Dual Geochemical Characteristics for the Basic Intrusions in the Yangtze Block , South China : New Evidence for the Breakup of Rodinia

Neoproterozoic intraplate magmatic rocks are widespread in the Yangtze Block (YZB). The contrasting interpretations on their petrogenesis and tectonic evolution induce stimulating discussions on the coeval tectonic setting, including the two competing models of rift-related (R-model) and arc-related (A-model). Their main evidence is dominantly from felsic magmatic rocks. In contrast, the less evolved basic rocks are more suitable for tectonic setting discrimination. Here we study the Longtanqing basic intrusions (LTQ) that are exposed to the central part of the N–S trending Kangdian rift in the western YZB, by detailed geochemical and geochronological investigations. Zircon U–Pb dating of the two diabases from LTQ yield identical ages within error of 777 ± 17 Ma and 780 ± 5.3 Ma, respectively. LTQ rocks are characterized by low SiO2 (49.83–50.71 wt %), high MgO (5.91–6.53 wt %), and Cr (140–150 ppm) contents, supporting the significant mantle affinity. They also display dual geochemical characteristics, including a series of features of continental within-plate basalts (WPB, Ti/V = 37.3–47.5, Zr/Y = 3.4–3.8, Ta/Hf = 0.19–0.23), and the typical signatures of island arc basalt (IAB), such as highly depleted in HFSE and HREE, and enriched in LREE and LILE. Most zircon εHf(t) values are positive (1.6–9.4) while the corresponding Hf depleted mantle model ages (TDM1) range from 1.0 Ga to 1.3 Ga. In combination with the occurrence of inherited zircons (991–1190 Ma), it is suggested that their sources are dominantly derived from the lithospheric mantle that was reconstructed in the late Mesoproterozoic. Thus, LTQ is mainly formed by partial melting of the enriched lithospheric mantle, and subsequently assimilated by a juvenile crust during upwelling. The melt compositions are controlled by different degrees of the crystal fractionation of the dominant clinopyroxene and plagioclase with minor amphibole under high f O2 conditions. Combined with previous geochronological and geochemical data in the YZB, our new results support the theory that the R-model can be responsible for the petrogenesis of Neoproterozoic magmatic rocks in South China.

Neoproterozoic magmatic rocks are widespread in the YZB, including dominantly felsic igneous rocks and relatively considerable basic rocks (Table S1).However, the petrogenesis and tectonic affinities of these magmatic rocks are still controversial [15][16][17][18].Two major but conflicting tectonic models, called rift-related (R-model) and arc-related (A-model), have been proposed.The R-model suggests that the magmatism is produced in the Neoproterozoic mantle plume related rift setting [4,8,[19][20][21][22][23][24][25][26][27], which is based on data about the geochemistry, geochronology, and paleomagnetism [3,7,20], as well as other aspects such as basin analysis and petrologic data [4,9,[28][29][30].The A-model argues that the arc magmatism around the margins of the YZB is responsible for the Neoproterozoic magmatic rocks [31][32][33][34][35][36][37], in terms of (1) arc signatures in geochemical compositions (e.g., Nb, Ta and Ti depletion); and (2) the presence of arc assemblages showing identical Neoproterozoic ages [17,18,38].The competing tectonic models have different implications, such as the relative location of SCB in Rodinia: whether SCB was the link between North America and Australia-East Antarctica, which was the core of the Rodinia [4,39], or located on the periphery of Rodinia [31,32].Hence, it requires further studies on tectonic affinity in order to understand the geodynamics of SCB.Previous studies have demonstrated that the less evolved basic rocks are better for tectonic affinity discrimination than those of mature felsic to intermediate rocks [40].Unfortunately, the samples for supporting both models are mainly from felsic rocks and intermediate rocks; few basic rocks are involved as a result of their rare occurrences in the SCB.[3,28,41,42]).The inset is a tectonic sketch of China showing the three Precambrian blocks (after [43]).Detailed data of the basic rocks in the Yangtze Block (YZB) can see in Table S1.[3,28,41,42]).The inset is a tectonic sketch of China showing the three Precambrian blocks (after [43]).Detailed data of the basic rocks in the Yangtze Block (YZB) can see in Table S1.The basic intrusions can play an important role on the study of the mechanism and processes of the supercontinent breakup [44].Recently, some Neoproterozoic basic intrusions have been recognized in the SCB (Table S1), in particular in the western and northern YZB, e.g., Wasigou gabbro intrusions [22], Xide diabase dykes [42], Hannan, and Micangshan mafic intrusions [45,46]-they all have already been considered as generating within an intraplate extension or subduction environment.In this study, we investigate the newly found Longtanqing basic intrusions (LTQ) exposed to the central part of the N-S trending Kangdian rift, and obtain a series of data, consisting of the U-Pb and Lu-Hf isotopic results of zircons, and whole-rock geochemical compositions.These new data, in combining with data from the literature, provide not only further constraints on the petrogenesis and tectonic setting of the Neoproterozoic rocks, but also insights into the response of the supercontinent breakup in the YZB.
In the western YZB, Proterozoic rift volcanic-sedimentary sequences occur in the Kangdian rift, including the late Paleo-Mesoproterozoic Dongchuan, Hekou, and Dahongshan Groups, and the Neoproterozoic Huili and Kunyang Groups [51, 52,57,58], which are along the Luzhijiang fault and a series of related NNE-trending faults.Among them, the Huili Group is mainly distributed in the Tong'an area, Huili County, southwestern China (Figure 2), and is a more than 10 km-thick sequence of meta-clastic and meta-carbonate rocks interbedded with volcanic rocks, which includes the Yinmin, Luoxue, Heishan, Qinglongshan, Limahe, Fenshan, and Tianbaoshan Formations, from the base upward.A meta-volcanic sample from the Tianbaoshan Formation gave a SHRIMP zircon U-Pb age of 1028 ± 9 Ma [57], which is consistent with those ages of the Upper Kunyang, Dengxiangying and Ebian Groups [57][58][59].The Huili Group is unconformably overlain by the Sinian Dengying Formation and younger strata, and intruded by numerous Meso-to Neoproterozoic magmatic intrusions, including LTQ (Figure 2).And these intrusions have closely spatial and temporal relationship to the iron oxide (copper) deposits in this region, especially for basic magmatism [60].
The LTQ crop out in the southern part of the Tong'an region (Figure 2).These intrusions, dominantly composed of basic rock bodies, occur as dykes and irregular intrusions that intrude the dolomite or shales of the Mesoproterozoic Heishan Formation, the Huili Group (Figures 2 and 3a).These intrusions are up to 3 km long and commonly 400-3000 m wide, striking NNW along with the fault.The samples were collected from the Longtanqing deposit (Figures 2b and 3a), which consist of fine-to medium-grained diabase (Figure 3b).The rock is mainly composed of sub-anhedral crystals of plagioclase (60-70%), hornblende (~15-25%), clinopyroxene (5~10%) and biotite (~10%), with minor apatite, opaque minerals (iron oxide minerals) (Figure 3c-f).Most of the intrusions may experience variable degrees of alteration, resulting in the albitization of some plagioclases, hornblende altered to chlorite, and some clinopyroxenes surfaces also had the phenomenon of iron precipitation (Figure 3e,f).In this research, we collected eight fresh samples to analyze the whole-rock geochemistry and two zircon samples for U-Pb dating and Hf isotopic analysis.

Major and Trace Element Analyses
The freshness of the samples analyzed during this study was ensured by sampling the cores of dikes and intrusions rather than the weathered exterior.Whole-rock major and trace elements were analyzed at the ALS Geochemistry Laboratory in Guangzhou.First, the steel jaw crusher was used to crush the fresh samples, and then the small blocks were powdered in an agate mill until the grain size <200 mesh.For major oxides concentrations, these were carried out on a standard wavelength dispersive X-ray fluorescence spectrometry (XRF).The determination of loss on ignition (LOI) was conducted after igniting the sample powders at 1000 • C for 1 h by gravimetric methods.Then, whole-rock powder (0.5 g) was added to 0.9 g of Li 2 B 4 O 7 -LiBO 2 , mixed well, fused in an auto-fluxer between 1050 • C and 1100 • C, and cooled to form a flat molten glass disk.This disk was analyzed by wavelength-dispersive XRF using an AXIOS Minerals spectrometer.The long term analytical uncertainties are generally within 0.1-1% (RSD) for major elements based on the duplicate measurements of silicate standards (BHVO-1 and AGV-1 from USGS).For trace and REE concentrations, a solution of the powdered samples was kept for two days in sealed beakers for digestion using a mixture of HF and HNO 3 acid in a Teflon screw-cap bomb.Then, this solution was run through an Elan DRC-II instrument (Element, Finnigan MAT) that used inductively coupled plasma mass spectrometry (ICP-MS).The uncertainties of the ICP-MS analyses are estimated to be better than 5%.Detailed analytical methods were described by Liu [61].

LA-ICPMS Zircon U-Pb Dating and Trace Element Analyses
Zircon grains were separated from samples 16LTQ-1 and 16LTQ-2 using magnetic and heavy liquid separation techniques, mounted in epoxy resin and polished to about half their thickness and then photographed in reflected and transmitted light.The structures of the zircon grains were imaged by cathodoluminescence (CL) techniques at the Analytical Center of the University of Science and Technology of China, Hefei (USTC).CL imaging was used to investigate crystal morphologies and internal structure and to select analytical spots.Zircon grains were analyzed for U-Pb dating and trace elements using the Laser Ablation Inductively-Coupled Plasma Mass Spectrometry (LA-ICPMS) method at the in situ Mineral Geochemistry Lab, Ore Deposit and Exploration Centre (ODEC), Hefei University of Technology, China.The analyses were carried out on an Agilent 7900 Quadrupole ICP-MS coupled to a Photon Machine Analyte HE 193-nm ArF Excimer laser ablation system.The ablated spot diameter of the ion beam was set at ~25 um.Argon was used as the make-up gas and Helium was applied as carrier gas.NIST SRM 610 glass was used as the external calibration standard and 29 Si was used as the internal standard to normalize the trace element.Zircon 91500 was used as the standard for U-Pb dating with a recommended 206 Pb/ 238 U age of 1065.4 ± 0.6 Ma [62].Quantitative calibration for the zircon U-Pb dating and trace elements were carried out on ICPMSDataCal 10.7 [63,64].Data reduction was carried out using the isoplot v3.0 program [65].

Zircon Lu-Hf Isotope Analyses
After the zircon U-Pb isotope measurement, the in situ Lu-Hf isotopic analysis was conducted at the laboratory of the Tianjin Institute of Geology and Mineral Resource, Chinese Academy of Geological Sciences.The Lu-Hf isotopes were measured by a Thermo Finnigan Neptune (Plus) MC-ICPMS, equipped with a 193-nm ArF-excimer laser ablation system.The instrumental parameter and data acquisition was followed according to the method described by Wu et al. [66] and Geng et al. [67].The laser beam diameter was 50 um, with a 10 Hz repetition rate and 15 J/cm 2 energy density.Helium was used as the carrier gas to transport the laser eroded matter in Neptune (MC-ICP-MS).Zircon standard GJ-1 was used as the external calibration to evaluate the reliability of the analytical data, the recommended 176 Hf/ 177 Hf ratio of 0.282006 ± 24 (2σ, [67]).Isobaric interferences of 176 Lu and 176 Yb were corrected by 176 Lu/ 175 Lu = 0.02655 (2σ, [68]) and 176 Yb/ 172 Yb = 0.5886 (2σ, [69]), respectively.Meanwhile, in order to calculate the mean β Yb value, a mean 173 Yb/ 171 Yb ratio was used, and then the 176 Yb signal intensity was calculated with the help of the 173 Yb signal intensity and the mean β Yb value [70].Time-drift correction and external calibration were done using zircon standard 91500.In this research, we adopted the decay constant for 176 Lu of 1.865 × 10 −11 a −1 [71], the present-day chondritic ratios of 176 Hf/ 177 Hf = 0.282772 and 176 Lu/ 177 Hf = 0.0332 [72], the present-day depleted mantle value of 176 Hf/ 177 Hf = 0.28325 [73], and 176 Lu/ 177 Hf = 0.0384 [74] to calculate initial 176 Hf/ 177 Hf ratios, ε Hf (t) values, and single-stage model ages (T DM1 ) when their ε Hf (t) values were positive.

Zircon LA-ICPMS U-Pb Dating and Trace Elements
The results of LA-ICPMS U-Pb isotopic analyses are listed in the supplementary data Table S2, and the data for all analyses are plotted on concordia diagrams within the analytical errors (Figure 4a,b).The representative zircon grains CL images are displayed in Figure 4c.The zircons are quite small (40-100 um), generally simple prismatic, colorless, transparent, and euhedral, with length to width ratios between 1:1 and 2:1.Most of them show obvious oscillatory zoning with different luminescence (Figure 4c), with Th/U ratios ranging from 0.42 to 1.03, almost more than 0.4, indicating a magmatic origin [75,76].Weighted mean 206 Pb/ 238 U dates are used to access their age, and inherited zircons and detrital zircon with variably older 206 Pb/ 238 U ages are not used when calculating crystallization ages.The data with concordance of less than 94% were excluded.

Zircon LA-ICPMS U-Pb Dating and Trace Elements
The results of LA-ICPMS U-Pb isotopic analyses are listed in the supplementary data Table S2, and the data for all analyses are plotted on concordia diagrams within the analytical errors (Figure 4a,b).The representative zircon grains CL images are displayed in Figure 4c.The zircons are quite small (40-100 um), generally simple prismatic, colorless, transparent, and euhedral, with length to width ratios between 1:1 and 2:1.Most of them show obvious oscillatory zoning with different luminescence (Figure 4c), with Th/U ratios ranging from 0.42 to 1.03, almost more than 0.4, indicating a magmatic origin [75,76].Weighted mean 206 Pb/ 238 U dates are used to access their age, and inherited zircons and detrital zircon with variably older 206 Pb/ 238 U ages are not used when calculating crystallization ages.The data with concordance of less than 94% were excluded.Sixteen analyses were conducted on 16 zircons from sample 16LTQ-1, uranium and thorium concentrations are variable, ranging from 51.7 to 342 ppm, and from 29.4 to 319 ppm, respectively.The Th/U ratios of the zircons range from 0.54 to 0.97.The zircons of sample 16LTQ-1 form a tight cluster on concordia and yield a weighted mean 206 Pb/ 238 U age of 780 ± 5.3 Ma (n = 16, MSWD = 1.6, 2σ) (Figure 4a), which is regarded as the crystallization of the sample.Seventeen zircons were analyzed from sample 16LTQ-2, the U and Th concentrations are ranging from 48 to 329 ppm, and from 38.9 to 339 ppm, respectively.The Th/U ratios of most of the zircons range from 0.42 to 1.03, except two zircons that have low U, Th concentrations and Th/U ratios, on which the inclusions can be seen under the CL images.Most zircon U-Pb analyses from 16LTQ-2 yield concordant U-Pb ages with weighted mean 206 Pb/ 238 U age of 777 ± 17 Ma (n = 11, MSWD = 1.1, 2σ) (Figure 4b).This age is Sixteen analyses were conducted on 16 zircons from sample 16LTQ-1, uranium and thorium concentrations are variable, ranging from 51.7 to 342 ppm, and from 29.4 to 319 ppm, respectively.The Th/U ratios of the zircons range from 0.54 to 0.97.The zircons of sample 16LTQ-1 form a tight cluster on concordia and yield a weighted mean 206 Pb/ 238 U age of 780 ± 5.3 Ma (n = 16, MSWD = 1.6, 2σ) (Figure 4a), which is regarded as the crystallization of the sample.Seventeen zircons were analyzed from sample 16LTQ-2, the U and Th concentrations are ranging from 48 to 329 ppm, and from 38.9 to 339 ppm, respectively.The Th/U ratios of most of the zircons range from 0.42 to 1.03, except two zircons that have low U, Th concentrations and Th/U ratios, on which the inclusions can be seen under the CL images.Most zircon U-Pb analyses from 16LTQ-2 yield concordant U-Pb ages with weighted mean 206 Pb/ 238 U age of 777 ± 17 Ma (n = 11, MSWD = 1.1, 2σ) (Figure 4b).This age is interpreted as the crystallization age of the sample 16LTQ-2.Some zircons have distinctive cores (Figure 4c), which may be inherited from previous events, all these inherited cores must also be of magmatic origin given their oscillatory zonings; four concordant analyses of inherited cores yielded 206 Pb/ 238 U ages of 991-1190 Ma (Figure 4).In addition, there are two captured zircons showing a relatively older age of Paleoproterozoic (1689 and 1852 Ma), which are consistent with the ancient basement (Dongchuan Group) of this area.
The results of the trace elements in zircons from the LTQ analyzed by LA-ICPMS are listed in the supplementary data Table S3.Except for one spot analysis (16LTQ-1-5), which has high concentrations of P and Ti (Table S3), there may be ablate apatite inclusion.The chondrite-normalized REE diagrams of the two samples both show enrichments in HREE, depletions in LREE, negative Eu anomalies and positive Ce anomalies in most zircons (Figure 5a,b), which are different from the zircons of metamorphic origin [77] but consistent with their magmatic origin [78,79].
Minerals 2018, 8, x FOR PEER REVIEW 7 of 24 interpreted as the crystallization age of the sample 16LTQ-2.Some zircons have distinctive cores (Figure 4c), which may be inherited from previous events, all these inherited cores must also be of magmatic origin given their oscillatory zonings; four concordant analyses of inherited cores yielded 206 Pb/ 238 U ages of 991-1190 Ma (Figure 4).In addition, there are two captured zircons showing a relatively older age of Paleoproterozoic (1689 and 1852 Ma), which are consistent with the ancient basement (Dongchuan Group) of this area.
The results of the trace elements in zircons from the LTQ analyzed by LA-ICPMS are listed in the supplementary data Table S3.Except for one spot analysis (16LTQ-1-5), which has high concentrations of P and Ti (Table S3), there may be ablate apatite inclusion.The chondrite-normalized REE diagrams of the two samples both show enrichments in HREE, depletions in LREE, negative Eu anomalies and positive Ce anomalies in most zircons (Figure 5a,b), which are different from the zircons of metamorphic origin [77] but consistent with their magmatic origin [78,79].
As shown in the chondrite-normalized REE pattern diagrams (Figure 8a), the LTQ rocks have similar REE distribution curves, and they also have ).Basically, all samples fall in the field between oceanic island basalt (OIB) and island arc basalt (IAB), and show slightly fractionated inner HREE (Figure 8a).These patterns are completely different from the typical OIB, which is intensively differentiated in LREE and HREE, but is similar to the island arc basalt (IAB).On the primitive mantle-normalized incompatible element diagrams (Figure 8b), the LTQ rocks also show broadly similar shapes, which are obviously enriched Chondritic values are from [80].The detailed data of metamorphic zircons come from [77].

Whole Rock Major and Trace Elements
The samples of the LTQ range from 49.83% to 50.71% SiO 2 , 3.64% to 4.49% K 2 O, 5.84% to 6.26% MgO, 16.58% to 17.10% Al 2 O 3 , 10.07% to 10.81% TFe 2 O 3 (abbreviation of total Fe 2 O 3 ), and 1.40% to 2.29% CaO, which expresses low SiO 2 , and high K 2 O, Al 2 O 3 , MgO, TFe 2 O 3 contents (Table S4).Thus, the samples are characterized by low SiO 2 contents and high magnesium number (Mg#, 52.2 to 54.5), which represent the typical basic rocks.In addition, the high concentrations of Na 2 O (5.39% to 5.77%) and LOI (2.21% to 2.96%) are also consistent with the widespread sodic alteration.On the Harker diagrams (Figure 6), Fe 2 O 3 , Al 2 O 3 , and K 2 O contents decrease, whereas SiO 2 , TiO 2 and P 2 O 5 contents increase with decreasing MgO contents, suggesting the crystallization of the pyroxene or amphibole.In the rock classification diagram, the samples belong to tholeiitic basalts (Figure 7).[82].Data for Xide diabase dykes and Wasigou gabbros of western YZB are from [42] and [22], respectively.The shaded areas outline the ranges of compositions for basic-ultrabasic rocks from the Hannan Massif of northwestern YZB with data source from [45].[82].Data for Xide diabase dykes and Wasigou gabbros of western YZB are from [42] and [22], respectively.The shaded areas outline the ranges of compositions for basic-ultrabasic rocks from the Hannan Massif of northwestern YZB with data source from [45].[82].Data for Xide diabase dykes and Wasigou gabbros of western YZB are from [42] and [22], respectively.The shaded areas outline the ranges of compositions for basic-ultrabasic rocks from the Hannan Massif of northwestern YZB with data source from [45].

Zircon Lu-Hf Isotopes
The in situ zircon Lu-Hf isotopic composition analyses come from the two samples of 16LTQ-1 and 16LTQ-2, and the results are given in supplementary data Table S5.Sixteen Lu-Hf spots are performed from sample 16LTQ-1, the results show variable 176 Lu/ 177 Hf ratios of 0.0006 to 0.0024, but present-day 176 Hf/ 177 Hf ratios of 0.282287 to 0.282569 are similar.The calculated initial 176 Hf/ 177 Hf ratios vary from 0.282268 to 0.282552 with a mean of 0.282394, the εHf(t) values (t = 780 Ma), which represent the εHf values of parental magma when the zircons crystallized.With the exception of one point, 16LTQ-1-1 (εHf(t) = −0.6),all zircon εHf(t) values have a positive variable range from 1.6 to 9.4 with a mean of 4.2.Young single-stage model ages (TDM1) range from 972 to 1285 Ma (Figure 9a and Table S5).Nine zircons from sample 16LTQ-2 are analyzed for Lu-Hf isotopes; the results show variable 176 Lu/ 177 Hf ratios of 0.0006 to 0.0022 and present-day 176 Hf/ 177 Hf ratios range from 0.282360 to 0.282477.The calculated initial 176 Hf/ 177 Hf ratios range from 0.282341 to 0.282457, with an average of 0.282380.The εHf(t) values (t = 777 Ma) vary from 1.9 to 6.0 with an average of 3.3.The model TDM1 ages range from 1107 to 1271 Ma (Figure 9a and Table S5).Zircon Hf model ages (TDM1) of the two samples show a defining peak at 1.24 Ga (Figure 9b).As shown in Figure 9, the samples all have the positive εHf(t) values that are below the evolution line of the deplete-mantle, which suggest that the initial magmas might be derived from the melting of the mantle [84].Meanwhile, the ages of TDM1 are only approximately 0.2-0.5 Ga higher than the zircon U-Pb ages of the samples (Table S5), suggesting the juvenile magmas may be partially melted directly from the depleted mantle and have assimilated minor crust [84,85].[42], and Wasigou gabbros [22], western YZB.The data for chondrite, primitive mantle values are from [80].The average compositions of enriched mid-ocean ridge basalt (E-MORB), normal mid-ocean ridge basalt (N-MORB), ocean island basalt (OIB), and island arc basalt (IAB) are from [80] and [83].The shaded areas outline the ranges of compositions for basic-ultrabasic rocks from the Hannan Massif of northwestern YZB with data source from [45].

Zircon Lu-Hf Isotopes
The in situ zircon Lu-Hf isotopic composition analyses come from the two samples of 16LTQ-1 and 16LTQ-2, and the results are given in supplementary data Table S5.Sixteen Lu-Hf spots are performed from sample 16LTQ-1, the results show variable 176 Lu/ 177 Hf ratios of 0.0006 to 0.0024, but present-day 176 Hf/ 177 Hf ratios of 0.282287 to 0.282569 are similar.The calculated initial 176 Hf/ 177 Hf ratios vary from 0.282268 to 0.282552 with a mean of 0.282394, the ε Hf (t) values (t = 780 Ma), which represent the ε Hf values of parental magma when the zircons crystallized.With the exception of one point, 16LTQ-1-1 (ε Hf (t) = −0.6),all zircon ε Hf (t) values have a positive variable range from 1.6 to 9.4 with a mean of 4.2.Young single-stage model ages (T DM1 ) range from 972 to 1285 Ma (Figure 9a and Table S5).Nine zircons from sample 16LTQ-2 are analyzed for Lu-Hf isotopes; the results show variable 176 Lu/ 177 Hf ratios of 0.0006 to 0.0022 and present-day 176 Hf/ 177 Hf ratios range from 0.282360 to 0.282477.The calculated initial 176 Hf/ 177 Hf ratios range from 0.282341 to 0.282457, with an average of 0.282380.The ε Hf (t) values (t = 777 Ma) vary from 1.9 to 6.0 with an average of 3.3.The model T DM1 ages range from 1107 to 1271 Ma (Figure 9a and Table S5).Zircon Hf model ages (T DM1 ) of the two samples show a defining peak at 1.24 Ga (Figure 9b).As shown in Figure 9, the samples all have the positive ε Hf (t) values that are below the evolution line of the deplete-mantle, which suggest that the initial magmas might be derived from the melting of the mantle [84].Meanwhile, the ages of T DM1 are only approximately 0.2-0.5 Ga higher than the zircon U-Pb ages of the samples (Table S5), suggesting the juvenile magmas may be partially melted directly from the depleted mantle and have assimilated minor crust [84,85].

Age of the LTQ and Regional Synchronous Magmatism
There are many Neoproterozoic basic rocks that have been discovered in the YZB (Table S1; [3,4]), but the limited studies of geochemistry and geochronology have been used for the LTQ in the Tong'an area, Huili County, western YZB.The LTQ intruded into the Huili Group, was previously considered to be formed during the Permian like Emeishan basalt (the geological maps in scale of 1:200,000) or Mesoproterozoic Era [87] with the absence of a certain dating.Therefore, we dated two diabase samples from the LTQ to constrain its age.It is generally accepted that the closed system of Pb isotopes in zircon may be destroyed by later strong hydrothermal alteration, resulting in the loss of radiogenic Pb, which eventually leads the calculated age to be lower than the actual age [88].In our studies, most zircons are characterized by obvious oscillatory zonings, high Th/U ratios (>0.4), which are identified as magmatic zircons (Figures 4 and 5; Tables S2 and S3).The two ages from zircon U-Pb dating were fairly consistent with each other within error; they yielded the weighted mean ages of 780 ± 5.3 Ma and 777 ± 17 Ma, respectively (Figure 4), and were interpreted as the best estimate of crystallization age and indicated that the emplacement age of the LTQ is ca.780 Ma.

Age of the LTQ and Regional Synchronous Magmatism
There are many Neoproterozoic basic rocks that have been discovered in the YZB (Table S1; [3,4]), but the limited studies of geochemistry and geochronology have been used for the LTQ in the Tong'an area, Huili County, western YZB.The LTQ intruded into the Huili Group, was previously considered to be formed during the Permian like Emeishan basalt (the geological maps in scale of 1:200,000) or Mesoproterozoic Era [87] with the absence of a certain dating.Therefore, we dated two diabase samples from the LTQ to constrain its age.It is generally accepted that the closed system of Pb isotopes in zircon may be destroyed by later strong hydrothermal alteration, resulting in the loss of radiogenic Pb, which eventually leads the calculated age to be lower than the actual age [88].In our studies, most zircons are characterized by obvious oscillatory zonings, high Th/U ratios (>0.4), which are identified as magmatic zircons (Figures 4 and 5; Tables S2 and S3).The two ages from zircon U-Pb dating were fairly consistent with each other within error; they yielded the weighted mean ages of 780 ± 5.3 Ma and 777 ± 17 Ma, respectively (Figure 4), and were interpreted as the best estimate of crystallization age and indicated that the emplacement age of the LTQ is ca.780 Ma.

Alteration Effects on Chemical Compositions
Major and trace elements for the LTQ rocks are listed in supplementary data Table S4.All samples in this study have undergone variable degrees of metamorphism and hydrothermal alterations, and are consistent with the high loss of ignition (LOI) values (average 2.58%) and petrographic features (albitization of some plagioclases and hornblende altered to chlorite) (Figure 3).Thus, the effects of alteration on the chemical compositions of these rocks must be evaluated.Zirconium in the basic magmatic rocks is generally considered to be most immobile during low-to medium-grade alterations and can be used as an alteration-independent index of geochemical variations [92].Therefore, bivariate plots of Zr against trace elements can be used for evaluating their mobility during alteration [10,87,93].As shown in supplementary Figure S1, the elements, including Y, Nb, Th, La, V, Hf, Rb, Sr, and Ba are plotted against Zr to evaluate their mobility during alteration.Rare earth elements (REE, e.g., La), high field strength elements (HFSE, e.g., Y, Nb, Th and Hf) and siderophile elements (e.g., V) are all slightly correlated with Zr, indicating that they were essentially immobile during alteration.In contrast, large ion lithophile elements (LILE, e.g., Rb, Sr and Ba) do not covariant with Zr, suggesting varying degrees of mobility caused by the alteration.Although the correlation of K 2 O and Na 2 O with MgO contents (Figure 6) suggests the effects of alteration are minor, the sums of major element oxides for all samples are still recalculated to be 100% volatile free.Only the immobile elements (REE, HSFE, and siderophile elements) are used for geochemical classification and petrogenetic discussion.

Fractional Crystallization
It is generally considered that primary magmas of basaltic melts have Ni > 400 ppm and Cr > 1000 ppm [94], Mg# > 73 [95].The relatively low Cr concentrations (140-150 ppm) and Mg# values (52.2-54.5) of the LTQ suggest that the rocks may have undergone significant fractionation of olivine and pyroxene.In the basic rocks, both K 2 O and Al 2 O 3 are mainly enriched in plagioclase and amphibole.Most samples show a slight decrease in CaO, Al 2 O 3 , and (K 2 O + Na 2 O) with decreasing MgO contents (Figure 6c,e), suggesting that plagioclase fractionation crystallization is involved in the magma evolution.The weak negative Sr and Eu anomalies in trace element distribution patterns (Figure 8) also support this view.Meanwhile, the decrease in K 2 O, Al 2 O 3 , and TFe 2 O 3 with decreasing MgO may reflect the fractionation of amphibole, which is consistent with the petrographic features (Figure 3c,d).A negative correlation between MgO and P 2 O 5 (Figure 6f) do not support the fractional crystallization of apatite.Moreover, Fe 2 O 3 and TiO 2 have different correlations with MgO (Figure 6b,d), which do not suggest the fractionation of Fe-Ti oxides.The samples show that while they are slightly fractionated in HREE (Figure 8), they are extremely enriched in zircon (Figure 5).These features precluded the fractional crystallization of garnet or its presence in residue, constraining a depth of less than 40 km.
The Zr/Y ratios in the melts are mainly affected by the major phases of clinopyroxene, amphibole, and garnet [96].As mentioned above, garnet was probably absent in the magma source, so it can be excluded.It is well known that the degree of compatible and incompatible elements is determined by the partition coefficients of the elements between mineral and melt (expressed as mineral/melt D element , abbr.mineral D element ).Thus, if mineral D element < 1, the element is incompatible in the mineral, whereas mineral D element > 1 indicates that the element is compatible in the mineral.Based on previously published data, the partition coefficients of Y and Zr in the amphibole are amphibole D Y = 1 and amphibole D Zr = 0.5 in the basic rocks, respectively [96][97][98], suggesting that Y contents remain constant in the melt if the amphibole dominates the fractionation process.Thus, the slope coefficient of Zr/Y to Zr would approximate to the value of 1/Y when the amphibole fractionation occurs [99].Here, we assume the Y content of 31.7 ppm in sample 16LTQ-2.The sample was characterized by the highest Mg# values and the lowest Zr content, and can therefore represent the Y content of the primary melt.However, the trend in Figure 10 argues against this probability, so the crystallization of the amphibole is also excluded.In contrast, the clinopyroxene dominated fractionation agrees well with this trend for the basic rocks ( clinopyroxene D Zr = 0.1 and clinopyroxene D Y = 0.5, [96]) (Figure 10).Therefore, it can be inferred that the crystal fractionation of clinopyroxene may be controlled by the melt components of the Neoproterozoic basic magmatism in the western YZB.
and the lowest Zr content, and can therefore represent the Y content of the primary melt.However, the trend in Figure 10 argues against this probability, so the crystallization of the amphibole is also excluded.In contrast, the clinopyroxene dominated fractionation agrees well with this trend for the basic rocks ( clinopyroxene DZr = 0.1 and clinopyroxene DY = 0.5, [96]) (Figure 10).Therefore, it can be inferred that the crystal fractionation of clinopyroxene may be controlled by the melt components of the Neoproterozoic basic magmatism in the western YZB.[96] for the Longtanqing, Xide [42], and Wasigou [22] in the western YZB.IAB-island arc basalt; WPB-within plate basalt; M + I-MORB and island arc basalt; M + W-MORB and within plate basalt.

Source Characteristics of the LTQ
The Neoproterozoic magmatic suites in the SCB display two age peaks of 830-800 Ma and 780-740 Ma [100].Zircon Hf isotope data from the magmatic rocks (in particular for granitoids) indicate that the Neoproterozoic magmatism not only involved the remelting of the juvenile late Mesoproterozoic lithosphere (crust and lithospheric mantle), but also included the reconstruction of ancient crustal components within the rifting setting [100,101].A detailed description can be seen in Table S1.Rocks from the LTQ can be compared to other Neoproterozoic magmatic rocks in the YZB, which are characterized by relatively large variations and positive zircon εHf(t) values.Their initial 176 Hf/ 177 Hf ratios are significantly higher than those of the Archaean to Palaeoproterozoic basement [101][102][103][104], which suggests they were not derived from the reconstruction of preexisting old crust.Most zircons shown positive εHf(t) values (1.6-9.4;Table S5), except at one negative point (−0.6) from the LTQ, indicating the source of these basic magma may relate to the mantle.In addition, these values are distinctively below the depleted mantle evolution line in the Hf evolution diagrams (Figure 9a), indicating the mantle magma sources also contain the addition of crustal materials.The involvement of pre-existing crustal materials is also evident by the presence of inherited zircons in the LTQ samples.However, the following lines of evidence showed that crustal contamination is insignificant, if any, in the generation of these basic intrusions.Zr/Hf and Nb/Ta ratios are insensitive and Wasigou [22] in the western YZB.IAB-island arc basalt; WPB-within plate basalt; M + I-MORB and island arc basalt; M + W-MORB and within plate basalt.

Source Characteristics of the LTQ
The Neoproterozoic magmatic suites in the SCB display two age peaks of 830-800 Ma and 780-740 Ma [100].Zircon Hf isotope data from the magmatic rocks (in particular for granitoids) indicate that the Neoproterozoic magmatism not only involved the remelting of the juvenile late Mesoproterozoic lithosphere (crust and lithospheric mantle), but also included the reconstruction of ancient crustal components within the rifting setting [100,101].A detailed description can be seen in Table S1.Rocks from the LTQ can be compared to other Neoproterozoic magmatic rocks in the YZB, which are characterized by relatively large variations and positive zircon ε Hf (t) values.Their initial 176 Hf/ 177 Hf ratios are significantly higher than those of the Archaean to Palaeoproterozoic basement [101][102][103][104], which suggests they were not derived from the reconstruction of preexisting old crust.Most zircons shown positive ε Hf (t) values (1.6-9.4;Table S5), except at one negative point Minerals 2018, 8, 228 13 of 25 (−0.6) from the LTQ, indicating the source of these basic magma may relate to the mantle.In addition, these values are distinctively below the depleted mantle evolution line in the Hf evolution diagrams (Figure 9a), indicating the mantle magma sources also contain the addition of crustal materials.The involvement of pre-existing crustal materials is also evident by the presence of inherited zircons in the LTQ samples.However, the following lines of evidence showed that crustal contamination is insignificant, if any, in the generation of these basic intrusions.Zr/Hf and Nb/Ta ratios are insensitive to fractionation crystallization but sensitive to crustal input due to the contrast in values between mantle-derived melts and crustal materials [105,106].The studied samples have nearly constant Zr/Hf (34.0 to 39.4, with an average with 36.7) and Nb/Ta (14.3 to 18.4, with an average with 15.9) ratios, which is similar to the OIB-like Na/Ta and Zr/Hf ratios (OIB with Nb/Ta = 15.9 ± 0.6 and Zr/Hf = 36.3)and inconsistent with the crustal contamination.Furthermore, the lack of country rock xenoliths in the intrusions does not support significant crustal contamination.
Zircon Hf isotopes from the LTQ display ε Hf (t) values from 1.6 to 9.4, corresponding to Hf depleted mantle model ages (T DM1 ) of 1.3-1.0Ga (Figure 9), which suggest that the initial magmas of the LTQ might be generated by a partial melting of the late Mesoproterozoic juvenile lithosphere.The presence of inherited zircons (991-1190 Ma) also support this interpretation (Figure 4).The other Neoproterozoic basic rocks in the western YZB exhibit similar Hf isotopic compositions (Figure 9a), such as the Kangdian bimodal plutons emplaced at 750-760 Ma, and exhibit zircon ε Hf (t) values as 3.5-9.9,with the Hf modal ages of 0.9-1.2Ga.[11].In addition, the basic plutons at 800-820 Ma in the western YZB, such as Tongde, Gaojiachun, and Lengshuiqing, are mainly composed of gabbros and the ε Hf (t) values are also positive from 5.3 to 7.0, with the T DM1 of 1.1-1.2Ga [31,35].However, the Guandaoshan dioritic pluton, which is the only published one that can be considered to come from the depleted mantle, represents high zircon ε Hf (t) values (11.3-17.7)and consistent U-Pb ages and T DM1 (Figure 9a; [86]).Thus, the Neoproterozoic magmatism in the western YZB extensively involved the remelting of the late Mesoproterozoic juvenile lithosphere and the limited accretion of juvenile crust [100].Furthermore, the low δ 18 O values are associated with the 830-740 Ma zircons in the region [11], suggesting the production of these magmas may be associated with high-T water-rock reaction in the rift setting.
Traditionally, zircon trace element data can be an efficient tracer to probe the composition and temperature of the melt [78,107,108].The REE patterns of the zircons from the samples show the steep MREE to HREE, with (Lu/Gd) N ratios of 7.6-42.4,which are regarded as the typical features of magmatic origin zircons forming in the source without garnet (Figure 5; [78,109]).The zircons also display obviously positive Ce anomalies (Ce/Ce N * 1, Figure 5 and Table S3), indicating that they were crystallized from the melt with a high oxidation fugacity [110].This is particularly conductive to the precipitation of the Fe, Cu and other ore-forming elements, consistent with the widespread Fe-Cu deposits in this region.In addition, the zircons exhibit relatively variable and low negative Eu anomalies (Eu/Eu N * = 0.08-0.71, Figure 5), which suggest a late crystallizing phase that formed after plagioclase crystallization [107].Ti contents in these zircons range from 1.99 to 40.1 ppm, yielding the zircon crystallization temperatures of 616-880 • C (Table S3), which are close to the zircon saturation temperatures [111].It is well known that it is hard for zirconium contents to reach the saturation level in basic magmas [111], and this may be caused by fluid/melt metasomatism from the subducted slab or crustal contamination during upwelling.
The geochemical features of LTQ samples have low SiO 2 (49.83-50.71wt %) contents, which indicate the mantle affinity.Furthermore, their relatively high MgO (5.91-6.53wt %) and Cr (140-150 ppm) contents also support their mantle source.In addition, in the Nb/Ta-Th/Yb and Nb/Ta-Th diagrams, the LTQ, Wasigou gabbros, and Xide diabase exhibit relative low but varied Th and Th/Yb ratios, as well as a negative correlation between Nb/Th and Th, which is similar to the basic-ultrabasic rocks from Hannan Massif, Northwestern YZB (Figure 11).These suggest the mantle sources of these basic rocks may have been reconstructed by the subduction.The continental basalts are generally considered to be generated by the interaction between the asthenosphere and Minerals 2018, 8, 228 14 of 25 lithosphere [112].The Nb/La ratio is quite different in the sub-continental lithospheric mantle (SCLM) and asthenospheric mantle, so it can be used as a distinguishing indicator [42].Traditionally, the asthenospheric mantle-derived melts are generally characterized by high Nb/La ratios, varying from 0.9 (N-MORB) to 1.3 (OIB and E-MORB) [80].On the contrary, the SCLM-derived melts display low Nb/La ratios, and are equivalent to that of continental crust [112].The LTQ have relatively constant Nb/La ratios from 0.60 to 0.86 with an average of 0.71.These ratios are significantly less than asthenosphere but close to or slightly higher than SCLM-derived melts.However, the significant Nb-Ta-Ti depletion in the trace element spider diagrams of the samples (Figure 8) indicates that the SCLM-derived melts have been reconstructed by the subduction or assimilated by crustal materials.Thus, the arc signatures of LTQ and other basic-ultrabasic rocks in the YZB could be inherited from juvenile lithosphere mantle/crust components which formed during Greenville Orogen in SCB [39].The asthenospheric mantle upwelling under the effect of mantle plume is considered to have supplied the heat and material to induce SCLM melting during Neoproterozoic.The SCLM source has been reconstructed by the subduction, then overprinted in the arc signature.Afterward, the melt components are controlled by the fractionation of clinopyroxene and plagioclase with minor amphibole under high oxidation fugacity.The absence of garnet in the residue phase or in the fractionation process indicates that the depth of magmatism production was less than 40 km.[42] and Wasigou [22], western YZB, SW China.Values of N-MORB, OIB and Primitive mantle are from [80].Values of the upper and lower crust are from [113].The shaded areas outline the ranges of compositions for basic-ultrabasic rocks from the Hannan Massif of northwestern YZB with data source from [45].

Tectonic Implications
The LTQ, Xide, and Wasigou basic rocks of western YZB and Hannan basic-ultrabasic rocks of northwestern YZB are characterized by negative Nb and Ta anomalies on their trace element spidergrams (Figure 8), which is considered to be the main feature of the typical arc basalts.Zhao and Zhou [33] obtained this similar arc-like geochemical features from Panzhihua gabbros, and they interpreted that it came from an arc environment.However, it is generally accepted that the Nb and Ta depletions also occur in many non-arc environments, like rift, these features may be derived from subduction-modified SCLM, contaminated by crustal materials, or inherited from the arc-derived crust [6,100,[114][115][116][117].Therefore, the characters of depletions in Nb and Ta cannot be used as the only criterion to distinguish between arc basalts and intraplate rift basalts; many other aspects of the evidence must be considered.
For the basic rocks of the YZB (e.g., the LTQ), there is geochemical evidence against the arc origin: (1) all the samples that are plotted in the field between the OIB and IAB (Figure 8) distinctly show that the contents of most of the trace elements are relatively higher than those of IAB; (2) like LTQ, the contents of Cr (140 to 150 ppm) and TiO2 (1.93 to 2.34 wt %) are also clearly higher than those of typical IAB (Cr = 50 ppm; TiO2 = 0.84 wt %) [94,118]; (3) the Ti/V ratios can be an efficient tracer to probe into the tectonic setting of basalts, because these ratios are affected by their source characters, oxygen fugacity, the degrees of crystallization, and partial melting of their magmas [118].[42] and Wasigou [22], western YZB, SW China.Values of N-MORB, OIB and Primitive mantle are from [80].Values of the upper and lower crust are from [113].The shaded areas outline the ranges of compositions for basic-ultrabasic rocks from the Hannan Massif of northwestern YZB with data source from [45].

Tectonic Implications
The LTQ, Xide, and Wasigou basic rocks of western YZB and Hannan basic-ultrabasic rocks of northwestern YZB are characterized by negative Nb and Ta anomalies on their trace element spidergrams (Figure 8), which is considered to be the main feature of the typical arc basalts.Zhao and Zhou [33] obtained this similar arc-like geochemical features from Panzhihua gabbros, and they interpreted that it came from an arc environment.However, it is generally accepted that the Nb and Ta depletions also occur in many non-arc environments, like rift, these features may be derived from subduction-modified SCLM, contaminated by crustal materials, or inherited from the arc-derived crust [6,100,[114][115][116][117].Therefore, the characters of depletions in Nb and Ta cannot be used as the only criterion to distinguish between arc basalts and intraplate rift basalts; many other aspects of the evidence must be considered.
For the basic rocks of the YZB (e.g., the LTQ), there is geochemical evidence against the arc origin: (1) all the samples that are plotted in the field between the OIB and IAB (Figure 8) distinctly show that the contents of most of the trace elements are relatively higher than those of IAB; (2) like LTQ, the contents of Cr (140 to 150 ppm) and TiO 2 (1.93 to 2.34 wt %) are also clearly higher than those of typical IAB (Cr = 50 ppm; TiO 2 = 0.84 wt %) [94,118]; (3) the Ti/V ratios can be an efficient tracer to probe into the tectonic setting of basalts, because these ratios are affected by their source characters, oxygen fugacity, the degrees of crystallization, and partial melting of their magmas [118].The LTQ samples display the high Ti/V ratios that are between 37.3 and 47.5 (mostly > 20), which are significantly higher than that of typical IABs (<20).On the plot of the Ti-V diagram, all samples are plotted into the field of continental flood basalt, similar to the other basic rocks of the YZB (Figure 12); (4) the diagram of Zr/Y vs. Zr can also be used to discriminate the tectonic setting of within plate basalt (WPB), MORB, and IAB [96].In this research, the Zr/Y ratios (3.37-3.75) of the LTQ are comparable to other basic rocks, and in the Zr-Zr/Y diagram, all samples are plotted in the field of WPB rather than the IAB (Figure 10), and the same results are also shown in the Zr-Ti and Ti-Zr-Y diagrams (Figure 13a,b).In addition, this view is further supported by the discriminant diagram of Wang [119]; most basic rocks from the YZB fall in the field of continental WPB and IAB (Figure 13c), which represent the obvious dual characteristics of these basic rocks.However, their geochemical characteristics share many affinities to extension setting, except for the depletion of Nb and Ta.Thus, the basic rocks of YZB should be interpreted as generational from the SCLM-derived melts in a rift environment.Furthermore, the nearly N-S trend of the LTQ, Xide, and Wasigou basic rocks and the roughly E-W trending Hannan basic-ultrabasic rocks are sub-parallel to the Kangdian and Bikou-Hannan rift, respectively (Figure 1), which is also consistent with this interpretation.It is well known that the Rodinia supercontinent was assembled between 1300 and 900 Ma through the Grenville and other global synchronous orogenic events [4].As a part fragment of Rodinia, the YZB is considered to be located between Australia and North America [4,39], or on the periphery of the supercontinent during the assembly of Rodina [32].In any case, the YZB was in an active continent margin setting at the late Mesoproterozoic to early Neoproterozoic, and the widespread Sibao Orogeny between Yangtze and Cathaysia is commonly regarded as one of the global Grenville-aged orogeny (Figure 14a; [123,124]).The old inherited zircons of 16LTQ-2 have 206 Pb/ 238 U age of 991-1190 Ma, and are contemporaneous with the peaks of the Sibao Orogeny [51, 123,124].We thus suggest the apparent arc-like geochemical signatures of the magmatic rocks were derived from the convergent tectonic setting during the Sibao Orogeny.The wildly distributed late Mesoproterozoic zircon model ages (1.0-1.3Ga; Tables S1 and S4) of the basic rocks also indicate the presence of juvenile lithosphere growth at that time in the YZB [11,100].However, there are widespread 830-750 Ma bimodal magmatic rocks including the LTQ, suggesting a possible continental rift environment at that time [125].Based on the geochemical and Nd isotopic data, the Wasigou (~779 Ma) and Xide (800-810 Ma) basic rocks in the Kangdian region were most likely formed in a continental rift environment [22,42].The discovery of ca.800 Ma high-MgO Tongde picrite is also confirmed by the presence of a hot mantle plume beneath the SCB [21].The recently identified A-type granites of ~780 Ma Mianning granites and ~801 Ma Xiatianba granites have been demonstrated to be produced within an intraplate extension environment [126].The widespread adakitic rocks from the Mopanshan (780 Ma), Xuelongbao (750 Ma), and Datian (760 Ma) are also considered to be derived from a juvenile, thickened lower crust in an intracontinental extension setting [127].Recent studies confirm that the sedimentary history of the Kangdian Rift can be well correlated with the Nanhua Rift [28].A SHRIMP zircon U-Pb age of tuffs from the lowermost part of the Luliang formation is 819 ± 9 Ma, which represents the initiation of the Kangdian Rift [90].More intriguingly, the latest proposed tectonic model and filling pattern of the Kangdian Rift [90,128] are comparable to those of the East Africa Rift, a typical continental rift [129].This evidence suggests that the YZB was a continental rift environment during the Neoproterozoic and the extensive magmatic rocks are triggered by these events (Figure 14b).
Wasigou (~779 Ma) and Xide (800-810 Ma) basic rocks in the Kangdian region were most likely formed in a continental rift environment [22,42].The discovery of ca.800 Ma high-MgO Tongde picrite is also confirmed by the presence of a hot mantle plume beneath the SCB [21].The recently identified A-type granites of ~780 Ma Mianning granites and ~801 Ma Xiatianba granites have been demonstrated to be produced within an intraplate extension environment [126].The widespread adakitic rocks from the Mopanshan (780 Ma), Xuelongbao (750 Ma), and Datian (760 Ma) are also considered to be derived from a juvenile, thickened lower crust in an intracontinental extension setting [127].Recent studies confirm that the sedimentary history of the Kangdian Rift can be well correlated with the Nanhua Rift [28].A SHRIMP zircon U-Pb age of tuffs from the lowermost part of the Luliang formation is 819 ± 9 Ma, which represents the initiation of the Kangdian Rift [90].More intriguingly, the latest proposed tectonic model and filling pattern of the Kangdian Rift [90,128] are comparable to those of the East Africa Rift, a typical continental rift [129].This evidence suggests that the YZB was a continental rift environment during the Neoproterozoic and the extensive magmatic rocks are triggered by these events (Figure 14b).[12]).Detailed description in the main text.Figure 14.A sketch cartoon showing the tectonic evolution of the western YZB from ca. 1300 Ma to 750 Ma (modified after [12]).Detailed description in the main text.
There is a wide distribution of Neoproterozoic basic rocks in the western YZB (Table S1), which underwent the reconstruction of the Mesoproterozoic subducted melt/fluid and displayed dual geochemical characters, and they are considered to be formed in the continental rifting environment, instead of the arc-related basalts.Combined with the synchronous felsic magmatism and typical rift deposition in this region, this suggests that the Neoproterozoic continental rifting once occurred in the YZB.In addition, the widely distributed Neoproterozoic anorogenic magmatism also occurred in other Rodinia blocks, such as Australia [10,116,130,131], Laurentia [2,14,132], India [133,134], South Africa [5,135], and Tarim [13,136].All these observations indicate that the Neoproterozoic anorogenic magmatism (including LTQ basic rocks) and continental rifting in the YZB belong to a series of global rifting magmatic events related to the breakup of the Rodinia supercontinent.

Conclusions
Based on geochronological, geochemical, and Hf isotopic studies of the LTQ samples, we draw the following conclusions: (1) LA-ICPMS zircon U-Pb dating yielded the ~780 Ma emplacement age of the Longtanqing intrusions, which are coeval with the widespread Neoproterozoic magmatic magmatism (830-750 Ma) in the western Yangtze Block.
(2) The Longtanqing samples belong to the tholeiitic series.They are generated by partial melting of the SCLM and may have been reconstructed by the Mesoproterozoic subduction.An absence of garnet in the residue phase constrain a depth of less than 40 km for the Neoproterozoic magmatism in the western Yangtze Block, and the melt compositions are controlled by the crystal fractionation of the dominant clinopyroxene and plagioclase with minor amphibole under high f O 2 conditions.They are most likely formed in a continental rift setting, rather than an arc-related setting.
(3) Zircon Hf single-stage model ages (972-1285 Ma) and the occurrences of inherited zircons with ages of 991-1190 Ma provide firm evidence for Mesoproterozoic juvenile crust involved in the shaping of the Longtanqing diabases trace elemental arc signature.
(4) The Yangtze Block once experienced the Neoproterozoic continental rifting, and extensively developed rift-related magmatism, generating the ~780 Ma Longtanqing intrusion, which is likely recorded in the response to the mantle activity during the breakup of Rodinia.

Supplementary Materials:
The following are available online at http://www.mdpi.com/2075-163X/8/6/228/s1, Figure S1: Diagrams of Y, Nb, Th, La, V, Hf, Rb, Sr, and Ba vs. Zr to evaluate the mobility of these elements during alteration, Table S1: Summary of published Neoproterozoic zircon U-Pb ages and corresponding Lu-Hf isotopes for basic rocks in YZB, Table S2: LA-ICPMS U-Pb isotopic compositions for zircons from the LTQ, Table S3: Trace elements (ppm) in zircons from the LTQ, Table S4: Major and trace elements data of the LTQ, Table S5: Lu-Hf isotopic data for zircons from the LTQ.
Author Contributions: S.S., X.Y., and L.L. conceived and designed the experiments; W.L. and J.C. took part to the field campaigns; E.G. took part in the discussion; S.S. and L.L. analyzed the data; S.S., X.Y., and L.L. wrote the paper.

Figure 1 .
Figure 1.Schematic map of Precambrian South China Block (SCB) emphasizing the three Neoproterozoic rift basins and distribution of Neoproterozoic basic rocks (after [3,28,41,42]).The inset is a tectonic sketch of China showing the three Precambrian blocks (after [43]).Detailed data of the basic rocks in the Yangtze Block (YZB) can see in TableS1.

Figure 1 .
Figure 1.Schematic map of Precambrian South China Block (SCB) emphasizing the three Neoproterozoic rift basins and distribution of Neoproterozoic basic rocks (after [3,28,41,42]).The inset is a tectonic sketch of China showing the three Precambrian blocks (after [43]).Detailed data of the basic rocks in the Yangtze Block (YZB) can see in TableS1.

Figure 2 .
Figure 2. (a) Simplified geological map of Mesoproterozoic to Neoproterozoic rocks in the Tong'an region; (b) Geological map of the LTQ and sample locations.

Figure 2 . 24 Figure 2 .
Figure 2. (a) Simplified geological map of Mesoproterozoic to Neoproterozoic rocks in the Tong'an region; (b) Geological map of the LTQ and sample locations.

Minerals 2018, 8 ,
x FOR PEER REVIEW 14 of 24 fugacity.The absence of garnet in the residue phase or in the fractionation process indicates that the depth of magmatism production was less than 40 km.

Figure 11 .
Figure 11.Plots of Nb/Ta vs. Th/Yb (a) and Nb/Th vs. Th (b) for the magmatic rocks in the Longtanqing, Xide[42] and Wasigou[22], western YZB, SW China.Values of N-MORB, OIB and Primitive mantle are from[80].Values of the upper and lower crust are from[113].The shaded areas outline the ranges of compositions for basic-ultrabasic rocks from the Hannan Massif of northwestern YZB with data source from[45].

Figure 11 .
Figure 11.Plots of Nb/Ta vs. Th/Yb (a) and Nb/Th vs. Th (b) for the magmatic rocks in the Longtanqing, Xide[42] and Wasigou[22], western YZB, SW China.Values of N-MORB, OIB and Primitive mantle are from[80].Values of the upper and lower crust are from[113].The shaded areas outline the ranges of compositions for basic-ultrabasic rocks from the Hannan Massif of northwestern YZB with data source from[45].
Minerals 2018, 8, x FOR PEER REVIEW 15 of 24 roughly E-W trending Hannan basic-ultrabasic rocks are sub-parallel to the Kangdian and Bikou-Hannan rift, respectively (Figure1), which is also consistent with this interpretation.

Figure 12 .
Figure 12.V-Ti discrimination diagram of[120] for the basic rocks from Longtanqing, Xide, and Wasigou, western YZB.The shaded areas outline the ranges of compositions for basic-ultrabasic rocks from the Hannan Massif of the northwestern YZB with data source from[45].

Figure 12 .
Figure 12.V-Ti discrimination diagram of[120] for the basic rocks from Longtanqing, Xide, and Wasigou, western YZB.The shaded areas outline the ranges of compositions for basic-ultrabasic rocks from the Hannan Massif of the northwestern YZB with data source from[45].

Figure 12 .
Figure 12.V-Ti discrimination diagram of[120] for the basic rocks from Longtanqing, Xide, and Wasigou, western YZB.The shaded areas outline the ranges of compositions for basic-ultrabasic rocks from the Hannan Massif of the northwestern YZB with data source from[45].

Figure 13 .
Figure 13.Tectonic discrimination diagrams for the magmatic rocks in the western Yangtze block.(a) The Zr-Ti diagram is after [121]; (b) the Ti-Zr-Y diagram is after [122]; (c) the Ta/Hf-Th/Hf diagram is after [119].WPB-within plate basalt; VAB-volcanic arc basalt; IAT-island arc tholeiite; CABcalc-alkaline basalt; M + I-MORB and island arc tholeiite.The shaded areas outline the ranges of compositions for basic-ultrabasic rocks from the Hannan Massif of northwestern YZB with data source from [45].

Figure 13 .
Figure 13.Tectonic discrimination diagrams for the magmatic rocks in the western Yangtze block.(a) The Zr-Ti diagram is after [121]; (b) the Ti-Zr-Y diagram is after [122]; (c) the Ta/Hf-Th/Hf diagram is after [119].WPB-within plate basalt; VAB-volcanic arc basalt; IAT-island arc tholeiite; CAB-calc-alkaline basalt; M + I-MORB and island arc tholeiite.The shaded areas outline the ranges of compositions for basic-ultrabasic rocks from the Hannan Massif of northwestern YZB with data source from [45].

Figure 14 .
Figure 14.A sketch cartoon showing the tectonic evolution of the western YZB from ca. 1300 Ma to 750 Ma (modified after[12]).Detailed description in the main text.Figure14.A sketch cartoon showing the tectonic evolution of the western YZB from ca. 1300 Ma to 750 Ma (modified after[12]).Detailed description in the main text.