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Article

Petrogenesis of the Early Cretaceous Tietonggou Diorite and Its Geological Implications

by
Guo Ye
1,
Guangzhou Mao
1,2,3,*,
Qinglin Xu
1,
Zhengjiang Ding
3,
Yanchao Han
1,4,
Huiji Zhao
1,4 and
Ying Shen
5
1
Shandong Key Laboratory of Depositional Mineralization & Sedimentary Minerals, College of Earth Sciences & Engineering, Shandong University of Science and Technology, Qingdao 266590, China
2
Functional Laboratory of Marine Mineral Resources Evaluation and Detection Technology, Qingdao National Laboratory of Marine Science and Technology, Qingdao 266237, China
3
Shandong Engineering Research Center of Application and Development of Big Data for Deep Gold Exploration, Weihai 264209, China
4
Shandong Geo-Surveying & Mapping Institute, Ji’nan 250003, China
5
Shandong Institute of Geological Sciences, Ji’nan 250013, China
*
Author to whom correspondence should be addressed.
Minerals 2024, 14(4), 390; https://doi.org/10.3390/min14040390
Submission received: 28 February 2024 / Revised: 3 April 2024 / Accepted: 4 April 2024 / Published: 9 April 2024
(This article belongs to the Special Issue Genesis, Geochemistry and Mineralization of Metallic Minerals)
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Versions Notes

Abstract

:
The Tietonggou pluton is mainly composed of gabbroic diorite and diorite. The petrology, zircon U-Pb age, and geochemistry of the Tietonggou diorite have been studied to determine its petrogenesis and metallogenic significance. The diorite samples have 56–58 wt% SiO2 and 11–14 wt% Al2O3 and are peraluminous and sodic (Na2O/K2O = 1.29–2.07). All the samples are enriched in light rare earth elements (LREEs) and large-ion lithophile elements (LILEs; e.g., Rb, Ba, and Sr) but depleted in heavy rare earth elements (HREEs) and high field strength elements (HFSEs; e.g., Zr, Nb, and Ta), suggesting subduction-related affinities. The rocks have narrow ranges of (206Pb/204Pb)t (18.5–19.0), (207Pb/204Pb)t (15.71–15.75), and (208Pb/204Pb)t (38.4–39.0) ratios, respectively. Zircons from the Tietonggou diorite yielded a weighted average U-Pb age of 132.86 ± 0.92 Ma (MSWD = 0.48), whilst those from the nearby Laowa diorite yielded 129.72 ± 0.61 Ma (MSWD = 1.05). This suggests that the rocks represent Early Cretaceous plutons, coeval with the peak lithospheric thinning in eastern North China Craton (NCC). The magma likely originated from partial melting of the enriched lithospheric mantle and was contaminated by ancient lower NCC crustal materials. Our study clarifies the tectonic background of the Tietonggou pluton and provides support for the study of the genesis of Fe–skarn deposits in western Shandong.

1. Introduction

Since the Triassic continental collision between the North China Craton (NCC) and Yangtze Craton, NCC has undergone lithospheric thinning and large-scale magmatism; post-collision magmatism produced several Triassic plutons on the southern and eastern margins of the NCC [1]. Western Shandong is located in the southeastern NCC, west of the Yishu fault (a section of the crustal Tanlu fault zone) and adjacent to the Sulu–Dabie UHP belt (Figure 1a). There are many Fe–skarn deposits closely associated with these Mesozoic plutons. As one of the four major Fe–skarn deposit concentration areas in China, the western Shandong shows extensive Mesozoic magmatism and mineralization, making it an important area for studying the NCC formation and evolution [1,2,3,4,5,6], especially in terms of crust–mantle interactions [7,8,9,10,11]. Tietonggou is one of the two Fe–skarn deposits related to diorite in western Shandong, which are mainly produced in the contact zone between intrusive bodies and Cambrian–Ordovician, with cumulative Fe reserves of 2.11 million tons. Compared with the Jiaodong Peninsula, there are far fewer Mesozoic magmatic rock outcrops in western Shandong, and the Tietonggou pluton is one of them; their ages were reported as 184.7–180.1 Ma, 133 ± 6 Ma, 120 Ma, etc. [3,4,12].
In recent years, many petrological, geochronological, and geochemical studies have been conducted regarding Mesozoic Fe–skarn deposits and related intermediate-basic intrusive rocks in western Shandong [1,2,3,4,5,6,7,8,9,10,11,12,13,14,15,16,17]. The Tietonggou pluton was considered to have originated from the partial melting of pure peridotite in the upper mantle with continental crust input [13,14,15,16], yet there are different views on the crustal input: (1) Yangtze plate materials introduced during its Triassic subduction and collision [15,16]; (2) Archean North China crustal material sunk into the mantle during lithospheric delamination [17]; (3) Paleo-Pacific materials introduced during its subduction beneath North China [13].
Previous researchers focused on the Mesozoic pluton and Fe–skarn deposits in the whole western Shandong area and the lack of special research on the Tietonggou pluton. They have different opinions on the source of crust input in the metallogenic material of the Tietonggou pluton, and there are no reports on the accurate metallogenic age of the Tietonggou pluton.
In this study, we carried out analyses in petrology, whole-rock geochemistry, and zircon U-Pb geochronology on the Tietonggou pluton. The precise metallogenic age of the Tietonggou rock mass was obtained, and the possible material sources were analyzed. We discuss its petrogenesis and regional tectonic significance in order to clarify the tectonic background of the Tietonggou pluton and point out the targets for iron ore prospecting. The precise U/Pb zircon ages of the plutonic rocks in China can be used to establish geodynamics models for future studies.
Minerals 14 00390 g001
Figure 1. (a) Regional geological maps of western Shandong (modified after [18,19]); (b) Tietonggou area (modified after [20,21]).
Figure 1. (a) Regional geological maps of western Shandong (modified after [18,19]); (b) Tietonggou area (modified after [20,21]).
Minerals 14 00390 g001

2. Geological Setting and Petrography

Western Shandong was tectonically affected by the Lüliang, Caledonian, Hercynian, Indosinian, and Yanshanian orogenic events, forming a WNW-NW-trending tectonic framework. Mesozoic intrusive rocks are well-developed in western Shandong [18], as represented by the Laiwu and Ji’nan intrusive complexes (Figure 1a). Local stratigraphy comprises mainly the Ordovician Majiagou Group and the Carboniferous–Permian Yuemengou–Taiyuan groups. There are three major sets of faults (NW-, NE-, and EW-trending). Local magmatic rocks are dominated by Yanshanian (Jurassic–Cretaceous) intermediate plutonic rocks (notably the Tietonggou pluton) and minor mafic and felsic rocks (Figure 1b). The magmatic rock emplacement is locally fault-controlled, and the wallrocks include mainly Ordovician and Triassic marble [22].
The Tietonggou pluton comprises mainly meladiorite and diorite, which were mainly developed along the intrusive contact with the Ordovician Majiagou Group and the Carboniferous–Permian Yuemengou–Taiyuan groups. Samples LW1-LW12 were taken from Laowa village (where the Tietonggou pluton is exposed). The intrusive contact with the altered wallrocks is distinct in the mine (Figure 2a). The diorite is grayish-black (Figure 2c) and contains mafic microgranular enclaves (peridotite, a few cm in dimension). These inclusions contain 60%–65% olivine, 10%–15% orthopyroxene, and accessory minerals such as apatite (Figure 2d).
Under the microscope, the olivine is granular and cracked. The pyroxene is euhedral to subhedral granular and ranges from coarse- to fine-grained (Figure 2e). The hornblende is greenish and unevenly distributed (Figure 2f). Plagioclase is euhedral–subhedral tabular, and some crystals are oscillatory-zoned (Figure 2g), whilst biotite is flaky, dark brown, and of different sizes (Figure 2h). Opaque minerals include mainly magnetite.

3. Methods

In this study, a total of twelve samples were collected, including 2 meladiorite and 10 diorite. Meladiorite is the transition from diorite to gabbro. The dark minerals are mainly clinopyroxene (25%), containing a small amount of amphibole and orthopyroxene (about 5%). All the samples were collected from fresh outcrops of the Tietonggou pluton (Figure 2). Whole-rock major oxides, trace elements analyses, Pb isotope analysis, and zircon U-Pb dating were used to determine the tectonic implications (Figure 3).

3.1. Whole-Rock Major Oxides and Trace Elements Analyses

The analyses were carried out at the Institute of Geochemistry, Chinese Academy of Sciences (IGCAS) with an Agilent 5110 ICP-OES (Agilent Technologies, Santa Clara, CA, USA). For each sample, 0.0400 g powder was weighed into a Teflon cup, and 0.5 mL HNO3 and 1 mL HF were successively added, sealed, and heated in an oven at 200 °C for 12 h. The sample solution was then dried at 150 °C on an electric heating plate and then redigested with 5 mL 12% (v/v) HNO3 at 150 °C for 5 h. The solution was then diluted and analyzed [23]. The analysis accuracy of major oxides and trace elements is less than ±1 and ±5.

3.2. Whole-Rock Pb Isotope Analysis

Wole-rock Pb isotopic composition was measured out in the IGCAS with a Neptune plus MC-ICP-MS (Thermo Fisher Scientific, Dreieich, Germany). The rock powder was placed in the polytetrafluoroethylene sample cartridge, and 0.5 mL concentrated HNO3 and 1.0 mL concentrated HCl were added. The sample dissolving bomb was heated (195 °C) in an oven for three days to ensure complete digestion. The solution was then evaporated on an electric heating plate and redissolved in 1.5 mL of HBr (0.2 mol/L) and HNO3 (0.5 mol/L). Detailed procedures were described by [24].

3.3. Zircon U-Pb Dating

Zircon grains were separated by conventional magnetic separation and heavy liquid techniques. Optical microscopic observation, scanning electron microscope (SEM) cathodoluminescence (CL) imaging, and analysis spot selection of zircons were completed at the Beijing Zircon Navigation Technology Co. Ltd., and the zircon U-Pb dating was carried out at the State Key Laboratory of Continental Dynamics of Northwestern University with an Agilent 7500a ICP-MS (Agilent Technologies, Santa Clara, CA, USA). The laser ablation used helium as the carrier gas, 20 μm spot size, 0.032–0.036 J/cm2 energy density, and 10 Hz repetition rate. The calibration was performed with standard zircon 91,500 and GJ-1 [25,26,27]. ISOPLOT 3.0 software was used to process the data results and calculate the age. Detailed procedures were as described by [28].

4. Results

4.1. Whole-Rock Geochemistry

In our study, 12 rock samples (2 meladiorite and 10 diorite) were analyzed for their major oxides and trace element compositions, which are listed in Table 1, respectively. The rock samples have SiO2 = 56–58 wt% (avg. 57.6 wt%), Al2O3 = 11.31–14.15 wt% (avg. 13.3 wt%), Na2O = 2.6–3.5 wt%, K2O = 1.63–2.55 wt%, Na2O+K2O = 4.50–5.99 wt%, and Na2O/K2O = 1.29–2.07. In the total alkali silica (TAS) diagram (Figure 4), the samples fall within the meladiorite–diorite field, and most of the samples are subalkaline. The rocks have MgO = 7.14–10.43 wt%, CaO = 5.99–7.29 wt%, and a loss on ignition (LOI) = 0.28–0.88 wt%. Na2O, TiO2, and K2O contents increase with increasing SiO2 content, while Fe2O3, CaO, and MgO decrease (Figure 5). In the A/CNK-A/NK diagram (Figure 6a), the meladiorite and diorite samples fall into the metaluminous and peraluminous fields, respectively. In the SiO2-AR diagram (Figure 6b), all Tietonggou samples are assigned as calc-alkaline.
The total REE contents (∑REEs) for the Tietonggou samples are 94.29–109.48 ppm, among which the ∑LREEs = 83.60–99.69 ppm and ∑HREEs = 8.91–10.69 ppm, and the (La/Yb)N = 8.99–13.30. The rocks have weakly negative Eu anomalies (δEu = 0.81–1.03) and no discernible Ce anomalies (δCe = 1.00–1.02). The chondrite-normalized REE patterns show LREE enrichments and HREE depletions (Figure 7). In the primitive-mantle normalized multi-element spidergram (Figure 8), the rock samples are enriched in large ion lithophile elements (LILEs, e.g., Rb, Ba, Sr) but depleted in high field strength elements (HFSEs, e.g., Zr, Nb, Ta), resembling typical subduction-related arc magmatic rocks [33,34].

4.2. Pb Isotope Characteristics

The Pb isotope analysis results for the Tietongou diorite are listed in Table 2. The samples have (206Pb/204Pb)t, (207Pb/204Pb)t, and (208Pb/204Pb)t of 17.89–17.96, 15.48–15.50, and 37.90–37.95, respectively. The initial Pb isotope data of the samples fall between the Tietonggou pyroxene diorite and Shangyu pyroxene diorite in western Shandong [37,38]. In the Pb isotopic composition diagram (Figure 9), the samples of the Tietonggou pluton are projected within the range of Mesozoic mafic rocks in the North China Craton and the Yangtze Craton (Figure 8), indicating that the magma source of the Tietonggou pluton is closely related to the Yangtze Craton [38,39].

4.3. Zircon U-Pb Geochronology

For the present study, 23 zircons from the Tietonggou diorite (in the mine) and 27 zircons from the Laowa diorite were U-Pb dated. The zircons are transparent to translucent and mostly short to long columnar. Many zircons show core-rim texture (Figure 10). The zircons have Th/U > 0.4, resembling typical magmatic zircons [42] (Table 3). All analysis spots fall on or near the concordia, yielding a weighted average zircon age of 132.86 ± 0.92 Ma (MSWD = 0.48) for the Tietonggou pluton and 129.72 ± 0.61 Ma (MSWD = 1.05) for the Laowa pluton (Figure 11), suggesting an Early Cretaceous pluton.

5. Discussion

5.1. Age of Pluton

Early Cretaceous magmatic rocks are widely distributed in western Shandong, with most of the reported Ar-Ar ages clustered around 132–124 Ma [43,44]. Our study reports Early Cretaceous LA-ICP-MS zircon U-Pb ages of 132.86 ± 0.92 Ma (Tietonggou diorite) and 129.72 ± 0.61 Ma (Laowa diorite). It shows that both the Tietonggou diorite and the Laowa diorite were produced in the Cretaceous, which is consistent with the peak time of the lithospheric thinning of the North China Craton. Similar zircon U-Pb ages were also reported for the Mesozoic intrusive rocks (granitoids and gabbros) (132–122 Ma) in the eastern North China Craton (Jiaodong and Liaodong) [7,45,46]. This shows strong Early Cretaceous magmatic activity in the eastern part of the North China Craton.

5.2. Petrogenesis

The Tietonggou meladiorite and diorite are rich in MgO, Na2O, Co, Ni, and other transitional elements, suggesting an upper mantle source [47]. The Nb/Ta value of the samples (14.27–16.82) is significantly higher than that of crust-derived magma (11.00) but basically consistent with that of mantle-derived magma (17.50) [48]. The Zr/Hf ratios (34.82–39.14) are close to the primitive mantle value (36.27) but much higher than the continental crust value (11.0) [34]. The samples also have Rb/Sr (0.10–0.16) and Ba/Rb (9.56–14.08) values close to the primitive mantle value (Rb/Sr = 0.03 [49], Ba/Rb = 11.00 [50]). The geochemical features of the Tietonggou pluton suggest a mantle-derived magma source. In the Ba/Rb-Rb/Sr diagram (Figure 12), the evolution trend of Tietonggou diorite samples is similar to that of the primitive mantle, suggesting that the rocks may have been mantle-sourced [51], consistent with the characteristics of compatible trace elements (e.g., Ni and Co). In addition, the Tietonggou pluton is rich in LILEs and depleted in HFSEs, giving a Ta/La value (0.01–0.03) that is lower than the primitive mantle value (0.06) [52], indicating that crustal input must be considered in the petrogenesis. The Ce/Pb values of the samples (2.32–2.94, avg. 2.58) are significantly lower than those of MORB and OIB (25) but close to that of the upper crust (3.2), indicating significant crustal contamination in the magma evolution. Ratios of HFSEs and REEs can effectively identify the Cl-rich or F-rich ore-forming fluids: Cl-rich fluids commonly have LREEs enrichment and have Nb/La, Th/La, and Hf/Sm values < 1, whereas F-rich fluids have both LREE and HFSE enrichments and have Nb/La, Th/La, and Hf/Sm values > 1 [53]. For most Tietonggou samples, the Nb/La, Th/La, and Hf/Sm values are < 1, suggesting Cl-rich fluids (Table 1).
Pb isotope study [39] showed that Mesozoic mafic rocks in Eastern China have low initial radiogenic Pb isotope ratios, i.e., 206Pb/204Pb < 17.80, 207Pb/204Pb < 15.00, and 208Pb/204Pb < 38.00, whereas those in the Yangtze Craton have high initial radiogenic Pb isotope ratios, i.e., 206Pb/204Pb > 17.80, 207Pb/204Pb > 15.50, and 208Pb/204Pb > 38.00. The Tietonggou diorite has similar 206Pb/204Pb (>17.80) to those from the Yangtze Craton but similar 207Pb/204Pb (<15.50) and 208Pb/204Pb (<3800) to those from the NCC. This suggests that the magma formation was caused by the subduction of the Yangtze Plate beneath North China, so the magma source may be a mixture of the Yangtze and North China basement rocks (Table 2). For the study of intrusive rocks in the adjacent areas of western Shandong, the 207Pb/204Pb values of the Yinan gabbro in western Shandong are higher than those of the North China basic rocks, which may be modified by the subduction of the Yangtze craton [38]. Yang showed a spatial variation trend of Sr-Nd-Pb isotope of Early Cretaceous high-Mg diorite in western Shandong, of which 87Sr/86Sr and 207Pb/204Pb and 208Pb/204Pb decrease from southeast to northwest, whereas εNd (t) increases [16,38]. This is consistent with the Yangtze plate subducted northwest beneath the North China Craton and the mixed Yangtze–North China magma source proposed for the Tietonggou pluton.

5.3. Tectonic Implications

The Tietonggou pluton emplacement is coeval with the earliest Cretaceous magmatism, which was the strongest Mesozoic magmatic event in the North China Craton and the whole of Eastern China [45,46,54,55,56]. During this time, large-scale magmatism, basin subsidence, and faulting occurred in the North China Craton, indicating strong lithospheric extension associated with the zenith of the North China decratonization [57,58]. Due to the subduction rollback, lithospheric delamination and asthenospheric upwelling occurred, forming extensive magmatism [59,60,61,62]. The formation of the Tietonggou pluton was closely related to this subduction event, and the magma was mainly sourced from the mantle. With the subduction of the Pacific plate to the North China plate, the asthenosphere upwelling from deep (>150 km) to shallow caused decompression melting, the partial melting of the enriched lithospheric mantle, and the partial melting of mantle peridotite and subducted oceanic slab to produce basic magma.

6. Conclusions

(1)
The western Shandong, located in the North China Craton, is one of the four major Fe–skarn deposit concentration areas in China, and the Tietonggou deposit is a representative deposit in this area. The study of the metallogenic age and source of ore-forming materials of the Tietonggou intrusion can contribute to the study of the Mesozoic magmatic evolution framework and the creation of the genetic model of Fe–skarn deposits in North China.
(2)
Geochemical characteristics of the Tietonggou pluton and its inclusions suggest that the parental magma may have originated mainly from the enriched lithospheric mantle with minor continental crustal input. The magma formation was caused by the subduction of the Yangtze beneath North China, and the Tietonggou pluton was formed under the extension during the thinning of the lithosphere in this period.
(3)
The view that the crustal input of metallogenic material in the Tietonggou deposit is derived from Archean North China or Paleo-Pacific materials could not be supported in this study.
(4)
More research is needed to compare the genetic conclusions of the Tietonggou pluton with other Mesozoic plutons in western Shandong and to summarize the similarities in the geneses of these plutons.

Supplementary Materials

The following supporting information can be downloaded at: https://www.mdpi.com/article/10.3390/min14040390/s1, Table S1: Major oxides composition and trace elements composition for the Tietonggou diorite and meladiorite samples *.

Author Contributions

Conceptualization, G.M.; methodology, G.Y.; software, Y.H.; validation, H.Z.; formal analysis, G.Y.; investigation, Q.X. and Z.D.; resources, G.M.; data curation, G.Y; writing—original draft preparation, G.Y; writing—review and editing, G.Y.; visualization, Y.S.; supervision, Q.X. and Z.D.; project administration, G.M.; funding acquisition, G.M. All authors have read and agreed to the published version of the manuscript.

Funding

This research was funded by the National Natural Science Foundation of China (42172087, 41772125, 41572063), the Shandong Engineering Research Center of Application and Development of Big Data for Deep Gold Exploration (SDK202208), and the Major Scientific and Technological Innovation Projects of Shandong Province (2017CXGC1603).

Data Availability Statement

The data supporting this article are available in the online Supplementary Materials.

Acknowledgments

Thanks to the staff from the Institute of Geochemistry, the Chinese Academy of Sciences, the Beijing Zircon Navigation Technology Co., Ltd., and the State Key Laboratory of Continental Dynamics of Northwestern University for their support during the experiment. Special thanks are given to the three anonymous reviewers for their detailed and constructive reviews.

Conflicts of Interest

Yanchao Han, Huiji Zhao, and Ying Shen work for the Shandong Geo-surveying & Mapping Institute and Shandong Institute of Geological Sciences. The paper reflects the views of the scientists and not the institute.

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Figure 2. Field photos and thin-section microphotographs of the Tietonggou pluton: (a) intrusive contact between diorite and marble; (b) meladiorite; (c) Laowa diorite; (d) diorite with augite xenoliths; (e) spindle olivine; (f) amphibole; (g) oscillatory-zoned plagioclase; (h) biotite. Py—Pyrite; Ol—olivine; Aug—augite; Pl—plagioclase; Amp—amphibole; Bt—biotite.
Figure 2. Field photos and thin-section microphotographs of the Tietonggou pluton: (a) intrusive contact between diorite and marble; (b) meladiorite; (c) Laowa diorite; (d) diorite with augite xenoliths; (e) spindle olivine; (f) amphibole; (g) oscillatory-zoned plagioclase; (h) biotite. Py—Pyrite; Ol—olivine; Aug—augite; Pl—plagioclase; Amp—amphibole; Bt—biotite.
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Minerals 14 00390 g003
Figure 3. Methods flow chart.
Figure 3. Methods flow chart.
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Figure 4. TAS diagram for the Tietonggou samples [29,30].
Figure 4. TAS diagram for the Tietonggou samples [29,30].
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Figure 5. Harker diagrams for the Tietonggou meladiorite and diorite samples.
Figure 5. Harker diagrams for the Tietonggou meladiorite and diorite samples.
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Minerals 14 00390 g006
Figure 6. (a) A/CNK-A/NK [31] and (b) AR-SiO2 [32] plots for the Tietonggou meladiorite and diorite samples. AR: Alkalinity ratio.
Figure 6. (a) A/CNK-A/NK [31] and (b) AR-SiO2 [32] plots for the Tietonggou meladiorite and diorite samples. AR: Alkalinity ratio.
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Minerals 14 00390 g007
Figure 7. Chondrite-normalized REE patterns for the Tietonggou meladiorite and diorite samples [35].
Figure 7. Chondrite-normalized REE patterns for the Tietonggou meladiorite and diorite samples [35].
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Minerals 14 00390 g008
Figure 8. Primitive mantle-normalized multi-element spidergram for the Tietonggou meladiorite and diorite samples [36].
Figure 8. Primitive mantle-normalized multi-element spidergram for the Tietonggou meladiorite and diorite samples [36].
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Figure 9. (a)208Pb/204Pb versus 206Pb/204Pb diagram and (b) 207Pb/204Pb versus 206Pb/204Pb diagram for the Tietonggou meladiorite and diorite samples [40]. Data source: Mesozoic mafic rocks of North China Craton [38]; Mesozoic mafic rocks [38,39]; Northern Hemisphere reference line [41]; Earth isochron [42].
Figure 9. (a)208Pb/204Pb versus 206Pb/204Pb diagram and (b) 207Pb/204Pb versus 206Pb/204Pb diagram for the Tietonggou meladiorite and diorite samples [40]. Data source: Mesozoic mafic rocks of North China Craton [38]; Mesozoic mafic rocks [38,39]; Northern Hemisphere reference line [41]; Earth isochron [42].
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Figure 10. Representative zircon CL images and U-Pb ages for the Tietonggou (a) and Laowa (b) diorite samples.
Figure 10. Representative zircon CL images and U-Pb ages for the Tietonggou (a) and Laowa (b) diorite samples.
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Minerals 14 00390 g011
Figure 11. Zircon U-Pb concordia plots and weighted average ages for the Tietonggou pluton (a) and Laowa pluton (b). The error of isotope ratio and age is 2σ, and the confidence of weighted average age error is 95%.
Figure 11. Zircon U-Pb concordia plots and weighted average ages for the Tietonggou pluton (a) and Laowa pluton (b). The error of isotope ratio and age is 2σ, and the confidence of weighted average age error is 95%.
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Minerals 14 00390 g012
Figure 12. Ba/Rb vs. Rb/Sr plots for the Tietonggou meladiorite and diorite samples [51].
Figure 12. Ba/Rb vs. Rb/Sr plots for the Tietonggou meladiorite and diorite samples [51].
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Table 1. Major oxides composition and trace elements composition for the Tietonggou diorite and meladiorite samples.
Table 1. Major oxides composition and trace elements composition for the Tietonggou diorite and meladiorite samples.
Major Oxides in wt%Diorite (n = 10)MeladioriteMajor Oxides in wt%Diorite (n = 10)Meladiorite
MinMeanMaxLW-5LW-6MinMeanMaxLW-5LW-6
Na2O2.943.283.462.573.49MnO0.110.110.120.130.11
MgO7.147.838.8310.437.58Fe2O36.677.117.598.217.16
Al2O312.2313.414.1511.3114.11LOI0.280.510.790.880.58
SiO256.457.658.3856.1756.91Total99.1599.499.6499.7799.3
P2O50.140.190.210.120.21K2O + Na2O5.025.555.994.55.54
K2O1.632.272.551.922.05A/NK2.332.422.662.512.55
CaO5.996.417.27.296.43A/CNK1.021.121.160.961.18
TiO20.620.670.720.730.68Na2O/K2O1.291.462.071.341.7
Trace and Rare Earth Elements in ppmDiorite (n = 10)MeladioriteTrace and Rare Earth Elements in ppmDiorite (n = 10)Meladiorite
MinMeanMaxLW-5LW-6MinMeanMaxLW-5LW-6
Li19.321.8324.823.621.3Ho0.470.5010.520.550.45
Be1.531.6431.751.51.54Er1.271.3481.421.461.2
Sc17.919.5622.525.918.2Tm0.180.1940.20.210.17
Ti37053907.6425843563912Yb1.151.2141.31.321.08
V139147.8164174146Lu0.170.1780.190.190.16
Cr587676.9857922651Hf2.943.4925.052.563.07
Mn813858.59191033852Ta0.390.4470.50.420.42
Co27.429.833.239.328.8Pb14.516.9518.812.716.3
Ni161178.7207247170Th5.346.5647.926.246.26
Cu2.0736.13117820551.4U1.421.8782.131.711.65
Zn70.979.0882.58376.3Nb/Ta14.4415.79216.8214.2714.76
Ga17.718.7519.716.418.4Rb/Sr0.10.130.160.160.11
As6.957.3927.996.766.24Ba/Rb9.5612.18314.0812.4813.6
Se0.540.6490.830.610.47Zr/Hf35.4237.65939.1434.8237.51
Rb51.663.168.259.656.8La/Sm4.515.2995.674.255.71
Sr419483.9525382523Zr/Nb14.7918.86928.0215.0318.62
Y12.413.451414.712.1Ta/La0.020.0210.030.020.02
Zr10413219889.2115Ce/Pb2.322.5472.842.942.57
Nb5.677.0387.615.946.18Hf/Sm0.710.8621.220.620.82
Mo3.854.6565.513.764.16Nb/La0.270.3290.390.340.29
Sn1.241.341.471.221.4Th/La0.260.3050.340.350.29
Cs4.074.585.123.694.05Y/Ho26.2626.80727.8326.6926.63
Ba493771.2840743773Co/Ni0.160.1680.170.160.17
La18.521.4623.217.621.3(La/Yb)N10.1311.95412.848.9913.3
Ce38.243.0145.737.542∑REEs95.08104.15109.4894.29100.25
Pr4.464.9015.214.44.63∑LREEs85.0994.31999.6983.691.33
Nd18.619.8320.618.918.6∑HREEs9.239.83210.2410.698.91
Sm3.744.0534.154.153.73LREEs/HREEs8.519.610.197.8210.25
Eu0.981.0681.131.041.14(Gd/Yb)N2.112.2052.282.172.27
Gd3.073.3123.393.563.03(La/Sm)N2.843.3333.562.673.59
Tb0.440.4730.490.510.43δCe11.011.021.021.02
Dy2.472.6152.732.892.39δEu0.810.8910.990.831.03
LOI: loss on ignition.
Table 2. Whole-rock Pb isotope compositions for the Tietonggou meladiorite and diorite samples.
Table 2. Whole-rock Pb isotope compositions for the Tietonggou meladiorite and diorite samples.
Sample No.208Pb/204Pb1σ207Pb/204Pb1σ206Pb/204Pb1σPb
(ppm)		Th
(ppm)		U
(ppm)		Age
(Ma)		(208Pb/204Pb)t(207Pb/204Pb)t(206Pb/204Pb)t
LW-138.09400.001315.49460.000418.05610.000316.15.952.07129.737.941915.486717.8946
LW-238.11110.001315.50540.000418.11330.000317.67.922.13129.737.926015.498017.9612
LW-338.08430.001715.49550.000518.06100.000417.47.211.96129.737.914415.488617.9200
LW-438.07310.001515.49010.000518.05050.000415.66.571.88129.737.900215.482717.8993
LW-538.13930.002015.50330.000618.10780.000512.76.241.71129.737.938215.495117.9391
LW-638.10580.001415.50390.000418.06070.000416.36.261.65129.737.948115.497717.9338
Table 3. LA-ICP-MS zircon U-Pb dating results of the Tietonggou (TTGN) and Laowa (LW) diorite samples.
Table 3. LA-ICP-MS zircon U-Pb dating results of the Tietonggou (TTGN) and Laowa (LW) diorite samples.
Sample No.232Th238UTh/UIsotopic RatioIsotopic Age
(ppm)(ppm)Pb207/Pb2061sigmaPb207/U2351σPb206/U2381σPb206/U2381σ
91500 0.074270.0024 1.829 0.049 0.179 0.0023 1059.212.78
GJ-10.061610.0018 0.841 0.02 0.099 0.0012 608.57
TTG-Z161.48115.970.530.04970.0051 0.1410.014 0.0210.0004 131.411.98
TTG-Z282.14150.10.550.048650.0038 0.1390.01 0.0210.0003 1328.32
TTG-Z3110.77230.750.480.049970.0034 0.1470.01 0.0210.0003 135.78.2
91500 0.076610.0023 1.892 0.047 0.179 0.0023 1061.912.71
TTG-Z4187.35161.641.160.049160.0047 0.140.013 0.0210.0004 132.17.23
TTG-Z5123.2188.380.650.04960.004 0.1430.011 0.0210.0004 133.38.34
TTG-Z6115.02198.110.580.048830.0034 0.140.009 0.0210.0003 133.17.82
TTG-Z7114.57154.570.740.050160.005 0.1410.014 0.020.0004 130.39.63
91500 0.072630.0023 1.807 0.048 0.18 0.0023 1069.312.78
GJ-10.061310.0018 0.826 0.019 0.098 0.0012 601.16.78
TTG-Z8267.55365.620.730.049470.0026 0.1410.007 0.0210.0003 132.24.8
TTG-Z9110.03179.110.610.051950.0059 0.1470.016 0.0210.0005 130.912.88
TTG-Z10386.74276.921.40.04930.0027 0.140.007 0.0210.0003 131.53.61
TTG-Z11384.12231.611.660.048840.0032 0.140.009 0.0210.0003 132.83.92
TTG-Z1284.14138.040.610.051770.0046 0.1470.013 0.0210.0004 131.69.73
TTG-Z1367.1156.020.430.049990.0043 0.1450.012 0.0210.0004 134.511.63
TTG-Z14252.55212.171.190.049710.004 0.1410.011 0.0210.0004 131.45.6
TTG-Z15134.69144.470.930.049440.0041 0.1410.011 0.0210.0004 132.26.9
TTG-Z16143.1206.130.690.050010.0038 0.1460.010.0210.0004 134.77.76
TTG-Z17128222.330.580.04960.0031 0.1430.008 0.0210.0003 133.46.8
91500 0.076130.0023 1.878 0.048 0.179 0.0023 1060.812.51
GJ-10.05970.0018 0.808 0.02 0.098 0.0012 603.86.84
TTG-Z1869.01126.70.550.050920.0041 0.1490.012 0.0210.0004 135.39.98
TTG-Z19493.64468.571.050.050860.004 0.1430.011 0.020.0004 130.56.72
TTG-Z20201.77318.280.630.048810.0031 0.140.008 0.0210.0003 133.26.67
TTG-Z21747.54357.872.090.049740.0029 0.1450.008 0.0210.0003 134.93.25
91500 0.076870.0024 1.902 0.049 0.179 0.0023 1063.712.58
TTG-Z2270.4142.060.50.048970.0046 0.1430.013 0.0210.0004 135.511.93
TTG-Z23219.24238.420.920.048750.0032 0.1390.009 0.0210.0003 131.75.62
91500 0.073060.0023 1.801 0.046 0.179 0.0023 1060.212.47
GJ-10.059310.0018 0.804 0.019 0.098 0.0012 604.56.83
91500 0.072520.002 1.792 0.045 0.179 0.0017 1062.89.35
GJ-10.059310.0014 0.801 0.017 0.098 0.0008 602.84.43
LW-Z1379.47273.911.390.050120.0027 0.1420.007 0.020.0002 130.71.52
LW-Z2190.8178.011.070.047990.0031 0.1340.009 0.020.0002 128.91.54
LW-Z3541.49367.171.480.048960.0021 0.1380.006 0.020.0002 130.51.29
LW-Z41213.2663.151.830.048570.0022 0.1360.006 0.020.0002 129.81.34
LW-Z5116.05171.040.680.047520.0035 0.1330.01 0.020.0003 129.31.77
91500 0.076750.0019 1.895 0.045 0.179 0.0017 1061.99.01
LW-Z6300.65286.171.050.049210.0026 0.1380.007 0.020.0002 130.11.43
LW-Z7580.1348.181.670.048020.0028 0.1340.008 0.020.0003 129.61.56
LW-Z8114.86175.50.650.048280.0035 0.1370.01 0.0210.0003 131.11.75
LW-Z9378.59324.781.170.047640.0025 0.1340.007 0.020.0002 130.61.43
LW-Z10427.37296.141.440.048890.0031 0.1340.008 0.020.0003 127.11.67
91500 0.075920.0019 1.875 0.043 0.179 0.0016 10628.9
GJ-10.06090.0014 0.824 0.017 0.098 0.0008 603.14.39
LW-Z11249.85313.260.80.049370.0023 0.1370.006 0.020.0002 128.11.26
LW-Z12396.86323.931.230.0480.0022 0.1350.006 0.020.0002 129.91.26
LW-Z13169.18141.851.190.051910.0054 0.1460.015 0.020.0004 130.62.57
LW-Z14168.21199.630.840.050830.0061 0.1410.016 0.020.0005 128.53.22
LW-Z15337.79256.871.320.048560.0025 0.1370.007 0.020.0002 130.81.45
LW-Z16550.37415.211.330.049710.0022 0.1380.006 0.020.0002 128.81.3
91500 0.074140.0021 1.827 0.048 0.179 0.0018 1059.69.75
LW-Z17354.96280.681.270.048560.0025 0.1340.007 0.020.0002 127.71.31
LW-Z18259.38224.881.150.049460.0036 0.1370.010.020.0003 128.21.96
LW-Z19723.6420.61.720.048280.0028 0.1320.007 0.020.0002 126.21.52
LW-Z20219.32186.641.180.049130.0035 0.140.010 0.0210.0003 131.61.8
91500 0.075490.002 1.873 0.047 0.18 0.0017 1066.59.29
GJ-10.059870.0014 0.806 0.017 0.098 0.0007 600.24.37
LW-Z21258.85222.751.160.048430.0042 0.140.012 0.0210.0004 133.32.3
LW-Z22488.92389.941.250.048380.0045 0.1380.012 0.0210.0004 131.52.59
LW-Z23241.98192.341.260.049530.0029 0.1430.008 0.0210.0003 133.51.58
LW-Z24256.51206.451.240.048520.0033 0.1370.009 0.0210.0003 130.81.68
LW-Z25199.1160.921.240.051350.0045 0.1460.012 0.0210.0004 131.12.19
91500 0.074870.0019 1.857 0.045 0.180 0.0017 1065.79.09
LW-Z26174.94198.490.880.050720.0046 0.1430.013 0.020.0004 130.62.44
LW-Z27165.69225.140.740.049540.0039 0.1370.011 0.020.0003 128.12.04
91500 0.074020.0020 1.822 0.045 0.178 0.0017 1058.29.12
GJ-10.06010.0015 0.819 0.019 0.099 0.0008 606.74.67
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MDPI and ACS Style

Ye, G.; Mao, G.; Xu, Q.; Ding, Z.; Han, Y.; Zhao, H.; Shen, Y. Petrogenesis of the Early Cretaceous Tietonggou Diorite and Its Geological Implications. Minerals 2024, 14, 390. https://doi.org/10.3390/min14040390

AMA Style

Ye G, Mao G, Xu Q, Ding Z, Han Y, Zhao H, Shen Y. Petrogenesis of the Early Cretaceous Tietonggou Diorite and Its Geological Implications. Minerals. 2024; 14(4):390. https://doi.org/10.3390/min14040390

Chicago/Turabian Style

Ye, Guo, Guangzhou Mao, Qinglin Xu, Zhengjiang Ding, Yanchao Han, Huiji Zhao, and Ying Shen. 2024. "Petrogenesis of the Early Cretaceous Tietonggou Diorite and Its Geological Implications" Minerals 14, no. 4: 390. https://doi.org/10.3390/min14040390

APA Style

Ye, G., Mao, G., Xu, Q., Ding, Z., Han, Y., Zhao, H., & Shen, Y. (2024). Petrogenesis of the Early Cretaceous Tietonggou Diorite and Its Geological Implications. Minerals, 14(4), 390. https://doi.org/10.3390/min14040390

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