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Review

Precambrian Tectonic Affinity of Hainan and Its Evolution from Columbia to Rodinia

by
Limin Zhang
1,2,
Xiang Cui
2,*,
Yong Yang
1,
Si Chen
1,*,
Bin Zhao
1 and
Xiguang Deng
1
1
Key Laboratory of Marine Mineral Resources, Ministry of Natural Resources, Guangzhou Marine Geological Survey, Guangzhou 511458, China
2
Guangdong Provincial Key Lab of Geodynamics and Geohazards, School of Earth Sciences and Engineering, Sun Yat-sen University, Guangzhou 510275, China
*
Authors to whom correspondence should be addressed.
Minerals 2023, 13(10), 1237; https://doi.org/10.3390/min13101237
Submission received: 14 August 2023 / Revised: 7 September 2023 / Accepted: 20 September 2023 / Published: 22 September 2023
(This article belongs to the Section Mineral Geochemistry and Geochronology)
Browse Figures
Versions Notes

Abstract

:
The assembly and break-up of supercontinents have been hot research topics in international earth sciences because they represent a breakthrough in reconstructing the history of continental evolution and deepening the theory of plate tectonics, which is of indispensable importance to the development of earth sciences. With the continuous enrichment of paleomagnetic, paleontological, chronological, and geochemical data in the last two decades, the evolution of the supercontinent from Columbia to Rodinia has gradually gained unified understanding, and the reconstruction of the major plates within the supercontinent has basically been constrained. In contrast, the reconstruction of microplates, such as South China, Tarim, and Kabul, is controversial and has now become a popular topic and frontier area of supercontinent reconstruction. Hainan lies at the southern tip of South China, and a few Proterozoic units are exposed on the island. At present, Hainan is often taken as a part of the Cathaysia Block. However, due to the lack of exposed Mesoproterozoic igneous and supercrustal rocks in Cathaysia, the reconstruction model of the Cathaysia Block and even the South China Craton based solely on Mesoproterozoic units in Hainan are distinct from those based on units in the Yangtze Block and younger Proterozoic units within the Cathaysia Block, which makes the paleoposition of the South China Craton controversial. In this paper, we provide new detrital zircon U–Pb age data for the Baoban Complex, Hainan, together with the available data to comment on the affinities between Hainan and the Yangtze and Cathaysia Blocks in the Proterozoic, and on this basis, we can reconstruct the South China Craton within the Proterozoic supercontinents.

1. Introduction

The South China Block (SCB) is an important part of the East Asian continent, formed by the collision of the Yangtze and Cathaysia Blocks along the Jiangnan (or Sibao) orogenic belt in the early Neoproterozoic (Figure 1a) [1,2,3,4,5]. A rich Precambrian geological record is preserved within the SCB, which is thought to have been involved in the evolution of the supercontinents from Columbia to Rodinia [6,7,8,9,10,11,12,13,14,15,16,17,18,19,20,21,22,23,24,25,26,27,28]. However, whether the SCB lies within or on the margin of the supercontinents is still highly controversial (see [8,29,30,31,32,33,34,35,36]). Hainan lies at the southern tip of the South China continent and plays an important role in reconstructing the SCB in Proterozoic supercontinents (Figure 1b,c) [6,8,37,38,39,40,41]. Sporadic Mesoproterozoic geochronological data led to early suggestions of a Grenvillian-age Sibao orogenic belt in South China [8]. And based on the comparable geochronological and geochemical records between the Mesoproterozoic Baoban Complex in Hainan and the Purcell Belt Supergroup in West Laurentia, as well as the Sibao orogenic belt, the SCB was placed in an internal location adjacent to Laurentia in the early Neoproterozoic (Figure 2a) [6,8,37]. However, an increasing number of studies conclude that the assembly between the Yangtze and Cathaysia blocks did not end until approximately 825–805 Ma [10,42,43,44,45,46,47,48], and the Grenvillian orogenic belt did not exist in South China [47], supporting that the SCB is located at the margin of the Rodinia supercontinent (Figure 2b) [12,31,33,46,47,48]. Recently, some studies have gradually recognized the differences between the Yangtze and Cathaysia blocks during the Proterozoic, separated and reorganized the metasedimentary rock units within the SCB, and reanalyzed the possible position of the SCB within the supercontinent on the basis of a comprehensive understanding of the tectonic properties of each unit [27,40]. This paper presents a new study on sample 14HN-08A from the Mesoproterozoic Baoban Complex in west Hainan, South China. Based on the new U–Pb age data, as well as the published data from both Hainan and potential neighboring continents, we present an updated interpretation of Hainan Proterozoic tectonics and their possible paleogeographic connections with other continents during Precambrian supercontinent cycles.

2. Geological Setting and Sampling

Hainan constitutes the southern exposed extent of the SCB and is geographically connected to the South China mainland by the Qiongzhou Strait (Figure 1b). Some researchers have argued that Hainan was already part of the Cathaysia Block during the Proterozoic (e.g., [6,8,51]) and reconstructed the connection between Cathaysia and Laurentia in Columbia on the basis of the Mesoproterozoic metamafic rocks in Hainan [8,37,38,39]. However, another group of researchers believes that Hainan consists of two different blocks in the north and south [52,53], with the northern part of Hainan belonging to the SCB and the southern part of Hainan belonging to the Indochina Block [54] or Western Australia [53]. The two blocks were not fully integrated until the Mesozoic [55] or the early Paleozoic [53] along the Jiusuo–Lingshui fracture zone. Others divided Hainan Island into northwestern and southeastern terranes, which sutured along the northeast-southwest-trending Baisha Fault during the late Paleozoic [56,57]).
Precambrian units in Hainan are only sporadically exposed in the southwestern part of Hainan and are tectonically located to the south of the Changjiang–Qionghai fracture zone and to the north of the Jiusuo–Lingshui fracture zone (Figure 1b). They consist of three major units, including the Baoban Complex, Shilu Group, and Shihuiding Formation [58,59]. Both the Shilu Group and the overlying Shihuiding Formation only occur in the Shilu Fe-Co-Cu ore district of western Hainan. They are dominated by siliciclastic and carbonate rocks and have been interpreted as Mesoproterozoic or early Neoproterozoic units [8,37,59,60,61]. The Baoban Complex is exposed sporadically in southwest Hainan and is the oldest unit recognized [58,62]. It consists mainly of supracrustal rocks, granitoids, and metamafic rocks and has experienced strong deformation and metamorphosed to upper amphibolite facies, resulting in migmatized gneisses and various schists. The tectonostratigraphic relationships between these units and the chronostratigraphic framework of metasedimentary rocks have long been controversial because of poor outcropping and chronological constraints. Initially, Xia et al. [63] considered the “Baoban Group” as a schist system modified by migmatization, while Shan [64] pointed out that the “Baoban Group” consisted of two parts, including the lower part of plagiogneiss and the upper part of schist. Ye et al. [65] considered it to be a migmatite, while Yu et al. [66] believed that it was mainly a granitic intrusion in the Mesoproterozoic. Hou et al. [67] and Liang [68] considered that the “Baoban Group” is dominated by granitic rocks, while the residual amphibolite was considered as barbertonite, and the whole “Baoban Group” was treated as a granite–greenstone belt. This has led to the realization that the “Baoban Group” is a set of granite–greenstone assemblages [66,67,68,69]. The Guangdong District Survey Team in Hainan described the “Baoban Group” as a Cambrian unit. The zircon U–Pb age of migmatite reported by Ye et al. [64] constrained the “Baoban Group” to the Meso-Neoproterozoic. Hou et al. [67] classified the amphibolite into the Paleoproterozoic and the granitic gneisses into the Mesoproterozoic with Sm–Nd ages of 1699 ± 3 Ma and 1379 ± 25 Ma, respectively. It can be seen that the disagreement mainly focuses on the age of each component unit of the “Baoban Group” and the relationship between them. With the continuous improvement of analytical methods and in-depth research, an increasing number of researchers have gradually realized that the “Baoban Group” mainly consists of supracrustal rocks and later intruded granitic and metamafic rocks and named it the “Baoban Complex” [37,38,39,52,60,70,71]. The supracrustal rocks are divided from bottom to top into the Gezhencun and Ewenling formations, and they were intruded by gneissic granitoids and amphibolites.
The metasedimentary sample analyzed in this study was collected from the Baoban Complex as shown in Figure 1. It is dominated by mica-quartz schists, composed of recrystallized quartz and plagioclase with biotite aligned along the schistosity plane.

3. Analytical Methods

Zircon grains from the sample were separated using heavy liquid and magnetic techniques and then handpicked under a binocular microscope. Their internal texture was examined by cathodoluminescence (CL) imaging using a scanning electron microprobe at the School of Earth Science and Engineering at Sun Yat-sen University. The operating conditions were an accelerating voltage of 15 Kv and a sample current of 10 nA with a beam diameter ranging from 1 to 5 μm. Zircon U-Pb dating was conducted by a laser ablation inductively coupled plasma mass spectrometry (LA-ICPMS) at the State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences in Wuhan, China. The instrumental settings and detailed analytical procedures are outlined in [72,73]. A laser repetition rate of 8 Hz with a spot size of 32 μm was used for ablating the zircons. Fractionation correction and subsequent calculations follow ICPMSDataCal (8.4) [73]. Data reduction was carried out using the Ludwig SQUID 1.0 and ISOPLOT program [74]. All measurements were monitored using standard zircons GJ-1 (608.53 ± 0.37 Ma [75]) and 91,500 (1062.4 ± 0.6 Ma [76]). Individual analyses in the data table are presented with 1 σ error. Apparent ages are based on the 207Pb/206Pb ages and relative probability versus age diagrams are based on spots with discordance <10%.

4. Tectonostratigraphic Relationships between the Baoban Complex, the Shilu Group, and the Shihuiding Formation

Ages from 69 grains from sample 14HN-08A yield 64 concordant results (Table 1). They are concentrated in the range of 2700–1430 Ma, forming a major age peak at ~1800 Ma and subordinate peaks at ~1610 Ma and ~1460 Ma, consistent with those in Yao et al. [37] and Zhang et al. [39]. The four youngest grains define the youngest age cluster and yield a weighted mean age of 1451 ± 45 Ma (MSWD = 1.6). Together with the U–Pb age data of authigenic monazite reported by [41], the Ewenling Formation that was metamorphosed to lower amphibolite facies should have been deposited during 1450–1300 Ma. The lower Gezhencun Formation in the Baoban Complex, which was metamorphosed to upper amphibolite facies, was deposited at 1550–1450 Ma [41]. Metamafic and granitic rocks are preserved as lenses, pods, and interlayers with exposure scales ranging from a few meters to hundreds of meters [38,39] and were emplaced at 1441–1424 Ma [38,41] and 1450–1421 Ma [6,39,41], respectively. Gneissic granites emplaced at 1550 Ma published by [41] is the oldest unit in the Baoban Complex.
The magmatic rocks within the Baoban Complex are dominated by contemporaneous metamafic rocks and A-type granite [8,38,39], forming a typical bimodal magmatic assemblage, supporting an extensional setting during the Mesoproterozoic. Previous regional investigations on Hainan have suggested that the Baoban Complex is in fault contact with the Shilu Group [58,59]. Due to the controversial depositional age of the Shilu Group, the tectonostratigraphic relationship between the Shilu Group, the Baoban Complex, and the Shihuiding Formation has not been well constrained. Li et al. [8] and Yao et al. [37] reported the Sensitive High Resolution Ion MicroProbe (SHRIMP) zircon U–Pb age of tuffs in the fifth layer of the Shilu Group to be 1439 ± 9 Ma, which is in line with the age of the Baoban Complex, and suggested that the lower five layers of the Shilu Group should have been deposited prior to ca. 1430 Ma. Furthermore, they limited the maximum depositional age of the sixth layer to 1063 ± 27 Ma based on the detrital zircon U-Pb age and thus considered that there was a sedimentary hiatus of no less than 400 Myr between the “fifth” and “sixth” layers of the Shilu Group, proposing that the sixth layer should be removed from the group and treated as a distinctive stratigraphic unit, namely the “Liuceng Formation”. Wang et al. [60] suggested that the Shilu Group (layers 4–6) and the Shihuiding Formation were deposited ca. 1.0 Ga and proposed that the Shihuiding Formation should be considered as the top, i.e., the seventh layer of the Shilu Group, based on their similar zircon U–Pb age distributions.
The Baoban Complex experienced amphibolite facies metamorphism, whereas the Shilu Group displays modification to low-temperature green schist facies, with the two in fault contact [58,59]. This suggests that a tectonic-metamorphic event should have occurred in Hainan prior to the precipitation of the Shilu Group and after the formation of the Baoban Complex. Metamorphic zircons of 1300–1000 Ma are widely exposed in the metasedimentary rocks, gneisses, and magmatic rocks of the Baoban Complex but are largely absent within the Shilu Group (layers 3–6) [37,38,39,70,77] (Figure 2), which indicates that these sedimentary and magmatic rocks experienced metamorphism during 1300–1000 Ma. Abundant detrital zircon U–Pb data for layers 3–6 of the Shilu Group constrain the maximum depositional age of the mid-upper Shilu Group to approximately 1100 Ma [60,70,71]. All of these results support that the mid-upper Shilu Group is a depositional system distinctively different from the metasedimentary rocks in the Baoban Complex. No age data are currently available for the first and second layers of the Shilu Group because of poor outcrops.
Sedimentary detritus from layers 3–6 of the Shilu Group are of low maturity, relatively enriched in high field strength elements and rare earth elements, and deficient in transition elements (e.g., Sc and Co) [71], implying their origination dominantly from felsic igneous rocks. This inference further indicates their deposition on active continental margins [78,79,80]. The first to fifth layers of the Shilu Group are relatively strongly deformed and intensely metamorphosed, whereas the sixth layer of the Shilu Group shows weak deformation and slight metamorphism. The Shihuiding Formation is a suite of siliciclastic clastic rocks that are unmetamorphosed and less deformed [81]. In contrast to the Shilu Group, it has a higher quartz content, is enriched in SiO2, and depleted in CaO, Na2O, and TiO2 with more remarkable differentiation between light and heavy rare earth elements [71,82], implying that it should originate dominantly from recycled sediments. Furthermore, it yields an additional age peak at ~1390 Ma and a slightly younger maximum depositional age of ~930 Ma [40,71] (Figure 3). Distinct metamorphic grades, sedimentary sources, and the unconformity between the Shilu Group and Shihuiding Formation argue against them as one unit.

5. Correlation to Sequences in the Cathaysia and Yangtze Blocks

Hainan has long been considered a part of the Cathaysia Block, and the Baoban Complex has been used as critical evidence for delimiting the position of the Cathaysia Block and even the South China Block in Precambrian supercontinent reconstructions (e.g., [8,37]). However, there has been no relevant evidence to prove the affinity between Hainan and the Cathaysia Block during the Proterozoic. The Precambrian units within the Cathaysia Block are dominated by early Neoproterozoic igneous rocks and a series of middle to late Neoproterozoic sedimentary rocks (e.g., [10,11,45,46,83,84]), which are absent in Hainan; furthermore, neither Mesoproterozoic sedimentary nor igneous rocks that crop out in Hainan have been reported from the Cathaysia Block [2,4,25,37,38,83,84,85,86,87,88,89,90], casting doubt on the Mesoproterozoic-early Neoproterozoic Cathaysia-Hainan connection.
Available zircon U–Pb chronology and Hf isotope data show that detrital zircons in Hainan with age ranges of 1700–1100 Ma have dominantly positive εHf(t) values [61,71], and most of these zircons have crustal incubation times of less than 300 Ma, indicating an important period for juvenile crust generation. In contrast, the crust of the Cathaysia Block showed episodic accretion, with major crustal growth occurring ca. 2500 Ma and 1000 Ma [86,87,88,89,90]. Therefore, these differences in crustal evolution and diachronous magmatism and sequence imply that Hainan was not closely linked to the Cathaysia Block during the Proterozoic.
In contrast, the Kunyang and Huili Groups as well as the Julin Group developed at the southwest margin of the Yangtze Block were deposited at approximately 1050 Ma and are dominated by siliceous clastic rocks and carbonates, similar to the Shilu Group [91,92,93,94,95]. Detrital zircons from the two groups yield age peaks at 1750 Ma, 1600 Ma, 1450 Ma, and 1160 Ma [91,92,93,94,95] (Figure 4), which matches well with the Shilu Group. These similarities, together with the comparable Hf isotope compositions (Figure 4) and geochemical compositions [71], indicate that the Kunyang Group and its equivalent in the Yangtze Block share a similar provenance with the Shilu Group. Moreover, detrital zircons of 1700–1100 Ma with dominantly depleted Hf isotope compositions (Figure 5) suggest comparable juvenile crustal generation between Hainan and Yangtze during the Mesoproterozoic. The ca. 1430 Ma metamafic and granitic rocks in Hainan show geochemical compositions and Sr-Nd-Hf isotopic signatures comparable to those of the 1530–1375 Ma magmatic rocks in the southwest Yangtze Block [40,96,97]. In summary, Hainan shows obvious similarities with the Yangtze Block in terms of crustal evolution, magmatic assemblages, and sedimentary facies and provenance, implying that Hainan and Yangtze might constitute a single, spatially unified domain in the Proterozoic. This interpretation is also supported by the similar mineralization style of iron deposits hosted in the Shilu Group and ore deposits in the Dahongshan, Dongchuan, Hekou and Sin Quyen groups in the western Yangtze Block [98], although the age of the iron deposit in Hainan is poorly constrained.

6. Hainan and Precambrian Supercontinent Evolution

6.1. Reconstructing West Hainan–Yangtze in Columbia

A range of paleogeographic reconstructions have been proposed to reconstruct Columbia [34,99,100,101]. Combined with the available data on magmatism, sedimentary rocks, and paleomagnetism, it is usually believed that the Siberia–Laurentia–Baltica constitutes the core of Columbia [101], while the South American–West African, Western Australian–South African, East Antarctic, North China, and India blocks are located in the margins [34,99].
The Baoban metasedimentary rocks have comparable depositional ages to the Mesoproterozoic sedimentary sequences deposited across the western margin of Laurentia, e.g., the 1.47–1.40 Ga Belt-Purcell, the 1.46–1.42 Ga PR1, the 1.48–1.44 Ga Yankee Joe/Hess Canyon-Defiance, and the 1.47–1.45 Ga Trampas and Marquenas basins [102,103,104,105,106,107,108,109]. Detrital zircons from the Baoban Complex yield comparable age populations and Hf isotope compositions to those in the lower Belt–Purcell Supergroup and their equivalents [102,103,104,106,107,108,110] (Figure 5, date should be seen in Tables S1 and S2), which may have originated from the Gawler Craton [111,112,113,114,115,116] and East Antarctica [117,118,119,120,121,122], in which many Mesoproterozoic igneous rocks have been identified and reported. Additionally, the Mesoproterozoic metamafic and felsic rocks from the Baoban Complex in Hainan share similar geochronological and geochemical characteristics with those in the Belt–Purcell Supergroup [8,37,38,39,103,123,124,125,126]. Such similarities suggest the close spatial affinity of West Hainan with west Laurentia, the Gawler Craton, and East Antarctica, and thus Hainan was more likely located in the center of the Columbia supercontinent.

6.2. Reconstructing West Hainan–Yangtze in Rodinia

Detrital zircons from the Shilu Group mainly yield Paleoproterozoic to Mesoproterozoic ages with a few Archean dates, forming age peaks at ~1780 Ma, ~1600 Ma, ~1450 Ma, and ~1170 Ma [37,60,71] (Figure 6a). This is significantly different from the ~1100–1000 Ma Buffo Hump Formation (Deer Trail Group) and its equivalent units, which overlie the Belt–Purcell Supergroup [104,105,127,128,129], but are comparable to the South Delhi Supergroup in NW India (Figure 7) [130,131,132] and its equivalent—the upper Vindhyan sequence of the Vindhyan Basin located in the central part of the Northern India [130,131,132,133,134]. All of these results suggest that the source of the Shilu Group is markedly different from that of the Buffo Hump Formation (Deer Trail Group) but similar to that of the South Delhi Supergroup and the upper Vindhyan sequence, perhaps due to Hainan having drifted away from the vicinity of western Laurentia and occupying an external position of the supercontinent, near the Indian Craton as shown in Figure 8, prior to ~1100 Ma.
Globally, the 1200~1100 Ma magmatism occurred mainly in Laurentia, Baltica, Africa, South America, and East Antarctica [135,136,137,138,139]. Among these continents, Laurentia and East Antarctica are the most likely sources for detritus of Hainan–Yangtze–India. Because magmatic events at approximately 2100 Ma were widely developed in Africa and South America, the sources they provided tend to carry many zircon grains with ages of 2100 Ma, whereas detrital material from the Baltic Craton tends to contain large amounts of zircon grains of 1900 Ma [136,137,140,141] (Figure 8). Detrital zircons from the sedimentary sequence in Laurentia mainly yield age peaks at ~1700 Ma, ~1450 Ma, and 1250 Ma and essentially contain no zircons of 1650–1550 Ma [104,105,127,128,129], which is distinct from those of Hainan–Yangtze–India. Although much of Antarctica is covered with ice, abundant ~1200–1100 Ma igneous and metamorphic clasts have been identified in the Gamburtsev Subglacial Mountains [119,139,142]. Together with the ~1606–1595 Ma felsic volcanic rocks found in moraines of the Terre Adélie Craton [117], 1578 Ma granite clasts from the Transantarctic Mountains [118] and 1486–1404 Ma mafic and felsic rocks observed on Mount Brown [120,121,122], igneous zircons in East Antarctica, may have served as a vital source for Hainan–Yangtze–India during the late Mesoproterozoic.
Minerals 13 01237 g007
Figure 7. Relative probability plots for zircon ages for late Mesoproterozoic sequence in west Hainan (a), southwest Yangtze (b), northwest India (c), and Antarctica (d). Data in west Hainan are from [37,41] and this study; west Laurentia are from [104,106,108]; northwest India are from [129,130,131,132]; East Antarctica are from [117,119,137,141].
Figure 7. Relative probability plots for zircon ages for late Mesoproterozoic sequence in west Hainan (a), southwest Yangtze (b), northwest India (c), and Antarctica (d). Data in west Hainan are from [37,41] and this study; west Laurentia are from [104,106,108]; northwest India are from [129,130,131,132]; East Antarctica are from [117,119,137,141].
Minerals 13 01237 g007
Minerals 13 01237 g008
Figure 8. Proposed configuration of west Hainan, Yangtze, India, Mawson continent (South Australia Gawler Craton and Antarctica) and Laurentia during extension of supercontinent Columbia ca. 1450 Ma and (a) assembly of supercontinent Rodinia ~1000 Ma (b). Y-Yangtze Block, C-Cathaysia Block, H-Hainan, NAC-North Australian Craton, SAC-South Australia Craton, KY-Kunyang Group, HL-Huili Group, JL-Julin Group. Inferred extraneous sedimentary provenance links are shown by magenta arrows. Red ellipses circled with dashed line on Mawson continent depict point sources in East Antarctica and Terre Adélie of unknown extent (for interpretation of the references to color in this figure legend, the reader is referred to the web version of this article).
Figure 8. Proposed configuration of west Hainan, Yangtze, India, Mawson continent (South Australia Gawler Craton and Antarctica) and Laurentia during extension of supercontinent Columbia ca. 1450 Ma and (a) assembly of supercontinent Rodinia ~1000 Ma (b). Y-Yangtze Block, C-Cathaysia Block, H-Hainan, NAC-North Australian Craton, SAC-South Australia Craton, KY-Kunyang Group, HL-Huili Group, JL-Julin Group. Inferred extraneous sedimentary provenance links are shown by magenta arrows. Red ellipses circled with dashed line on Mawson continent depict point sources in East Antarctica and Terre Adélie of unknown extent (for interpretation of the references to color in this figure legend, the reader is referred to the web version of this article).
Minerals 13 01237 g008

7. Conclusions

New U-Pb geochronology of zircon in metasedimentary rocks from the Mesoproterozoic Baoban Complex in SW Hainan, together with published data for South China, indicate the following:
  • There are three Proterozoic units in Hainan, including the Mesoproterozoic Baoban Complex, the late Mesoproterozoic Shilu Group, and the Neoproterozoic Shihuiding Formation.
  • Hainan was linked to the Yangtze Block rather than the Cathaysia Block in the late Mesoproterozoic–early Neoproterozoic.
  • The connected Hainan–Yangtze blocks likely drifted from the core to the margin of the supercontinents in the Proterozoic.

Supplementary Materials

The following are available online at https://www.mdpi.com/article/10.3390/min13101237/s1, Table S1: Published zircon U-Pb geochronological data of Meso-Neoproterozoic samples from the Hainan,Yangtze Block, India, western Laurentia and East Antarctica; Table S2: Published zircon Hf isotopic data of Meso-Neoproterozoic samples from the Hainan, Yangtze Block, India, western Laurentia and East Antarctica.

Author Contributions

Writing—original draft, data analysis, L.Z.; conceptualization, supervision, writing—reviewing and editing, L.Z. and X.C.; sample collection, sample preparation, L.Z.; conception of experiment, S.C.; data curation, Y.Y., B.Z. and X.D. All authors have read and agreed to the published version of the manuscript.

Funding

This study was jointly funded by the National Science Foundation of China (42102262, U2244222 and 42002237), the Scientific and Technological Planning Project of Guangzhou City (202201011487), and the China Geological Survey (DD20221718).

Data Availability Statement

The data presented in this work are available on request from the corresponding author.

Acknowledgments

We would like to thank G-F Zhao and H-Y He for their help during field work. We also appreciate the editor and two anonymous reviewers who have provided insightful suggestions, which greatly improved the manuscript.

Conflicts of Interest

The authors declare no conflict of interest.

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Minerals 13 01237 g001
Figure 1. (a) Tectonic outline of the South China Craton (after [49]), (b) simplified geological map of Hainan Island showing the distribution of Mesoproterozoic rocks (revised after [50]), and (c) simplified stratigraphic column of the Mesoproterozoic Baoban Complex (revised after [50]).
Figure 1. (a) Tectonic outline of the South China Craton (after [49]), (b) simplified geological map of Hainan Island showing the distribution of Mesoproterozoic rocks (revised after [50]), and (c) simplified stratigraphic column of the Mesoproterozoic Baoban Complex (revised after [50]).
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Minerals 13 01237 g002
Figure 2. Representative models showing the location of the South China block in Rodinia (after [8,31]). Panel (a) shows internal locations and panel (b) shows external locations of the South China block in Rodinia.
Figure 2. Representative models showing the location of the South China block in Rodinia (after [8,31]). Panel (a) shows internal locations and panel (b) shows external locations of the South China block in Rodinia.
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Minerals 13 01237 g003
Figure 3. Relative probability density plots (a–f) and Th/U characteristics (g–l) for Proterozoic unit detrital zircons from Hainan (data from [37,39,41,60,71] and this study).
Figure 3. Relative probability density plots (a–f) and Th/U characteristics (g–l) for Proterozoic unit detrital zircons from Hainan (data from [37,39,41,60,71] and this study).
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Figure 4. Simplified stratigraphic columns and relative probability density plots for the representative samples from the (a) Shilu Group in Hainan and (b) Kunyang and Huili groups in the Yangtze Block. Simplified stratigraphic column is modified after [13,69,71,93,94,95]. Data for the Shilu Group are from [37,60,71] and the Kunyang and Huili groups are from [23,91,92,93,94,95].
Figure 4. Simplified stratigraphic columns and relative probability density plots for the representative samples from the (a) Shilu Group in Hainan and (b) Kunyang and Huili groups in the Yangtze Block. Simplified stratigraphic column is modified after [13,69,71,93,94,95]. Data for the Shilu Group are from [37,60,71] and the Kunyang and Huili groups are from [23,91,92,93,94,95].
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Figure 5. Hf isotopic composition of detrital zircon from the Shilu Group in Hainan and Kunyang and Huili groups in the Yangtze Block. Data for the Shilu Group are from [37,68,70] and the Kunyang and Huili groups are from [23,86,88].
Figure 5. Hf isotopic composition of detrital zircon from the Shilu Group in Hainan and Kunyang and Huili groups in the Yangtze Block. Data for the Shilu Group are from [37,68,70] and the Kunyang and Huili groups are from [23,86,88].
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Figure 6. Comparisons of Mesoproterozoic sequences in west Hainan and Laurentia. (a,b) show age distribution and (c,d) show Hf isotopic composition of detrital zircon. Data for Hainan are from [37,39], West Laurent are from [103,106,108].
Figure 6. Comparisons of Mesoproterozoic sequences in west Hainan and Laurentia. (a,b) show age distribution and (c,d) show Hf isotopic composition of detrital zircon. Data for Hainan are from [37,39], West Laurent are from [103,106,108].
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Table 1. Zircon U–Pb dating results for the representative sample from the metasedimentary rocks in Baoban Complex, west Hainan.
Table 1. Zircon U–Pb dating results for the representative sample from the metasedimentary rocks in Baoban Complex, west Hainan.
SpotsTh/UIsotopic RatiosApparent Age (Ma)Conc.
(%)
207Pb/206Pb1σ207Pb/235U1σ206Pb/238U1σ207Pb/206Pb1σ207Pb/235U1σ206Pb/238U1σ
14HN08A-010.130.1103910.0034174.8888210.1860530.3168830.00856418062818001617742198
14HN08A-020.600.0915790.0022023.0648740.0781180.2391000.0034601459231424101382997
14HN08A-030.210.1042820.0026104.4422450.1222510.3046800.00463617022317201217141299
14HN08A-040.180.0927470.0022593.2712800.0815210.2521330.0034871483231474101449998
14HN08A-050.280.1487860.0039958.8021230.2658020.4226760.00811323322323181422731998
14HN08A-060.200.1053820.0029554.2475380.1265910.2882130.00485917212616831216331296
14HN08A-070.450.1260450.0031786.4506140.2084430.3644650.00747620442220391420031898
14HN08A-080.120.0999230.0023373.8995370.0921490.2792110.00379616331916141015871098
14HN08A-090.130.0986730.0026792.8680540.0827260.2075140.0032711599261374111216987
14HN08A-100.330.1100660.0029684.5661790.1202210.2980040.00477418112517431116811296
14HN08A-110.490.1666550.0038799.4613480.2379840.4069130.00759125242023841222011892
14HN08A-120.180.1089330.0026814.6371950.1245890.3050420.00532017832317561117161397
14HN08A-130.120.1109980.0028524.8705990.1353930.3145550.00565618172417971217631498
14HN08A-140.260.1129700.0033154.8934830.1495390.3103670.00531118482718011317431396
14HN08A-150.350.1079640.0032624.5615160.1418000.3039480.00598717652817421317111598
14HN08A-160.270.1731660.00462811.2099020.2990450.4651950.00803725892325411324621896
14HN08A-170.130.0893270.0022062.9343090.0768500.2359100.00379114132313911013651098
14HN08A-180.170.1127750.0031115.0047780.1362190.3203240.00590718562518201217911598
14HN08A-190.650.1070030.0028664.5594420.1353970.3055260.00576917502517421317191498
14HN08A-200.390.1068520.0029594.0036080.1087470.2696080.00394917472616351115391093
14HN08A-211.100.1005580.0034233.9959980.1488060.2866570.00568416353216331516251499
14HN08A-220.290.1017810.0025374.0816970.1064790.2883150.00445716572316511116331198
14HN08A-230.460.1122270.0030254.8483940.1505690.3096360.00549518362417931317391496
14HN08A-240.620.1001310.0028553.9506130.1063660.2862530.00569216282716241116231599
14HN08A-250.350.1065480.0030034.4975710.1304710.3050090.00536617432617311217161499
14HN08A-260.360.1130040.0026135.0537660.1245710.3223900.00533318502418281118011398
14HN08A-270.230.1314120.0031886.8518960.2153360.3733910.00757021172220921420451897
14HN08A-280.730.1315440.0034516.7769830.2090660.3705710.00687321202320831420321697
14HN08A-290.120.1252230.0039265.0657870.1635860.2903870.00498120322818301416431389
14HN08A-300.630.1196890.0029805.5693810.1374500.3343550.00452819522219111118591197
14HN08A-310.430.1109230.0026374.5734290.1059400.2961870.00407218152217441016721095
14HN08A-320.210.1360120.0038105.5142240.1830670.2907790.00632221772519031516451685
14HN08A-330.290.1128680.0037734.6901510.1298800.2992030.00661418463017651216871795
14HN08A-340.030.0993400.0027053.3641210.0886230.2430830.0034221613251496111403993
14HN08A-350.170.1101260.0028344.4849060.1123080.2923950.00425118112417281116531195
14HN08A-360.550.1063900.0026354.5219620.1114960.3053290.00438517392317351117181198
14HN08A-370.450.1074770.0052153.8439430.1715920.2584380.00612917674516021814821692
14HN08A-380.190.1078280.0028854.5826840.1592190.3058040.00833617652517461517202198
14HN08A-390.310.1832430.00415212.9825080.2992900.5095130.00720726821626781126551699
14HN08A-400.270.1088190.0026994.7777530.1224250.3158470.00507217802117811117691399
14HN08A-410.110.1141720.0029345.2104900.1402420.3290530.00544819332618541218341398
14HN08A-420.170.1556850.0041018.7271320.2459920.4024390.00679524102223101321801694
14HN08A-430.510.1105770.0036434.5383450.1596700.2948680.00560718094717381516661495
14HN08A-440.580.1561800.0038569.2948050.2377750.4273300.00666424152223681222941596
14HN08A-450.400.1049950.0029613.7303740.1044570.2553770.00419517152615781114661192
14HN08A-460.080.1037780.0025314.0836070.0996980.2823700.00396016942316511016031097
14HN08A-470.470.1107890.0035024.9668130.1736410.3209020.00611918132918141517941598
14HN08A-480.270.1065600.0029574.4222480.1193080.2976910.00423417432317171116801197
14HN08A-490.410.1131630.0029725.0416480.1296480.3194380.00445518512418261117871197
14HN08A-500.170.1094770.0031474.6373380.1348250.3036230.00457017902617561217091297
14HN08A-510.500.1133540.0033965.0992840.1594730.3234580.00607918542718361418071598
14HN08A-520.640.1127210.0039634.9801680.1663490.3183530.00552018442918161417821498
14HN08A-530.120.0993370.0055683.8905360.2195260.2783240.00430616135516122315831198
14HN08A-540.290.0981600.0037152.2317280.0799100.1641720.002972159136119113980880
14HN08A-550.060.0825480.0033872.0472970.0913640.1784750.0028451258401131151059893
14HN08A-560.520.0976600.0037263.7935260.1706640.2782650.00497515803615911815831399
14HN08A-570.060.0967370.0025722.6977940.0763710.2011700.0025551562231328111182788
14HN08A-580.230.0975020.0025523.1534520.0868080.2332580.0029301577251446111352893
14HN08A-590.440.1827040.00505712.8912290.3719900.5094450.00725826772326721426541699
14HN08A-600.260.1086180.0030014.7252100.1408800.3137220.00489117762617721317591299
14HN08A-610.460.1501410.0042609.0016260.2634260.4328500.00619923472423381423191499
14HN08A-620.160.1184840.0027265.0650770.1219350.3081950.0036611944211830101732994
14HN08A-630.100.1486820.0034907.2238110.1727200.3506790.00523423311821391119381390
14HN08A-640.430.1042320.0030023.8680910.1272740.2677810.00522817022716071415301495
14HN08A-650.450.0910600.0019172.6529010.0604760.2104830.002736144820131591231893
14HN08A-660.190.0990740.0021593.8680750.1152540.2790040.00529416062016071215861498
14HN08A-670.480.0980610.0020953.7399140.1188310.2740320.00573015872015801315611598
14HN08A-680.120.1417320.0038107.2293190.2171860.3688270.00586422502321401420241494
14HN08A-690.130.0990610.0021803.7296500.0890680.2720950.0033381606211578101551998
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Zhang, L.; Cui, X.; Yang, Y.; Chen, S.; Zhao, B.; Deng, X. Precambrian Tectonic Affinity of Hainan and Its Evolution from Columbia to Rodinia. Minerals 2023, 13, 1237. https://doi.org/10.3390/min13101237

AMA Style

Zhang L, Cui X, Yang Y, Chen S, Zhao B, Deng X. Precambrian Tectonic Affinity of Hainan and Its Evolution from Columbia to Rodinia. Minerals. 2023; 13(10):1237. https://doi.org/10.3390/min13101237

Chicago/Turabian Style

Zhang, Limin, Xiang Cui, Yong Yang, Si Chen, Bin Zhao, and Xiguang Deng. 2023. "Precambrian Tectonic Affinity of Hainan and Its Evolution from Columbia to Rodinia" Minerals 13, no. 10: 1237. https://doi.org/10.3390/min13101237

APA Style

Zhang, L., Cui, X., Yang, Y., Chen, S., Zhao, B., & Deng, X. (2023). Precambrian Tectonic Affinity of Hainan and Its Evolution from Columbia to Rodinia. Minerals, 13(10), 1237. https://doi.org/10.3390/min13101237

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