Progressive crushing 40Ar/39Ar dating of gold-bearing quartz vein from the Liaotun Carlin-type gold deposit at the northwest of Guangxi

doi:10.21203/rs.3.rs-1418453/v1

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Progressive crushing 40Ar/39Ar dating of gold-bearing quartz vein from the Liaotun Carlin-type gold deposit at the northwest of Guangxi

https://doi.org/10.21203/rs.3.rs-1418453/v1

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Progressive crushing ⁴⁰Ar/³⁹Ar dating has been performed on a gold-bearing quartz vein from the Liaotun Carlin-type gold deposit at the northwest of Guangxi for the first time. Gases liberated from the secondary and primary fluid inclusions yielded two age plateau with ages of 168.4 ± 1.9 Ma and 200.5 ± 1.9 Ma, respectively. The data points constituting the age plateau yielded excellent inverse isochrons with isochron ages of 167.0 ± 1.9 Ma and 200.7 ± 2.1 Ma. The initial ⁴⁰Ar/³⁶Ar ratios corresponding to the two isochrons are 308.9 ± 6.8 and 298.0 ± 4.3, which are statistically indistinguishable from the air, indicating that the ore-forming fluids probably mainly derived from the basin pressure flow dominated by atmospheric precipitation. The age from the PFIs of 200.5 ± 1.9 Ma can be taken as the timing of Au mineralization. In contrast, the age of 167.0 ± 1.9 Ma recorded by SFIs represents the timing of late hydrothermal fluid superposition and transformation after the formation of gold deposit. Our preliminary study shows the feasibility and great potential of ⁴⁰Ar/³⁹Ar dating by progressive crushing of fluid inclusions from quartz vein to date the mineralization age and decipher the fluid origins of Carlin-type gold deposits.

The Yunnan(Dian)-Guizhou(Qian)-Guangxi(Gui)-area of southwestern China is well known as the “Golden Triangle” since this region contains the second-largest concentration of Carlin-type gold deposits in the world (Fig. 1a, b), with a total resource of > 800 tons of contained Au at Au an average grade of 4.5 g/t^1–10. Precise geochronological data of mineralization within micro-fine disseminated rocks, such as the Carlin-type/like gold deposits are not always available, since they are generally lack datable minerals for conventional isotopic dating techniques^5,11−14. However, with the progress of mineral separation and isotopically analytical technologies, as well as the development and utilization of new techniques, great progress has been made in constraint the metallogenic ages of Carlin-type gold deposits during the past decades^4,14,15. For example, the metallogenic ages of Carlin-type gold deposits in Nevada, USA, have been well constraint on 42 − 36 Ma by applied Rb-Sr and ⁴⁰Ar/³⁹Ar dating methods of galkhaite and adularia, respectively^11,16,17.

There is no galkhaite and adularia in Carlin-type gold deposits from the Dian-Qian-Gui area “Golden Triangle” have been reported, thus, the published isotopic dating results from this region (Fig. 1b) mainly derived from hydrothermal altered minerals and fluid inclusions Rb-Sr dating^19–21,28, arsenopyrite, pyrite and pyrobitumen Re-Os dating^6,8,22, hydrothermal rutile/monazite/calcite/apatite U-(Th)-Pb method^4,9,15,23, zircon U-Th-He method²⁹, sericite and illite ⁴⁰Ar/³⁹Ar dating²⁷, and hydrothermal calcite Sm-Nd method^24–26. In summary, the reported geochronological data suggested that the Dian-Qian-Gui “Golden Triangle” region underwent two independent gold mineralization events during the late Triassic to early Jurassic (230 ~ 195 Ma) and the late Jurassic to early Cretaceous (150 ~ 122 Ma).

As one of the typical Carlin-type gold deposit in Bama County, northwest Guangxi (Fig. 1c), precise mineralization age of the Liaotun gold deposit is still poorly constrained mainly because no suitable minerals can be selected for traditional isotopic dating methods. Gold deposit in the district is hosted by middle Permian Baifeng Formation (T₂bf) that consists of mudstone, sandstone and siltstone, and the orebodies are mainly controlled by NW-trending or EW-trending faults (Fig. 1c). A felsic dike intruded Carboniferous limestone and Triassic sandstone along an ENE- to NE-trending fault and cut off the biggest orebody (No. I). The ⁴⁰Ar/³⁹Ar dating of muscovite phenocryst from this dike yielded a plateau age of 95.5 ± 0.7 Ma, which is interpreted as the upper limit of the metallogenic epoch¹⁸. Later, SIMS zircon U-Pb dating result shows that the Liaotun dike was emplaced at 97.2 ± 1.1 Ma (MSWD = 2.9), and the authors inferred that there is no genetic link between the felsic dike and Liaotun carlin-type gold deposit³⁰. Therefore, in order to unravel the precise mineralization age of this gold deposit, there still needs more accurate direct metallogenic data.

The ⁴⁰Ar/³⁹Ar in vacuo progressive crushing technique for dating the ages of fluid inclusions has been improved and developed for thirty-five years³¹. This method has been widely applied to constrain the formation ages of hydrocarbon accumulation^32,33, high-ultrahigh pressure retrograde metamorphism^34,35, and especial on direct dating of hydrothermal deposit minerals (Cassiterite, sphalerite, wolframite) and gangue minerals like mineralization quartz vein^36–43. Nevertheless, there is still no successful report by this technique on sediment-hosted Carlin-type gold deposits yet, although mineralization quartz veins with abundant fluid inclusions are widely developing in this type of ore deposit.

In this contribution, we chose the Liaotun Carlin-type gold deposit, northwest Guangxi, as the research object, applying the ⁴⁰Ar/³⁹Ar in vacuo progressive crushing dating technique on the main mineralization stage pyritized gold-bearing quartz vein for the first time (Fig. 2c). Based on a combined approach of fluid inclusions petrographic observation and micro-thermometric measurement, our study is try to decipher the origin of fluid flow and constrain the age of quartz vein formation by using a direct approach. Furthermore, we believe our attempt not only can evaluate the feasibility of ⁴⁰Ar/³⁹Ar dating by in vacuo progressive crushing of fluid inclusions, but also could exploit a new approach to constraint the mineralization age of the lack datable minerals Carlin-type/like gold deposits.

Geological setting

The Dian-Qian-Gui ore concentration area is restricted to the Devonian-Triassic Youjiang basin, which is bound to the northeast by the Ziyun-Du’an fault, to the northwest by the Mile-Shizong fault, and to the southeast by the Pingxiang fault (Fig. 1b), which separates the basin from the Cathaysia block¹. It widely developed Au-As-Sb-Hg low-temperature hydrothermal deposits and contains one of the largest concentrations of Carlin-type gold deposits in the world^1–3,8,10.

Evolution of the Youjiang Basin can be divided into six stages from Early Devonian to Cretaceous⁴⁴, while gold deposits in this region mainly formed in the tectonic transformation period from Indosinian compression Orogeny to Yanshanian extensional tectonic environment, that is, the extension stage after the collision of Youjiang fold belt formed by the evolution of foreland basin in Youjiang Basin^1,2,4,6,44. All gold deposits over the Golden Triangle are mainly hosted in the Permian limestone and volcaniclastic sedimentary rocks or Triassic siliciclastic rocks and carbonates and are structurally controlled by various folds and associated faults, likely produced during the Indosinian orogenic deformation^1,45.

Geology of the Liaotun Deposits

The fault type Liaotun gold deposit, in Bama County, Northwest Guangxi, is a medium-sized Carlin-type gold deposit, which located on southwest margin of the isolated Longtian carbonate platform (Fig. 1b)^18,30,46. The exposed sedimentary rocks in the platform are mainly limestone intercalated with dolomite of Carboniferous Du’an Formation (C_1 − 2d) and Permian sponge reef limestone (Pbls). The strata around the platform is the Triassic Baifeng Formation (T₂bf), which consists of interbedded deep-water basin facies sandstone and mudstone (Fig. 2a)^18,30.

The study area contains well-developed faults and linear folds and individual gold orebodies are structurally controlled by high-angle faults. There are five NW-trending and four EW-trending faults have been recognized in the mine area (Fig. 1c). Among them, the NW-trending faults F1 and F2 are syn-sedimentary faults, while the NW-trending F4 and the EW-trending F5, F6, F9 faults are ore-controlling/bearing structures, hosting the I, III, IV, and V orebodies, respectively (Fig. 1c)^18,46. A later Yanshanian (97 − 95 Ma) quartz porphyry veins intruded Carboniferous limestone and Triassic sandstone along an ENE- to NE-trending fault across the Longtian dome^18,30.

The deposit consists of five orebodies and the largest orebody (No. I) is cut off by the later Yanshanian quartz porphyry vein from the middle and respectively named as I-1 and I-2 (Fig. 1c). Gold mineralization occurred in shallow part is oxidized ore, dominant by silicification and limonitization detrital quartz greywacke and cataclasite. Primary to semi-primary ore minerals in deeper part are disseminated pyrite and minor Arsenopyrite. Hydrothermal alterations associated with gold mineralization in the deposit have identified silicification, pyritization, arsenopyrite, (de)carbonatination, clayization and sulfidation. In additionally, the occurrence, textures, and mineral assemblages of the ores at Liaotun indicate that the main-mineralization stages can be further divided into: (1) decarbonination + silicification stage; (2) quartz + pyrite + arsenopyrite stage; (3) quartz + stibnite stage; (4) quartz + calcite + clayization stage^18,46.

The NW-trending F4-controlling largest I orebody is 656 m long and average 9 m thick, with steep dip angles of 50° to 85° and an average grade of 1.62 g/t Au. The smaller III and V orebodies are controlled by EW-trending vertical F5 and F6, which are 230 to 194 m long and 7.20 to 1.16 m thick with average gold grades varying from7.33 to 0.34 g/t Au^18,46. The V orebody is hosted in siltstone, mudstone and thick bedded sandstone at the second member of middle Triassic Baifeng Formation. In this orebody, the dominant ore are taupe and purplish red silicified fine-sandstone, cataclasite, crushed rock, minor silicified siltstone and bedded mud, and veinlet quartz usually can be observed locally (Fig. 1c). The ore structures are disseminated, spotted, micro-veined-network, brecciated, porous and earthy¹⁸. The sample LT19-1-2 used in this study for fluid inclusion in vacuo crushing ⁴⁰Ar/³⁹Ar dating was collected from the goaf of V orebody (Fig. 2b, c). It is a 0.5-2 cm wide pyritized gold-bearing quartz vein with grade of 4.02 g/t Au⁴⁶.

Fluid inclusion analyses

Petrographic observation and micro-thermometric measurements have been applied to the gold-bearing vein quartz samples from the Liaotun Carlin-type gold deposit. The total salinities (W) are calculated with the reduction formula based on the final ice-melting temperatures (|T_m|)⁴⁷: W = 1.78|T_m| – 0.0442|T_m|² + 0.000557|T_m|³. Two or three single fluid inclusions in each cluster were selected for measurement.

Abundant fluid inclusions developed in the quartz and can be separated into primary (PFIs) and secondary (SFIs) inclusions based on the textural criteria. Most of the PFIs are generally less than > 5 µm in diameter and characterized by two-phase (liquid-vapor) with an extremely small CO₂ bubble at room temperature (Fig. 3a). They normally have negative crystal, round, elongate, or irregular shapes, and observed as isolated, random or clustered distributions (Fig. 3b, c), suggesting a primary origin. Heating-freezing stage analysis shows that the type-b inclusions have T_m between − 6.5 and − 9.5°C, corresponding to salinities of 9.9–13.4 wt.% NaCl equivalent. The homogenization temperature is between 245 and 180°C. The tiny linear distributions SFIs (~ 1–3 µm in size) are mainly occurring along cross-cutting healed fractures and have round, oval, tubular or irregular shapes (Fig. 3a, d, e), but some irregular SFIs can reach 5–10µm. These inclusions are commonly pure aqueous inclusions, but two-phase (CO₂ + H₂O) inclusions have been observed occasionally. The measured results gave T_m values between − 2.1 and − 7.5°C, corresponding to salinities of 3.5–11.1 wt.% NaCl equivalent. Values for T_h were measured between 200 and 160°C.

⁴⁰ Ar/ ³⁹ Ar Dating Result

During in vacuo crushing experiment, quartz separates LT19-1-2Qz underwent 33 stages and around 16990 number of stokes. The age spectra for this sample, shown in Fig. 4, yield a monotonically decreasing staircase-shaped age spectrum with apparent ages from 268 to 191 Ma in the first four stages. Subsequently, upon continued crushing, the apparent ages from steps 5 to 11 gradually stabilize to reveal age plateaux, with plateau age of 168.4 ± 1.9 Ma (Fig. 4a, ³⁹Ar = 42%, MSWD = 5.5) and K/Ca ratios of 11.6 ± 3.7(Fig. 4b). The data points of these steps defining the plateau age yields isochron with age of 167.0 ± 1.9 Ma (MSWD = 2.3), corresponding to an initial ⁴⁰Ar/³⁶Ar ratio of 308.9 ± 6.8 (Fig. 4c). Apparent ages rise from 175.7 Ma at step 12 to 191.5 Ma at step 15 and then followed by a flat plateau by steps 16 to 33, with plateau age of 200.5 ± 1.9 Ma (Fig. 4a, ³⁹Ar = 24%, MSWD = 0.6) and K/Ca ratios of 4.1 ± 1.0 (Fig. 4b). On the inverse isochron diagram of ³⁶Ar/⁴⁰Ar vs. ³⁹Ar/⁴⁰Ar, these data points define an excellent linear array, and yield an age of 200.7 ± 2. Ma (MSWD = 1.6) with an initial ⁴⁰Ar/³⁶Ar ratio of 298.0 ± 4.3, which are consistent with the plateau age as well as the atmospheric value for the ⁴⁰Ar/³⁶Ar ratio (Fig. 4c).

Age significances of ⁴⁰Ar/³⁹Ar crushing dating. Fluid inclusions in mineral-hosted analysis is one of the most important techniques in modern studies of hydrothermal mineral deposits, as the trapped fossil fluids inclusions could directly provide pivotal information on the geochemistry and geochronology of mineralization systems^48–51. The key point and the most difficulties of fluid inclusions geochronological study is how to effectively distinguish and extract the gases from the SFs and PFs respectively^{31,37–39,41,52,53}. Just as described by Bodnar⁵⁴, “PFIs are formed during, and as a direct result of, growth of the surrounding host crystal. If a crystal fractures after it has been formed, some fluid may enter the fracture and become trapped as SFIs as the fracture heals. Thus, SFIs are trapped after crystal growth is complete”. As a result, the SFIs and PFIs are generally yield different in volume and have distinctive distribution characteristics. Generally, in the process gas-extraction by in vacuo crushing method, SFIs are easily crushed and liberated gases at the initial steps, while the PFs can be extracted in the later crushing steps^31,39,55. Part of the bigger PFIs which occur along the healed micro-cracks are probably also extracted during the earlier steps. Additionally, experiments show that as long as the crushing times are enough, gases from most of the > 1 µm fluid inclusions can be extracted effectively^38,41.

In the case of sample LT19-1-2Q, SFIs are crushed and liberated gases at the initial steps yields inverse isochron age of 167.0 ± 1.9 Ma (Fig. 4c). This age represents an episode of late hydrothermal fluid superposition and transformation after the formation of gold deposit. Published isotopic ages indicating the metallogenic ages of the Carlin-type gold deposits in the north of “Golden Triangle” are mainly concentrated at 150 − 130 Ma^1–4,24, while the magmatic activities in this region are concentrated at 96 − 77 Ma^18,30,56. Thereby, this age whether represents another period of mineralization still need to be further studied. With crushing continues, the SFIs were gradually exhausted whereas PFs dominate the gas contribution and yield an isochron age of 200.5 ± 1.9 Ma (Fig. 4c). Since the pyritized gold-bearing quartz vein in Liaotun is the main-metallogenic stage production and its Au grade as high as ca. 4 g/t, the age of PFs then can be taken as the best estimate for the timing of Au mineralization, which is basically coeval with the metallogenic age of the main Carlin-type gold deposits in the central and southern part of Youjiang ore concentration area of South China^1,2,4. Combined with previous studies, we suggest that the Liaotun gold deposit formed in the tectonic transformation period from Indosinian compression Orogeny to Yanshanian extensional tectonic environment, that is, the extension stage after the collision of Youjiang fold belt formed by the evolution of foreland basin in Youjiang Basin.

Fluids origin and evolution constraints. Reported noble gas (He, Ne, Ar) isotope data of fluid inclusions extracted from arsenian pyrite, quartz, calcite and fluorite from Shuiyindong, Nibao and Yata Carlin-type gold deposits indicate that the main ore-stage fluids are a mixture of ascending magmatic fluid and sedimentary pore fluid, whereas the late ore-stage fluids are a mixture of sedimentary pore fluid or deeply sourced metamorphic fluid and shallow meteoric groundwater^1,3,20,45. On the other hand, In situ SIMS analysis on Au-bearing pyrites from the Jinya, a Carlin-type gold deposit close to Liaotun (Fig. 1c), yields similar δ³⁴S values (ca. − 6.22‰) with the surrounding sedimentary basin (ca. − 7‰), suggesting that the fluids that formed the deposit may meteoric waters transported by regional faults derived from the surrounding sedimentary basin⁵⁷.

The initial ⁴⁰Ar/³⁶Ar ratio of fluid inclusions provides information on fluid origins^40,42. Previous studies have demonstrated the deep magmatic metallogenic hydrothermal fluids, especially mantle derived hydrothermal fluids, generally contain excess ⁴⁰Ar^{39,40,42,43,53}. In terms of in vacuo progressive ⁴⁰Ar/³⁹Ar dating of fluid inclusions from this study, as shown in Fig. 4c, the initial values of ⁴⁰Ar/³⁶Ar of SFIs and PFIs in gold bearing quartz vein are 308.9 ± 6.8 and 298.0 ± 4.3, respectively, which are consistent with the modern atmospheric ⁴⁰Ar/³⁶Ar ratio, indicating that there is basically no excess ⁴⁰Ar in either SFIs or PFIs. Therefore, we prefer to consider the ore-forming fluids of the Liaotun gold deposit is mainly derived from meteoric waters transported by regional ore-controlling faults and/or basinal fluids derived by gravitational pressure.

The Ar-isotopic compositions trapped in fluid inclusions also carries a signature of source of the fluid and the processes which have affected them ^{34,39,40,42,55,58}. As shown in Fig. 5, the SFIs have higher ³⁹Ar_K, ³⁸Ar_Cl and ³⁷Ar_Ca signals, reflecting relatively higher potassium and chlorine contents dissolved in the SFI fluid. This fact may indicate that the SFIs had a strong water-rock reaction with the country rocks resulting in much potassium dissolved. This is consistent with the ore deposit occurs in rich potassium-bearing minerals (mica/sericite and K-feldspar) Triassic siltstone and mudstone. In other words, the SFIs may derive from the regional faults transported meteoric waters and the high potassium in the SFIs is probably correlated with Cl⁻ and/or HCl⁻ dissolved in the fluids. It should be noted that the PFIs have higher signals of ³⁷Ar_Ca than ³⁸Ar_Cl and relatively lower K/Ca ratio (Fig. 4b and Fig. 5). This fact may imply that the ore-forming hydrothermal fluids should have intensive water-rock reaction with calcium-rich rather than potassium-rick rocks, and the potassium in the PFIs is probably correlated with HCO₃⁻ and CO₂⁻ dissolved in the ore-forming fluid³⁹. In other words, the origin of the PFIs more likely gravitational pressure derived basinal fluids, which was once mainly carried and migrated by carbonate or/and dolomite rocks within the sedimentary basin.

Fluid inclusions heating and freezing measurements were performed on doubly polished thick sections of the gold-bearing quartz vein by using a Linkam THMS 600 freezing/heating stage coupled to a BX51 Olympus polarizing microscope, at Guilin University of Technology. The rate of heating and cooling are normally ~ 10°C/min and reduced to 2°C/min near phase changes. The homogenization temperatures (T_h) of aqueous fluid inclusions that homogenize to the liquid phase and the temperatures of ice-melting (T_m) were measured. Homogenization temperatures are the minimum trapping temperatures, whereas ice-melting temperatures provide a measure of the fluid salinity⁴⁷.

The sample was crushed with the jaw crusher and sieved to obtain a size fraction of 500–1000 µm, and then put in HNO₃ to dissolve the carbonate fraction. Finally, all the samples were hand-picked under the binocular microscope. Samples were wrapped in aluminium foil and loaded into aluminium vessels together with standards and irradiated at the China Mianyang Research Reactor. Irradiation times were 40 hrs for irradiation WH01. As flux monitor standards for J-value calculation for this project were using ZBH-2506 with an assumed age of 132.7 ± 0.5 Ma, which was carried out in the Australian National University⁵⁹. The monitor standard was inserted between every two to four samples, for irradiation J-value calculation. In vacuo crushing experiments were carried out in an in-house designed crushing apparatus which was connected to a three stage extraction line and connected with an ARGUS VI® noble gas mass spectrometer in MOE key Laboratory of Tectonics and Petroleum Resources, China University of Geosciences (Wuhan). The gases released were purified by a Zr/Al getter pump operated at room temperature and another Zr/Al pump operated at 400°C for 400 seconds. Mass discrimination (0.99745–0.99749 per atomic mass unit) was monitored by frequent analysis of ⁴⁰Ar/³⁸Ar reference gas pipette aliquots. Correction factors for interfering argon isotopes derived from Ca and K isotopes are: (³⁹Ar/³⁷Ar)_Ca = 0.0006175, (³⁶Ar/³⁷Ar)_Ca = 0.002348, (⁴⁰Ar/³⁹Ar)_K = 0.002323 and (³⁸Ar/³⁹Ar)_K = 0.009419. The ⁴⁰Ar/³⁹Ar data were calculated and plotted using the ArArCALC software package of⁶⁰. Detailed data and relevant parameters for ⁴⁰Ar/³⁹Ar progressive crushing experiments are listed in Supplementary Table S1. Age spectrum and inverse isochron of the sample is illustrated in Fig. 4. Both the plateau and inverse isochron age uncertainties are given at the 2σ level.

Data availability

All the data are reported in the Supplementary Information.

Acknowledgments

We sincerely thank Dr. Zhipeng Xia and Mr. Guofeng Zheng for their kind help in thin section preparation and technical support for fluid inclusions analyses. This work was funded by the Natural Science Foundation of China (41362006; 41873017) and the Guangxi Natural Science Foundation Program (2020GXNSFAA297049).

Author Contributions

R.G.H defined the research theme, interpreted the results and wrote the paper. B.C.P revised the manuscript and provided financial support. X.J.B and H.N.Q helped to Ar-Ar dating and reviewed the manuscript. The other authors helped to collect and pretreat the samples, prepared Figure 1-3 and reviewed the manuscript. All authors reviewed the manuscript.

Competing Interests

The authors declare no competing interests.

Additional Information

Correspondence and requests for materials should be addressed to B.C.P. or R.G.H.

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Table 1 ⁴⁰Ar/³⁹Ar dating result for pyritization Au-bearing quartz vein from Liaotun gold deposit

step	Pestle drop numbers	³⁶Ar_A	³⁷Ar_Ca	³⁸Ar_Cl	³⁹Ar_K	⁴⁰Ar*	Age ± 2σ (Ma)	⁴⁰Ar* (%)	³⁹Ar_K (%)	K/Ca ± 2σ
Quartz (LT19-1-2Q) by in vacuo progressive crushing, J= 0.01985044, I₀=298.56
1	10	49.72289	51.0166	0.688294	272.04	2189.75	268.1±27.8	12.85	0.20	2.1±1.6
2	20	66.55181	78.8949	0.914396	559.97	3937.38	236.3±18.4	16.54	0.41	2.7±1.7
3	40	79.95092	116.2493	1.329468	1250.14	7878.45	213.1±10.0	24.81	0.92	4.2±2.1
4	60	65.68980	174.3908	1.571137	2101.32	11760.71	190.5±5.0	37.48	1.55	4.7±1.8
5	80*	53.17219	163.3638	1.379358	3446.83	17360.23	172.3±2.6	52.22	2.54	8.2±3.0
6	100*	46.14375	204.6715	1.284667	4426.46	21803.15	168.7±1.8	61.26	3.26	8.4±2.1
7	140*	45.02404	217.0730	3.093739	6338.39	31498.58	170.1±1.3	70.07	4.67	11.3±4.1
8	180*	41.30535	231.5330	4.032405	8083.37	40078.07	169.8±1.0	76.44	5.95	13.5±3.6
9	220*	38.32218	217.8073	2.109376	10209.53	50028.87	167.9±0.9	81.36	7.52	18.1±6.6
10	260*	33.71465	250.7197	1.285718	11277.99	55436.53	168.4±0.8	84.60	8.30	17.4±4.0
11	300*	26.54074	203.8769	0.866962	12624.09	61663.00	167.3±0.7	88.58	9.29	24.0±5.3
12	350	23.41560	270.7132	0.769880	12526.18	64380.58	175.7±0.7	90.17	9.22	17.9±3.1
13	400	20.50324	218.2483	0.475983	11889.65	62951.96	180.7±0.7	91.10	8.75	21.1±3.0
14	450	18.49947	221.5877	0.224589	10158.23	55482.84	186.1±0.8	90.91	7.48	17.7±3.3
15	500	17.05097	200.5896	0.730391	8517.96	47935.95	191.5±0.8	90.37	6.27	16.4±4.3
16	550*	14.84095	220.8006	0.232163	6378.95	37605.09	200.1±0.8	89.43	4.70	11.2±2.1
17	630*	13.63239	186.1162	0.140307	5176.19	30446.97	199.7±0.9	88.18	3.81	10.8±2.5
18	700*	12.62736	171.2247	0.220453	3891.86	23014.44	200.7±0.9	85.90	2.86	8.8±3.2
19	800*	13.90444	163.7289	0.169922	3171.94	18843.68	201.6±1.0	81.92	2.33	7.5±2.9
20	800*	11.95218	178.5112	0.200370	2303.52	13674.35	201.4±1.2	79.28	1.70	5.0±1.3
21	800*	11.10584	158.4684	0.169977	1745.70	10384.65	201.8±1.3	75.78	1.29	4.3±1.4
22	800*	9.29043	195.4351	0.180257	1434.75	8538.00	201.9±1.3	75.46	1.06	2.8±0.7
23	800*	8.74064	100.6876	0.208530	1222.97	7237.53	200.9±1.4	73.48	0.90	4.7±2.3
24	800*	8.20593	87.8952	0.237676	1034.93	6097.41	200.0±1.5	71.32	0.76	4.6±3.4
25	800*	7.47681	75.7225	0.214813	914.01	5377.38	199.7±1.6	70.65	0.67	4.7±3.7
26	800*	6.80959	65.7761	0.270734	811.30	4772.63	199.7±1.6	70.11	0.60	4.8±3.5
27	800*	7.11494	84.4261	0.237051	769.97	4528.62	199.7±1.7	68.05	0.57	3.5±2.6
28	800*	6.71301	59.9597	0.220296	689.95	4063.12	199.9±1.8	66.95	0.51	4.5±2.4
29	800*	6.09843	68.1724	0.228236	622.25	3663.64	199.9±1.8	66.78	0.46	3.5±2.5
30	800*	5.49046	60.5975	0.202530	560.52	3319.69	201.0±1.9	66.93	0.41	3.6±2.1
31	800*	5.47876	72.3795	0.268878	530.42	3126.51	200.1±1.9	65.63	0.39	2.8±1.8
32	800*	4.70585	75.3493	0.182742	471.27	2773.73	199.8±1.9	66.36	0.35	2.4±1.6
33	800*	4.64396	51.9939	0.250278	438.76	2588.19	200.2±2.0	65.10	0.32	3.3±1.9

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Progressive crushing 40Ar/39Ar dating of gold-bearing quartz vein from the Liaotun Carlin-type gold deposit at the northwest of Guangxi

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