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Article

Lithospheric Architecture and Metallogenesis in Liaodong Peninsula, North China Craton: Insights from Zircon Hf-Nd Isotope Mapping

by
Zhichao Zhang
1,
Yuwang Wang
1,*,
Dedong Li
1 and
Chunkit Lai
2
1
Beijing Institute of Geology for Mineral Resources, Beijing 100012, China
2
Faculty of Science, Universiti Brunei Darussalam, Gadong BE1410, Brunei
*
Author to whom correspondence should be addressed.
Minerals 2019, 9(3), 179; https://doi.org/10.3390/min9030179
Submission received: 17 January 2019 / Revised: 19 February 2019 / Accepted: 8 March 2019 / Published: 14 March 2019
(This article belongs to the Special Issue Polymetallic Metallogenic System)
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Abstract

:
The Liaodong Peninsula is an important mineral province in northern China. Elucidating its lithospheric architecture and structural evolution is important for gold metallogenic research and exploration in the region. In this study, Hf-Nd isotope maps from magmatic rocks are constructed and compared to geological maps to correlate isotopic signatures with geological features. It is found that gold deposits of different age periods in Liaodong are located in areas with specific εHf(t) and εNd ranges (Triassic: from −8 to −4 and from −12 to −8, Jurassic: from −22 to −8 and from −14 to −8, Cretaceous: from −12 to −10 and from −22 to −20), respectively. This may reflect that when the Paleo-Pacific plate was subducted beneath the North China Craton, the magma was derived from the juvenile lower crust and the ancient lower crust, and formed the low-to-moderate hydrothermal Au-(Ag) and Pb-Zn deposits in the Triassic. In the Jurassic, continued subduction may have led to lithospheric thickening. Subsequently, the magma from the ancient lower crust upwelled and formed low-to-moderate hydrothermal Au deposits and porphyry Mo deposits. In the Cretaceous, crustal delamination may have taken place. The magma from the ancient lower crust upwelled and formed various low-to-moderate hydrothermal Au deposits.

1. Introduction

The North China Craton (NCC), containing the Liaodong and Jiaodong gold provinces, is the top gold producer in northeast Asia [1,2,3,4,5,6]. The Liaodong Peninsula is located between the Yalujiang and TanLu fault zones (Figure 1) [7,8,9] and represents an important mineral province in the NCC. The peninsula has undergone complex magmato-tectonic modifications, during which many important polymetallic (Pb-Zn, Au, Ag, and Mo) deposits have been formed (Figure 1 and Figure 2) [10,11]. Most of these deposits are interpreted to be genetically linked with granitoid in the peninsula [11]. Granitoid in the Liaodong peninsula include the diorite and the granite that formed in the Paleoproterozoic, Permian, Jurassic, and Cretaceous [7,12,13]. These many phases of magmatism provide a window into the study of the lithospheric architecture and its control on metallogenesis.
Tectonic evolution and the characteristics of gold deposits in Liaodong and Jiaodong are similar [14,15,16,17,18]; however, whether or not the lithospheric architecture played a role in controlling the tectonic evolution and gold ore formation remains poorly understood.
The Hf and Nd isotopes are powerful tools to trace the nature of basement rocks and the age of the continental crust [19,20,21], and Hf-Nd isotope mapping has been used to reveal the lithospheric architecture and evolution, and their control on the distribution of mineral deposits [22,23,24,25,26,27,28,29].
In this study, we summarize the spatial distribution, age, and geochemical and isotopic data of the Paleoproterozoic to Cretaceous magmatic rocks in the Liaodong Peninsula, and we use Hf-Nd isotope mapping to reveal the crustal architecture and its controls on the regional mineralization.

2. Geological Setting

2.1. Regional Tectonics

The Liaodong Peninsula is located in the eastern margin of the NCC (Figure 1). It is bounded by the Yalujiang fault in the east and by the Tanlu fault in the north [31,32]. The Liaodong Peninsula can also be subdivided into the Longgang terrane in the north, the Liaoji orogenic belt in the middle, and the Langlin terrane in the south. This study only focuses on the Longgang terrane and the Liaoji orogenic belt. The Longgang terrane is composed of Archean to Paleoproterozoic basement rocks, and unmetamorphosed Mesoproterozoic to Cenozoic sedimentary and volcanic rocks [7]. The Liaoji orogenic belt consists mainly of Paleoproterozoic to Cretaceous magmatic rocks. In the Longgang terrane, the Paleoproterozoic sequences are missing, and the magmatic rocks are largely Triassic (Figure 3) [33].

2.2. Magmatism

The Liaodong Peninsula consists of Paleoproterozoic granite, Triassic granite and diorite, Jurassic granite and diorite, and Cretaceous granite and diorite (Table 1 and Table S1) (Figure 4 and Figure 5) [34,35,36,37,38,39]. During the Paleoproterozoic, the voluminous granitoid and the mafic intrusions in the peninsula were emplaced (Figure 5) and then metamorphosed at 1.93 Ga [40], marking the cratonization of the NCC eastern block. The Triassic magmatism is characterized by metaluminous mafic and felsic magmatic rocks (Figure 5), which are also identified in the southern Liaodong Peninsula [7,30]. Late Mesozoic intrusive rocks include Jurassic (180–153 Ma) ductile-deformed, peraluminous/metaluminous granite (Figure 5), and undeformed to slightly deformed early Cretaceous (131–120 Ma) metaluminous granite and diorite (Figure 5) [7,41,42].

2.3. Mineralization

The Liaodong Peninsula contains Pb-Zn, Au, Ag, and Mo polymetallic deposits, which are mainly distributed in the Qingchengzi, Wulong, and Maoling orefields (Figure 1) (Table 2) [11,43,44]. The Qingchengzi orefield is in the northern part of the Liaodong Peninsula, which hosts a number of magmatic-hydrothermal (low-to-moderate hydrothermal) Au-(Ag) and Pb-Zn deposits and porphyry Mo deposits (Figure 2) [45,46]. The magmatic-hydrothermal Au-(Ag) deposits were mainly formed in the Triassic (225–240 Ma), as exemplified by the Baiyun and Yangshu deposits (Table 2). The mineralization of these deposits has been correlated to the granite and the diorite, which are the result of lithospheric thinning associated with the Paleo-Pacific plate subduction [30,35]. The magmatic-hydrothermal Pb-Zn deposits (e.g., Xiquegou and Zhenzigou) were also formed in the Triassic (221–232 Ma), whilst the Yaojiagou porphyry Mo deposit was formed in the Jurassic (168 Ma). The mineralization of these Pb-Zn deposits has been correlated to the granite and the diorite, and that of the Mo deposit has been correlated to the granite. The Pb-Zn and Mo deposits have been correlated to large-scale delamination [7,35].
The Wulong orefield contains the Wulong and Sidaogou magmatic-hydrothermal (low-to-moderate hydrothermal) Au deposits. The largest Wulong deposit was formed at 122 Ma [62], whilst the Sidaogou deposit in southern Liaodong has no reliable mineralization age data.
The Maoling orefield contains the Jurassic, Maoling, Fenshui, and Wangjiawaizi magmatic-hydrothermal (low-to-moderate hydrothermal) Au deposits (186–189 Ma) [44,60,61].

3. Methods

Published zircon U-Pb age and Hf isotope data (35 samples) and whole-rock Sr-Nd isotope data (35 samples) from the Liaodong Peninsula have been compiled. Data compiled were from Paleoproterozoic to Cretaceous rocks, including (porphyritic) granite, monzogranite, lamprophyre, plagiogranite, (gneissic) granodiorite, (quartz) diorite, and syenodiorite. New data were also added in this study via collecting and analyzing (for zircon Lu-Hf isotopes) samples from the Qingchengzi orefield. The Zircon U-Pb age of the Miaonangou gabbro near the Baiyun gold deposit was in 1252 Ma [63], and the porphyrie (diorite, monzogranite) in the Baiyun deposit were emplaced in 229–222 Ma [63,64]. The Gujiapuzi granite porphyry in the Qingchengzi orefield was in 219 Ma [63].
Zircon Hf isotopes were analyzed using a 193-nm laser ablation (LA) system attached to a Neptune multi-collector (MC)-ICP-MS (Laboratory of Isotope Geology, Tianjin Institute of Geology and Mineral Resources, China). A laser pulse (100 mJ energy, 10 Hz frequency, 50 μm beam size) was used for the laser ablation [65]. Isobaric interference of 176Lu on 176Hf was corrected on the basis of the measured 175Lu value and the recommended 176Lu/175Lu ratio of 0.02655. Similarly, the 176Yb/172Yb value of 0.5887 and mean β Yb value obtained during Hf analysis on the same spot were used for interference correction of 176Yb on 176Hf [66,67]. A 176Lu decay constant of 1.865 × 10−11-year−1 [68] and the chondritic ratios of 176Hf/177Hf = 0.282785 and 176Lu/177Hf = 0.0336 [69] were used to calculate the εHf(t) values [70,71,72].
The Hf-Nd contour maps were produced using the inverse distance weighted interpolation method in the MapGIS 6.7 (Manufacturer is Zondy Cyber, Wuhan, China) program to contour the Hf and Nd dataset, which accounts for the distance between sample points in the most representative manner [73,74,75]. In order to produce the most robust spatial representation of the isotopic dataset, this method used 12 nearest neighbors at a power of 2 following [24]. All isotope data were grouped by the geometric interval method designated for class breaks. This ensured that each class range had approximately the same number of values, and that the change between intervals was fairly consistent. All point data shown in the contour maps represent the median for a range of Hf-Nd isotope values from an individual sample, which helped to minimize data anomalies [23,28,76].

4. Results

4.1. Zircon Hf Isotope Features

Zircon εHf(t) values of the Longgang terrane vary from −18.9 to 5.8 (average −3.3), and the old crustal Hf model ages (TDMC) range from 994 to 2058 Ma (average 1349 Ma). Zircon εHf(t) values of the Liaoji orogenic belt vary from −33 to 11.7 (average −11.4), and the TDMC range from 763 to 2785 Ma (average 1449 Ma).
For the Paleoproterozoic rocks, the εHf(t) and TDMC ranged from −17.4 to 7.9 (average −0.8) and from 2036 to 3874 Ma (average 2948 Ma), respectively. For the Triassic rocks, the zircon εHf(t) and TDMC ranged from −18.9 to 5.2 (average −11.5) and from 763 to 2613 Ma (average 1422 Ma), respectively. For the Jurassic rocks, the zircon εHf(t) and TDMC range from −28.9 to −1.1 (average −16.3) and from 1505 to 2785 Ma (average 2041 Ma), respectively (Table S2).
Contour maps of the zircon εHf(t) values for the Paleoproterozoic-Cretaceous Liaodong magmatic rocks show four high εHf(t) domains and two low εHf(t) domains, among which two high εHf(t) domains are in the Longgang terrane, and the other two are in the Liaoji orogenic belt (Figure 6). There are two low εHf(t) domains in the Longgang terrane and the Liaoji orogenic belt, respectively (Figure 6).

4.2. Whole-Rock Sr-Nd Isotope Features

The (87Sr/86Sr)i ratios of the Liaoji orogenic belt and the Longgang terrane range from 0.7044 to 0.7215 (average 0.7098) and from 0.7037 to 0.7306 (average 0.7085), respectively. The εNd values of the Liaoji belt and the Longgang terrane range from −24.9 to −0.9 (average −14.1) and from −18.9 to 3.82 (average −5.1), respectively (Table S3).
For the Cretaceous rocks, the εNd and TDM values range from −19.3 to −11.9 (average −15.1) and from 1388 to 2191 Ma (average 1831 Ma). For the Jurassic rocks, the (87Sr/86Sr)i, εNd, and TDM values range from 0.7044 to 0.7215 (average 0.7104), −24.9 to −9.6 (average −11.2), and 1110 to 2826 Ma (average 1888 Ma), respectively. For the Triassic rocks, the (87Sr/86Sr)i, εNd, and TDM values range from 0.7037 to 0.7306 (average 0.7082), −18.9 to 3.82 (average −9.5), and 726 to 2290 Ma (average 1541 Ma), respectively. For the Paleoproterozoic rocks, the εNd and TDM values range from −16.2 to −0.9 (average −5.8) and from 2480 to 2813 Ma (average 2279 Ma), respectively (Table S3).
The Contour maps of whole-rock Nd isotopes for the Paleoproterozoic-Cretaceous magmatic rocks show three high εNd domains and four low εNd domains in the region. One high εNd and one low εNd domain are in the Longgang terrane, and the other two high εNd domains and three low εNd domains are in the Liaoji belt (Figure 7).

5. Discussion

5.1. Lithospheric Architecture of the Liaodong Peninsula

In the Longgang terrane, there are two domains characterized by high εHf values (Figure 6), that are present in the area of the Triassic and Paleoproterozoic granite and diorite (Figure 1) and indicate that the granite and the diorite of this area are derived from the mantle or juvenile lower crust. There are also two domains characterized by low-εHf in the Longgang terrane (Figure 6), that indicate the magmatic rocks of this area are derived from the lower crust. In the Liaoji orogenic belt, there are two domains characterized by high-εHf (Figure 6), which are present in the area of Triassic and Paleoproterozoic granite and diorite (Figure 1), and indicate that the rocks are derived from the mantle or juvenile lower crust. There are also two low-εHf domains in the Liaoji orogenic belt (Figure 6) that indicate the crustal origin of the magmatic rocks in this area.
There is one high εNd domain in the Longgang terrane, and there are two high εNd domains in the Liaoji orogenic belt (Figure 7). However, the εNd values of the two domains in the Liaoji orogenic belt are still below zero. Therefore, the magmatic rocks in the Liaoji orogenic belt are derived from the lower crust. The high εNd domain in the Longgang terrane is present in the area of the Triassic granite and the diorite (Figure 7). This also can indicate that the granite and the diorite are mostly derived from the mantle or juvenile lower crust.
In the Longgang terrane, the area of the Triassic granite and the diorite with high-εHf and high-εNd shows that the magmatic rocks are derived from the juvenile lower crust (Figure 8). The high (87Sr/86Sr)i ratios also support this evidence (Figure 9). The area of Paleoproterozoic granite and diorite with high-εHf in the Longgang terrane shows that the magmatic rocks are from juvenile lower crust (Figure 8). In the Liaoji orogenic belt, the area of Triassic granite and diorite with high-εHf shows that the magmatic rocks are from the juvenile lower crust (Figure 8). The area of Paleoproterozoic granite and diorite with high-εHf shows that the magmatic rocks are from the depleted mantle (Figure 8).
In the Paleoproterozoic, the Tanlu fault may have experienced dextral shear movement, and the intense regional extension creating the Liaodong rift valley [77], although the actual timing and number of stages (argued variably from four to six) of the rifting process remain controversial. The timing of rifting is also variably attributed from 2.3 to 1.7 Ga or from 2.3 to 1.8 Ga [9,77]. The magmatic rocks in the Longgang terrane are from the juvenile lower crust and the ancient lower crust, but the magmatic rocks in the Liaoji orogenic belt are from the depleted mantle and the ancient lower crust (Figure 6, Figure 7 and Figure 8).
In the Mesozoic, the Liaodong Peninsula was likely in a post-collisional extensional setting [9,78,79], and the Paleo-Pacific plate may have subducted beneath the NCC [6,9]. Zircon and monazite SHRIMP U-Pb dating suggested that the continental collision took place in 220–240 Ma [80,81,82]. In the Triassic, the collision between North China and Paleo-Pacific plate likely caused the lithospheric thickening in the Liaoji rift [30,35,83]. The Triassic magmatic rocks are derived from the juvenile lower crust and the ancient lower crust (Figure 6, Figure 7, Figure 8 and Figure 9). The rocks have positive whole rock εNd(t) and zircon εHf(t) values, indicating a juvenile lower crustal source. In addition, the Triassic magmatic rocks with high SiO2 contents and low MgO concentrations have strong negative and variable whole rock εNd(t) and zircon εHf(t) values, indicating that they were derived from partial melting of the ancient lower crustal materials with involvement of mantle components [12]. In the Jurassic, the lithospheric thickening continued [1,84,85,86,87,88]. The sources of the magmatic rocks are from the ancient lower crust (Figure 6, Figure 7, Figure 8 and Figure 9). The rocks with strong negative and variable whole rock εNd(t) and zircon εHf(t) values indicate that they were derived from partial melting of the Precambrian basement [7]. In the Cretaceous, large-scale delamination may have taken place [35,89]. The magmatic rocks have the same characteristics of whole rock εNd(t) and zircon εHf(t) values as those of Cretaceous magmatic rocks. Therefore, the sources of the magmatic rocks are also derived from the ancient lower crust (Figure 6, Figure 7 and Figure 9).

5.2. Regional Tectonic Evolution and Relation to Mineralization

The Triassic is the principal metallogenic epoch in Liaodong. Deposits formed in the Triassic include the Zhenzigou, Nanshan, Diannan, and Xiquegou low-to-moderate hydrothermal Pb-Zn deposits, the Baiyun and Xiaotongjiapuzi low-to-moderate hydrothermal Au-Ag deposits, and the Gaojiapuzi low-to-moderate hydrothermal Ag deposits, that are all located in the Qingchengzi orefield (Table 2). The mineralization ages (221–240 Ma) are consistent with the magmatic ages (210–230 Ma), suggestive of a magmatic-hydrothermal genesis for these deposits [8]. The Sr and Pb isotope characteristics of the deposits in the Qingchengzi orefield show that the ore-forming materials were derived from the magma and metamorphosed sequences [8,64]. The deposits of the Qingchengzi orefield are clustered in regions with high-εHf (Figure 6, Figure 8 and Figure 9). This infers that the deposits are correlated to the magma, and that the magma is derived from the juvenile lower crust and the ancient lower crust (Figure 10a).
In the Jurassic, the Maoling and Fenshui low-to-moderate hydrothermal Au deposits were formed in the Maoling orefield, and the Yaojiagou porphyry Mo deposit was formed in the Qingchengzi orefield (Table 2). Sulfur isotopes from the Miaoling deposit show typical magmatic sulfur characteristics [90]. The Pb isotope characteristics of the deposit show that the ore-forming materials came from the magma and the metamorphic sequences [90]. The deposits are clustered in regions with low εHf and εNd values (Figure 6, Figure 7, Figure 8 and Figure 9). This infers that the deposits are correlated to the magma, which is derived from the ancient lower crust (Figure 10b).
The Cretaceous is another important metallogenic epoch. The Wulong orefield contains Wulong and Sidaogou low-to-moderate hydrothermal Au deposits. The characteristics of Sr and Pb isotopices suggest that the rock- and ore-forming and diagenetic materials of the Sanguliu granite near the Wulong orefield were derived from the magmatic rocks [62]. The H-O isotopes characteristics demonstrate that the ore-forming fluid came from magmatic fluid [62]. The deposits are clustered in regions with low εHf and εNd values (Figure 6, Figure 7, Figure 8 and Figure 9). This infers that the deposits are correlated to the magma, which is derived from the ancient lower crust (Figure 10c).

6. Conclusions

In the Triassic, the Paleo-Pacific plate subducted beneath the NCC and caused the lithospheric thickening. The Triassic ore deposits are characterized by high εHf(t) values, and are correlated to the magma, which is derived from the juvenile lower crust and the ancient lower crust. In the Jurassic, the lithospheric thickening continued. The Jurassic ore deposits are characterized by low εHf(t) and εNd values and are correlated to the magma derived from the ancient lower crust. In the Cretaceous, large-scale delamination may have taken place in this period. The Cretaceous ore deposits are characterized by low εHf(t) and εNd values, and are correlated to the magma, which is derived from the ancient lower crust.

Supplementary Materials

The following are available online at https://www.mdpi.com/2075-163X/9/3/179/s1, Table S1: Major elements datas, Table S2: Hf isotope, Table S3: Sr-Nd isotope.

Author Contributions

Z.Z. and Y.W. conceived and designed the ideas; Z.Z. and D.L. collected and analyzed the data; Z.Z. wrote the manuscript; Y.W., D.L. and C.L. revised and edited the manuscript.

Funding

This study was financially supported by the National Key R&D Program of China (Grant No. 2018YFC0603804).

Acknowledgments

We thank the geologists from Team 103 of the Bureau of Non-ferrous Metal Geology (Dandong, Liaoning Province) for their field assistance.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. (a) Simplified tectonic map of the Liaodong Peninsula showing the major suture zones and blocks. (b) Geological map of the Liaodong Peninsula showing the distribution of magmatic rocks, and the locations of major mineral deposits [30].
Figure 1. (a) Simplified tectonic map of the Liaodong Peninsula showing the major suture zones and blocks. (b) Geological map of the Liaodong Peninsula showing the distribution of magmatic rocks, and the locations of major mineral deposits [30].
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Figure 2. Simplified geologic map of the Qingchengzi orefield showing the distribution of deposits [11].
Figure 2. Simplified geologic map of the Qingchengzi orefield showing the distribution of deposits [11].
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Figure 3. Stratigraphic columns showing the basement rocks, sedimentary cover, and magmatic history of the Longgang Terrane and the Liaoji orogenic belt.
Figure 3. Stratigraphic columns showing the basement rocks, sedimentary cover, and magmatic history of the Longgang Terrane and the Liaoji orogenic belt.
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Figure 4. (a) Histogram of geochronological dating of zircon U-Pb ages of magmatic rocks. (b) Histogram of geochronological dating of mineralization.
Figure 4. (a) Histogram of geochronological dating of zircon U-Pb ages of magmatic rocks. (b) Histogram of geochronological dating of mineralization.
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Figure 5. (a) Total alkali (Na2O + K2O) versus SiO2 diagram. (b) A/CNK (molecular Al2O3/(CaO + Na2O + K2O)) versus zircon U-Pb age diagram. Dates are in Table 1 and the Supplementary Material Table S1.
Figure 5. (a) Total alkali (Na2O + K2O) versus SiO2 diagram. (b) A/CNK (molecular Al2O3/(CaO + Na2O + K2O)) versus zircon U-Pb age diagram. Dates are in Table 1 and the Supplementary Material Table S1.
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Figure 6. Contour maps of the Hf isotope for the magmatic rocks in the Liaodong Peninsula. Data are from Supplementary Material Table S2.
Figure 6. Contour maps of the Hf isotope for the magmatic rocks in the Liaodong Peninsula. Data are from Supplementary Material Table S2.
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Figure 7. Contour maps of the Nd isotope for the magmatic rocks in the Liaodong Peninsula. Data are from Supplementary Material Table S3.
Figure 7. Contour maps of the Nd isotope for the magmatic rocks in the Liaodong Peninsula. Data are from Supplementary Material Table S3.
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Figure 8. Plot of zircon U-Pb age versus εHf(t) values for the magmatic rocks from the Liaodong Peninsula. Data are from Supplementary Material Table S2.
Figure 8. Plot of zircon U-Pb age versus εHf(t) values for the magmatic rocks from the Liaodong Peninsula. Data are from Supplementary Material Table S2.
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Figure 9. (a) Plot of whole-rock (87Sr/86Sr)i versus εNd(t) values for the magmatic rocks from the Liaodong Peninsula. (b) Plot of age versus whole-rock εNd(t) values for the magmatic rocks from the Liaodong Peninsula. Data are from Supplementary Material Table S3.
Figure 9. (a) Plot of whole-rock (87Sr/86Sr)i versus εNd(t) values for the magmatic rocks from the Liaodong Peninsula. (b) Plot of age versus whole-rock εNd(t) values for the magmatic rocks from the Liaodong Peninsula. Data are from Supplementary Material Table S3.
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Figure 10. (a) Lithospheric architecture of the Liaodong Peninsula in the Triassic. (b) Lithospheric architecture of the Liaodong Peninsula in the Jurassic. (c) Lithospheric architecture of the Liaodong Peninsula in the Cretaceous.
Figure 10. (a) Lithospheric architecture of the Liaodong Peninsula in the Triassic. (b) Lithospheric architecture of the Liaodong Peninsula in the Jurassic. (c) Lithospheric architecture of the Liaodong Peninsula in the Cretaceous.
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Table
Table 1. Zircon U-Pb ages for the magmatic rocks from the Liaodong Peninsula.
Table 1. Zircon U-Pb ages for the magmatic rocks from the Liaodong Peninsula.
PeriodNo.PlutonPhaseAge/MaSampleMethodReferences
Cretaceous1WulongbeiQuartz diorite126–127ZirconSHRIMP U-Pb[7]
2SanguliuPorphyritic granite125 ± 3ZirconSHRIMP U-Pb[7]
3YinmawanshanGneissic granodiorite122 ± 2ZirconLA-ICP-MS U-Pb[7]
YinmawanshanMonzogranite (dike)124 ± 5ZirconLA-ICP-MS U-Pb[7]
YinmawanshanMonzogranite122 ± 6ZirconLA-ICP-MS U-Pb[7]
4QianshanGranite126 ± 2ZirconLA-ICP-MS U-Pb[32]
Jurassic5XiaoheshanGranodiorite173–174 ± 4ZirconLA-ICP-MS U-Pb[7]
6HanjialingGranodiorite179 ± 3ZirconLA-ICP-MS U-Pb[7]
Monzogranite164 ± 4ZirconLA-ICP-MS U-Pb[7]
7YutunMylonitic granite157 ± 3ZirconLA-ICP-MS U-Pb[7]
8HeigouMonzogranite161 ± 6, 163 ± 7ZirconLA-ICP-MS U-Pb[7]
9JiulianchengMonzogranite156 ± 3ZirconLA-ICP-MS U-Pb[7]
10GaoliduntaiPlagiogranite156 ± 5ZirconLA-ICP-MS U-Pb[7]
11Baiyun gold minePorphyritic dyke168 ± 3ZirconLA-ICP-MS U-Pb[7]
12HuaziyuLamprophyres155 ± 4ZirconLA-ICP-MS U-Pb[47]
13WalingMonzonitic granite162.4 ± 1.9ZirconSHRIMP U-Pb[36]
14DandongGranite157–167ZirconLA-ICP-MS U-Pb[14]
Triassic15Shuangdinggoubiotite monzogranite224.2 ± 1.2 ZirconLA-ICP-MS U-Pb[9]
16XinlingGranites225.3 ± 1.8ZirconSHRIMP U-Pb[8]
17XiuyanMonzogranite210 ± 1ZirconLA-ICP-MS U-Pb[30]
18NankouqianMonzogranite224 ± 2ZirconSIMS[12]
Monzogranite221 ± 2ZirconLA-ICP-MS U-Pb[12]
Granite224 ± 1ZirconLA-ICP-MS U-Pb[48]
Triassic19MayihePyroxene diorite222 ± 2ZirconSIMS[12]
Pyroxene syenodiorite223 ± 2ZirconSIMS[12]
Fine-grained diorite222 ± 2ZirconSIMS[12]
Biotite monzogranite220 ± 2, 223 ± 3, 221 ± 2ZirconLA-ICP-MS U-Pb[12]
20XidadingziMonzogranite220 ± 2, 221 ± 2ZirconLA-ICP-MS U-Pb[12]
21ChaxinziMonzogranite222 ± 2, 219 ± 2ZirconLA-ICP-MS U-Pb[12]
Diorite219 ± 4ZirconLA-ICP-MS U-Pb[12]
Monzodiorite222 ± 2ZirconLA-ICP-MS U-Pb[12]
Diorite221 ± 2ZirconSIMS[12]
Granodiorite222 ± 1ZirconSIMS[12]
22XiaoweishaheGranodiorite218 ± 2ZirconLA-ICP-MS U-Pb[12]
Quartz diorite220 ± 2, 219 ± 4ZirconLA-ICP-MS U-Pb[12]
23LongtouGranodiorite224 ± 2ZirconSIMS[12]
Granodiorite220 ± 2ZirconLA-ICP-MS U-Pb[12]
Fine-grained granite221 ± 2ZirconLA-ICP-MS U-Pb[12]
24QingchengziLamprophyres224–230 ZirconLA-ICP-MS U-Pb[9]
25SaimaSyenite222 ± 3.4ZirconLA-ICP-MS U-Pb[49]
Syenite221 ± 2.3ZirconLA-ICP-MS U-Pb[49]
26BailinchuanSyenite221 ± 2.3ZirconLA-ICP-MS U-Pb[49]
Paleo-proterozoic27JiguanshanGranite2175 ± 13ZirconSHRIMP U-Pb[38,50]
28LaoheishanGranite2166 ± 14ZirconSHRIMP U-Pb[38,50]
29DadingziGranite1869 ± 16ZirconSHRIMP U-Pb[39]
30WuleishanGranite1830.5 ± 5.9ZirconSHRIMP U-Pb[39]
31SimenziGranite2157 ± 14ZirconSHRIMP U-Pb[39]
32GujiapuGranite2169 ± 11ZirconSHRIMP U-Pb[39]
Table
Table 2. Summary of the geological characteristics of major ore deposits in the Liaodong Peninsula.
Table 2. Summary of the geological characteristics of major ore deposits in the Liaodong Peninsula.
NumberDepositsOrefieldTypeMetallic Comm.Tonnage (t)GradeHost RockAge (Ma)Data Source
1ZhenzigouQingchengziMagmatic hydrothermalPb-Zn 0.37, 450Marble, Amphibolite, Schist221[8,51]
2NanshanQingchengziMagmatic hydrothermalPb-Zn 0.5, 153 227[9,11]
3DiannanQingchengziMagmatic hydrothermalPb-Zn 0.08, 650 232[11]
4XiquegouQingchengziMagmatic hydrothermalPb-Zn 0.28, 250 225[8,11]
5BaiyunQingchengziMagmatic hydrothermalAu31.72.85 g/tMetamorphic rock and quartz veins225[10,11]
6XiaotongjiapuziQingchengziMagmatic hydrothermalAu-Ag20–500.07~2.92, 0.14~6.12Marble239[11,43,52,53]
7GaojiapuziQingchengziMagmatic hydrothermalAg 312Marble240[11,45,52,54]
8YangshuQingchengziMagmatic hydrothermalAu-Ag3.721.61, 3.72Metamorphic rock and marble [11,55]
9TaoyuanQingchengziMagmatic hydrothermalAu-Ag 0.005~0.06, 0.0025~0.1Metamorphic rock [11,56]
10BaiyundasandaogouQingchengziMagmatic hydrothermalAu-Ag 7.28, 1.28 [11,54]
11LinjiasandaogouQingchengziMagmatic hydrothermalAu 0.031, 0.034Metamorphic rock [11,56]
12YaojiagouQingchengziporphyryMo 0.34Metamorphic rock and skarn168[57,58]
13SidaogouWulongMagmatic hydrothermalAu20–50 Metamorphic rock [43]
14WulongWulongMagmatic hydrothermalAu>40 Metamorphic rock and quartz veins122[43,59]
15WangjiawaiziMaolingMagmatic hydrothermalAu-Ag>58.9, 16.9Metamorphic rock, quartz veins and Breccia [60]
16MaolingMaolingMagmatic hydrothermalAu253.2 g/tMetamorphic rock and quartz veins196[44]
17FenshuiMaolingMagmatic hydrothermalAu1.83~5Quartz veins186[61]

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Zhang, Z.; Wang, Y.; Li, D.; Lai, C. Lithospheric Architecture and Metallogenesis in Liaodong Peninsula, North China Craton: Insights from Zircon Hf-Nd Isotope Mapping. Minerals 2019, 9, 179. https://doi.org/10.3390/min9030179

AMA Style

Zhang Z, Wang Y, Li D, Lai C. Lithospheric Architecture and Metallogenesis in Liaodong Peninsula, North China Craton: Insights from Zircon Hf-Nd Isotope Mapping. Minerals. 2019; 9(3):179. https://doi.org/10.3390/min9030179

Chicago/Turabian Style

Zhang, Zhichao, Yuwang Wang, Dedong Li, and Chunkit Lai. 2019. "Lithospheric Architecture and Metallogenesis in Liaodong Peninsula, North China Craton: Insights from Zircon Hf-Nd Isotope Mapping" Minerals 9, no. 3: 179. https://doi.org/10.3390/min9030179

APA Style

Zhang, Z., Wang, Y., Li, D., & Lai, C. (2019). Lithospheric Architecture and Metallogenesis in Liaodong Peninsula, North China Craton: Insights from Zircon Hf-Nd Isotope Mapping. Minerals, 9(3), 179. https://doi.org/10.3390/min9030179

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