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. 2021 Jul 21;11:14882. doi: 10.1038/s41598-021-94492-y

Microcontinent subduction and S-type volcanism prior to India–Asia collision

Zongyao Yang 1,2, Juxing Tang 1,2,✉, M Santosh 3,4, Xiaoyan Zhao 1,✉, Xinghai Lang 5, Ying Wang 1, Shuai Ding 5, Fengqin Ran 5
PMCID: PMC8295362  PMID: 34290342

Abstract

Continental crust has long been considered too buoyant to be subducted beneath another continent, although geophysical evidence in collision zones predict continental crust subduction. This is particularly significant where upper continental crust is detached allowing the lower continental crust to subduct, albeit the mechanism of such subduction and recycling of the upper continental crust remain poorly understood. Here, we investigate Paleocene S-type magmatic and volcanic rocks from the Linzizong volcanic succession in the southern Lhasa block of Tibet. These rocks exhibit highly enriched 87Sr/86Sr, 207Pb/206Pb and 208Pb/206Pb together with depleted 143Nd/144Nd isotope ratios. The geochemical and isotopic features of these rocks are consistent with those of modern upper continental crust. We conclude that these Paleocene S-type volcanic and magmatic rocks originated from the melting of the upper continental crust from microcontinent subduction during the late stage of India–Asia convergence.

Subject terms: Geochemistry, Geodynamics, Tectonics

Introduction

The amalgamation of the Indian and Asian lithospheric plates and the construction of the Himalayan–Tibetan orogens mark one of the most prominent collisional events on the globe1,2. The rise of the Qinghai–Tibet Plateau as the highest plateau in the world with an average elevation of around 3000 m is a remarkable outcome of the India–Asia collision along the Indus–Yarlung suture zone (IYSZ)3 (Fig. 1). The Linzizong volcanic succession (LVS) and the coeval intrusive rocks in southern Tibet, which cover more than 50% of the Gangdese Belt extending E–W for more than 1200 km (Fig. 2A) are prominent markers of the magmatic activity associated with the India–Asia collision4–9.

Figure 1.

Figure 1

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Tectonic and geomorphic map of the Himalayan–Tibetan orogen showing major tectonic units. Base map is made with Natural Earth (https://www.naturalearthdata.com). The map was

modified by Zongyao Yang, using CorelDRAW X8 version 18.0.0.448. AKMSZ Anyimaqen–Kunlun–Muztagh suture zone, JSSZ Jinsha suture zone, BNSZ Bangong–Nujiang suture zone, IYSZ Indus–Yarlung suture zone, MBT Main boundary thrust.

Figure 2.

Figure 2

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(A) Simplified tectonic framework of the southern margin of the Lhasa block showing the location of the study area. (B) Regional geological map showing the study area, modified from the China Geological Survey (www.cgs.gov.cn) based on our field observations. The maps were generated by Zongyao Yang, using CorelDRAW X8 version 18.0.0.448. Yellow diamonds represent literature data of Paleocene S-type magma9–12. Blue dashed circles represent the approximate extent of the s-type granitic rocks. LMF Luobadui–Milashan Fault.

The LVS has a total thickness of more than 6500 m in the Linzhou Basin and can be subdivided into three groups from the bottom to the top as: the lower Dianzhong, middle Nianbo, and upper Pana Formations with approximate thicknesses of > 3326 m, 845 m, and 2350 m, respectively4. Previous geochronological studies defined the eruption boundaries of the Dianzhong, Nianbo, and Pana Formations as 65–60 Ma, 60–54 Ma and ~ 54–43 Ma, respectively6,7,9. As evident from their thicknesses, the Dianzhong and Pana Formations indicate more intense volcanic activity than the Nianbo Formation. The Dianzhong and Nianbo Formations show arc-like geochemical signature with significant mantle contributions5–9,13, in contrast to the geochemically heterogeneous of the Pana Formation7,9. The same inference can also be made for the coeval intrusive rocks as they show similar whole-rock geochemistry and Sr–Nd isotope, and zircon Hf isotope compositions with the Cretaceous I-type Gangdese batholith6,14–16. Besides, some hypabyssal granitic rocks show increased crustal contribution similar to S-type granite with radiogenic Sr–Nd–Pb and zircon Hf isotope compositions10,13,17,18. In general, the geodynamic setting of the Paleocene Dianzhong volcanic and intrusive rocks was either an Andean-type convergent margin formed by the northward subduction of the Neo-Tethys oceanic crust beneath the Lhasa block19, or a syn-collision orogen formed during the rollback of the Neo-Tethys slab accompanied by crustal melting induced by asthenospheric upwelling and magma mixing8,14–17. However, our recent studies on the Dianzhong Formation in the southern Lhasa block reveal geochemical characteristics of wholly continental crust-derived melts that are in sharp contrast to the concept of oceanic crust- and mantle source. The origin of these continental crust-derived volcanic and granitic rocks has not been investigated in detail.

In this paper, we report the finding of Paleocene (ca. 65–60 Ma) S-type magmatism in the LVS from the Sinongduo area in southern Tibet. We propose a novel model for the India–Asia collision and the formation of the S-type magma where we envisage of the subduction of microcontinent during the India–Asia convergence, and that the partial melting of the upper continental crust (UCC) of the subducted microcontinent significantly contributed to the formation of the Paleocene S-type volcanic rocks and granitoids.

Geological background and sampling

The Tibetan Plateau from north to south comprises the Songpan-Ganzi, Qiangtang, Lhasa, and Himalaya blocks (Fig. 1). These continental blocks associated with flysch complexes, and island arcs are considered to have accreted successively to the Asia plate since the early Paleozoic1. The Lhasa block, the last block that accreted to the Asia plate before the India–Asia collision, is sandwiched between the Qiangtang block and the Himalayas. Subsequent to this amalgamation and the northward subduction of the Neo-Tethys oceanic crust, the Himalaya (Indian plate) finally collided with Asia in the early Cenozoic along the IYSZ resulting in the uplift of the Tibetan Plateau2,3,20.

The Sinongduo area is located in Xietongmen County, Tibet (Fig. 2A). Widespread volcanic rocks and Carboniferous-Permian strata are exposed in the area (Fig. 2B). The volcanic rocks that consist mainly of rhyolite, tuff, dacite, and volcanic breccia overlying the Cretaceous Gangdese batholith were intruded by a granitic pluton (Fig. 3A,B). Detailed geochronological studies indicate that these volcanic rocks erupted during ~ 65–60 Ma and belong to the Dianzhong Formation of the LVS21,22. Therefore, these rocks preserve important information relating to India–Asia collision. In this study, we collected representative samples of both volcanic and intrusive rocks and conduct systematic whole-rock major and trace element, geochronologic, and Sr–Nd–Pb isotope studies with a view to assess their magma sources. Two representative samples (T473 and F15-1) collected from granitoids were used for zircon U–Pb dating. Twelve samples (SND-1 to SND-12) were used for whole-rock major and trace element analyses which were collected from the inner parts of the granitoids. We collected the least-altered and -weathered samples. Microscopic observation indicates that the granitoids are composed mainly of quartz, corundum, and minor orthoclase, muscovite (Fig. 3C–F) with fine-grained porphyritic-like texture. The whole-rock major and trace element data on these volcanic rocks were reported by Ding et al.21.

Figure 3.

Figure 3

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(A, B) Field photographs showing contact relationships between different types of magmatic rocks. (C–F) Photomicrographs showing the mineral composition of the granitoids in the Sinongduo area. Crn Corundum, Qz Quartz, Ser Sericite.

Geochronology and geochemistry

In the granitoid samples the U–Pb data on 26 zircon grains from sample T473 and 13 from F15-1 yielded concordant 206Pb/238U ages of 60.8 ± 0.4 Ma (Fig. 4A) (MSWD = 0.3) and 60.5 ± 1.0 Ma (Fig. 4B) (MSWD = 0.7), respectively. Zircons are euhedral and have crystal lengths of ~ 100–250 μm, with length/width ratios from 1:1 to 3:1. The dated zircon grains from samples T473 and F15-1 display oscillatory zoning in cathodoluminescence (CL) images and have variable Th (97–430 ppm and 287–1, 031 ppm, respectively) and U (119–490 ppm and 208–1, 016 ppm, respectively) contents, with Th/U ratios ranging from 0.64 to 1.22 and 0.43 to 1.88, respectively (Supplementary Table S1), suggesting magmatic crystallization. In addition, inherited zircons are not present in both granitoid and volcanic rocks21.

Figure 4.

Figure 4

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Zircon U–Pb concordia diagram and weighted ages for the Sinongduo Linzizong granitoids T473 (A) and F15-1 (B) showing typical cathodoluminescence (CL) images of representative zircons with 238U/206Pb ages.

The chemical compositions of the Linzizong granitoids are listed in Supplementary Table S2. The granitoids from Sinongduo have high SiO2 (73.47–81.13 wt%) and K2O (4.00–6.77 wt%), moderate Al2O3 (9.46–14.03 wt%), and uniformly low Na2O (0.09–0.18 wt%), CaO (0.14–0.19 wt%), MgO (0.10–0.23 wt%), and FeOT (0.82–1.40 wt%) contents compared with the normal Dianzhong magmatic rocks5,6,8,9. The volcanic rocks and granitoids plot within the rhyolite and granite fields, respectively, on the total alkalis vs. silica (TAS) diagram (Fig. 5A). The alumina saturation index (ASI = mol. Al2O3/(CaO + Na2O + K2O)) values of these rocks are in the range of 1.64–2.10, indicating that they are strongly peraluminous (Fig. 5B) and similar to the S-type granites such as those from the Lachlan fold belt23,24 (Fig. 5B). As shown in the chondrite-normalized rare earth element (REE) patterns (Fig. 5C), the Linzizong granitoids have enriched light REE (LREE) and relatively flat heavy REE (HREE) patterns with obvious negative Eu anomalies (Eu/Eu* = 0.56–0.82). Their primitive mantle-normalized incompatible trace element patterns (Fig. 5D) exhibit enrichment in some large ion lithophile elements (LILEs) (e.g., Rb, Th, U, and Pb) and depletions in Ba, Sr, and high field strength elements (HFSEs), particularly Nb, Ta, and Ti. The normalized REE and incompatible element abundance curves of the Linzizong granitoids are similar to those of the volcanic rocks from the Sinongduo area, indicating they formed from similar primary magma21. Whole-rock Sr–Nd–Pb isotope data for the Linzizong granitoids are listed in Supplementary Table S3. The granitoids have uniform 87Sr/86Sr ratios of 0.7247–0.7293 and 143Nd/144Nd ratios of 0.5122–0.5123, whereas the volcanic samples of rhyolite, tuff and dacite exhibit variable 87Sr/86Sr (0.7146–0.7531) but homogeneous 143Nd/144Nd (0.5120–0.5122) ratios. The Pb isotope compositions of granitoids are also uniform, with 206Pb/204Pb, 207Pb/204Pb, and 208Pb/204Pb ratios ranging from 18.7522 to 18.7660, 15.7091 to 15.7098, and 39.3622 to 39.4055, respectively.

Figure 5.

Figure 5

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Geochemical characteristics of Paleocene S-type granitic rocks from the southern Lhasa block. (A) Total alkali versus silica (TAS) diagram. (B) A/NK versus A/CNK classification diagram. (C) Chondrite-normalized REE patterns and (D) primitive mantle-normalized trace element patterns for Paleocene granitoids from the Sinongduo area. (E) Nb/Ta versus Zr and (F) Nb/Ta versus Nb diagrams25. Chondrite and primitive mantle data are from Sun and McDonough26. Data for the UCC, BCC and LCC are from Taylor and McLennan27. Data for the Himalayan highly fractionated leucogranite are from Liu et al.28, and Lin et al.29. Data for the Xuru Tso granitoids and volcanic rocks are from Lee et al.9, and Gao et al.10. Other data for the Sinongduo granitoids and volcanic rocks are from Yang11, Zhou et al.12, and Ding et al.21.

Alteration, assimilation and fractional crystallization

Our petrographic observation shows that the rocks underwent low degree sericite alteration (Fig. 3B). The loss-on-ignition (LOI) values of the samples are uniform and vary from 2.04 to 4.18 wt% (average = 2.99 wt%), implying slight alteration. Here, we argue that the geochemical composition can still be employed as a tracer to discuss the magma origin because the content of oxides does not show significant geochemical variation. Besides, the samples are characterized by sub-parallel patterns of REE and trace element concentrations (Fig. 5C,D), indicating they still preserve their original geochemical signatures30.

Both the granitoids and volcanic rocks have high SiO2, which chemically correspond to the high silica granites (HSGs) with SiO2 > 70 wt%. The HSGs are considered can be formed by highly fractional crystallization of the mafic parents31. The important question is whether the granitoids and volcanic rocks inherited their peraluminous geochemistry from the source region or evolved from a relatively mafic parent32 by assimilation and fractional crystallization (AFC). Previous studies consider the Dianzhong volcanic rocks as I-type rocks originated from mantle wedge that containing some crustal component followed by the AFC processes5–7,9. However, these S-type volcanic and magmatic rocks have extremely low Na2O, CaO, MgO, FeOT, Cr (5.20–15.42), Ni (1.09–3.57), and Co (0.60–1.54) contents with radiogenic Sr and Pb isotope composition compared with Dianzhong I-type series5,6,8,9, which indicate that they are not likely originated from partial melting of the mantle wedge or the mafic lower continental crust (LCC). Besides, the initial 87Sr/86Sr ratios and εNd(t) of the granitoids and volcanic rocks exhibit inconsistent relations rather than any correlation with SiO2 contents (Fig. 6A,B), and the volcanic rocks and granitoids also yield relatively uniform Pb isotope compositions (Supplementary Table S3), thus precluding significant crustal assimilation. With respect to the fractional crystallization, we apply high-field-strength elements Nb, Ta and Zr to evaluate the degree of fractional crystallization25,33. The Nb and Ta concentrations show a positive correlation with the degree of fractional crystallization, while the Nb/Ta and Zr concentration progressively decrease33. The isotope compositions indicate that these magmatic rocks were derived from the upper continental crust. Their Nb/Ta ratios (9.12–10.33) are slightly lower than the upper continental crust (11.36) and different from the highly fractionated Himalaya leucogranites (< 5) (Fig. 5E,F). The low Nb, Ta and high Nb/Ta ratios indicate the granitoids and volcanic rocks from the Sinongduo area could not have experienced strongly fractional crystallization and the geochemistry of these magmatic rocks reflects the composition of the source region.

Figure 6.

Figure 6

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(A) SiO2 versus εNd(t) and (B) SiO2 versus (87Sr/86Sr)i diagrams. Whole-rock initial 87Sr/86Sr ratios and εNd(t) show low correlation with SiO2.

Magma source and petrogenesis

The granitoids and volcanic rocks from the Sinongduo area are strongly peraluminous and plot in the S-type magma field (Figs. 5B, 7), in contrast to the I-type Gangdese batholith and coeval volcanic rocks elsewhere in the Lhasa block. The Lhasa terrane was not under a post-collisional setting in the Paleocene, and therefore these rocks cannot be correlated to post-collisional strongly peraluminous granites formed in such settings34. Even though the Sinongduo granitoids and volcanic rocks have elevated Fe-index (0.82–0.92) which is an indicator of the ferroan (A-type) granitoids35, the characteristics such as the absence of dark-colored minerals, low 10,000*Ga/Al ratios (1.76–2.58) and Zr + Nb + Ce + Y values (174–257 ppm), indicate that the Sinongduo granitoids are different from the A-type granites36,37.

Figure 7.

Figure 7

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Al2O3-(Na2O + K2O) versus CaO versus FeOT + MgO diagram23. Data for the Paleocene I-type volcanic rocks are Mo et al.5,6, and Lee et al.9.

Chappell and White24 defined S-type granites as: (1) being strongly peraluminous with ASI > 1.1, (2) containing > 1% CIPW38 normative corundum, and (3) having restricted to high SiO2 compositions with relatively low Na2O (generally < 3.2%) but high K2O (~ 5%) contents. As mentioned above, the characteristics of high SiO2 and K2O, low Na2O contents, and ASI values of 1.64–2.10 imply that these granitoids and volcanic rocks have affinity to S-type granite. The normative corundum (Fig. 3E,F) contents of 3.78–6.39% based on the CIPW calculation is even more enriched than the peraluminous felsic S-type series in the Lachlan fold belt and contrasts with the depleted I-type series24. The classification of the Sinongduo magmatic rocks as S-type is also supported by their whole-rock initial Sr87/Sr86 isotopes (0.707–0.732, except ZK0602-2), as Sr is more radiogenic in S-type granites with initial Sr87/Sr86 > 0.70824.

Given that the geochemical characteristics are similar to those of upper crustal sedimentary rocks, S-type magma is considered to form by melting of a sedimentary UCC source that had experienced at least one cycle of weathering24 rather than from the more mafic LCC27 or oceanic crust. A long-term weathering process can remove Na and Ca and maintain high K in the abundant clay minerals39, which leads to the high ASI in sediments. Therefore, the key factor for the generation of S-type granitic magma is a sedimentary source40. Since such sediments are deposited only in the Earth’s upper continental crust, S-type granitic magma is considered to be product of anatexis40,41.

As seen in the chondrite-normalized REE patterns (Fig. 5C), all the granitoids in our study display nearly overlapping patterns with that of the UCC, indicating more enriched LREE compositions than for the LCC and the Indian Ocean sediments. In addition, both granitoids and volcanic rocks from our study have significant negative Eu anomalies, which are very similar to those of the UCC (average Eu/Eu* = 0.6527) and contrast with the positive Eu anomalies in the LCC (average Eu/Eu* = 1.1427). Although these negative Eu anomalies are generally interpreted as the residues of plagioclase feldspar, a more direct cause is assumed here that reflects the Eu-depleted primary magma because of the low degree of fractional crystallization. In the 87Sr/86Sr–143Nd/144Nd isotope space (Fig. 8), it is seen that compared with other magmatic rocks, including other Linzizong volcanic rocks, the Paleocene S-type magmatism shows an obvious increase in 87Sr/86Sr, confirming UCC affinity. The same conclusion also can be reached from the radiogenic Pb isotopes (Supplementary Table S3).

Figure 8.

Figure 8

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Isotopic evidence for UCC components in Paleocene magma from the Sinongduo area. (A) 87Sr/86Sr versus 143Nd/144Nd42 for Paleocene magma from the Sinongduo area. Data from the Indian Ocean sediments43 are plotted for comparison. Data for global subducting sediment (GLOSS) are from Plank and Langmuir44. Fields of UCC42, LCC45 and Indian Ocean MORB46 are obtained from the literature.

Two potential scenarios can be envisaged for formation of the Sinongduo S-type granitic rocks: (1) crustal anatexis40,41; (2) extraction from shallow andesitic magma reservoir by fractional crystallization12. For the crustal anatexis hypothesis, a deep buried metasedimentary source is required for the generation of S-type magma47. Exhumation of the overthickened crust is a widely accepted mechanism for the formation of strongly peraluminous S-type granites in post-collisional setting34,47. However, this model is inapplicable for the S-type granites formed non-collisional setting. A two-stage rollback of the subducted oceanic crust that caused crustal extension is proposed to account for the S-type granites in the Phanerozoic circum-Pacific orogenic belts40. S-type granites formed by this mechanism are consistently associated with high-temperature–low-pressure (HTLP) metamorphic complexes, or even some core complexes which were exhumed during continental extension48,49. A thinned lithosphere is also required for a substantial transient heat flux to the crust40. Overall, the Sinongduo S-type magmatic rocks cannot be correlated to both these models because HTLP metamorphic complex is absent and continental collision had not yet occurred at that time. Besides, the S-type magma cannot be extracted from shallow andesitic magma reservoir because of the low degree fractional crystallization. This hypothesis is also limited in explaining the large outcrop of these volcanic and intrusive rocks that cover more than 300 km2 in the study area (Fig. 2A,B).

As the Gangdese batholith and Linzizong volcanic rocks are treated as products of the northward subduction of the Neo-Tethys oceanic crust6,9, we propose an alternative scenario in which the Linzizong S-type volcanic rocks and granitoids are derived from subducted materials of UCC geochemical affinity. Zircon saturation temperatures (Tzr) of the Sinongduo granitoids are in the range of 768–804 °C (mean = 793 °C) based on the method of Boehnke et al.50. The absence of inherited zircons in the granitoids indicates that partial melting took place at high-temperature conditions and the initial magmas were undersaturated in zirconium. In this case, the calculated zircon saturation temperatures provide minimum estimates of melting temperature51. Besides, microscopic observation indicates that the granitoids contain fewer zircon crystals. These features, together with the wide distribution of the volcanic rocks suggest that the melting temperature exceeded 804 °C, comparable to hot granites51. The substantial heat flux for melting can be achieved if these UCC subducted to a depth of lithospheric mantle.

Implications for the India–Asia convergence

Our first assumption is that the subducted UCC represents a portion of the northern edge of the Indian plate, in which case the initial India–Asia collision started at approximately 65 Ma, which is in accordance with the popular geophysical collision model that shows continental lithosphere beneath southern Tibet52,53. However, it conflicts with most published studies that support collision ages to range from Late Cretaceous to Oligocene54, especially the recently accepted 55 ± 5 Ma age for the onset of collision54–57. On the other hand, Andean-type calc-alkaline magmatism with consistent isotopic compositions from the Early Jurassic to the middle Eocene6,9 naturally implies the persistence of Neo-Tethys oceanic crust subduction beyond a collisional background and suggests that the 65 Ma age for the India–Asia collision should be excluded56. Hence, the subducted UCC cannot be the northern edge of the Indian plate, and should be attributed to other continental subduction systems.

An alternate possibility would be the subduction of microcontinents (microplates). Fragmentation and microcontinent formation are common phenomena in many continental margins57. The opening of the embryonic Neo-Tethys may have caused rifting of the northern margin of the Indian plate under a divergent tectonic setting and formed a cluster of microcontinents (Fig. 9) between the Indian plate and the Asia plate58. Besides, thermo-mechanical study reveals that the thermal and buoyancy effects of mantle plume impingement on the bottom of the continental part of a subducting plate can also induce the separation of microcontinents from the main body of the continent59. With the initiation of the northward subduction of the Neo-Tethys crust in early Mesozoic60, possibly induced by the impingement of mantle plume at the transition zone between oceanic and continental lithosphere61, these microcontinents are thought to have accreted to the Lhasa block along the IYSZ in the early Cenozoic, similar to the Burma terrane62 and the Oaxaquia in North America63. However, no geological records have been reported to document the accretion in the IYSZ.

Figure 9.

Figure 9

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Conceptual model showing the subduction of the microcontinent and the formation of S-type magma. Not drawn to scale. See text for discussion.

In general, strong rheological coupling of UCC and LCC can separate the continental crust from the downgoing mantle lithosphere, while low rheological coupling of the UCC and LCC allows the LCC to sink into the mantle, resulting in continental subduction64. Numerical models indicate subduction of the Indian LCC65, which is also confirmed from geophysical evidence52,53. However, the possibility and mechanism of the subduction and recycling of the UCC remain poorly understood. Numerical modelling studies indicate that the UCC can subduct to a great depth if the continental crust is strongly coupled with the mantle lithosphere under a relatively low Moho temperature66–68. Another critical factor controlling the accretion and scale of continental subduction is the continental mass69, and compared with the short-subducted lengths of intact continental crust, microcontinents can be entirely subducted70. The coherence may play an important role in the subducting plate if the detachment did not occur71. A so called “crustal pocket” can subduct to a depth of 50–120 km67. Microcontinents might undergo subduction process comparable to that of the “crustal pocket” in the subduction zone. The melts derived from the subducted UCC are immediately transported to the surface across the rheologically coupled lithosphere72 along deep-seated lithospheric-scale faults that formed in the overriding plate73. We consider this mechanism for the S-type magmatic rocks that are distributed along the regional Luobadui-Milashan fault (LMF) as clusters (Fig. 2A). We thus propose that the microcontinents rifted from the India plate could have been wholly subducted without any accretion to the collision boundary.

If the whole UCC was subducted, then little or possibly no trace of accretion may be recorded in the suture zone, as these were entirely erased. Only the melting of UCC components can induce secondary geochemical consequences which are traceable from magmatic signatures42. After the subduction of the UCC, a significant period of oceanic crust subduction must have followed prior to the continental collision (Fig. 9). Our model has the advantage of reconciling the heterogeneity of the Linzizong volcanic rocks and coeval batholiths and can also support the subsequent India–Asia collision geodynamics.

Previous studies considered S-type magma to be a product of crustal anatexis40. However, our proposal opens up alternate possibilities of partial melting and recycling of subducted UCC, particularly involving microcontinents.

Methods

Zircon U–Pb dating

The granitoid samples for LA–ICP–MS zircon U–Pb dating were crushed, and zircons were separated using conventional heavy liquid and magnetic separation techniques. Zircons were handpicked under a microscope, mounted in epoxy resin, polished to approximately half their original thickness, and studied under both reflected and transmitted light. To examine the internal structure, cathodoluminescence (CL) images of zircon grains were obtained using a JSM6510 scanning electron microscope. Zircon U–Pb dating was performed using a Neptune MC-ICP-MS coupled with a New Wave UP213 laser ablation system at the Institute of Mineral Resources, Chinese Academy of Geological Sciences. The operating conditions and detailed analytical procedures followed those described by Hou et al.74. The U–Pb ages of the zircons were calculated and plotted using the Isoplot3 software (Ludwig, 2003). Individual analyses are presented with 1σ error, whereas age uncertainties are quoted at the 95% level (2σ).

Whole-rock major and trace element analyses

Whole-rock major element analyses and trace element analyses were conducted with an X-ray fluorescence (XRF) spectrometer (Primus II, Rigaku, Japan) and an Agilent 7700e ICP-MS system, respectively, at the Wuhan Sample Solution Analytical Technology Co., Ltd., Wuhan, China. The sample powder was accurately weighed and mixed with the cosolvent (Li2B4O7: LiBO2: LiF = 9:2:1) and oxidant (NH4NO3) in a Pt crucible, which was then placed in the furnace at 1150 °C for 14 min. Next, the melted sample was saturated with air for 1 min to produce flat disks on the firebrick for the XRF analyses. Approximately 1 ml of HNO3 and 1 ml of HF were slowly added to a 50 mg sample of powder in a Teflon bomb, which was placed in a stainless-steel pressure jacket and heated to 190 °C in an oven for > 24 h. After evaporating the sample to dryness twice, 1 ml of HNO3, 1 ml of Milli-Q (MQ) water, and 1 ml of 1 ppm internal standard solution were added, and the Teflon bomb was resealed and placed in the oven at 190 °C for > 12 h. The final solution was transferred to a polyethylene bottle and diluted to 100 g by the addition of 2% HNO3 for ICP-MS analysis. Analyses of international rock standards (AGV-2, BHVO-2 and BCR-2) indicated that the precision and accuracy of the results were better than 5%.

Whole-rock Sr–Nd–Pb isotope analyses

The Sr–Nd–Pb isotope ratios were determined by using a Finnigan Triton thermal ionization mass spectrometer (TIMS) at the State Key Laboratory for Mineral Deposits Research, Nanjing University. The measured 87Sr/86Sr and 143Nd/144Nd isotope ratios were normalized to 86Sr/88Sr = 0.1194 and 146Nd/144Nd = 0.7219, respectively, for mass fractionation correction. During the period of data acquisition, the mean 87Sr/86Sr ratio of the Sr standard (NBS987) and the 143Nd/144Nd ratio of the Nd standard (JNDi-1) were 0.710261 ± 0.00006 and 0.512128 ± 0.00004 (2σ), respectively. Further, the measured 87Sr/86Sr and 143Nd/144Nd values for the standard BCR-2 were 0.705018 ± 0.000003 and 0.512624 ± 0.000004, respectively (the equivalent reference values obtained from Weis et al.75 are 0.705019 ± 0.000016 and 0.512634 ± 0.000012). The analytical procedures for Sr and Nd isotopes followed those described in detail by Pu et al.76. The value of εNd(t) was calculated with reference to the chondritic uniform reservoir (CHUR) 143Nd/144Nd ratio of 0.512638.

For Pb isotope analysis, sample powders were weighed into a Teflon bomb and dissolved by a combination of purified HNO3 and HF at 190 °C for 48 h. Pb was separated and purified on ion exchange columns with diluted HBr as the eluant. Finally, the Pb fraction was eluted using 6.0 M HCl and gently evaporated to dryness prior to mass spectrometric measurement. The detailed procedures used in measuring Pb isotopes can be found in White et al.77. The measured Pb isotopic ratios were rectified for instrumental mass fractionation by performing replicate analyses of the standard NIST-981. The standard NIST-981 yielded 206Pb/204Pb = 16.9318 ± 0.0003, 207Pb/204Pb = 15.4858 ± 0.0003, and 208Pb/204Pb = 36.6819 ± 0.0008. In addition, the international standard BCR-2 was verified using an unknown sample by employing this method. The measured values for the BCR-2 Pb standard were 18.7881 ± 0.0005 for 206Pb/204Pb, 15.6196 ± 0.0004 for 207Pb/204Pb, and 38.8005 ± 0.0010 for 208Pb/204Pb (reference values can be found in Weis et al.75).

Supplementary Information

Supplementary Table S1. (15KB, xlsx)
Supplementary Table S2. (15.8KB, xlsx)
Supplementary Table S3. (12.3KB, xlsx)

Acknowledgements

This work was supported by the National Natural Science Foundation of China (Grant Numbers 41772075, 42072313); the Deep Resources Exploration and Mining, the National Key R&D Program of China (Grant Numbers 2018YFC0604101, 2018YFC0604105); and the Geological Survey Program of China (DD20190167). The authors would like to thank Prof. J. Gregory Shellnutt, Dr. Alexander Koptev and an anonymous reviewer for their insightful and constructive comments that greatly improved the manuscript.

Author contributions

Z.Y. performed most of the experimental work and wrote the manuscript. J.T. conceived the project and provided geologic and tectonic background. M.S., X.Z. and Y.W. participated in the discussion and interpretation of results. X.L. and S.D. contributed to the sample collection and field investigation. F.R. improved the figures and provided analytical assistance.

Data availability

All data generated or analysed during this study are included in this published article (and its Supplementary Information files).

Competing interests

The authors declare no competing interests.

Footnotes

Publisher's note

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Contributor Information

Juxing Tang, Email: tangjuxing@126.com.

Xiaoyan Zhao, Email: xyzhao2@swjtu.cn.

Supplementary Information

The online version contains supplementary material available at 10.1038/s41598-021-94492-y.

References

  • 1.Yin A, Harrison TM. Geologic evolution of the Himalayan–Tibetan orogen. Ann. Rev. Earth Planet. Sci. 2000;28:211–280. doi: 10.1146/annurev.earth.28.1.211. [DOI] [Google Scholar]
  • 2.Tapponnier P, et al. Oblique stepwise rise and growth of the Tibet Plateau. Science. 2001;294:1671–1677. doi: 10.1126/science.105978. [DOI] [PubMed] [Google Scholar]
  • 3.Botsyun S, et al. Revised paleoaltimetry data show low Tibetan Plateau elevation during the Eocene. Science. 2019;363:eaaq1436. doi: 10.1126/science.aaq1436. [DOI] [PubMed] [Google Scholar]
  • 4.Dong G, Mo X, Zhao Z, Wang L, Zhou S. A new understanding of the stratigraphic successions of the Linzizong volcanic rocks in the Linzhou basin, Tibet. Geol. Bull. China. 2005;24:549–557. [Google Scholar]
  • 5.Mo XX, et al. Mantle contributions to crustal thickening during continental collision: Evidence from Cenozoic igneous rocks in southern Tibet. Lithos. 2007;96:225–242. doi: 10.1016/j.lithos.2006.10.005. [DOI] [Google Scholar]
  • 6.Mo XX, et al. 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. doi: 10.1016/j.chemgeo.2008.02.003. [DOI] [Google Scholar]
  • 7.Lee HY, et al. Eocene Neotethyan slab breakoff in southern Tibet inferred from the Linzizong volcanic record. Tectonophysics. 2009;477:20–35. doi: 10.1016/j.tecto.2009.02.031. [DOI] [Google Scholar]
  • 8.Yan H, et al. Arc andesitic rocks derived from partial melts of Mélange diapir in subduction zones: Evidence from whole-rock geochemistry and Sr–Nd–Mo isotopes of the Paleogene Linzizong volcanic succession in Southern Tibet. JGR: Solid Earth. 2019;124:456–475. [Google Scholar]
  • 9.Lee HY, et al. 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. doi: 10.1016/j.jseaes.2011.08.019. [DOI] [Google Scholar]
  • 10.Gao S, et al. Timing and genetic link of porphyry Mo and skarn Pb–Zn mineralization in the Chagele deposit, Western Nyainqentanglha belt, Tibet. Ore Geol. Rev. 2021;129:103929. doi: 10.1016/j.oregeorev.2020.103929. [DOI] [Google Scholar]
  • 11.Yang, Y. A study on geochemistry of the Narusongduo silver–zinc–lead deposit Tibet Province, China. Ph.D. Thesis, Chinese Academy of Sciences (2010) (in Chinese with English abstract).
  • 12.Zhou JS, et al. Extraction of high-silica granites from an upper crustal magma reservoir: Insights from the Narusongduo magmatic system, Gangdese arc. Am. Miner. 2020;105:1572–1584. doi: 10.2138/am-2020-7369. [DOI] [Google Scholar]
  • 13.Zhou XY, et al. Petrogenesis of Early Paleocene Dengtong volcanic-plutonic complex in central Lhasa Terrane and evolution of crustal high-silica magma. Earth Sci. 2021;46:474–488. [Google Scholar]
  • 14.Ji WQ, Wu FY, Chung SL, Li JX, Liu CZ. Zircon U-Pb geochronology and Hf isotopic constraints on petrogenesis of the Gangdese batholith, southern Tibet. Chem. Geol. 2009;262:229–245. doi: 10.1016/j.chemgeo.2009.01.020. [DOI] [Google Scholar]
  • 15.Wen DR, et al. Zircon SHRIMP U-Pb ages of the Gangdese Batholith and implications for Neotethyan subduction in southern Tibet. Chem. Geol. 2008;252:191–201. doi: 10.1016/j.chemgeo.2008.03.003. [DOI] [Google Scholar]
  • 16.Wang XH, et al. Eocene diabase dikes in the Tangbai area, southern margin of Lhasa terrane, Tibet: Evidence for the slab break-off of the Neo-Tethys Ocean. Geology in China. 2019;46:1336–1355. [Google Scholar]
  • 17.Xu J, Zheng Y, Sun X, Li X, Mao G. Genesis of the Yaguila Pb-Zn-Ag-Mo skarn deposit in Tibet: Insights from geochronology, geochemistry, and fluid inclusions. J. Asian Earth Sci. 2019;172:83–100. doi: 10.1016/j.jseaes.2018.08.007. [DOI] [Google Scholar]
  • 18.Duan ZM, et al. Geochronology and geochemical characteristics of ore-bearing porphyry in Longgen lead-zinc deposit of middle-Gangdese metallogenic belt, Tibet. Miner. Deposits. 2014;33:625–638. [Google Scholar]
  • 19.Scharer U, Xu R, Allegre CJ. U-Pb geochronology of Gangdese (Transhimalaya) plutonism in the Lhasa-Xigaxe region, Tibet. Earth Planet. Sci. Lett. 1984;69:311–320. doi: 10.1016/0012-821X(84)90190-0. [DOI] [Google Scholar]
  • 20.Zheng D, et al. Rapid exhumation at ~ 8 Ma on the Liupan Shan thrust fault from apatite fission-track thermochronology: Implications for growth of the northeastern Tibetan Plateau margin. Earth Planet. Sci. Lett. 2006;248:198–208. doi: 10.1016/j.epsl.2006.05.023. [DOI] [Google Scholar]
  • 21.Ding S, et al. Relationship between Linzizong volcanic rocks and mineralization: A case study of Sinongduo epithermal Ag–Pb–Zn deposit. Miner. Depos. 2017;36:1074–1092. [Google Scholar]
  • 22.Yang Z, et al. Geology, geochronology, and geochemistry of the Sinongduo Ag–Pb–Zn deposit in the Gangdese metallogenic belt: Implications of intermediate sulfidation mineralization in the Linzizong volcanic succession. Ore Geol. Rev. 2020;127:103796. doi: 10.1016/j.oregeorev.2020.103796. [DOI] [Google Scholar]
  • 23.Chappell BW, White AJR. I-type and S-type granites in the Lachlan fold belt. Trans. R. Soc. Edinb. Earth Sci. 1992;83:1–26. [Google Scholar]
  • 24.Chappell BW, White AJR. Two contrasting granite types: 25 years later. Aust. J. Earth Sci. 2001;48:489–499. doi: 10.1046/j.1440-0952.2001.00882.x. [DOI] [Google Scholar]
  • 25.Ballouard C, et al. Nb–Ta fractionation in peraluminous granites: A marker of the magmatic-hydrothermal transition. Geology. 2016;44:231–234. doi: 10.1130/G37475.1. [DOI] [Google Scholar]
  • 26.Sun SS, McDonough W. Chemical and isotopic systematics of oceanic basalts: Implications for mantle composition and processes. Geol. Soc. Lond. Spec. Publ. 1989;42:313–345. doi: 10.1144/GSL.SP.1989.042.01.19. [DOI] [Google Scholar]
  • 27.Taylor SR, McLennan SM. The geochemical evolution of the continental crust. Rev. Geophys. 1995;33:241–265. doi: 10.1029/95RG00262. [DOI] [Google Scholar]
  • 28.Liu ZC, et al. Highly fractionated Late Eocene (~ 35Ma) leucogranite in the Xiaru Dome, Tethyan Himalaya, South Tibet. Lithos. 2016;240–243:337–354. doi: 10.1016/j.lithos.2015.11.026. [DOI] [Google Scholar]
  • 29.Lin C, et al. Oligocene initiation of the South Tibetan Detachment System: Constraints from syn-tectonic leucogranites in the Kampa Dome. Northern Himalaya. Lithos. 2020;354–355:105332. [Google Scholar]
  • 30.Bienvenu P, Bougault H, Joron JL, Treuil M, Dmitriev L. MORB alteration: Rare-earth element/non-rare-earth hygromagmaphile element fractionation. Chem. Geol. 1990;82:1–14. doi: 10.1016/0009-2541(90)90070-N. [DOI] [Google Scholar]
  • 31.Lee CTA, Morton DM. High silica granites: Terminal porosity and crystal settling in shallow magma chambers. Earth Planet. Sci. Lett. 2015;409:23–31. doi: 10.1016/j.epsl.2014.10.040. [DOI] [Google Scholar]
  • 32.Chappell BW, Bryant CJ, Wyborn D. Peraluminous I-type granites. Lithos. 2012;153:142–153. doi: 10.1016/j.lithos.2012.07.008. [DOI] [Google Scholar]
  • 33.Dostal J, Chatterjee AK. Contrasting behaviour of Nb/Ta and Zr/Hf ratios in a peraluminous granitic pluton (Nova Scotia, Canada) Chem. Geol. 2000;163:207–218. doi: 10.1016/S0009-2541(99)00113-8. [DOI] [Google Scholar]
  • 34.Sylvester PJ. Post-collisional strongly peraluminous granites. Lithos. 1998;45:29–44. doi: 10.1016/S0024-4937(98)00024-3. [DOI] [Google Scholar]
  • 35.Frost CD, Frost BR. On ferroan (A-type) granitoids: Their compositional variability and modes of origin. J. Petrol. 2011;52:39–53. doi: 10.1093/petrology/egq070. [DOI] [Google Scholar]
  • 36.Eby GN. Chemical subdivision of the A-type granitoids: Petrogenetic and tectonic implications. Geology. 1992;20:641–644. doi: 10.1130/0091-7613(1992)020&#x0003c;0641:CSOTAT&#x0003e;2.3.CO;2. [DOI] [Google Scholar]
  • 37.Whalen JB, Currie KL, Chappell BW. A-type granites: Geochemical characteristics, discrimination and petrogenesis. Contrib. Mineral. Petrol. 1987;95:407–419. doi: 10.1007/BF00402202. [DOI] [Google Scholar]
  • 38.Le Maitre RW. The chemical variability of some common igneous rocks. J. Pet. 1976;17:589–598. doi: 10.1093/petrology/17.4.589. [DOI] [Google Scholar]
  • 39.Nesbitt HW, Markovics G, Price RC. Chemical processes affecting alkalis and alkaline-earths during continental weathering. Geochim. Cosmochem. Acta. 1980;44:1659–1666. doi: 10.1016/0016-7037(80)90218-5. [DOI] [Google Scholar]
  • 40.Collins WJ, Richards SW. Geodynamic significance of S-type granites in circum-Pacific orogens. Geology. 2008;36:559–562. doi: 10.1130/G24658A.1. [DOI] [Google Scholar]
  • 41.Zhu Z, Campbell IH, Allen CM, Burnham AD. S-type granites: Their origin and distribution through time as determined from detrital zircons. Earth Planet. Sci. Lett. 2020;536:116140. doi: 10.1016/j.epsl.2020.116140. [DOI] [Google Scholar]
  • 42.Jackson MG, et al. The return of subducted continental crust in Samoan lavas. Nature. 2007;448:684–687. doi: 10.1038/nature06048. [DOI] [PubMed] [Google Scholar]
  • 43.Othman DB, White WM, Patchett J. The geochemistry of marine sediments, island arc magma genesis, and crust-mantle recycling. Earth Planet. Sci. Lett. 1989;94:1–21. doi: 10.1016/0012-821X(89)90079-4. [DOI] [Google Scholar]
  • 44.Plank T, Langmuir CH. The chemical composition of subducting sediment and its consequences for the crust and mantle. Chem. Geol. 1998;145:325–394. doi: 10.1016/S0009-2541(97)00150-2. [DOI] [Google Scholar]
  • 45.McCulloch MT, Arculus RJ, Chappell BW, Ferguson J. Isotopic and geochemical studies of nodules in kimberlite have implications for the lower continental crust. Nature. 1982;300:166–169. doi: 10.1038/300166a0. [DOI] [Google Scholar]
  • 46.Rehkämper M, Hofmann AW. Recycled ocean crust and sediment in Indian Ocean MORB. Earth Planet. Sci. Lett. 1997;147:93–106. doi: 10.1016/S0012-821X(97)00009-5. [DOI] [Google Scholar]
  • 47.Barbarin B. A review of the relationships between granitoid types, their origins and their geodynamic environments. Lithos. 1999;46:605–626. doi: 10.1016/S0024-4937(98)00085-1. [DOI] [Google Scholar]
  • 48.Sandiford M, Powell R. Deep crustal metamorphism during continental extension: Modern and ancient examples. Earth Planet. Sci. Lett. 1986;79:151–158. doi: 10.1016/0012-821X(86)90048-8. [DOI] [Google Scholar]
  • 49.Wickham, S. M. & Oxburgh, E. R. Continental rifts as a setting for regional metamorphism. Nature318, 330–333 (1985).
  • 50.Boehnke P, Watson EB, Trail D, Harrison TM, Schmitt AK. Zircon saturation re-revisited. Chem. Geol. 2013;351:324–334. doi: 10.1016/j.chemgeo.2013.05.028. [DOI] [Google Scholar]
  • 51.Miller CF, McDowell SM, Mapes RW. Hot and cold granites? Implications of zircon saturation temperatures and preservation of inheritance. Geology. 2003;31:529–532. doi: 10.1130/0091-7613(2003)031&#x0003c;0529:HACGIO&#x0003e;2.0.CO;2. [DOI] [Google Scholar]
  • 52.Gao R, et al. Crustal-scale duplexing beneath the Yarlung Zangbo suture in the western Himalaya. Nat. Geosci. 2016;9:555–560. doi: 10.1038/ngeo2730. [DOI] [Google Scholar]
  • 53.Zhao W, et al. Deep seismic reflection evidence for continental underthrusting beneath southern Tibet. Nature. 1993;366:557–559. doi: 10.1038/366557a0. [DOI] [Google Scholar]
  • 54.Hu XM, Garzanti JW, Huang WT, Wei A, An W. The timing of India–Asia collision onset–Facts, theories, controversies. Earth-Sci. Rev. 2016;160:264–299. doi: 10.1016/j.earscirev.2016.07.014. [DOI] [Google Scholar]
  • 55.Hu X, Garzanti E, Moore T, Raffi I. Direct stratigraphic dating of India–Asia collision onset at the Selandian (middle Paleocene, 59 ± 1 Ma) Geology. 2015;43:859–862. doi: 10.1130/G36872.1. [DOI] [Google Scholar]
  • 56.Zhu DC, et al. Magmatic record of India–Asia collision. Sci. Rep. 2015;5:14289. doi: 10.1038/srep14289. [DOI] [PMC free article] [PubMed] [Google Scholar]
  • 57.Molnar NE, Cruden AR, Betts PG. Unzipping continents and the birth of microcontinents. Geology. 2018;46:451–454. doi: 10.1130/G40021.1. [DOI] [Google Scholar]
  • 58.Roy S. A possible Himalayan microcontinent. Nature. 1976;263:117–120. doi: 10.1038/263117a0. [DOI] [Google Scholar]
  • 59.Koptev A, et al. Plume-induced breakup of a subducting plate: Microcontinent formation without cessation of the subduction process. Geophys. Res. Lett. 2019;46:3663–3675. doi: 10.1029/2018GL081295. [DOI] [Google Scholar]
  • 60.Lang X, et al. Geochronology and geochemistry of volcanic rocks of the Bima Formation, southern Lhasa subterrane, Tibet: Implications for early Neo-Tethyan subduction. Gondwana Res. 2020;80:335–349. doi: 10.1016/j.gr.2019.11.005. [DOI] [Google Scholar]
  • 61.Cloetingh S, et al. Plume-induced sinking of intracontinental lithospheric mantle: An overlooked mechanism of subduction initiation. Geochem. Geophys. Geosyst. 2021;22:e2020GC009482. doi: 10.1029/2020GC009482. [DOI] [Google Scholar]
  • 62.Westerweel J, et al. Burma Terrane part of the Trans-Tethyan arc during collision with India according to palaeomagnetic data. Nat. Geosci. 2019;12:863–868. doi: 10.1038/s41561-019-0443-2. [DOI] [PMC free article] [PubMed] [Google Scholar]
  • 63.Ortega-Gutierrez F, Ruiz J, Centeno-Garcia E. Oaxaquia, a Proterozoic microcontinent accreted to North America during the late Paleozoic. Geology. 1995;23:1127–1130. doi: 10.1130/0091-7613(1995)023&#x0003c;1127:OAPMAT&#x0003e;2.3.CO;2. [DOI] [Google Scholar]
  • 64.Vogt K, Matenco L, Cloetingh S. Crustal mechanics control the geometry of mountain belts. Insights from numerical modelling. Earth Planet. Sci. Lett. 2017;460:12–21. doi: 10.1016/j.epsl.2016.11.016. [DOI] [Google Scholar]
  • 65.Capitanio FA, Morra G, Goes S, Weinberg RF, Moresi L. India–Asia convergence driven by the subduction of the Greater Indian continent. Nat. Geosci. 2010;3:136–139. doi: 10.1038/ngeo725. [DOI] [Google Scholar]
  • 66.Burov EB. Rheology and strength of the lithosphere. Mar. Pet. Geol. 2011;28:1402–1443. doi: 10.1016/j.marpetgeo.2011.05.008. [DOI] [Google Scholar]
  • 67.Burov E, Yamato P. Continental plate collision, P-T–t–z conditions and unstable vs. stable plate dynamics: Insights from thermo-mechanical modelling. Lithos. 2008;103:178–204. doi: 10.1016/j.lithos.2007.09.014. [DOI] [Google Scholar]
  • 68.Liao J, Gerya T. Partitioning of crustal shortening during continental collision: 2-D thermomechanical modeling. JGR: Solid Earth. 2017;122:592–606. [Google Scholar]
  • 69.Santosh M, Maruyama S, Yamamoto S. The making and breaking of supercontinents: Some speculations based on superplumes, super downwelling and the role of tectosphere. Gondwana Res. 2009;15:324–341. doi: 10.1016/j.gr.2008.11.004. [DOI] [Google Scholar]
  • 70.Molnar P, Gray D. Subduction of continental lithosphere: Some constraints and uncertainties. Geology. 1979;7:58–62. doi: 10.1130/0091-7613(1979)7&#x0003c;58:SOCLSC&#x0003e;2.0.CO;2. [DOI] [Google Scholar]
  • 71.Cloetingh SAPL, et al. Thermo-mechanical controls on the mode of continental collision in the SE Carpathians (Romania) Earth Planet. Sci. Lett. 2004;218:57–76. doi: 10.1016/S0012-821X(03)00645-9. [DOI] [Google Scholar]
  • 72.Koptev A, Cloetingh S, Kovács IJ, Gerya T, Ehlers TA. Controls by rheological structure of the lithosphere on the temporal evolution of continental magmatism: Inferences from the Pannonian Basin system. Earth Planet. Sci. Lett. 2021;565:116925. doi: 10.1016/j.epsl.2021.116925. [DOI] [Google Scholar]
  • 73.Koptev A, Ehlers TA, Nettesheim M, Whipp DM. Response of a rheologically stratified lithosphere to subduction of an indenter-shaped plate: Insights into localized exhumation at orogen syntaxes. Tectonics. 2019;38:1908–1930. doi: 10.1029/2018TC005455. [DOI] [Google Scholar]
  • 74.Hou KJ, Li YH, Tian YY. In situ U-Pb zircon dating using laser ablation-multi ioncouting-ICP-MS. Miner. Depos. 2009;28:481–492. [Google Scholar]
  • 75.Weis D, et al. High-precision isotopic characterization of USGS reference materials by TIMS and MC-ICP-MS. Geochem. Geophys. Geosyst. 2006;7:139–149. doi: 10.1029/2006GC001283. [DOI] [Google Scholar]
  • 76.Pu W, Zhao KD, Ling HF, Jiang SY. High precision Nd isotope measurement by Triton TI mass spectrometry. Acta Geosci. Sin. 2004;25:271–274. [Google Scholar]
  • 77.White WM, Albarède F, Télouk P. High-precision analysis of Pb isotope ratios by multi-collector ICP-MS. Chem. Geol. 2000;167:257–270. doi: 10.1016/S0009-2541(99)00182-5. [DOI] [Google Scholar]

Associated Data

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Supplementary Materials

Supplementary Table S1. (15KB, xlsx)
Supplementary Table S2. (15.8KB, xlsx)
Supplementary Table S3. (12.3KB, xlsx)

Data Availability Statement

All data generated or analysed during this study are included in this published article (and its Supplementary Information files).

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