA-ICP-MS dating methods. These rocks are covered directly by the sandstones of the Changzhougou Formation, suggesting that the age of the base of the Changzhougou Formation should be younger than 1682 Ma. Li et al. (2011, 2013) [70,71] obtained granite-porphyry dike ages of 1673 ± 10 Ma and 1669 ± 20 Ma by LA-MC-ICP-MS and SHRIMP U-Pb dating methods, and these dykes are unconformably overlain by the conglomerates and sandstones of the Changzhougou Formation, further suggesting that the base age of the Changchengian System in the NCC should be younger than 1670 Ma. This also implies that the Chuanlinggou Formation deposition age is not older than 1670 Ma.
In this study, a total of 186 U-Pb analyses of detrital zircon grains from two samples of the Chuanlinggou Formation in the Xuanhua area yield apparent 207Pb/206Pb ages (Th/U value > 0.4) ranging from 1657–3109 Ma. The two samples display similar age population ranges. The detrital zircon age spectra can be broadly subdivided into three major age populations: 1.74–1.8 Ga, with a peak age of 1765 Ma; 1.84–1.86 Ga, with a peak age of 1848 Ma; and 2.44–2.48 Ga, with a peak age of 2450 Ma (Figure 7). There is a distinctly young age in each of the two samples: 1565 Ma (JJZ12-08-14) and 1391 Ma (PJB12-11-95) with Th/U values of 0.24 and 0.07, respectively, and the reason for these clear outlier ages is uncertain. Minimum depositional ages are interpreted from populations of multiple grains. There are four zircon grain U-Pb ages in the youngest zircon age group (JJZ12-08-2, 1657 ± 17 Ma; JJZ12-08-1, 1661 ± 12 Ma; JJZ12-08-84, 1683 ± 20 Ma; and JJZ12-08-17, 1694 ± 30 Ma), with high Th/U values (0.75–1.49) and oscillatory zoning. Conventionally, the maximum depositional age of the sediments can be constrained by the age of the youngest zircon grains, which has not been altered since deposition. Therefore, the zircon U-Pb age constrains the depositional age of the Xuanlong type iron deposit to be not older than 1657 Ma. Combining this information with previous studies, and considering the considerable thickness of this formation, this type of iron deposit was deposited at 1634–1657 Ma, close to 1650 Ma.

5.2. Crustal Growth and Evolution of the Trans-North China Orogen

5.2.1. Evolution of the Trans-North China Orogen

The North China Craton has experienced a long geological evolutionary history (ca. 3.8 Ga) [1,2,3,72,73,74,75,76]. Its central segment, the TNCO, is most significant, as it is a result of the collision between the Eastern and Western blocks, and preserves important clues for revealing the tectonic evolution history of the NCC. Zhao et al. (2005, 2012) [2,7] and Lu et al. (2008) [9] reviewed the geochronological data of nearly all metamorphic complexes (Chengde, Xuanhua, Huai’an, Hengshan, Wutai, Fuping, Zanhuang, Lvliang, and Taihua) in this area, and discovered that the age of the final amalgamation of the NCC was ~1.85 Ga. Recently, Tang and Santosh (2018) [77] summarized the geology, geochemical, and geochronology data of the Neoarchean to Paleoproterozoic rocks from the TNCO. They attempted to reconstruct the major Precambrian events of the NCC, which experienced amalgamation (Ordos, Qianhuai and Xuchang microblocks; 2.58–2.48 Ga, leading to the initial cratonisation of the NCC), post-collisional extension (2.50–2.45 Ga), subduction (which occurred in the Hengshan, Huai’an-Xuanhua and Lvliang Complexes), rifting (which occurred in the Fuping, Wutai and Zanhuang Complexes, and slightly later in the Hengshan, Huai’an-Xuanhua, and Zanhuang Complexes; 2.45–1.98 Ga), the assembly of the separated terranes (or complexes) driven by the amalgamation of the Western and Eastern blocks (1.96–1.80 Ga), and finally, the termination of the collisional event (1.80–1.74 Ga). It is recognized that the NCC is one part of the Columbia Supercontinent [7,18,78,79,80,81,82]. During the period of 1.85–1.7 Ga, the NCC was evolved in an extensional tectonic regime [16,44], with extension and uplift in the interior and at the edge of the craton. This led to the intrusion of Mg-rich mafic dykes, plagioclasites, gabbros, mangerites, rapakivi granites, A-type granite, and potassium-rich volcanic rocks, corresponding to late Paleoproterozoic to early Mesoproterozoic global non-orogenic magmatic activity during the breakup of the Columbia supercontinent [4,6,22,45,78,83,84,85,86,87,88,89,90,91,92,93,94]. The dyke swarms represent the initial breakup of the supercontinent [81]. Lu et al. (2008) [9] reviewed the geochronology data of the intrusive and volcanic rocks and suggested that during the period 1.8–1.6 Ga, the extensional tectonic events of the NCC could be divided into three peak stages (at 1.78 Ga, 1.70 Ga, and 1.62 Ga).
Detrital zircon ages from the Chuanlinggou Formation contain zircon populations defining peaks similar to the two major events at 1848 Ma and 2450 Ma, which align with the ages mentioned above. These two major tectonic-thermal event ages (ca. 1.85 Ga and ca. 2.5 Ga) have been widely recognized [7,16,19,20,21,24,93,95,96,97,98,99]. However, there is still debate surrounding the processes of the crustal amalgamation and cratonisation. In this work, another age population of 1.74–1.80 Ga from the Chuanlinggou Formation has been discovered. This is consistent with the age of the mafic dyke swarms which must have caused crustal melting, which recorded the extension, uplift, crust–mantle interaction and mantle upwelling events after 1.8 Ga in the central part of the NCC.

5.2.2. Crustal Growth

Detrital zircon U-Pb age spectra coupled with Hf isotope data can be used to provide insight into crustal growth and recycling, as well as provenance [100,101,102,103]. Hf isotope data from the Chuanlinggou Formation show two obvious groups, with different εHf (t) values. Most of the detrital zircon grains with U-Pb age ranges of 1.7–1.9 Ga have modest negative εHf (t) values, clustering at −1 to −8, suggesting that the source rocks of these zircon grains were derived from the recycling of somewhat more ancient crust. Most of the detrital zircons with age ranges of 2.3–2.6 Ga have εHf (t) values, clustering at +1 to +8. However, these older zircon grains’ Hf two-stage model ages do not show the expected ca. 2.5 Ga peak, but instead indicate a peak at 2.6–2.9 Ga, which is slightly older than the apparent age and single stage Hf model peak age (Figure 9), suggesting that the rocks were not directly derived from the differentiation of the depleted mantle; i.e., from basalt. The source rocks of these zircon grains might be derived from juvenile crust with a short period of reworking while residing in the crust [104]. It is obvious that there is a trend of decreasing εHf (t) values with ages (Figure 8), which also suggests that, within this period, the younger zircon grains are being derived from greater amounts of reworking of an older crust, or the reworking of recently formed crust; i.e., 2.6 Ga crust has been reworked to form 2.3 Ga crust. In addition, the two ancient grains found hint at the presence of truly ancient crust in this reworking period. These features are earmarks of the crustal evolution of the North China Craton and are consistent with previous studies in the TNCO (Zhang et al., 2013 [105] and references therein) and similar to those in the East Block and West Block [104,106,107,108,109,110,111,112]. Furthermore, detrital zircon grains from all of these studies have a similar two-stage Hf model age (TDM2) ranges of 2.4–3.0 Ga, with a peak age of 2.65–2.85 Ga, implying the possibility of crust–mantle differentiation during this period, marking the most significant stage of crustal growth of the NCC. This is similar to the Nd model age peak at 2.8–2.4 Ga obtained by Wu et al. (2005) [113].

6. Conclusions

The following are the conclusions of this study.
(1)
Three zircon grain population age ranges within the Chuanlinggou Formation have been observed, with peak ages of 2450 Ma, 1848 Ma, and 1765 Ma, representing periods of magmatism associated with the amalgamation and breaking up events of the NCC;
(2)
Combined with previous studies, the sedimentary type of iron deposit hosted by the Chuanlinggou Formation was formed at 1634–1657 Ma, close to 1650 Ma;
(3)
Detrital zircon grains from the Chuanlinggou Formation form two obvious groups, with different εHf (t) values ranging from −1 to −8 and from 1 to 8, which correspond to the age ranges of 1.7–1.9 Ga and 2.3–2.6 Ga, respectively. They have a similar two-stage Hf model age peak at 2.65–2.85 Ga, suggesting that the source rocks were derived from the recycling of ancient crusts. It also implies the possibility of crust–mantle differentiation during this period, marking the most significant stage of crustal growth of the NCC.

Author Contributions

Y.L. (Yanhe Li) and C.D. conceived this contribution. C.D., Y.L. (Yanhe Li), Y.Y., Y.L. (Yongsheng Liang) and M.W. made field investigation. C.D. performed the zircon U-Pb dating and Lu-Hf isotope analysis. C.D., Y.L. (Yanhe Li) and K.H. interpreted all the data. C.D. wrote the original draft of the paper. Y.L. (Yanhe Li) reviewed the original draft of paper.

Funding

This work was jointly funded by the National Natural Science Foundation of China (No. 41402078 and 41473014), National Basic Research Program of China (973 Program) (2012CB416801), and a Grant of the Chinese Ministry of Land and Resources Public Benefit Research Foundation of China (No. 201211074).

Acknowledgments

We gratefully thank Chunli Guo and Qian Wang from the Institute of Mineral Resources, Chinese Academy of Geological Sciences for their important guidance and assistance in zircon age testing, Hf isotope testing, and data analysis. We would like thank two anonymous reviewers for their helpful comments and insightful reviews, which have greatly improved the manuscript.

Conflicts of Interest

The authors declare no conflict of interest.

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Minerals 08 00547 g001 550
Figure 1. Tectonic subdivision of the North China Craton (modified after Zhao et al., 2012 [7]). Pangjiabu and Jiangjiazhai are the sampling locations.
Figure 1. Tectonic subdivision of the North China Craton (modified after Zhao et al., 2012 [7]). Pangjiabu and Jiangjiazhai are the sampling locations.
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Minerals 08 00547 g002 550
Figure 2. (a) Ironstone and related sedimentary successions in the Chuanlinggou Formation at the Xuanhua area (modified after Tang et al., 2015 [47]); (b) A representative iron ore-bearing sequence of the Chuanlinggou Formation (modified after Zhao, 1994 [48]).
Figure 2. (a) Ironstone and related sedimentary successions in the Chuanlinggou Formation at the Xuanhua area (modified after Tang et al., 2015 [47]); (b) A representative iron ore-bearing sequence of the Chuanlinggou Formation (modified after Zhao, 1994 [48]).
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Minerals 08 00547 g003 550
Figure 3. (a) Outcrop photo of the sandy shale; (b) photo of the stromatolith hematite ore with oolitic hematite appearing at the top; (c) photo of the oolitic hematite ore; (d) micrograph of the sandy shale.
Figure 3. (a) Outcrop photo of the sandy shale; (b) photo of the stromatolith hematite ore with oolitic hematite appearing at the top; (c) photo of the oolitic hematite ore; (d) micrograph of the sandy shale.
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Minerals 08 00547 g004 550
Figure 4. Representative zircon grain cathodoluminescence (CL) images with 207Pb/206Pb ages, and εHf (t) values (within parentheses). The analysis positions are shown, with solid lines for 207Pb/206Pb ages and dashed lines for Hf isotope values.
Figure 4. Representative zircon grain cathodoluminescence (CL) images with 207Pb/206Pb ages, and εHf (t) values (within parentheses). The analysis positions are shown, with solid lines for 207Pb/206Pb ages and dashed lines for Hf isotope values.
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Figure 5. Th/U values of zircon grains with 207Pb/206Pb ages.
Figure 5. Th/U values of zircon grains with 207Pb/206Pb ages.
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Figure 6. U-Pb concordia and peak age distribution diagrams of zircon grains from samples JJZ12-08 (a–d) and PJB12-11 (e–h) collected from the Chuanlinggou Formation.
Figure 6. U-Pb concordia and peak age distribution diagrams of zircon grains from samples JJZ12-08 (a–d) and PJB12-11 (e–h) collected from the Chuanlinggou Formation.
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Figure 7. Relative probability of the detrital zircon grains’ U-Pb ages.
Figure 7. Relative probability of the detrital zircon grains’ U-Pb ages.
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Figure 8. εHf (t) values versus U-Pb ages of detrital zircon grains from JJZ12-08 and PJB12-11. The dashed lines indicate the evolution trends of average continental crust (176Lu/177Hf = 0.015).
Figure 8. εHf (t) values versus U-Pb ages of detrital zircon grains from JJZ12-08 and PJB12-11. The dashed lines indicate the evolution trends of average continental crust (176Lu/177Hf = 0.015).
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Figure 9. (a) Histogram of the one-stage Hf model ages of detrital zircon grains from JJZ12-08 and PJB12-11; (b) Histogram of the two-stage Hf model ages of detrital zircon grains from JJZ12-08 and PJB12-11.
Figure 9. (a) Histogram of the one-stage Hf model ages of detrital zircon grains from JJZ12-08 and PJB12-11; (b) Histogram of the two-stage Hf model ages of detrital zircon grains from JJZ12-08 and PJB12-11.
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Table
Table 1. LA-MC-ICP-MS U-Pb dating data for detrital zircons from the Chuanlinggou Formation.
Table 1. LA-MC-ICP-MS U-Pb dating data for detrital zircons from the Chuanlinggou Formation.
No.Conent (ppm)Th/UIsotopic RatiosAge (Ma)
ThU207Pb/206Pb1 Sigma207Pb/235U1 Sigma206Pb/238U1 Sigma207Pb/206Pb1 Sigma207Pb/235U1 Sigma206Pb/238U1 Sigma
JJZ12-08
127360.750.10200.00074.07390.04450.28930.002416611216499163812
218220.840.10170.00073.93920.05340.28090.0035165717162211159618
329550.530.10870.00064.59190.03990.30650.00221777917487172411
4771100.700.11270.00064.96300.04540.31970.00271844918138178813
522300.720.11360.00105.20770.08180.33300.0049185715185413185324
7791300.610.11270.00094.90490.05450.31620.002818431418039177114
8731190.620.16760.001110.65380.12630.46120.0044260011249311244519
9541100.490.14710.00138.43170.21110.41590.0096231315227923224244
1059830.700.15950.00149.71770.12700.44260.0045245015240812236220
11871590.550.11330.00145.19590.09840.33280.0040185422185216185219
1248580.830.16030.001710.17900.13780.46160.0036245919245113244616
14291190.240.09690.00103.47600.08840.26080.0063156519152220149432
151852060.890.10950.00104.80030.08750.31840.0051179217178515178225
161181860.630.14770.00159.20730.12830.45310.0042232018235913240919
1732390.810.10380.00174.29540.09170.30020.0037169430169318169319
1872750.970.10780.00274.62150.16660.30740.0040176546175330172820
1991741.230.10700.00244.61410.13940.31310.0051175042175225175625
20291220.240.10690.00164.42030.11120.30070.0069174727171621169534
2184721.170.10720.00224.48180.13230.30260.0042175239172825170421
22100771.290.10740.00214.48940.12570.30320.0055176735172923170727
23601260.480.11340.00245.16770.13700.33090.0051185438184723184325
241231900.650.11280.00344.81050.26750.30890.0079185654178747173539
25136991.380.10680.00184.41780.10830.29990.0049174631171620169124
2647341.370.10760.00144.46870.08980.30030.0038176123172517169319
271841531.210.11300.00175.13140.13840.32840.0061185028184123183130
28130821.590.17060.002911.47500.41840.48300.0104256528256334254045
292021911.060.11550.00115.41940.09230.33960.0047188817188815188523
3094671.400.11310.00135.01310.06010.32100.0022185020182210179511
3165401.620.10680.00244.25640.10650.28930.0097174641168521163848
3266631.060.16080.001310.32290.08710.46470.002224651324648246010
332201461.510.15850.001010.38770.18680.47430.0077244011247017250234
3446361.260.10710.00084.55520.05450.30830.0033175014174110173216
3685761.130.11250.00165.04860.11210.32350.0036184359182819180718
37161971.670.11280.00155.07520.37720.32520.0204185624183263181599
3852530.980.11230.00194.86430.11060.31270.0039183963179619175419
3969720.950.13870.00197.82120.15020.40850.0058221124221117220827
401341690.790.13590.00107.52260.10140.40070.0045217612217612217221
41123612.010.12300.00166.08610.16060.36010.0097200023198823198246
422312181.060.11850.00255.73480.17580.34880.0057194537193727192927
4335460.770.10980.00144.70070.08330.31060.0051179823176715174425
4548401.190.10860.00084.74880.04590.31700.002117761517768177511
461041090.950.12050.00155.79630.12100.34570.0027196522194618191413
4735380.940.14610.00138.24820.12070.40900.0049230215225913221023
481681181.420.17440.000911.50790.07890.47780.0021261192565625189
491201260.950.11930.00095.68540.05360.34530.002419461319298191211
5096721.330.16680.000811.00260.08760.47840.003625264225237252016
5160770.770.14410.00077.88260.14050.39640.006922778221816215332
5228201.450.11340.00105.13750.12530.32790.0073185516184221182836
5334810.420.11610.00165.47460.09530.34110.0029189825189715189214
542211981.110.11530.00115.41130.09040.33980.00441887−16188714188621
55781030.760.11670.00215.52300.13330.33990.0026190733190421188613
5664870.730.12280.00136.15490.08530.36250.0033199819199812199416
5726410.630.11560.00155.35380.08090.33540.0032190024187813186515
5828281.000.17240.001411.33570.16000.47540.0053258113255113250723
5932460.680.11360.00125.12780.08400.32680.0042185719184114182320
6029261.140.16040.00149.83910.13450.44390.0050246110242013236823
611551690.920.11310.00084.91370.06420.31430.0035185012180511176217
6229350.840.16750.001311.05090.15920.47760.0063253313252713251728
63580.690.15420.00309.13260.38020.43400.0184239433235138232483
641471101.340.16060.001010.25820.14700.46300.0066246210245813245329
6524360.660.10820.00104.58300.06590.30690.0037176916174612172618
6629700.420.14870.00118.56530.24700.41790.0126233212229326225157
672261561.450.10750.00164.60640.27180.31010.0169176726175049174183
6817151.110.10920.00114.80710.14370.31840.0085178719178625178242
692882201.310.11290.00115.07660.20140.32540.0104184718183234181651
7043440.970.10840.00104.69070.07190.31340.0040177412176613175820
715611244.520.11320.00105.05630.11240.32380.0068185115182919180833
7253730.730.13370.00137.24090.08820.39230.0027214717214211213312
732151541.390.12070.00155.89220.08200.35360.001919692319601219529
7452341.500.12290.00096.06970.07820.35790.0038199913198611197218
75110492.260.15810.002110.36580.27540.47510.0110243623246825250648
761911461.310.15120.00128.94030.24310.42900.0117235913233225230153
7744411.070.12780.00386.43750.30470.36340.0092206853203742199844
78124811.540.10870.00154.76700.10730.31590.0034178926177919177016
7977980.780.11260.00135.08500.07460.32770.0036184321183413182717
80921940.480.11450.00145.31130.07510.33670.0032187222187112187116
812711132.390.12140.00135.88600.07550.35150.0031197819195911194215
8280621.290.10890.00104.76710.05140.31740.002317831617799177711
832151601.340.11270.00124.99410.05690.32140.0024184319181810179712
8437251.490.10320.00114.22730.08760.29670.0051168320167917167525
8653590.900.11000.00094.86500.04520.32060.00191799151796817939
8736321.110.11310.00125.10920.07540.32720.0033185019183813182516
881781121.580.16080.001410.18900.13900.45860.0037246515245213243417
8978850.920.11640.00135.43590.06390.33890.0024190222189110188112
9082771.060.11660.00125.44770.07260.33780.0022190620189211187610
91951170.810.15890.00119.93870.08360.45290.002524441324298240811
92841010.830.11340.00184.96490.07180.31790.001818552818131217799
9355870.630.17210.002011.48090.19340.48230.0059258920256316253726
9461880.700.15880.001010.01740.07990.45710.003224431124367242714
95169682.480.12250.00126.03970.06600.35720.0023199419198210196911
9625360.690.10640.00114.49910.06610.30620.0034173923173112172217
97541080.500.11300.00134.97410.09090.31840.0038185021181515178219
98741080.680.11340.00304.98930.15810.31840.0021185448181827178210
100981490.660.10750.00124.60690.06250.30990.0022175826175111174011
PJB12-11
1100881.140.16590.002410.82500.38940.47330.0167251725250833249873
21611401.160.15210.00119.21080.24690.43910.0122236913235925234755
374661.120.15230.00179.07680.27980.43180.0125237319234628231456
460441.350.10720.00104.43070.07850.29980.0047175417171815169123
514480.290.16930.003010.82390.39760.46350.0154255030250834245568
695761.250.15390.00129.38890.43500.44210.0202239114237743236091
71241990.620.15330.00089.11270.09180.43090.00362383923499231016
821151.400.10770.00164.64310.17480.31320.0110176127175732175754
941301.390.11570.00165.36710.10160.33640.0044189026188016187021
101581061.490.16030.001210.22620.16380.46290.006524588245615245229
11109791.370.12320.00096.09700.07560.35900.0037200313199011197818
12931270.730.16810.001510.96480.28700.47320.0122253915252024249854
1322211.080.11350.00165.13240.15340.32810.0084185526184225182941
14641080.590.15910.00089.98900.11730.45540.004924468243411241922
1533760.430.12360.00095.99710.08660.35120.0041201018197513194020
17631000.630.14510.00078.41930.12990.42110.006622899227714226630
183192681.190.15890.00099.94610.28810.45350.012124449243027241154
192803490.800.15890.00099.87810.45720.45070.02282444102424432398101
201992060.970.11200.00214.77830.16380.31080.0151183134178129174574
211641770.930.12090.00165.93090.16710.35510.0085196923196625195940
221321001.310.11390.00105.26000.07330.33450.0037186315186212186018
23192962.000.11640.00085.49660.09370.34200.005319028190015189626
2432400.800.10700.00084.46590.06030.30240.0035175013172511170317
25125921.350.13550.00067.47120.07220.39940.00362172821709216617
26104691.500.15860.00129.99100.12840.45600.0047244312243412242221
2770780.890.12970.00086.67490.06230.37300.003020941120698204314
2898951.030.15940.001110.04820.19350.45630.0082245011243918242336
3045460.980.10660.00114.51360.05890.30610.0023174319173411172212
3144361.220.10720.00114.40990.05310.29810.0025175218171410168212
32175652.700.11240.00135.07220.06680.32640.001818392118321118219
331981521.300.23820.001320.23040.16940.61480.00413109931028308916
341061190.890.14670.00088.70700.05580.42990.002123091023086230510
352231601.400.11210.00095.05220.03990.32680.00161833131828718238
3633231.410.10720.00104.43620.07340.29990.0045175417171914169122
37941090.860.12390.00116.13530.06300.35870.002220131519959197610
3891671.350.11640.00105.47880.05690.34080.002019021518979189110
4034410.830.14500.00138.10090.17940.40410.0074228715224220218834
411061770.600.15110.00089.16030.08450.43870.00282358923548234513
421481351.090.16070.001110.30590.09530.46450.002524631324639245911
43691050.660.15970.001310.14500.10430.45980.0027245413244810243912
44931080.860.15910.00129.88190.08830.45000.003024471224248239514
4635390.900.16680.001510.63310.11570.46190.0033252816249210244815
4744261.710.15430.00169.44270.13040.44370.0045239418238213236720
48101991.020.16180.001910.45110.28710.46670.0085247620247626246937
4998951.030.12260.00186.10280.10830.36070.0033199426199116198516
5174910.810.10750.00194.57970.13430.30750.0059175833174624172929
53128871.470.17010.005411.36901.04570.47470.03082558522554862504135
541531501.020.16900.002411.21080.40010.48110.0170254824254133253274
5599901.100.11790.00195.54640.11440.34070.0040192430190818189019
5699721.370.11260.00214.89000.11920.31470.0047184333180121176423
5778741.040.11330.00195.20160.11430.33200.0043185425185319184821
581751281.370.15380.00079.24580.15100.43580.007023888236315233231
5983631.310.15300.00149.24030.14020.43790.0057238015236214234126
6050520.960.10670.00124.52070.09540.30660.0053174322173518172426
61771260.610.15240.00269.36630.65600.44400.02702373292375642369121
63911030.880.15010.00118.85020.25740.42710.0117234713232327229353
6424102.410.12180.00625.47720.16470.33800.0098198486189726187747
652081161.790.15600.00099.68190.46410.44990.0223241316240544239599
66971380.710.15860.00109.86060.15830.45050.0068244310242215239830
67381350.280.11350.00165.18900.13570.33100.0072185726185122184335
6833380.870.10710.00124.55420.05810.30840.0022175022174111173311
69871320.650.11290.00134.94280.06220.31710.001818565518101117769
70161930.090.14380.00137.91420.08310.39820.0021227322222110216110
7132370.880.17280.003111.55990.51710.48320.0173258731256942254175
72145642.250.15950.002210.12400.25460.46070.0141245023244623244262
732261211.870.15820.001710.01080.16740.45800.0057243718243615243125
74112881.280.11510.00115.32230.07430.33450.0033188317187312186016
7595851.120.22800.001518.76530.23710.59620.0068303811303012301528
7694472.020.15790.00129.79230.14220.44880.0054243513241513239024
771692410.700.15380.00099.45540.15020.44520.006623895238315237429
7826181.440.10800.00114.36050.08990.29290.0057176619170517165629
791521391.100.11230.00115.03010.06560.32520.0038183617182411181518
8033390.850.10680.00084.54070.05400.30850.0034174614173910173317
8127221.240.10780.00084.61870.08970.31040.0057176313175316174328
8249570.870.11240.00114.77730.07100.30760.0030183919178113172915
8398611.610.10680.00084.55270.04260.30930.002417461417418173812
841151650.700.16070.001010.29600.10030.46400.003324651024629245715
8556580.970.11310.00145.05170.07490.32310.001818502218281318059
8687531.640.12600.00106.37530.06210.36680.002420431420299201411
87902240.400.11260.00115.13360.05860.33050.0021184313184210184110
881281171.090.16860.002011.14880.19210.47790.0039254420253616251817
891081081.000.16290.001910.57460.18160.46940.0040248720248716248118
9041570.710.11420.00125.23940.06140.33280.0021193317185910185210
9273850.860.17000.001011.40920.08550.48670.002725581025577255712
9357790.730.17040.001011.33590.09650.48210.003125611025518253714
9479631.250.16980.002711.32230.22970.48330.0067255527255019254229
956820.070.08840.00122.87450.08780.23380.0057139126137523135530
9629281.070.10730.00114.57920.06030.30930.0028175418174611173714
971101110.990.14730.00097.28720.08120.35850.0038231510214710197518
9848421.160.13590.00137.32010.07760.39030.0024217617215110212411
9943391.110.17770.001512.23450.12850.49840.0033263119262310260714
10088481.810.16880.002310.75110.28610.46080.0078254524250225244335
Table
Table 2. In situ Lu-Hf isotopes analytical data for detrital zircons from the Chuanlinggou Formation.
Table 2. In situ Lu-Hf isotopes analytical data for detrital zircons from the Chuanlinggou Formation.
No.Conent (ppm)Th/UIsotopic RatiosAge (Ma)
ThU207Pb/206Pb1 Sigma207Pb/235U1 Sigma206Pb/238U1 Sigma207Pb/206Pb1 Sigma207Pb/235U1 Sigma206Pb/238U1 Sigma
JJZ12-08
127360.750.10200.00074.07390.04450.28930.002416611216499163812
218220.840.10170.00073.93920.05340.28090.0035165717162211159618
329550.530.10870.00064.59190.03990.30650.00221777917487172411
4771100.700.11270.00064.96300.04540.31970.00271844918138178813
522300.720.11360.00105.20770.08180.33300.0049185715185413185324
7791300.610.11270.00094.90490.05450.31620.002818431418039177114
8731190.620.16760.001110.65380.12630.46120.0044260011249311244519
9541100.490.14710.00138.43170.21110.41590.0096231315227923224244
1059830.700.15950.00149.71770.12700.44260.0045245015240812236220
11871590.550.11330.00145.19590.09840.33280.0040185422185216185219
1248580.830.16030.001710.17900.13780.46160.0036245919245113244616
14291190.240.09690.00103.47600.08840.26080.0063156519152220149432
151852060.890.10950.00104.80030.08750.31840.0051179217178515178225
161181860.630.14770.00159.20730.12830.45310.0042232018235913240919
1732390.810.10380.00174.29540.09170.30020.0037169430169318169319
1872750.970.10780.00274.62150.16660.30740.0040176546175330172820
1991741.230.10700.00244.61410.13940.31310.0051175042175225175625
20291220.240.10690.00164.42030.11120.30070.0069174727171621169534
2184721.170.10720.00224.48180.13230.30260.0042175239172825170421
22100771.290.10740.00214.48940.12570.30320.0055176735172923170727
23601260.480.11340.00245.16770.13700.33090.0051185438184723184325
241231900.650.11280.00344.81050.26750.30890.0079185654178747173539
25136991.380.10680.00184.41780.10830.29990.0049174631171620169124
2647341.370.10760.00144.46870.08980.30030.0038176123172517169319
271841531.210.11300.00175.13140.13840.32840.0061185028184123183130
28130821.590.17060.002911.47500.41840.48300.0104256528256334254045
292021911.060.11550.00115.41940.09230.33960.0047188817188815188523
3094671.400.11310.00135.01310.06010.32100.0022185020182210179511
3165401.620.10680.00244.25640.10650.28930.0097174641168521163848
3266631.060.16080.001310.32290.08710.46470.002224651324648246010
332201461.510.15850.001010.38770.18680.47430.0077244011247017250234
3446361.260.10710.00084.55520.05450.30830.0033175014174110173216
3685761.130.11250.00165.04860.11210.32350.0036184359182819180718
37161971.670.11280.00155.07520.37720.32520.0204185624183263181599
3852530.980.11230.00194.86430.11060.31270.0039183963179619175419
3969720.950.13870.00197.82120.15020.40850.0058221124221117220827
401341690.790.13590.00107.52260.10140.40070.0045217612217612217221
41123612.010.12300.00166.08610.16060.36010.0097200023198823198246
422312181.060.11850.00255.73480.17580.34880.0057194537193727192927
4335460.770.10980.00144.70070.08330.31060.0051179823176715174425
4548401.190.10860.00084.74880.04590.31700.002117761517768177511
461041090.950.12050.00155.79630.12100.34570.0027196522194618191413
4735380.940.14610.00138.24820.12070.40900.0049230215225913221023
481681181.420.17440.000911.50790.07890.47780.0021261192565625189
491201260.950.11930.00095.68540.05360.34530.002419461319298191211
5096721.330.16680.000811.00260.08760.47840.003625264225237252016
5160770.770.14410.00077.88260.14050.39640.006922778221816215332
5228201.450.11340.00105.13750.12530.32790.0073185516184221182836
5334810.420.11610.00165.47460.09530.34110.0029189825189715189214
542211981.110.11530.00115.41130.09040.33980.00441887−16188714188621
55781030.760.11670.00215.52300.13330.33990.0026190733190421188613
5664870.730.12280.00136.15490.08530.36250.0033199819199812199416
5726410.630.11560.00155.35380.08090.33540.0032190024187813186515
5828281.000.17240.001411.33570.16000.47540.0053258113255113250723
5932460.680.11360.00125.12780.08400.32680.0042185719184114182320
6029261.140.16040.00149.83910.13450.44390.0050246110242013236823
611551690.920.11310.00084.91370.06420.31430.0035185012180511176217
6229350.840.16750.001311.05090.15920.47760.0063253313252713251728
63580.690.15420.00309.13260.38020.43400.0184239433235138232483
641471101.340.16060.001010.25820.14700.46300.0066246210245813245329
6524360.660.10820.00104.58300.06590.30690.0037176916174612172618
6629700.420.14870.00118.56530.24700.41790.0126233212229326225157
672261561.450.10750.00164.60640.27180.31010.0169176726175049174183
6817151.110.10920.00114.80710.14370.31840.0085178719178625178242
692882201.310.11290.00115.07660.20140.32540.0104184718183234181651
7043440.970.10840.00104.69070.07190.31340.0040177412176613175820
715611244.520.11320.00105.05630.11240.32380.0068185115182919180833
7253730.730.13370.00137.24090.08820.39230.0027214717214211213312
732151541.390.12070.00155.89220.08200.35360.001919692319601219529
7452341.500.12290.00096.06970.07820.35790.0038199913198611197218
75110492.260.15810.002110.36580.27540.47510.0110243623246825250648
761911461.310.15120.00128.94030.24310.42900.0117235913233225230153
7744411.070.12780.00386.43750.30470.36340.0092206853203742199844
78124811.540.10870.00154.76700.10730.31590.0034178926177919177016
7977980.780.11260.00135.08500.07460.32770.0036184321183413182717
80921940.480.11450.00145.31130.07510.33670.0032187222187112187116
812711132.390.12140.00135.88600.07550.35150.0031197819195911194215
8280621.290.10890.00104.76710.05140.31740.002317831617799177711
832151601.340.11270.00124.99410.05690.32140.0024184319181810179712
8437251.490.10320.00114.22730.08760.29670.0051168320167917167525
8653590.900.11000.00094.86500.04520.32060.00191799151796817939
8736321.110.11310.00125.10920.07540.32720.0033185019183813182516
881781121.580.16080.001410.18900.13900.45860.0037246515245213243417
8978850.920.11640.00135.43590.06390.33890.0024190222189110188112
9082771.060.11660.00125.44770.07260.33780.0022190620189211187610
91951170.810.15890.00119.93870.08360.45290.002524441324298240811
92841010.830.11340.00184.96490.07180.31790.001818552818131217799
9355870.630.17210.002011.48090.19340.48230.0059258920256316253726
9461880.700.15880.001010.01740.07990.45710.003224431124367242714
95169682.480.12250.00126.03970.06600.35720.0023199419198210196911
9625360.690.10640.00114.49910.06610.30620.0034173923173112172217
97541080.500.11300.00134.97410.09090.31840.0038185021181515178219
98741080.680.11340.00304.98930.15810.31840.0021185448181827178210
100981490.660.10750.00124.60690.06250.30990.0022175826175111174011
PJB12-11
1100881.140.16590.002410.82500.38940.47330.0167251725250833249873
21611401.160.15210.00119.21080.24690.43910.0122236913235925234755
374661.120.15230.00179.07680.27980.43180.0125237319234628231456
460441.350.10720.00104.43070.07850.29980.0047175417171815169123
514480.290.16930.003010.82390.39760.46350.0154255030250834245568
695761.250.15390.00129.38890.43500.44210.0202239114237743236091
71241990.620.15330.00089.11270.09180.43090.00362383923499231016
821151.400.10770.00164.64310.17480.31320.0110176127175732175754
941301.390.11570.00165.36710.10160.33640.0044189026188016187021
101581061.490.16030.001210.22620.16380.46290.006524588245615245229
11109791.370.12320.00096.09700.07560.35900.0037200313199011197818
12931270.730.16810.001510.96480.28700.47320.0122253915252024249854
1322211.080.11350.00165.13240.15340.32810.0084185526184225182941
14641080.590.15910.00089.98900.11730.45540.004924468243411241922
1533760.430.12360.00095.99710.08660.35120.0041201018197513194020
17631000.630.14510.00078.41930.12990.42110.006622899227714226630
183192681.190.15890.00099.94610.28810.45350.012124449243027241154
192803490.800.15890.00099.87810.45720.45070.02282444102424432398101
201992060.970.11200.00214.77830.16380.31080.0151183134178129174574
211641770.930.12090.00165.93090.16710.35510.0085196923196625195940
221321001.310.11390.00105.26000.07330.33450.0037186315186212186018
23192962.000.11640.00085.49660.09370.34200.005319028190015189626
2432400.800.10700.00084.46590.06030.30240.0035175013172511170317
25125921.350.13550.00067.47120.07220.39940.00362172821709216617
26104691.500.15860.00129.99100.12840.45600.0047244312243412242221
2770780.890.12970.00086.67490.06230.37300.003020941120698204314
2898951.030.15940.001110.04820.19350.45630.0082245011243918242336
3045460.980.10660.00114.51360.05890.30610.0023174319173411172212
3144361.220.10720.00114.40990.05310.29810.0025175218171410168212
32175652.700.11240.00135.07220.06680.32640.001818392118321118219
331981521.300.23820.001320.23040.16940.61480.00413109931028308916
341061190.890.14670.00088.70700.05580.42990.002123091023086230510
352231601.400.11210.00095.05220.03990.32680.00161833131828718238
3633231.410.10720.00104.43620.07340.29990.0045175417171914169122
37941090.860.12390.00116.13530.06300.35870.002220131519959197610
3891671.350.11640.00105.47880.05690.34080.002019021518979189110
4034410.830.14500.00138.10090.17940.40410.0074228715224220218834
411061770.600.15110.00089.16030.08450.43870.00282358923548234513
421481351.090.16070.001110.30590.09530.46450.002524631324639245911
43691050.660.15970.001310.14500.10430.45980.0027245413244810243912
44931080.860.15910.00129.88190.08830.45000.003024471224248239514
4635390.900.16680.001510.63310.11570.46190.0033252816249210244815
4744261.710.15430.00169.44270.13040.44370.0045239418238213236720
48101991.020.16180.001910.45110.28710.46670.0085247620247626246937
4998951.030.12260.00186.10280.10830.36070.0033199426199116198516
5174910.810.10750.00194.57970.13430.30750.0059175833174624172929
53128871.470.17010.005411.36901.04570.47470.03082558522554862504135
541531501.020.16900.002411.21080.40010.48110.0170254824254133253274
5599901.100.11790.00195.54640.11440.34070.0040192430190818189019
5699721.370.11260.00214.89000.11920.31470.0047184333180121176423
5778741.040.11330.00195.20160.11430.33200.0043185425185319184821
581751281.370.15380.00079.24580.15100.43580.007023888236315233231
5983631.310.15300.00149.24030.14020.43790.0057238015236214234126
6050520.960.10670.00124.52070.09540.30660.0053174322173518172426
61771260.610.15240.00269.36630.65600.44400.02702373292375642369121
63911030.880.15010.00118.85020.25740.42710.0117234713232327229353
6424102.410.12180.00625.47720.16470.33800.0098198486189726187747
652081161.790.15600.00099.68190.46410.44990.0223241316240544239599
66971380.710.15860.00109.86060.15830.45050.0068244310242215239830
67381350.280.11350.00165.18900.13570.33100.0072185726185122184335
6833380.870.10710.00124.55420.05810.30840.0022175022174111173311
69871320.650.11290.00134.94280.06220.31710.001818565518101117769
70161930.090.14380.00137.91420.08310.39820.0021227322222110216110
7132370.880.17280.003111.55990.51710.48320.0173258731256942254175
72145642.250.15950.002210.12400.25460.46070.0141245023244623244262
732261211.870.15820.001710.01080.16740.45800.0057243718243615243125
74112881.280.11510.00115.32230.07430.33450.0033188317187312186016
7595851.120.22800.001518.76530.23710.59620.0068303811303012301528
7694472.020.15790.00129.79230.14220.44880.0054243513241513239024
771692410.700.15380.00099.45540.15020.44520.006623895238315237429
7826181.440.10800.00114.36050.08990.29290.0057176619170517165629
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8249570.870.11240.00114.77730.07100.30760.0030183919178113172915
8398611.610.10680.00084.55270.04260.30930.002417461417418173812
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8556580.970.11310.00145.05170.07490.32310.001818502218281318059
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881281171.090.16860.002011.14880.19210.47790.0039254420253616251817
891081081.000.16290.001910.57460.18160.46940.0040248720248716248118
9041570.710.11420.00125.23940.06140.33280.0021193317185910185210
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9479631.250.16980.002711.32230.22970.48330.0067255527255019254229
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10088481.810.16880.002310.75110.28610.46080.0078254524250225244335

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MDPI and ACS Style

Duan, C.; Li, Y.; Yang, Y.; Liang, Y.; Wei, M.; Hou, K. U-Pb Ages and Hf Isotopes of Detrital Zircon Grains from the Mesoproterozoic Chuanlinggou Formation in North China Craton: Implications for the Geochronology of Sedimentary Iron Deposits and Crustal Evolution. Minerals 2018, 8, 547. https://doi.org/10.3390/min8120547

AMA Style

Duan C, Li Y, Yang Y, Liang Y, Wei M, Hou K. U-Pb Ages and Hf Isotopes of Detrital Zircon Grains from the Mesoproterozoic Chuanlinggou Formation in North China Craton: Implications for the Geochronology of Sedimentary Iron Deposits and Crustal Evolution. Minerals. 2018; 8(12):547. https://doi.org/10.3390/min8120547

Chicago/Turabian Style

Duan, Chao, Yanhe Li, Yun Yang, Yongsheng Liang, Minghui Wei, and Kejun Hou. 2018. "U-Pb Ages and Hf Isotopes of Detrital Zircon Grains from the Mesoproterozoic Chuanlinggou Formation in North China Craton: Implications for the Geochronology of Sedimentary Iron Deposits and Crustal Evolution" Minerals 8, no. 12: 547. https://doi.org/10.3390/min8120547

APA Style

Duan, C., Li, Y., Yang, Y., Liang, Y., Wei, M., & Hou, K. (2018). U-Pb Ages and Hf Isotopes of Detrital Zircon Grains from the Mesoproterozoic Chuanlinggou Formation in North China Craton: Implications for the Geochronology of Sedimentary Iron Deposits and Crustal Evolution. Minerals, 8(12), 547. https://doi.org/10.3390/min8120547

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