Next Article in Journal
Xenophyllite, Na4Fe7(PO4)6, an Exotic Meteoritic Phosphate: New Mineral Description, Na-ions Mobility and Electrochemical Implications
Next Article in Special Issue
Genesis of Early–Middle Jurassic Intrusive Rocks in the Erguna Block (NE China) in Response to the Late-Stage Southward Subduction of the Mongol–Okhotsk Oceanic Plate: Constraints from Geochemistry and Zircon U–Pb Geochronology and Lu–Hf Isotopes
Previous Article in Journal
Element Patterns of Primary Low-Magnesium Calcite from the Seafloor of the Gulf of Mexico
Previous Article in Special Issue
Provenance and Implication of Carboniferous–Permian Detrital Zircons from the Upper Paleozoic, Southern Ordos Basin, China: Evidence from U-Pb Geochronology and Hf Isotopes
 
 
Search for Articles:
Title / Keyword
Author / Affiliation / Email
Journal
Article Type
 
 
Advanced Search
 
Section
Special Issue
Volume
Issue
Number
Page
 
Journals
Minerals
Volume 10
Issue 4
10.3390/min10040301
minerals-logo
Submit to this Journal Review for this Journal Propose a Special Issue
► Article Menu

Article Menu

share Share announcement Help format_quote Cite question_answer Discuss in SciProfiles thumb_up
...
Endorse textsms
...
Comment
first_page
settings
Order Article Reprints
Font Type:
Arial Georgia Verdana
Font Size:
Aa Aa Aa
Line Spacing:
Column Width:
Background:
Article

Petrogenesis and Geological Implications of the Oligocene Mingze monzodiorites, Southern Lhasa

by
Kailiang Zhang
1,*,
Zeming Shi
1,2,*,
Rong Liao
1 and
Feilin Zhu
1,2
1
College of Earth Science, Chengdu University of Technology, Chengdu 610059, China
2
Applied Nuclear Technology in Geosciences Key Laboratory of Sichuan Province, Chengdu University of Technology, Chengdu 610059, China
*
Authors to whom correspondence should be addressed.
Minerals 2020, 10(4), 301; https://doi.org/10.3390/min10040301
Submission received: 25 February 2020 / Revised: 18 March 2020 / Accepted: 25 March 2020 / Published: 27 March 2020
(This article belongs to the Special Issue U-Pb Dating and Chemistry of Zircon in Metamorphic, Magmatic and Sedimentary Rocks)
Browse Figures
Versions Notes

Abstract

:
The Mingze Cu-Mo deposit is located in the southern margin of the Lhasa block of the Himalayan Tibetan Plateau. Here, we report the geochronological and geochemical data from Mingze monzodiorites, which hosts the Mingze deposit. Zircon dating indicates that the Mingze monzodiorites were emplaced at ca. 31 Ma (i.e., the Oligocene). The monzodiorites have variable SiO2 and MgO contents, strongly negative high field-strength element (HFSE, such as Ta, Nb, Zr and Hf) anomalies on the normalized trace element diagram and show uniform (87Sr/86Sr)i (0.7066–0.7076), εNd(t) (−2.50 to −4.04) and εHf(t) (+1.50 to +7.50). Their geochemical compositions are different from coeval (40–30 Ma) adakite-like rocks but comparable to coeval mafic enclaves and gabbros. We propose that Mingze monzodiorites were derived from partial melting of the lithospheric mantle, which previously metasomatized by the subducted Indian continental plate that probably subducted into the overlying mantle. The concurrency of the genetically related mafic enclaves and associated intermediate to mafic rocks implies the heterogeneity of the Lhasa lower crust.

1. Introduction

The Himalayan Tibetan Plateau is interpreted as the result of the Cenozoic collision between the Indian and Asian continents and subsequent continental subduction. It is considered as the most outstanding natural laboratory for studying the evolution of a continental collision orogenesis [1]. The Lhasa block is part of the Tibetan Plateau and an archetype of a Cenozoic collisional orogen related to the India–Asia collision [1,2,3,4,5]. Thus far, it has attracted much attention from numerous scholars.
The Mingze deposit is located in the Gangdese Kelu-Chongmuda metallogenic belts, which include the Chongmuda Cu-Au deposit, Chengba Cu-Mo deposit, Nuri Cu-Mo-Au deposit and Mingze Cu deposit [6]. Most of the previous studies were concentrated on the Chongmuda, Nuri and Chengba deposit, whereas the Mingze deposit was relatively understudied. Moreover, numerous previous geochronological works have been conducted, though few integrate the geochronologic data with petrogenesis studies [7,8,9,10,11]. The Mingze deposit is regionally near to the Chengba deposit (~500 m), and people could have treated them as equivalent. In reality, their genesis and ore-associated intrusions are different as pointed out in this study.
In recent years, the Oligocene to the Miocene adakite-like rocks, which are mostly acid granitoid, have gotten plenty of attention, while the Late Eocene to the Oligocene intermediate-basic rocks have gotten far less interest [2,6,7,9,12,13,14,15,16]. In fact, the adakite-like rocks commonly contain a large number of mafic enclaves [17,18], which possibly derived from the enriched lithospheric mantle. However, most of the mafic enclaves may have undergone a certain degree of evolution. Thus, it is hard to address the mantle enriching process through the studies of the mafic enclaves. Various models of the mantle enrichment have been proposed, including (1) metasomatized by the partial melting of the Neo-Tethyan Oceanic slab [2], (2) metasomatized by the Indian continental ancient sediments [19] and (3) metasomatized by the ancient crust of Central Lhasa [15]. The rocks formed as mantle-derived magma may provide an opportunity to address this issue. Furthermore, understanding the mechanism of the enrichment can also provide critical constraints on deep geodynamic processes under the Lhasa crust. However, the exact processes, such as whether the Indian continental crust was ever subducted into the Lhasa lithospheric mantle, are still unclear. On the other hand, the Eocene and Oligocene adakite-like rocks were interpreted as melts relative to the juvenile lower crust [2,9,14]. Therefore, it is worth exploring the relationship between the rocks relative to mantle and the coeval adakite-like rocks with mafic enclaves, as well as the reason for the formation of different types of rock.
In this study, we present geochronological, geochemical, and Sr-Nd-Hf isotopic data for the Mingze monzodiorites from southern Tibet. These data indicate that Mingze monzodiorites were emplaced in the Early Oligocene (~31 Ma). Moreover, their geochemical and isotopic compositions are distinct from the contemporary adakite-like rocks, but comparable to the coeval mafic enclaves observed elsewhere in granitoids and the gabbros from south Tibet. Therefore, these data provide us an opportunity to better understand the age and petrogenesis of the Mingze area and to address the processes responsible for Cu-Mo ore genesis.

2. Geologic Background

The Tibetan Plateau area is located in southwestern China (Figure 1a) and consists of four continental blocks. From south to north, they are the Himalaya, the Lhasa, the Qiangtang and the Songpan-Ganze blocks. The Lhasa block is bound by the Indus-Yarlung Tsangpo suture (IYTS) to the south and the Bangong–Nujiang suture (BNS) to the north [1].
The Lhasa block has been separated into a northern, central and southern sub-block by the Shiquan River–Nam Tso Mélange zone (SNMZ) and Luobadui-Milashan fault (LMF), respectively (Figure 1b) [21].
The central Lhasa sub-block was once a microcontinent, which acted as a nucleus for the forming of the northern and southern blocks, and it has ancient basement rocks of Proterozoic and Archean ages [21]. The southern Lhasa sub-block contains widely distributed Mesozoic to Cenozoic intrusive and volcanic rocks (Figure 1c), which are composed of Upper Jurassic–Upper Cretaceous (136–93 Ma) Sangri Formation, lower Jurassic (190–174 Ma) Yeba formation, Paleogene Linzizong volcanic rocks and Cretaceous to Eocene Gangdese granitoids [20].
The Mingze area, which is located in Zedong county of Tibet, is within the southern Lhasa sub-block south of Yalung Tsangpo River. The Mingze ore block and Chengba ore block, named after their respective region, are also collectively named the Mingze deposit (Figure 1d) [6].
Zheng et al. [7] studied the Chengba granitoids, which were treated as Mingze rocks. The Mingze deposit is a typical skarn Cu deposit. The strata in the Mingze Cu deposit are mainly Triassic metamorphic siltstone, Cretaceous metamorphic siltstone, andesitic tuff and sericite hornfels. In this study, we focused on the petrogenesis of the monzodiorites from the area containing the Mingze Cu deposit.

3. Samples and Methods

Seven monzodiorite samples were collected from the least altered out crops of the Mingze Cu deposit. The Mingze monzodiorites show a typical massive structure and a medium-grained granular texture (Figure 2a,b). These monzodiorites are mainly composed of plagioclase (55–60%), K-feldspar (15–20%) and amphibole (10–15%), with minor amounts of pyroxene, quartz, biotite, epidote and zircon (Figure 2c,d). Some minerals have suffered slight alteration, such as Fe oxides occurring along the margins of biotites. Plagioclase and K-feldspar crystals are euhedral or subhedral, whereas quartz crystals are subhedral grains and show rounded outlines. Amphibole grains are subhedral and their colors range from yellow to brown. All samples were analyzed for whole-rock major- and trace-element geochemistry, five of which were further analyzed for whole-rock Sr-Nd isotopes, and a sample was selected for laser-ablation inductively coupled plasma mass spectrometer (LA-ICP-MS) zircon U-Pb isotope and in situ Hf isotope analyses.
Zircon crystals separation was performed by Yuneng Rock Ore Sorting Technique Services Limited, who used conventional heavy liquid and magnetic separation techniques [22]. After separation, zircons for U-Pb and Lu-Hf isotopic detection were handpicked under a binocular microscope, and then mounted on epoxy resin discs.
The zircon U-Pb ages and cathodoluminescence (CL) images were provided by Wuhan Sample-Solution Analytical Technology Co., Ltd. The instrument for the zircon U-Pb isotopic detection used an Agilent 7700 LA-ICP-MS (Agilent, Santa Clara, CA, USA) and a 193 nm excimer laser ablation system. For this study, the ablation spot size was set to 32 μm, the ablated material was carried by He-Ar gas and the external standard used for U-Th-Pb isotopic ratios was the Harvard zircon 91500 [23]. Details of the analytical technique are provided by [24]. All the calculations and Concordia diagrams were completed using Isoplot 3.0 [25].
In situ Lu-Hf isotopic detections were conducted at the Geochemistry Lab of College of Earth sciences, Chengdu University of Technology, Chengdu, China by using a Finnigan Neptune Plus multicollector inductively coupled plasma mass spectrometer (MC-ICP-MS) and a Coherent GeoLasPro 193-nm laser-ablation system. The detections were performed on the same zircons, which had been analyzed for U-Pb ages. Details of the analytical technique are provided by [26].
The major and trace element analyses were performed by the ALS Chemex (ALS Limited, Guangzhou, China). The Samples for major element analyses were prepared with lithium borate–lithium nitrate solvent and detected by X-ray fluorescence (XRF) with detection limits of 0.01 wt.%. The Samples for trace element analyses were prepared with lithium borate solvent and detected by ICP-MS.
High precision isotopic (Sr, Nd) measurements were carried out at Nanjing FocuMS Technology Co. Ltd (Nanjing, China). The Sr-, Nd- bearing elution were dried down and re-dissolved in 1.0 mL 2 wt.% HNO3. Small aliquots of each were analyzed using an Agilent Technologies 7700x quadrupole ICP-MS (Hachioji, Tokyo, Japan) to determine the Sr, Nd abundances. Raw data of isotopic ratios were corrected for mass fractionation by normalizing to 86Sr/88Sr = 0.1194 for Sr, 146Nd/144Nd = 0.7219 for Nd with exponential law. International isotopic standards (NIST SRM 987 for Sr, JNdi-1 for Nd) were periodically analyzed to correct instrumental drift. Geochemical reference materials of USGS BCR-2, BHVO-2, AVG-2 and RGM-2 were used as quality control [27].

4. Results

4.1. U-Pb Zircon Ages and Hf Isotopes

The zircons separated from the sample MZ-12 were euhedral to subhedral crystal shapes exhibiting short prismatic forms. Most of the zircons were transparent and colorless, their average size is 60–150 μm and the length-to-width ratio is from 1:1 to 3:1, and show euhedral oscillatory zoning in cathodoluminescence (CL) images (Figure 3a). Zircon analyses from sample MZ-12 presented high Th and U contents (Th = 408–4692 ppm, U = 553–3925 ppm, Table S1) and high ratios of Th/U (0.40–1.78). The features of CL images and the Th, U contents indicated that all crystals have a magmatic origin [28,29,30].
Twenty-four spots were analyzed on these zircons, and all yielded concordant 206Pb/238U ages ranging from 28.6 Ma to 34.3 Ma (Table S1). These analyses give a weighted mean age of 31.4 ± 0.6 Ma (MSWD = 7.9, 1σ for errors), which was identical to their concordant age of 34 ± 6 Ma (MSWD = 2.1) (Figure 3b,c). Thus, the weighted mean age suggested that the monzodiorites were generated in the early Oligocene.
Twenty-one Hf analyses were corrected to the magmatic crystallization age of ca. 31.4 Ma, and yielded positive εHf(t) values of +1.50 to +7.50. The values of 176Yb/177Hf and176Lu/177Hf ranged from 0.007383 to 0.083558 and 0.000194 to 0.002016, respectively (Table S2). Most values of 176Lu/177Hf were less than 0.002, indicating that those zircons had not experienced a significant accumulation of radiogenic Hf after formation; thus, these ratios can be used as a representation of the Hf isotopic composition at the time of zircon formation [26]. The single-stage Hf model ages (TDM) were 403.71 to 642.61 Ma and the two-stage ages were 632.75 to 1013.62 Ma.

4.2. Whole-Rock Geochemistry

Whole-rock major and trace-element data for rocks from the Mingze monzodiorites are presented in Table S3. The Mingze monzodiorites are mainly shoshonitic and metaluminous (Figure 4b, A/CNK = 0.67–0.91), with relatively low SiO2 contents (52.70–64.98 wt.%), high K2O contents (3.06–4.29 wt.%), relatively high MgO contents (1.86–5.76 wt.%) and Mg# values (48.39–65.57), TFe2O3 contents (3.94–7.78 wt.%).
All the samples from Mingze exhibit obvious right-dipping chondrite-normalized fractionated REE (rare earth element) patterns (Figure 5b) characterized by enrichment of LREE (light rare earth element), depletion of HREE (heavy rare earth element) [(La/Yb)N ratios (22.9–56.1)]. They also present relatively high values of total rare earth element (REE) values ranging from 228.93 ppm to 343.05 ppm. There is a slight negative anomaly (δEu = 0.68–0.81). In the primitive mantle-normalized trace element variation diagram, these samples are enriched in large-ion lithophile elements (LILEs, such as Rb, Ba, Th, U and Sr) and are depleted in high field strength element (HFSE, such as Ta, Nb, Zr and Hf) (Figure 5a).

4.3. Whole-Rock Sr-Nd Isotopes

Whole-rock Sr-Nd isotope data are presented in Table S3. All isotopic ratios were calculated using the zircon U-Pb age of 31.4 Ma. Samples have relatively low initial Sr isotopic ratios [(87Sr/86Sr)i = 0.7066–0.7076] and low εNd(t) values of −4.04 to −2.49 (Figure 6). They have high Nd model ages (TDM(Nd)) ranging from 922 Ma to 990 Ma.

5. Discussion

5.1. Coeval Magmatism in the Mingze Region

The relatively high Th/U ratios (Table S1), as well as the well-developed oscillatory growth zoning in the zircons from the Mingze monzodiorites, indicate a magmatic origin. The weighted mean age (31.4 ± 0.6 Ma) of zircon 206Pb/238U has relatively less error than the concordant age (34 ± 6 Ma). These data are within the range reported by Zheng et al., [7], who suggested that the crystallization age of Chongmuda-Mingze granodiorites and monzogranites were ~30 Ma. Mo et al. [8] reported that the crystallization age of Chongmuda monzogranites was ~28 Ma. Several Zircon U-Pb age studies have been carried out in Cenozoic granitoids from the same area. For instance, Harrison et al. [41] and Chung et al. [9] reported ages of ~30 Ma from the Chengba granodiorites, and Jiang et al. [10] provided a ~30 Ma age for the Chongmuda quartz monzogranites. The above results are consistent with this study. Accordingly, we regard ~31 Ma as the crystallization time of Mingze monzodiorites, indicating that this intrusion of Mingze was emplaced in Early Oligocene.

5.2. Petrogenesis of the Mingze Monzodiorites

5.2.1. Fractional Crystallization

The major element compositions of the Mingze monzodiorites have a large range in composition (e.g., SiO2, 52.70–64.98 wt.%), relatively low Mg# values (48.39–65.68) and Cr abundances (32–190 ppm) compared to typical mantle-derived magmas. The compositional ranges are compatible with the concepts of a combination of fractional crystallization and/or crystal accumulation [42]. This suggestion is supported by the oxides versus SiO2 and MgO diagrams (Figure 7a,c,d,f and Figure 9a,b,d), in which plots generally yield linear arrays, supporting the proposed fractional crystallization process to account for the geochemical trends.
The trend of La/Sm and Dy/Yb ratios variations are relative to the concentration of SiO2 (Figure 7h,i) suggesting the possibility of amphibole fractionation [44]. Given that Cr is compatible in clinopyroxene, the relatively good linear relationship of Cr vs. MgO (Figure 9c), the low CaO/Al2O3 ratios of 0.2–0.5 and the good linear relationship of the CaO/Al2O3 ratios vs. MgO abundances (Figure 9e) indicate that the clinopyroxene fractionation also played a significant role during the evolution of the magmatic system. Furthermore, plagioclase fractionation is supported by a slight negative Eu anomaly (Figure 5b, δEu = 0.68–0.81). Neither layered structure in the outcrop nor textural evidence for crystal accumulation in thin sections have been observed. Together with the negative Eu anomaly, this precludes the possibility of crystal accumulation or that the initial source rock was relatively depleted in Eu2+.

5.2.2. Mechanism of Enriched Lithosphere Mantle

The relatively low (87Sr/86Sr)i (0.7077 to 0.7076) and negative εNd(t) (−2.49 to −4.04) of Mingze monzodiorites differ from the coeval Dagze mafic rocks (40–38 Ma, εNd(t), +5.2 to +3.6; (87Sr/86Sr)i, 0.7044–0.7062), which are 50 km east to Mingze and likely originated from an enriched asthenospheric mantle source [35]. The Yeba volcanic rocks (εNd(t), +2.4 to +4.5; (87Sr/86Sr)i, 0.70427–0.70505) and the Linzizong volcanic rocks (e.g., ultrapotassic, εNd(t), −6.1 to +0.7; (87Sr/86Sr)i, 0.7058–0.7140) in southern Tibet with depleted mantle isotopic compositions [26,32] further indicate that the Mingze monzodiorites did not originate from a relatively depleted mantle source region. However, the isotopic signatures of Mingze monzodiorites are similar to the coeval basaltic dykes (εNd(t), −3.1 to −0.3; (87Sr/86Sr)i, 0.7066–0.7088) in the Gaoligong–Tengliang belt of 40–42 Ma [29], as well as to ∼30 Ma Chengba mafic enclaves (εNd(t), −2.6 to −4.9; (87Sr/86Sr)i, 0.7060–0.7072) [25]. We suggest that the monzodiorites and mafic enclaves both originated from enriched lithospheric mantle beneath the Lhasa terrane. The coeval mafic enclaves in the Wolong granitoids (εNd(t), −2.7 to −1.4; (87Sr/86Sr)i, 0.7053–0.7055) of ~38 Ma [24] and coeval Quguosha gabbros (~35 Ma, εNd(t), −2.2 to −3.6; (87Sr/86Sr)i, 0.7056–0.7058) [26] (Figure 6b), which are lithospheric mantle-derived, further indicate that the Mingze monzodiorites were derived from enriched lithospheric mantle beneath the Lhasa terrane.
Additionally, Mingze monzodiorites are characterized by relatively large content ranges of MgO (1.86–5.76 wt.%), Mg# (48.39–65.58), SiO2 (52.70–64.98 wt.%) and TFe2O3 (3.94–7.78 wt.%), which are not similar to typical crustal materials nor to mantle materials. Mingze monzodiorites are enriched in LILEs (e.g., Rb, Ba, Th and U) and LREE, and depleted in HFSEs (e.g., Ta, Nb, Zr and Hf) (Figure 5). These features collectively suggest that the origin of Mingze monzodiorites were derived as melts from an enriched mantle and/or mantle-derived mafic magmas that experienced crustal contamination. The following mechanisms can explain these geochemical features above: (1) magma mixing of mantle- and crustal-derived members, (2) crustal contamination and (3) metasomatism by an older source material within subduction or thickened crustal delamination [45].
The SiO2 and MgO contents of Mingze monzodiorites are variable, and Mg# values of Mingze monzodiorites are lower than the mantle melt but higher than the partial melting of crustal materials (Figure 7g). These features are consistent with those of the mantle mafic enclaves in adakite-like rocks, which were generated by the mixing of mantle- and crustal-derived magmas. However, relatively homogeneous Sr-Nd- Hf isotopic compositions ((87Sr/86Sr)i, 0.7066–0.7076; εNd(t),−2.50 to −4.04;εHf(t), +1.50 to +7.50; Figure 6a,b) and the absence of linear trend between isotopic ratios and certain elements (e.g., SiO2 and MgO) in the Mingze monzodiorites are inconsistent with the magma mixing model (Figure 8). Thus, the magma mixing model is not favored in this study.
Crustal contamination is almost inevitable during the ascent of mantle-derived melts through the continental crust [46]. In addition, crustal assimilation during magma ascent can cause an increase in (87Sr/86Sr)i and a decrease in εNd(t) as the magmas are emplaced in the upper crust [47]. Therefore, we can compare major elements and radiogenic isotopes compositions to evaluate the effect of crustal contamination on basaltic rocks [16,20]. The data show that the (87Sr/86Sr)i and εNd(t) do not vary with respect to MgO and SiO2 contents (Figure 8). This feature suggests limited crustal assimilation. The suggestion is further supported by the following evidence: (1) absence of a correlation between the Sr content, Lu/Yb and Zr/Hf ratios with SiO2 contents (Figure 7j–l); (2) the relatively homogenous zircon εHf(t) (+1.50 to +7.46), which argues for little or no crustal contamination involved in the parental magma [48]; (3) the negative Zr-Hf anomalies in the N-MORB-normalized trace element diagram (Figure 5a), which suggest the parent magmas might have not undergone crustal contamination, because crustal assimilation during emplacement would result in positive Zr and Hf anomalies [49]. Therefore, we conclude that crustal contamination played an insignificant role in the formation of the Mingze monzodiorites.
Metasomatism in lithospheric mantle could possibly have been triggered by both subduction and thickened crustal delamination [50,51]. However, the coeval Chengba-Chongmuda (~30 Ma) and Linzi (~28 Ma) adakitic intrusions have been interpreted as a partial melting of the lower crust that contained a certain amount of juvenile mantle-derived basaltic melts [7,52]. However, Mingze monzodiorites exhibited different major element compositions from those coeval adakite-like rocks (Figure 4, Figure 7 and Figure 9). This probably suggests that Mingze monzodiorites have different origin compared to those adakite-like rocks and have insignificant affinity to thickened crustal delamination (Figure 4d). We suggest, therefore, that the parent magma of Mingze monzodiorites was metasomatized by an older source material within a subduction setting.
The Mingze monzodiorites with relatively high MgO abundances (up to 5.76 wt.%) and Mg# (up to 65.58), low SiO2 (52.7–64.98 wt.%) contents suggest that these monzodiorites could originally have been basaltic in composition. Oceanic basalts (i.e., mid-ocean ridge basalts [MORBs] and ocean island basalts [OIBs]) typically exhibit positive Nb-Ta-Ti anomalies in primitive-mantle-normalized trace element diagrams [53]. However, all the Mingze samples exhibit significantly negative Nb-Ta anomalies (Figure 5a). Moreover, Th/Ce (0.21–0.49) and Th/La (0.39–0.91) of the Mingze monzodiorites are much higher than mantle-derived magmas, with low Th/Ce (0.02–0.05) and Th/La (~0.12) [32]. These features collectively suggest neither normal MORB- nor OIB-mantle material can be the source of Mingze monzodiorites. This suggestion is also supported by the diagram of εNd(t) versus εHf(t) (Figure 10a).
In the Lu/Yb ratio and Zr/Hf ratio versus SiO2 contents diagrams, some of the Mingze monzodiorites plotted in or near the field of crust composition (Figure 7k,l) suggest their continental arc affinity. This suggestion is supported by εNd(t) versus εHf(t) plots that shift away from the mantle array (Figure 10a). Moreover, whole rock Th and Nb elements are useful indicators for crustal input [54]. Thus, when no crustal contamination was involved, the Nb/Yb versus Th/Yb ratio diagram is useful for distinguishing subduction-related and subduction-unrelated rocks [55]. Plots of Mingze monzodiorites in the diagram show continental arc affinity (Figure 10b).

5.2.3. Origin of the Ancient Crustal Signature

We propose that the parental magmas of the Mingze monzodiorites were derived from the enriched lithospheric mantle metasomatized by crustal materials in a subduction setting beneath the Lhasa terrane. However, there remains uncertainty about the origin of crustal materials. Previous work has proposed three potential metasomatic agents for forming enriched lithospheric mantle beneath the Lhasa terrane: (1) ancient crust within Central Lhasa block; (2) subducted Tethyan oceanic slab; and (3) subducted Indian continental materials ([16] and references therein).
It has been proposed that Early Eocene gabbros (~53 Ma) from the Longge’er pluton in the western segment of the Gangdese batholith were derived from the partial melting of an enriched mantle wedge metasomatism by Central-Lhasa ancient crust-derived magmas [45]. However, the εHf(t) values of the Mingze monzodiorites (εHf(t) = +1.5 to +7.5) are significantly different from Longge’er gabbros (εHf(t) = −1.2 to +1.0). Positive and negative zircon εHf(t) values are attributed to juvenile and ancient crustal sources, respectively [58]. The εHf(t) data indicates that fluids derived from the ancient Central-Lhasa crust were not the source of metasomatism. Moreover, previous work has demonstrated that the ancient crustal basement rocks of Proterozoic and Archean ages exist only in the central Lhasa sub-block and there is no known mechanism to bring the basement rocks of central sub-block to the mantle beneath the southern sub-block during the Cenozoic [21,59]. Thus, we posit that no Central-Lhasa ancient crust-derived materials were involved in the origin of Mingze monzodiorites.
Lithospheric mantle metasomatized by subducted oceanic slab is generally characterized by relatively high εNd(t), low (87Sr/86Sr)i and HFSE enrichment [31,60], which is not observed in the Mingze monzodiorites. The Mingze monsodiorites have relatively low εNd(t), high (87Sr/86Sr)i and depleted HFSE. Moreover, partial melting of subducted oceanic crust is a common formation mechanism of adakite [61,62], while Mingze monzodiorites exhibited no affinity to adakitic compositions (e.g., high Sr, low Y contents, Figure 4d). Thus, we rule out the possibility of a melt of subducted oceanic crust. Late Cretaceous (~94 Ma) gabbros from Zhengga are suggested to originate from the mantle wedge metasomatized by sediment melts/fluids derived from the subducted Neo-Tethyan oceanic slab and characterized by relatively positive εNd(t) (−0.2 to +4.1) [20]. Their εNd(t) values are distinct from the Mingze monzodiorites (Figure 6b), which have negative εNd(t) (−4.04 to −2.49). Therefore, Neo-Tethyan oceanic slab can be excluded as a potential metasomatic agent.
The remaining candidate to explain the enriched mechanism of the Mingze monzodiorites magma source, therefore, is the metasomatism by subducted Indian continental materials. The εNd(t), (87Sr/86Sr)i, and εHf(t) values of the Mingze monzodiorites are quite similar to those of Quguosha gabbros, which were interpreted as the result of lithospheric mantle metasomatized by melts of Indian continental sediments (Figure 6a,b). As shown in the εNd(t) versus (87Sr/86Sr)i diagram (Figure 6b), Mingze monzodiorites exhibit a limited range of values that fall on or near a mixing line between depleted mantle and the subducted Himalayan sediments represented by the Cenozoic Himalayan leucogranites. This indicates that such rocks can be interpreted to be the result of the depleted mantle that has been, to a certain degree, metasomatized by subducted Himalayan sediments. The isotopic compositions of the Mingze monzodiorites could have been generated by the mixing of approximately 15% Himalayan sediments and 85% mantle-derived components.

5.3. Implications for Geodynamic Processes

The addition of components derived from the subducted Indian continental crust could lead to the enrichment of the upper mantle below south Tibet [63]. In addition, as mentioned above, the parent magma of the Mingze monzodiorites is compatible with an interpretation of having incorporated approximately 10–15% Himalayan-derived sediments. Moreover, Zheng et al., [7] suggested that the Indian continent subducted into the lithospheric mantle beneath the Lhasa block and accelerated the detachment of the Lhasa lithospheric root. Nábělek et al. [64] proposed that a ca. 15 km thick layer above the seismic Moho observed in the seismic cross-section is the subducted Indian lower continental crust. Taken together, the evidence suggests that the Indian continental crust had subducted into the lithospheric mantle beneath the Lhasa block before ~31 Ma.
The Mingze monzodiorites are similar in composition to those coeval mafic enclaves from Wolong and Chengba-Chongmuda, and to the gabbros from Quguosha in terms of geochemistry and petrogenesis (Figure 4, Figure 7 and Figure 9). Their crystallization ages were all about 40–30 Ma, implying that they originated from the same magmatic system that resulted from partial melts from an enriched lithospheric mantle. This system not only formed intermediate-basic intrusions, but also formed the mafic enclaves in granitoids. Chengba-Chongmuda and Wolong adakite-like rocks, which are the host rocks of the mafic enclaves, are interpreted as the results of partial melting of thickened low crust under the Lhasa terrane. The heat source for lower crust melting was proposed to be the intrusion of mantle-derived magma [7,15]. Thus, the presence of coeval mafic enclaves and intermediate-basic composition intrusions allows for two possibilities: (1) mantle-derived magma melted a part of the lower crust and mixed with it, then formed adakite-like rocks with mafic enclaves or (2) the mantle-derived magma did not melt the lower crust, yet formed as intermediate-basic intrusions. These possibilities suggest that the mantle-derived magma was heterothermal or that a different part the lower crust had a different melt point. The suggestion implies that the presence of coeval mafic enclaves and intermediate-basic intrusions is due to either the heterogeneity of the mantle-derived magma or the heterogeneity of the lower crust. It is hard to imagine heterogeneous mantle-derived magma forming similar rocks. In addition, the relatively homogeneous Sr-Nd-Hf (Figure 6) isotopic compositions of those rocks conflict with the heterogeneity of the mantle-derived magma. However, variable degrees of modification, by the underplated mantle-derived basaltic melts at the base of the Lhasa crust, can lead to heterogeneity [21,65,66]. Therefore, we proposed that the lower crust is highly heterogeneous in composition along the strike of the Lhasa terrane, and that the heterogeneity of the lower crust led to the concurrency of the intermediate-basic intrusions and adakite-like rocks with mafic enclaves.

6. Conclusions

  • The Mingze monzodiorites in southern Tibet were emplaced in the Early Oligocene (~31 Ma).
  • The Mingze monzodiorites are the result of partial melting of the lithospheric mantle beneath the Lhasa terrane metasomatized by melts of Indian continental sediments.
  • The Indian continental crust was subducted into the lithospheric mantle beneath the Lhasa block prior to ~30 Ma.
  • The concurrency of mafic enclaves and intermediate intrusions (~40 to 30 Ma) indicates that the lower crust is heterogeneous along the strike of the Lhasa terrane.

Supplementary Materials

The following are available online at https://www.mdpi.com/2075-163X/10/4/301/s1, Table S1: LA-ICP-MS zircon U-Pb age data for the Mingze monzodiorites, Table S2: In-situ zircon Hf isotopic data of for the Mingze monzodiorites, Table S3: Major (wt.%), trace element (ppm) and Sr-Nd isotopic composition of the Mingze monzodiorites.

Author Contributions

Wrote the paper, K.Z.; designed the experiments, Z.S. and F.Z.; took part in the data collection, R.L. All authors have read and agreed to the published version of the manuscript.

Funding

This study was funded by the China Geological Survey (grant no. 12120113095700, 121201010000150011-08).

Acknowledgments

The authors thank Fuhao Xiong for the zircon U–Pb dating. The authors are grateful to the critical and thoughtful comments from the editors and the anonymous reviewers, which profoundly enhanced the quality of this manuscript.

Conflicts of Interest

The authors declare no conflict of interest.

References

  1. Yin, A.; Harrison, T.M. Geologic evolution of the Himalayan-Tibetan orogen. Annu. Rev. Earth Planet. Sci. 2000, 28, 211–280. [Google Scholar] [CrossRef] [Green Version]
  2. Mo, X.X.; Hou, Z.Q.; Niu, Y.L.; Dong, G.C.; Qu, X.M.; Zhao, Z.D.; Yang, Z.M. Mantle contributions to crustal thickening during continental collision: Evidence from Cenozoic igneous rocks in southern Tibet. Lithos 2007, 96, 225–242. [Google Scholar] [CrossRef]
  3. Mo, X.X.; Niu, Y.L.; Dong, G.C.; Zhao, Z.D.; Hou, Z.Q.; Zhou, S.; Ke, S. Contribution of syncollisional felsic magmatism to continental crust growth: A case study of the Paleogene Linzizong volcanic Succession in southern Tibet. Chem. Geol. 2008, 250, 49–67. [Google Scholar] [CrossRef]
  4. Aitchison, J.C.; Xia, X.P.; Baxter, A.T.; Ali, J.R. Detrital zircon U-Pb ages along the Yarlung-Tsangpo suture zone, Tibet: Implications for oblique convergence and collision between India and Asia. Gondwana Res. 2011, 20, 691–709. [Google Scholar] [CrossRef]
  5. Xia, L.Q.; Li, X.M.; Ma, Z.P.; Xu, X.Y.; Xia, Z.C. Cenozoic volcanism and tectonic evolution of the Tibetan plateau. Gondwana Res. 2011, 19, 850–866. [Google Scholar] [CrossRef]
  6. Sun, X.; Zheng, Y.Y.; Wu, S.; You, Z.M.; Wu, X.; Li, M.; Zhou, T.C.; Dong, J. Mineralization age and petrogenesis of associated intrusions in the Mingze-Chengba porphyry-skarn Mo-Cu deposit, Gangdese. Acta Petrol. Sin. 2013, 29, 1392–1406. (In Chinese) [Google Scholar]
  7. Zheng, Y.C.; Hou, Z.Q.; Li, W.; Liang, W.; Huang, K.X.; Li, Q.Y.; Sun, Q.Z.; Fu, Q.; Zhang, S. Petrogenesis and Geological Implications of the Oligocene Chongmuda-Mingze Adakite-Like Intrusions and Their Mafic Enclaves, Southern Tibet. J. Geol. 2012, 120, 647–669. [Google Scholar] [CrossRef]
  8. Mo, J.H.; Liang, H.Y.; Yu, H.X.; Chen, Y.; Sun, W.D. Zircon U-Pb age of biotite hornblende monzonitic granite for Chongmuda Cu-Au (Mo) deposit in Gangdese belt, Xizang, China and its implications. Geochemica 2008, 3, 206–212. [Google Scholar]
  9. Chung, S.L.; Chu, M.F.; Ji, J.Q.; O’Reilly, S.Y.; Pearson, N.J.; Liu, D.Y.; Lee, T.Y.; Lo, C.H. The nature and timing of crustal thickening in southern Tibet: Geochemical and zircon Hf isotopic constraints from post collisional adakites. Tectonophysics 2009, 477, 36–48. [Google Scholar] [CrossRef]
  10. Jiang, Z.Q.; Wang, Q.; Wyman, D.A.; Tang, G.J.; Jia, X.H.; Yang, Y.H.; Yu, H.X. Origin of ~30 Ma Chongmuda adakitic intrusive rocks in southern Gangdese region, southern Tebit: Partial melting of the northward subducted Indian continent crust? Geochemica 2011, 40, 126–146. (In Chinese) [Google Scholar]
  11. Chen, L.; Qin, K.Z.; Li, G.M.; Li, J.X.; Xiao, B.; Zhao, J.X.; Fan, X. Zircon U-Pb ages, geochemistry, and Sr-Nd-Pb-Hf isotopes of the Nuri intrusive rocks in the Gangdese area, southern Tibet: Constraints on timing, petrogenesis, and tectonic transformation. Lithos 2015, 212, 379–396. [Google Scholar] [CrossRef]
  12. Williams, H.; Turner, S.; Kelley, S.; Harris, N. Age and composition of dikes in Southern Tibet: New constraints on the timing of east-west extension and its relationship to postcollisional volcanism. Geology 2001, 29, 339–342. [Google Scholar] [CrossRef]
  13. Chung, S.L.; Liu, D.Y.; Ji, J.Q.; Chu, M.F.; Lee, H.Y.; Wen, D.J.; Lo, C.H.; Lee, T.Y.; Qian, Q.; Zhang, Q. Adakites from continental collision zones: Melting of thickened lower crust beneath southern Tibet. Geology 2003, 31, 1021–1024. [Google Scholar] [CrossRef] [Green Version]
  14. Hou, Z.Q.; Gao, Y.F.; Qu, X.M.; Rui, Z.Y.; Mo, X.X. Origin of adakitic intrusives generated during mid-Miocene east-west extension in southern Tibet. Earth Planet. Sci. Lett. 2004, 220, 139–155. [Google Scholar] [CrossRef]
  15. Guan, Q.; Zhu, D.C.; Zhao, Z.D.; Dong, G.C.; Zhang, L.L.; Li, X.W.; Liu, M.; Mo, X.X.; Liu, Y.S.; Yuan, H.L. Crustal thickening prior to 38 Ma in southern Tibet: Evidence from lower crust-derived adakitic magmatism in the Gangdese Batholith. Gondwana Res. 2012, 21, 88–99. [Google Scholar] [CrossRef]
  16. Ma, L.; Wang, Q.; Li, Z.X.; Wyman, D.A.; Yang, J.H.; Jiang, Z.Q.; Liu, Y.S.; Gou, G.N.; Guo, H.F. Subduction of Indian continent beneath southern Tibet in the latest Eocene (similar to 35 Ma): Insights from the Quguosha gabbros in southern Lhasa block. Gondwana Res. 2017, 41, 77–92. [Google Scholar] [CrossRef]
  17. Hou, Z.Q.; Cook, N.J. Metallogenesis of the Tibetan collisional orogen: A review and introduction to the special issue. Ore Geol. Rev. 2009, 36, 2–24. [Google Scholar] [CrossRef]
  18. Yang, Z.M.; Hou, Z.Q.; White, N.C.; Chang, Z.S.; Li, Z.Q.; Song, Y.C. Geology of the post-collisional porphyry copper-molybdenum deposit at Qulong, Tibet. Ore Geol. Rev. 2009, 36, 133–159. [Google Scholar] [CrossRef]
  19. Mo, X.X.; Dong, G.C.; Zhao, Z.D.; Zhu, D.C.; Zhou, S.; Niu, Y.L. Mantle Input to the Crust in Southern Gangdese, Tibet, during the Cenozoic: Zircon Hf Isotopic Evidence. J. Earth Sci. 2009, 20, 241–249. [Google Scholar] [CrossRef]
  20. Ma, L.; Wang, Q.; Wyman, D.A.; Jiang, Z.Q.; Yang, J.H.; Li, Q.L.; Gou, G.N.; Guo, H.F. Late Cretaceous crustal growth in the Gangdese area, southern Tibet: Petrological and Sr-Nd-Hf-O isotopic evidence from Zhengga diorite-gabbro. Chem. Geol. 2013, 349, 54–70. [Google Scholar] [CrossRef]
  21. Zhu, D.C.; Zhao, Z.D.; Niu, Y.L.; Mo, X.X.; Chung, S.L.; Hou, Z.Q.; Wang, L.Q.; Wu, F.Y. The Lhasa Terrane: Record of a microcontinent and its histories of drift and growth. Earth Planet. Sci. Lett. 2011, 301, 241–255. [Google Scholar] [CrossRef]
  22. AutKeith, N.S.; Richard, A.S. An investigation of artificial biasing in detrital zircon U-Pb geochronology due to magnetic separation in sample preparation. Geochim. Cosmochim. Acta 2002, 66, 2379–2397. [Google Scholar]
  23. Wiedenbeck, M.; Alle, P.; Corfu, F. Three Natural Zircon Standards for U-Th-Pb, Lu-Hf, Trace Element and REE Analyses. Geostand. Geoanal. Res. 1995, 19, 1–23. [Google Scholar] [CrossRef]
  24. Yongsheng, L.; Zhaochu, H.; Shan, G.; Günther, D.; Juan, X.; Changgui, G.; Haihong, C. In situ analysis of major and trace elements of anhydrous minerals by LA-ICPMS without applying an internal standard. Chem. Geol. 2008, 257, 34–43. [Google Scholar]
  25. Ludwig, K.R. Berkeley Geochronology Center; Berkeley Geochronology Center: Berkeley, CA, USA, 2003. [Google Scholar]
  26. Wu, F.Y.; Yang, Y.H.; Xie, L.W.; Yang, J.H.; Xu, P. Hf isotopic compositions of the standard zircons and baddeleyites used in U-Pb geochronology. Chem. Geol. 2006, 234, 105–126. [Google Scholar] [CrossRef]
  27. Weis, D.; Kieffer, B.; Maerschalk, C.; Barling, J.; de Jong, J.; Williams, G.A.; Hanano, D.; Pretorius, W.; Mattielli, N.; Scoates, J.S.; et al. High-precision isotopic characterization of USGS reference materials by TIMS and MC-ICP-MS. Geochem. Geophys. Geosyst. 2006, 7, Q08006. [Google Scholar] [CrossRef]
  28. Corfu, F.; Hanchar, J.M.; Hoskin, P.W.O.; Kinny, P. Atlas of zircon textures. Rev. Mineral. Geochem. 2003, 53, 469–500. [Google Scholar] [CrossRef]
  29. Hoskin, P.W.O.; Schaltegger, U. The composition of zircon and igneous and metamorphic petrogenesis. Rev. Mineral. Geochem. 2003, 53, 27–62. [Google Scholar] [CrossRef]
  30. Wu, Y.B.; Zheng, Y.F. Genetic mineralogy of zircon and its constraints on the interpretation of U-Pb age. Chin. Sci. Bull. 2003, 49, 1589–1604. (In Chinese) [Google Scholar]
  31. Defant, M.J.; Drummond, M.S. Derivation of somemodern arc magmas by melting of young subducted lithosphere. Nature 1990, 347, 662–665. [Google Scholar] [CrossRef]
  32. Sun, S.S.; McDonough, W.F. Chemical and isotopic systematics of oceanic basalts: Implications for mantle composition and processes. Geol. Soc. Lond. Spec. Publ. 1989, 42, 313–345. [Google Scholar] [CrossRef]
  33. Chu, M.F.; Chung, S.L.; O’Reilly, S.Y.; Pearson, N.J.; Wu, F.Y.; Li, X.H.; Liu, D.Y.; Ji, J.Q.; Chu, C.H.; Lee, H.Y. India’s hidden inputs to Tibetan orogeny revealed by Hf isotopes of Transhimalayan zircons and host rocks. Earth Planet. Sci. Lett. 2011, 307, 479–486. [Google Scholar] [CrossRef]
  34. Xu, Y.G.; Lan, J.B.; Yang, Q.J.; Huang, X.L.; Qiu, H.N. Eocene break-off of the Neo-Tethyan slab as inferred from intraplate-type mafic dykes in the Gaoligong orogenic belt, eastern Tibet. Chem. Geol. 2008, 255, 439–453. [Google Scholar] [CrossRef]
  35. Mahoney, J.J.; Frei, R.; Tejada, M.; Mo, X.; Leat, P.; Nägler, T. Tracing the Indian Ocean mantle domain through time: Isotopic results from old West Indian, East Tethyan, and South Pacific seafloor. J. Petrol. 1998, 39, 1285–1306. [Google Scholar] [CrossRef]
  36. Wei, Y.Q.; Zhao, Z.D.; Niu, Y.L.; Zhu, D.C.; Liu, D.; Wang, Q.; Hou, Z.Q.; Mo, X.X.; Wei, J.C. Geochronology and geochemistry of the Early Jurassic Yeba Formation volcanic rocks in southern Tibet: Initiation of back-arc rifting and crustal accretion in the southern Lhasa Terrane. Lithos 2017, 278, 477–490. [Google Scholar] [CrossRef]
  37. Lee, H.Y.; Chung, S.L.; Ji, J.; Qian, Q.; Gallet, S.; Lo, C.H.; Lee, T.Y.; Zhang, Q. Geochemical and Sr-Nd isotopic constraints on the genesis of the Cenozoic Linzizong volcanic successions, southern Tibet. J. Asian Earth Sci. 2012, 53, 96–114. [Google Scholar] [CrossRef]
  38. Zhao, Z.D.; Mo, X.X.; Dilek, Y.; Niu, Y.L.; DePaolo, D.J.; Robinson, P.; Zhu, D.C.; Sun, C.G.; Dong, G.C.; Zhou, S.; et al. Geochemical and Sr-Nd-Pb-O isotopic compositions of the post-collisional ultrapotassic magmatism in SW Tibet: Petrogenesis and implications for India intra-continental subduction beneath southern Tibet. Lithos 2009, 113, 190–212. [Google Scholar] [CrossRef]
  39. Guo, Z.F.; Wilson, M. The Himalayan leucogranites: Constraints on the nature of their crustal source region and geodynamic setting. Gondwana Res. 2012, 22, 360–376. [Google Scholar] [CrossRef]
  40. Ma, L.; Wang, Q.; Wyman, D.A.; Jiang, Z.Q.; Wu, F.Y.; Li, X.H.; Yang, J.H.; Gou, G.N.; Guo, H.F. Late Cretaceous back-arc extension and arc system evolution in the Gangdese area, southern Tibet: Geochronological, petrological, and Sr-Nd-Hf-O isotopic evidence from Dagze diabases. J. Geophys. Res. Solid Earth 2015, 120, 6159–6181. [Google Scholar] [CrossRef]
  41. Harrison, T.M.; Yin, A.; Grove, M.; Lovera, O.M.; Ryerson, F.J.; Zhou, X.H. The Zedong Window: A record of superposed Tertiary convergence in southeastern Tibet. J. Geophys. Res. Solid Earth 2000, 105, 19211–19230. [Google Scholar] [CrossRef] [Green Version]
  42. Perfit, M.R.; Gust, D.A.; Bence, A.E.; Arculus, R.J.; Taylor, S.R. Chemical Characteristics of Island-Arc Basalts—Implications for Mantle Sources. Chem. Geol. 1980, 30, 227–256. [Google Scholar] [CrossRef]
  43. Zhao, X.; Fu, L.B.; Wei, J.H.; Bagas, L.; Santosh, M.; Liu, Y.; Zhang, D.H.; Zhou, H.Z. Late Permian back-arc extension of the eastern Paleo-Tethys Ocean: Evidence from the East Kunlun Orogen, Northern Tibetan Plateau. Lithos 2019, 340, 34–48. [Google Scholar] [CrossRef]
  44. Davidson, J.; Turner, S.; Handley, H.; MacPherson, C.; Dosseto, A. Amphibole “sponge” in arc crust? Geology 2007, 35, 787. [Google Scholar] [CrossRef]
  45. Zhang, Y.H.; Cao, H.W.; Hollis, S.P.; Tang, L.; Xu, M.; Jiang, J.S.; Gao, S.B.; Wang, Y.S. Geochronology, geochemistry and Sr-Nd-Pb-Hf isotopes of the Early Paleogene gabbro and granite from Central Lhasa, southern Tibet: Petrogenesis and tectonic implications. Int. Geol. Rev. 2019, 61, 868–894. [Google Scholar] [CrossRef]
  46. Castillo, P.R.; Janney, P.E.; Solidum, R.U. Petrology and geochemistry of Camiguin Island, southern Philippines: Insights to the source of adakites and other lavas in a complex arc setting. Contrib. Mineral. Petrol. 1999, 134, 33–51. [Google Scholar] [CrossRef]
  47. Rogers, N.; Macdonald, R.; Fitton, J.G.; George, R.; Smith, M.; Barreiro, B. Two mantle plumes beneath the east African rift system: Sr, Nd and Pb isotope evidence from Kenya Rift basalts. Earth Planet. Sci. Lett. 2000, 176, 387–400. [Google Scholar] [CrossRef]
  48. Griffin, W.L.; Wang, X.; Jackson, S.E.; Pearson, N.J.; O’Reilly, S.Y.; Xu, X.S.; Zhou, X.M. Zircon chemistry and magma mixing, SE China: In-situ analysis of Hf isotopes, Tonglu and Pingtan igneous complexes. Lithos 2002, 61, 237–269. [Google Scholar] [CrossRef]
  49. Zhou, M.F.; Micheal lesher, C.; Yang, Z.Z.; Li, J.W.; Sun, M. Geochemistry and petrogenesis of 270 Ma Ni-Cu-(PGE) sulfidebearing mafic intrusions in the Huangshan district, Eastern Xinjiang, Northwest China: Implications for the tectonic evolution of the Central Asian orogenic belt. Chem. Geol. 2004, 209, 233–257. [Google Scholar] [CrossRef]
  50. Aulbach, S. Craton nucleation and formation of thick lithospheric roots. Lithos 2012, 149, 16–30. [Google Scholar] [CrossRef]
  51. Gu, X.Y.; Ingrin, J.; Deloule, E.; France, L.; Xia, Q.K. Metasomatism in the sub-continental lithospheric mantle beneath the south French Massif Central: Constraints from trace elements, Li and H in peridotite minerals. Chem. Geol. 2018, 478, 2–17. [Google Scholar] [CrossRef] [Green Version]
  52. Zheng, Y.C.; Hou, Z.Q.; Li, Q.Y.; Sun, Q.Z.; Liang, W.; Fu, Q.; Li, W.; Huang, K.X. Origin of Late Oligocene adakitic intrusives in the southeastern Lhasa terrane: Evidence from in situ zircon U-Pb dating, Hf-O isotopes, and whole-rock geochemistry. Lithos 2012, 148, 296–311. [Google Scholar] [CrossRef]
  53. Hofmann, A.W.; Jochum, K.P.; Seufert, M.; White, W.M. Nb and Pb in Oceanic Basalts—New Constraints on Mantle Evolution. Earth Planet. Sci. Lett. 1986, 79, 33–45. [Google Scholar] [CrossRef]
  54. Pearce, J.A. Geochemical fingerprinting of oceanic basalts with applications to ophiolite classification and the search for Archean oceanic crust. Lithos 2008, 100, 14–48. [Google Scholar] [CrossRef]
  55. Dilek, Y.; Furnes, H. Ophiolite genesis and global tectonics: Geochemical and tectonic fingerprinting of ancient oceanic lithosphere. Geol. Soc. Am. Bull. 2011, 123, 387–411. [Google Scholar] [CrossRef]
  56. Wang, R.Q.; Qiu, J.S.; Yu, S.B.; Lin, L.; Xu, H. Magma mixing origin for the Quxu intrusive complex in southern Tibet: Insights into the early Eocene magmatism and geodynamics of the southern Lhasa subterrane. Lithos 2019, 328, 14–32. [Google Scholar] [CrossRef]
  57. Chauvel, C.; Marini, J.C.; Plank, T.; Ludden, J.N. Hf-Nd input flux in the Izu-Mariana subduction zone and recycling of subducted material in the mantle. Geochem. Geophys. Geosyst. 2009, 10, Q01001. [Google Scholar] [CrossRef]
  58. Iizuka, T.; Yamaguchi, T.; Itano, K.; Hibiya, Y.; Suzuki, K. What Hf isotopes in zircon tell us about crust-mantle evolution. Lithos 2017, 274, 304–327. [Google Scholar] [CrossRef]
  59. Ma, L.; Wang, B.D.; Jiang, Z.Q.; Wang, Q.; Li, Z.X.; Wyman, D.A.; Zhao, S.R.; Yang, J.H.; Gou, G.N.; Guo, H.F. Petrogenesis of the Early Eocene adakitic rocks in the Napuri area, southern Lhasa: Partial melting of thickened lower crust during slab break-off and implications for crustal thickening in southern Tibet. Lithos 2014, 196, 321–338. [Google Scholar] [CrossRef]
  60. Yang, C.H.; Xu, W.L.; Yang, D.B.; Wang, W.; Wang, W.D.; Liu, J.M. Petrogenesis of Shangyu gabbro-diorites in western Shandong: Geochronological and geochemical evidence. Sci. Chin. Ser. D Earth Sci. 2008, 51, 481–492. [Google Scholar] [CrossRef]
  61. Qu, X.M.; Hou, Z.Q.; Li, Y.G. Melt components derived from a subducted slab in late orogenic ore-bearing porphyries in the Gangdese copper belt, southern Tibetan plateau. Lithos 2004, 74, 131–148. [Google Scholar] [CrossRef]
  62. Zhao, Z.D.; Mo, X.X.; Zhang, S.Q.; Guo, T.Y.; Zhou, S.; Dong, G.C.; Wang, Y. Post-collisional magmatism in Wuyu basin, central Tibet: Evidence for recycling of subducted Tethyan oceanic crust. Sci. Chin. Ser. D Earth Sci. 2001, 44, 27–34. [Google Scholar] [CrossRef]
  63. Guo, Z.F.; Wilson, M.; Zhang, M.L.; Cheng, Z.H.; Zhang, L.H. Post-collisional Ultrapotassic Mafic Magmatism in South Tibet: Products of Partial Melting of Pyroxenite in the Mantle Wedge Induced by Roll-back and Delamination of the Subducted Indian Continental Lithosphere Slab. J. Petrol. 2015, 56, 1365–1405. [Google Scholar] [CrossRef]
  64. Nabelek, J.; Hetenyi, G.; Vergne, J.; Sapkota, S.; Kafle, B.; Jiang, M.; Su, H.; Chen, J.; Huang, B.S.; Hi, C.T. Underplating in the Himalaya-Tibet collision zone revealed by the Hi-CLIMB experiment. Science 2009, 325, 1371–1374. [Google Scholar] [CrossRef]
  65. Mo, X.Z.; Dong, G.C.; Zhao, Z.D.; Guo, T.Y.; Wang, L.; Chen, T. Timing of magma mixing in the Gangdise magmatic belt during the India-Asia collision: Zircon SHRIMP U-Pb dating. Acta Geol. Sin. Engl. 2005, 79, 66–76. [Google Scholar]
  66. Annen, C.; Blundy, J.D.; Sparks, R.S.J. The genesis of intermediate and silicic magmas in deep crustal hot zones. J. Petrol. 2006, 47, 505–539. [Google Scholar] [CrossRef] [Green Version]
Minerals 10 00301 g001 550
Figure 1. (a–c) Simplified geological map of the Tibetan Plateau and magmatic rocks in the Lhasa Block of southern Tibet (modify from [20] and references therein). (d) Geologic sketch map of the Mingze skarn Cu–Mo deposit (modified from No.2 Geological Institute of the China Metallurgical Geology Bureau (CMGB), 2011). Abbreviations: SL = Southern Lhasasub-block, CL = Central Lhasa sub-block, NL = Northern Lhasa sub-block, IYTSZ = Indus-Yarlung Tsangpo Suture Zone, LMF = Luobadui-Milashan Faul, SNMZ = Shiquan River-Nam Tso Mélange Zone, BNSZ = Bangong-Nujiang suture zone JSSZ = Jinsha suture zone.
Figure 1. (a–c) Simplified geological map of the Tibetan Plateau and magmatic rocks in the Lhasa Block of southern Tibet (modify from [20] and references therein). (d) Geologic sketch map of the Mingze skarn Cu–Mo deposit (modified from No.2 Geological Institute of the China Metallurgical Geology Bureau (CMGB), 2011). Abbreviations: SL = Southern Lhasasub-block, CL = Central Lhasa sub-block, NL = Northern Lhasa sub-block, IYTSZ = Indus-Yarlung Tsangpo Suture Zone, LMF = Luobadui-Milashan Faul, SNMZ = Shiquan River-Nam Tso Mélange Zone, BNSZ = Bangong-Nujiang suture zone JSSZ = Jinsha suture zone.
Minerals 10 00301 g001
Minerals 10 00301 g002 550
Figure 2. Photographs and photomicrographs of Mingze monzodiorites. (a) and (b): Two selected hand specimens of monzodiorite. (c) and (d): Mineral assemblage of monzodiorite. Abbreviations: Qz—quartz, Pl—plagioclase, Kfs—K-feldspar, Pyr—pyroxene, Amp—amphibole, Bt—biotite.
Figure 2. Photographs and photomicrographs of Mingze monzodiorites. (a) and (b): Two selected hand specimens of monzodiorite. (c) and (d): Mineral assemblage of monzodiorite. Abbreviations: Qz—quartz, Pl—plagioclase, Kfs—K-feldspar, Pyr—pyroxene, Amp—amphibole, Bt—biotite.
Minerals 10 00301 g002
Minerals 10 00301 g003 550
Figure 3. Representative CL images of zircons and concordia diagrams (a) and LA-ICP-MS U–Pb zircon Concordia diagrams and weighted ages of the Mingze monzodiorites (b,c).
Figure 3. Representative CL images of zircons and concordia diagrams (a) and LA-ICP-MS U–Pb zircon Concordia diagrams and weighted ages of the Mingze monzodiorites (b,c).
Minerals 10 00301 g003
Minerals 10 00301 g004 550
Figure 4. Variation diagrams for representative major and trace elements. (a) Total alkalis versus silica (TAS) diagram; (b) SiO2 vs. K2O diagram; (c) K2O–SiO2 diagram; (d) Sr/Y–Y classification diagrams. The adakitic and arc calc-alkalic magmatic rocks from [31]. Data for comparison are from [7,15,16].
Figure 4. Variation diagrams for representative major and trace elements. (a) Total alkalis versus silica (TAS) diagram; (b) SiO2 vs. K2O diagram; (c) K2O–SiO2 diagram; (d) Sr/Y–Y classification diagrams. The adakitic and arc calc-alkalic magmatic rocks from [31]. Data for comparison are from [7,15,16].
Minerals 10 00301 g004
Minerals 10 00301 g005 550
Figure 5. Primitive-mantle-normalized multi-element spider grams (a) and Chondrite-normalized rare earth element (REE) patterns (b) of the Mingze monzodiorites. Chondrite-normalized and primitive-mantle-normalized values are from [32].
Figure 5. Primitive-mantle-normalized multi-element spider grams (a) and Chondrite-normalized rare earth element (REE) patterns (b) of the Mingze monzodiorites. Chondrite-normalized and primitive-mantle-normalized values are from [32].
Minerals 10 00301 g005
Minerals 10 00301 g006 550
Figure 6. (a) εHf(t) values versus U-Pb zircon ages and (b) εNd(t) versus (87Sr/86Sr)idiagrams (after [16]) for the Mingze monzodiorites, southern Tibet. Data sources are as follows: Cretaceous-Paleocene Gangdese are from [33]; Chengba mafic enclaves are from [7]; Wolong mafic enclaves are from [15]; Gaoligong-Tengliang basaltic dykes are from [34]; Zhengga gabbros are from [20]; IYTS (Indus-Yarlung Tsangpo Suture) ophiolites are from [35]; Yeba volcanic rocks are from [36]; Linzizong volcanic rocks are from [37] post-collisional ultrapotassic rocks are from [38]; Quguosha Gabbros are from [16]; Himalayan leucogranites are from [39]; data for the Dagze diabases are from [40].
Figure 6. (a) εHf(t) values versus U-Pb zircon ages and (b) εNd(t) versus (87Sr/86Sr)idiagrams (after [16]) for the Mingze monzodiorites, southern Tibet. Data sources are as follows: Cretaceous-Paleocene Gangdese are from [33]; Chengba mafic enclaves are from [7]; Wolong mafic enclaves are from [15]; Gaoligong-Tengliang basaltic dykes are from [34]; Zhengga gabbros are from [20]; IYTS (Indus-Yarlung Tsangpo Suture) ophiolites are from [35]; Yeba volcanic rocks are from [36]; Linzizong volcanic rocks are from [37] post-collisional ultrapotassic rocks are from [38]; Quguosha Gabbros are from [16]; Himalayan leucogranites are from [39]; data for the Dagze diabases are from [40].
Minerals 10 00301 g006
Minerals 10 00301 g007 550
Figure 7. Selected elements and their ratios plot for the Mingze monzodiorites. SiO2 versus (a) TiO2, (b) Al2O3, (c) TFe2O3, (d) CaO, (e) Na2O, (f) P2O5, (g) Mg#, (h) La/Sm ratio, (i) Dy/Yb ratio, (j) Sr, (k) Lu/Yb ratio and (l) Zr/Hf ratio. Modify after [43]. Data sources are the same as in Figure 4.
Figure 7. Selected elements and their ratios plot for the Mingze monzodiorites. SiO2 versus (a) TiO2, (b) Al2O3, (c) TFe2O3, (d) CaO, (e) Na2O, (f) P2O5, (g) Mg#, (h) La/Sm ratio, (i) Dy/Yb ratio, (j) Sr, (k) Lu/Yb ratio and (l) Zr/Hf ratio. Modify after [43]. Data sources are the same as in Figure 4.
Minerals 10 00301 g007
Minerals 10 00301 g008 550
Figure 8. Plots of (a) εNd(t) versus MgO, (b) (87Sr/88Sr)i versus MgO, (c) εNd(t) versus SiO2 and (d) (87Sr/88Sr)i versus SiO2.
Figure 8. Plots of (a) εNd(t) versus MgO, (b) (87Sr/88Sr)i versus MgO, (c) εNd(t) versus SiO2 and (d) (87Sr/88Sr)i versus SiO2.
Minerals 10 00301 g008
Minerals 10 00301 g009 550
Figure 9. Representative major, trace elements plots of Mingze monzodiorites. (a) MgO versus SiO2; (b) MgO versus TiO2; (c) MgO versus Cr; (d) MgO versus CaO; (e) MgO versus CaO/Al2O3; (f) MgO versus Nb/Th ratio.
Figure 9. Representative major, trace elements plots of Mingze monzodiorites. (a) MgO versus SiO2; (b) MgO versus TiO2; (c) MgO versus Cr; (d) MgO versus CaO; (e) MgO versus CaO/Al2O3; (f) MgO versus Nb/Th ratio.
Minerals 10 00301 g009
Minerals 10 00301 g010 550
Figure 10. (a) εNd(t) versus εHf(t) (modify after [56]) and (b) Th/Yb ratio versus Nb/Yb ratio(modify after [45]) discrimination diagram for Mingze monzodiorites. MORB (mid-ocean ridge basalt) + OIB (ocean island basalt) array and fields for DM (depleted mantle), MORB and OIB are from [57].
Figure 10. (a) εNd(t) versus εHf(t) (modify after [56]) and (b) Th/Yb ratio versus Nb/Yb ratio(modify after [45]) discrimination diagram for Mingze monzodiorites. MORB (mid-ocean ridge basalt) + OIB (ocean island basalt) array and fields for DM (depleted mantle), MORB and OIB are from [57].
Minerals 10 00301 g010

Share and Cite

MDPI and ACS Style

Zhang, K.; Shi, Z.; Liao, R.; Zhu, F. Petrogenesis and Geological Implications of the Oligocene Mingze monzodiorites, Southern Lhasa. Minerals 2020, 10, 301. https://doi.org/10.3390/min10040301

AMA Style

Zhang K, Shi Z, Liao R, Zhu F. Petrogenesis and Geological Implications of the Oligocene Mingze monzodiorites, Southern Lhasa. Minerals. 2020; 10(4):301. https://doi.org/10.3390/min10040301

Chicago/Turabian Style

Zhang, Kailiang, Zeming Shi, Rong Liao, and Feilin Zhu. 2020. "Petrogenesis and Geological Implications of the Oligocene Mingze monzodiorites, Southern Lhasa" Minerals 10, no. 4: 301. https://doi.org/10.3390/min10040301

APA Style

Zhang, K., Shi, Z., Liao, R., & Zhu, F. (2020). Petrogenesis and Geological Implications of the Oligocene Mingze monzodiorites, Southern Lhasa. Minerals, 10(4), 301. https://doi.org/10.3390/min10040301

Note that from the first issue of 2016, this journal uses article numbers instead of page numbers. See further details here.

Article Metrics

Back to TopTop