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Article

Petrogenesis and Tectonic Significance of Middle Jurassic Mafic–Ultramafic Cumulate Rocks in Weiyuanpu, Northern Liaoning, China: Insights from Zircon Geochronology and Isotope Geochemistry

by
Yifan Zhang
1,
Xu Ma
1,2,*,
Jiafu Chen
1,2,
Yuqi Liu
1,
Yi Zhang
1 and
Yongwei Ma
1
1
Department of Geology, School of Resources and Civil Engineering, Northeastern University, Shenyang 110819, China
2
Northeast Geological Science and Technology Innovation Center of China Geological Survey, Shenyang 110034, China
*
Author to whom correspondence should be addressed.
Minerals 2025, 15(6), 651; https://doi.org/10.3390/min15060651
Submission received: 25 April 2025 / Revised: 29 May 2025 / Accepted: 2 June 2025 / Published: 17 June 2025
(This article belongs to the Special Issue Selected Papers from the 7th National Youth Geological Congress)
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Abstract

The tectonic evolution of the Paleo-Pacific Ocean and the destruction mechanism of the North China Craton (NCC) are still controversial. In this study, we conducted zircon U-Pb dating, whole-rock geochemistry, and Sr-Nd-Hf isotope analyses on the Weiyuanpu mafic–ultramafic intrusions in the eastern segment of the northern margin of the NCC to discuss their petrogenesis and tectonic implications. The Weiyuanpu mafic–ultramafic intrusions consist of troctolite, hornblendite, hornblende gabbro, gabbro, and minor diorite, anorthosite, characterized by cumulate structure. The main crystallization sequence of minerals is olivine → pyroxene → magnetite → hornblende. The zircon U-Pb ages of hornblendite, hornblende grabbro, and diorite are ~170Ma. Geochemical characteristics exhibit low-K tholeiitic to calc-alkaline series, enriched in light rare-earth elements (LREE) and significant large-ion lithophile elements (LILE), and depleted in high-field-strength elements (HFSE). Sr-Nd isotopic compositions are ISr = 0.7043–0.7055, εNd(t) = −0.7 to +0.9, and zircon εHf (t) values range from +3.4 to +8.7. These results suggest that the source region was a phlogopite-bearing garnet lherzolite mantle metasomatized by subduction fluids. The study reveals that the northeastern margin of the NCC was in a back-arc extensional setting due to the subduction of the Paleo-Pacific Ocean during the Middle Jurassic, which caused lithosphere thinning and mantle melting in this region.

1. Introduction

The eastern segment of the northern margin of the North China Craton (NCC) is sandwiched between the Yitong–Yilan Fault Zone and the Xilamulun–Changchun–Yanji Suture Zone, bordering the central NCC towards the south [1,2,3,4] (Figure 1A). From the Late Paleozoic to Early Mesozoic, the region experienced multiphase tectonic events by the Paleo-Asian Ocean tectonic events [5,6,7]; during the Mesozoic, it was superimposed by the distant effects of subduction in the Paleo-Pacific Ocean tectonic domain and the closure of the Mongol–Okhotsk Ocean [8,9]. These multi-phase tectonic events resulted in a complex geological framework and major magmatic activities, making it an ideal area for studying petrogenesis and tectonic evolution of Paleo-Pacific ocean. This research study focuses on the initiation time and subduction of Paleo-Pacific Ocean subduction, as well as the mechanisms of NCC destruction.
The subduction of the Paleo-Pacific Ocean is closely related to the large-scale magmatic activities in the northern margin of the NCC during the Mesozoic [10]. However, the subduction time of the Paleo-Pacific Ocean is still vague. Previous literature supports the initial opening of the Paleo-Pacific Ocean during the Devonian [11], Permian [8], Late Triassic (227–222 Ma) [12], Late Late Triassic [13], and early to Late Jurassic [14,15]. There are also controversies regarding subduction directions: NW-directed from 180 to 145 Ma, shifting to NNW-directed from 145 to 85 Ma [16]; NW-directed from 150 to 130 Ma, due north-directed from 130 to 110 Ma, and re-shifting to NNW-directed from 110 to 100 Ma [17].
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Figure 1. (A) A simplified tectonic map of Northeast China. (B) Geological background diagram of the study area. I: Erguna Block; II: Xing’an Block; III: Songnen–Zhangguangcailing Range Block; IV: Jiamusi—Khanka Block; V: Nadanhada Terrane; VI: Liaoyuan Terrane; a: Solonker Suture Zone; b: Xiguitu Suture Zone; c: Hegenshan Suture Zone; d: MudanJiang Suture Zone; e: Yuejinshan Suture Zone; F1: Chifeng–Kaiyuan Fault; F2: Yilan–Yitong Fault; F3: Dunhua–Mishan Fault; F4: Tanlu Fault; (revised according to [18]).
Figure 1. (A) A simplified tectonic map of Northeast China. (B) Geological background diagram of the study area. I: Erguna Block; II: Xing’an Block; III: Songnen–Zhangguangcailing Range Block; IV: Jiamusi—Khanka Block; V: Nadanhada Terrane; VI: Liaoyuan Terrane; a: Solonker Suture Zone; b: Xiguitu Suture Zone; c: Hegenshan Suture Zone; d: MudanJiang Suture Zone; e: Yuejinshan Suture Zone; F1: Chifeng–Kaiyuan Fault; F2: Yilan–Yitong Fault; F3: Dunhua–Mishan Fault; F4: Tanlu Fault; (revised according to [18]).
Minerals 15 00651 g001
The intense modification of the NCC since the Late Paleozoic, characterized by the lithospheric thinning of nearly 100 km and large-scale Mesozoic magmatic-mineralization activities, has made it an significant geoscientific research hotspot [19]. Debates on the initiation time of craton destruction focus on the Early Mesozoic (Triassic mantle-derived magmatism) [20,21], Late Mesozoic (Jurassic tectonic transition) [22], and Cenozoic (asthenospheric upwelling after 100 Ma) [23]. The mainstream view emphasizes multi-stage modification during the Jurassic–Cretaceous (180–120 Ma), where early-phase plate collisions laid the tectonic foundation for subsequent destruction [24,25].
In this study, we presented systematic study of zircon U-Pb dating, major and trace-element analyses, and Sr-Nd-Hf isotopic analyses for Middle Jurassic basic–ultrabasic cumulate rocks exposed along the northern margin of the North China Craton (Tables S1–S4). This study investigation aims to (1) clarify the petrogenesis of these cumulate rocks; (2) trace the characteristics of the mantle source region during the Jurassic period in the northern margin of the NCC; and (3) focus on the Mesozoic tectonic evolution and mantle properties of the northern margin of the NCC, offering new insights into the destruction of the NCC.

2. Geological Setting and Sampling

The Weiyuanpu mafic–ultramafic complex is located along the northwestern side of the Tan-Lu Fault Zone at the northern margin of the NCC (Figure 1B). It is divided into two adjacent pluton, i.e., the Beidalazi and Zhaojiatai plutons that are separated by the Tan-Lu Fault Zone (Figure 2). The Beidalazi pluton is located along the eastern side of Weiyuanpu Town, extending NE-SW with a total area of ~1 km2, and intruded by the Triassic granitic gneisses (Figure 3A). Within the intrusion, eye-shaped felsic gneiss xenoliths are visible, along with centimeter-scale horizontal rhythmic layers characteristic of cumulate rocks, displayed by rock layers of different colors and grain sizes (Figure 3B). The intrusion profile is ~4 km long and ~200 m deep, undeformed, with the primary lithology composed of hornblendite, followed by hornblende gabbro, gabbro, and diorite, showing transitional contacts between different lithologies.

2.1. Beidalazi Pluton

Hornblendite (23KY17C/D/E/F and 23KYZ02A/B): The hornblendite is the dominant lithology of the Beidalazi pluton, which is dark-green to black-green, with a medium-coarse grained subhedral granular texture and layered cumulate structure (Figure 3B,C). The primary minerals include hornblende (75%–90%) and pyroxene (5%–20%), with accessory minerals of magnetite, spinel, apatite, titanite, and olivine. Nearly all samples exhibit two-stage accretionary cumulate textures (Figure 4A–D): 40% of hornblende occurs as tabular–columnar large grains (1–4 mm in size) in close packing, and 60% as acicular–columnar radiating grains (0.05–0.2 mm in size). The large hornblende grains are partially altered to chlorite and clay, while the alteration in small grains is rare, confirming the two-stage cumulation. Pyroxene xenocrysts with harbor-shaped dissolution edges and magnetite xenocrysts are observed within hornblende grains, suggesting hornblende formed later than pyroxene and magnetite. Pyroxene grains show evenly distributed magnetite exsolution lamellae (Figure 4B).
Hornblende gabbro (23KYZ05 and 06A): Black-green, with a layered cumulate texture (Figure 3D). Primary minerals include plagioclase (45%–55%), hornblende (30%–40%), and pyroxene (5%–10%), with accessory minerals of minor titanite (1%–2%) and apatite (<1%). Hornblende and pyroxene in hornblende gabbro samples are subhedral granular, compactly arranged in a cumulate texture. At the same time, plagioclase is anhedral, filling intercumulate spaces (Figure 4E,F), indicating that plagioclase formed later than hornblende and pyroxene. Most plagioclase suffered sericitization and carbonatization alteration to varying degrees.
Gabbro (21LN02C and D): Petrological characteristics are similar to hornblende gabbro, also black-green with a layered cumulate texture (Figure 3E). Primary minerals include hornblende (20%–30%), pyroxene (20%), and plagioclase (50%–60%), with minor olivine and apatite (Figure 4G).
Diorite (23KYZ14A and 21LN06B): Light gray, medium-fine grained, containing basic enclaves, showing transitional contact with host granitic gneiss, and some samples exhibit obvious mylonitization. Primary minerals include plagioclase (40%–55%), quartz (15%–20%), and hornblende (25%–30%), with minor magnetite and pyroxene. Hornblende is subhedral, plagioclase is subhedral to euhedral, and quartz is anhedral, filling interstices. Harbor-shaped dissolution edges of hornblende eroded by quartz are visible (Figure 4H). Plagioclase is severely altered to clay.
The Zhaojiatai intrusion is located 8 km southwest of the Beidalazi pluton, covering ~1 km2, with Early Mesozoic granitic gneiss host rocks. The primary lithology is hornblende gabbro, intruded by layered veins of biotite tonalite containing hornblende gabbro xenoliths (xenocrysts). The core of the hornblende gabbro contains troctolite and anorthosite enclaves, with transitional contacts between lithologies.

2.2. Zhaojiatai Pluton

Troctolite (23KYZ16F): The troctolite is the most mafic component exposed in the Zhaojiatai pluton, black, medium-coarse grained, with a cumulate texture (Figure 3F). Primary minerals include plagioclase (50%), olivine (20%–30%), hornblende (10%–15%), pyroxene (5%–10%), and biotite (5%), with accessory minerals minor magnetite and apatite. Olivine is euhedral, with various cracks, reaching up to second-order top interference color, ~1 mm in size. Pyroxene shows nearly orthogonal cleavage, ~0.5 mm. Hornblende, pyroxene, and olivine are arranged in a cumulate texture, with anhedral plagioclase filling interstices (Figure 4I,J). Small pyroxene and hornblende xenocrysts are visible in plagioclase, with occasional pressure cracks. Biotite is mostly anhedral, wrapping around olivine, and some biotite contains plagioclase with harbor-shaped dissolution edges, indicating that part of the basic plagioclase formed earlier than biotite, nearly coeval with olivine.
Hornblende gabbro (23KYZ16B/L and P): The hornblende gabbro is the dominant lithology of the Zhaojiatai pluton, which is black-green to grayish-white, medium-coarse grained, with cumulate and gabbroic textures (Figure 3G). Primary minerals include hornblende (13%–40%), plagioclase (35%–60%), and pyroxene (5%–25%), with minor biotite and magnetite. Hornblende and pyroxene are closely packed, with plagioclase filling interstices, forming a typical orthocumulate texture. Pyroxene is smaller (0.5–1 mm), euhedral hexagonal, with cracks. Hornblende is euhedral, larger (3–5 mm), with individual grains exceeding 5 mm, showing prominent cleavage, and containing biotite and pyroxene xenocrysts internally. Plagioclase (~1 mm), anhedral, fills intercumulate spaces, developing numerous inclusion structures with embedded small pyroxene and hornblende grains (0.1 mm). Biotite is euhedral (~0.2 mm), commonly found inside hornblende grains, with dissolution edges (Figure 4K). These features indicate biotite formed later than pyroxene but earlier than hornblende.
Anorthosite (23KYZ16N): Light-colored, medium-grained, also with cumulate texture (Figure 3H), composed of plagioclase (85%), magnetite (5%–8%), biotite (4%–5%), and minor pyroxene and olivine. Plagioclase (~0.5 mm) is closely packed in a cumulate arrangement (Figure 4L), with occasional magnetite xenocrysts inside. Magnetite and biotite are anhedral, filling intercumulate spaces. The microscopic features of anorthosite further confirm that basic–ultrabasic plagioclase crystallized early in magmatic evolution.

3. Analytical Methods

3.1. Zircon U-Pb Dating

In this study, we have carried out U-Pb zircon dating for four samples, including hornblendite (23KY17B), hornblende gabbro (23KYZ05/23KYZ16C), and diorite (23KY16SC-1A). Zircon epoxy resin mounts for geochronological analysis were prepared at Langfang Yuneng Rock and Mineral Separation Technology Service Co., Ltd. (Langfang, China) The procedure was as follows: representative fresh, unaltered mafic–ultramafic rock samples were cleaned and dried to avoid contamination. Samples were crushed to below 100 mesh using a crushing device. Zircon grains were separated sequentially, including rinsing, soaking, magnetic separation, and heavy liquid separation. Under a binocular microscope, zircon grains with intact morphology, free of inclusions or fractures, were manually selected. These grains and the zircon reference material Qinghu were mounted on glass slides using PVC molds filled with epoxy resin and hardener. After curing, the mounts were detached, ground, and polished to expose pristine zircon surfaces for structural analysis. The polished mounts were gold-coated and imaged using a TESCAN MIRA3 (Brno, Czech Republic) field-emission scanning electron microscope (FE-SEM) at 7 kV, with an average scanning duration of 30 min per sample.
Zircon U-Pb analyses were performed at the Isotope Laboratory of the National Geological Experimental Testing Center using a laser ablation–inductively coupled plasma-mass spectrometer (LA-ICP-MS; Agilent 8900 Santa Clara, CA, USA). Laser ablation parameters included a 5 Hz repetition rate and 32 μm spot size to minimize isotopic fractionation. Helium carrier gas transported ablated aerosols through a signal homogenization device mixed with argon, enhancing signal stability by expanding aerosol dispersion. Before analysis, mounts were ultrasonically cleaned with deionized water and ethanol, followed by high-purity helium purging to reduce common Pb contamination. Instrument tuning was performed using a 32 μm line scan on NIST SRM 610 (Gaithersburg, MD, USA) to ensure U signal intensities > 8 × 105 counts per second (cps) with signal stability (RSD) < 1.5%. Oxide yields (ThO+/Th+) were maintained below 0.15%. Pre-ablation with a large beam spot was applied to remove surface contaminants. Each analysis comprised 120 s: 40 s background acquisition, 40 s sample ablation, and 40 s washout.
Zircon reference materials 91500 and NIST SRM 610 were used for U-Pb isotopic ratio and trace-element calibration, respectively. Plešovice zircon served as a secondary reference to verify age accuracy. A standard set (2 Plešovice, 2 91500, and 1 NIST SRM 610) was analyzed after every 10 unknown sample points to correct for instrumental drift. Data reduction utilized ICPMSDataCal12.2 (Liu et al., 2010) [26], with consistent blank and signal integration intervals for all samples and standards. The standard sample data obtained from the tests and their recommended reference values are provided in Table S5.
The standard zircon 91500 was used to correct for interelement fractionation. Common lead corrections followed Anderson’s method [27]. The uncertainty quoted in the data table is ±1σ, whereas the weighted mean ages are quoted at ±2σ, which are at the 95% confidence level, following analytical procedures detailed in [28].

3.2. Zircon Hf Isotope Analyses

In this study, we have performed Hf isotope analyses for four samples, including hornblendite (23KY17B), hornblende gabbro (23KYZ05/23KYZ16C), and diorite (23KY16SC-1A). Zircon in situ Hf isotope analysis used a resolution SE 193 laser ablation system attached to a Thermo Fisher Scientific Neptune Plus MC–ICP–MS (Waltham, MA, USA). A spot size of 32 μm was used for most analyses, and the ablation spot for Hf analysis was situated at the same and/or near the domain for the U-Pb dating. The standard sample data obtained from the tests and their recommended reference values are provided in Table S5. Detailed operating conditions for the laser ablation system, the MC-ICP-MS instrument, and the analytical method can be found in [29,30]. Offline selection, analysis of analyte signals, and mass bias calibrations were performed using ICPMSDataCal12.2 [26]. The depleted mantle model ages (TDM) and average crustal model ages (T-crust) were calculated using the methods suggested by [31].

3.3. Whole-Rock Major and Trace Element Analyses

Six hornblendite (23KY17C/D/E/F and 23KYZ02A/B), five hornblende gabbro (23KYZ05/06A/16B/16L and 23KYZ16P), two diorite (23KYZ14A and 21LN06B), two gabbro (21LN02C/D), one troctolite (23KYZ16F), and one anorthosite (23KYZ16N) were collected for whole-rock major and trace-element analyses. Major-element concentrations were analyzed using X-ray fluorescence spectroscopy on fused-glass disks at the National Geological Experimental Testing Center. Loss on ignition (LOI) values were measured using 1 g of powder heated to 1100 °C for one hour. The accuracy of the analyses is within 1% for most significant elements, which is determined on the Chinese National standard GBW07104 [32] and GBW07105 [33]. Trace-element concentrations were determined on inductively coupled plasma–mass spectrometry (ICP–MS, Agilent 8900) after acid digestion of samples, following the procedures of [34]. Analytical uncertainties for major and trace elements are generally less than 5% and 10%, respectively. The standard sample data obtained from the tests and their recommended reference values are provided in Table S5.

3.4. Whole-Rock Sr-Nd Isotope Analyses

Two hornblendite (23KYZ02A-1/B-1), two hornblende gabbro (23KYZ06A-1 and 23KYZ16B-1), one diorite (23KYZ14A-1), and one troctolite (23KYZ16F-1) were collected for whole-rock Sr-Nd isotope analyses. The Isotope Laboratory of the National Geological Experimental Testing Center measured part of the whole-rock Sr-Nd isotopic compositions using the method of [35]. MAT262 (Waltham, MA, USA) and Nu Plasam HR MC-ICP-MS (Nu Instruments Wrexham, UK) were certified reference standard solutions for 87Sr/86Sr and 143Nd/144Nd isotope ratios, respectively. The standard sample data obtained from the tests and their recommended reference values are shown in Table S5.

4. Analytical Results

4.1. Zircon U-Pb Age and Hf Isotopes

Supplementary Tables S1 and S2 show the zircon U-Pb ages and Hf isotope results for the Weiyuanpu pluton.
Zircon U-Pb ages were determined for hornblendite, hornblende gabbro, and diorite from the Weiyuanpu pluton. For hornblendite (sample 23KY17B), the zircon U-Pb concordia diagram, weighted mean age plot, and representative cathodoluminescence (CL) images are shown in Figure 5A. Zircons exhibit subhedral to euhedral shape, with clear oscillatory zoning in CL images, which is characteristic of magmatic zircon [36]. Th/U ratios of eleven analyzed zircons range from 0.0165 to 0.633 (mean = 0.314); excluding two abnormally low values, all others exceed 0.2, consistent with magmatic zircon characteristics. The two zircons with low Th/U ratios appear darker in CL images, suggesting U enrichment possibly caused by hydrothermal fluid alteration. The weight mean 206Pb/238U age is 171 ± 1 Ma (MSWD = 0.82). The Th contents range from 10.8 to 784.8 ppm, and U contents from 160.6 to 1343.2 ppm. Hf isotope analysis shows 176Hf/177Hf ratios of 0.282783–0.282857, εHf(t) values of +3.70 to +6.29 (Figure 6), and two-stage Hf isotope model ages of 788–953 Ma.
For diorite (sample 23KY16SC-1A), the zircon U-Pb concordia diagram, weighted mean age plot, and CL images are shown in Figure 5B. Zircons are subhedral to euhedral, with clear oscillatory zoning clear indicative of magmatic origin [36]. The weight mean 206Pb/238U age of 18 zircons is 171 ± 1 Ma (MSWD = 0.86). The Th contents range from 4.3 to 1701.4 ppm, U contents from 35.9 to 1452.8 ppm, and Th/U ratios from 0.013 to 1.619, all consistent with magmatic zircon characteristics. Hf isotope results show 176Hf/177Hf ratios of 0.282637–0.282764, εHf(t) values of −1.6 to +3.0 (Figure 6), and two-stage model ages of 1000–1293 Ma.
For hornblende gabbro (sample 23KYZ05), the zircon U-Pb concordia diagram, weighted mean age plot, and CL images are shown in Figure 5C. Zircons are subhedral to euhedral, ~100 μm in size, with obvious oscillatory zoning in CL images [36]. The weight mean 206Pb/238U age of 13 zircons is 170 ± 1 Ma (MSWD = 1.6). The Th contents range from 59.8 to 1219.2 ppm, U contents from 104.4 to 1744.4 ppm, and Th/U ratios from 0.353 to 0.847 (all >0.2, typical of magmatic zircons). Hf isotope analysis yields 176Hf/177Hf ratios of 0.282781–0.282931, εHf(t) values of +3.5 to +8.7 (Figure 6), and two-stage model ages of 631–968 Ma.
The concordia, weight mean age, and CL image diagram of hornblende gabbro from the Zhaojiatai pluton (sample 23KYZ16C) are shown in Figure 5D, with euhedral zircons displaying clear oscillatory zoning, a hallmark of magmatic origin [36]. The weighted 206Pb/238U age of 12 zircons is 170 ± 4 Ma (MSWD = 1.18). The Th contents range from 38.4 to 581.9 ppm, U contents from 104.4 to 1181.9 ppm, and Th/U ratios from 0.105 to 0.904, consistent with magmatic zircon characteristics. Hf isotope results show 176Hf/177Hf ratios of 0.282777–0.282924, εHf(t) values of +3.4 to +8.4 (Figure 6), and two-stage model ages of 651–971 Ma.
The ages of hornblende gabbro from Zhaojiatai and Beidalazi plutons are consistent within error margins, with similar Th, U contents, Th/U ratios and CL morphological features. Both plutons exhibit nearly identical Hf isotope characteristics, including 176Hf/177Hf ratios, εHf(t) values, and two-stage model ages. These features confirm that the Zhaojiatai and Beidalazi plutons are different plutons of the same magmatic body, hereafter collectively referred to as the Weiyuanpu pluton.

4.2. Whole-Rock Major and Trace-Element Analysis

The major and trace-element geochemical data for whole rocks are presented in Supplementary Table S3 and plotted in Figure 7A,B.
Anorthosite, a unique lithology, has the second-lowest SiO2 content (44.7%, just above troctolite) and is in the low-K tholeiitic series, metaluminous (A/CNK = 1.02). It features the highest Al2O3 (29.8%) and high CaO (13.8%), similar Fe2O3T (7.4%) to other mafic lithologies, and negligible MgO (0.4%). REE content is low (18.15 ppm), with a strongly “right-dipping” pattern and the most pronounced LREE/HREE fractionation (LaN/YbN = 48.8) among all lithologies, accompanied by a distinct positive Eu anomaly (Figure 8A,B). N-MORB-normalized plots show depletion in Nb, Ce, and Pr, and strong positive anomalies in Ba, La, Pb, Sr, Eu, and Ti.
Troctolite belongs to the low-K tholeiitic series, metaluminous (A/CNK = 0.838), with the lowest SiO2 content (42.8%) in the mafic–ultramafic complex, representing the ultramafic component alongside hornblendite. It has similar Fe2O3T values (10.8%) to hornblendite, the highest Mg# (75.8) and MgO content (17.1%), high Al2O3 (16.2%), and very low MnO (0.14%) and TiO2 (0.16%). Troctolite has extremely low REE content (ΣREE = 22.4 ppm), with a low-slope right-dipping REE pattern (LaN/YbN = 5.2; Figure 8A,B), weak LREE/HREE fractionation (LREE/HREE = 1.19), and a slight positive Eu anomaly. N-MORB-normalized plots show noticeable depletion in Nb, Ti, and Pr and strong positive Sr anomalies.
Hornblendite from the Weiyuanpu pluton belongs to the low-K tholeiitic to calc-alkaline series, with metaluminous composition (A/CNK = 0.242–0.417). SiO2 contents can be divided into 43.5%–46.0% and 49.4%–49.8%. All hornblendites have the highest Fe2O3T values (10.7%–13.8%) and TiO2 contents (1.1%–2.6%) among all lithologies, along with relatively high MgO (6.1%–10.7%), CaO, and Al2O3 (11.7%–15.6%) contents, and very low MnO (0.14%–0.19%). Mg# values range from 66.4 to 76.2. Hornblendites exhibit moderate to high REE contents (ΣREE = 79–176.7 ppm). Low-SiO2 hornblendites show an “up-convex” REE distribution pattern with peaks at Sm or Eu (Figure 8C,D), featuring LaN/SmN ratios of 0.5–0.6, weak LREE/HREE fractionation (LREE/HREE = 0.35–0.39), and LaN/YbN ratios of 1.9–2.8. In contrast, high-SiO2 hornblendites lack the “up-convex” shape, with LaN/SmN = 1.3–1.4, more obvious LREE/HREE fractionation (LREE/HREE = 0.6–1.1), and higher LaN/YbN ratios (4.9–5.7). N-MORB-normalized diagrams show significant depletion in Nb, P, Zr, and Hf, and enrichment in K, Pb, Nd, and Sr.
Hornblende gabbro, the dominant mafic lithology and most widely exposed in the Zhaojiatai pluton, belongs to the low-K tholeiitic to calc-alkaline series (one sample shows high-K characteristics), metaluminous (A/CNK = 0.368–0.745), with SiO2 contents of 44.9%–53.0%. It has Fe2O3T and MgO contents (4.9%–9.9%, 7.3%–11.1%), second only to hornblendite and troctolite, along with high CaO (8.8%–17.7%) and Al2O3 (12.8%–19.7%), and very low MnO (0.10%–0.16%). REE contents range from 52.5 to 129.5 ppm, displaying a “right-dipping” pattern with LREE enrichment and HREE depletion in chondrite-normalized diagrams (LaN/YbN = 3–6.7; Figure 8E,F). N-MORB-normalized plots show significant depletion in Nb, Ti, P, and Pr, and strong positive anomalies in Sr, Nd, and Pb.
Gabbro, rare in pluton and similar to hornblende gabbro in field appearance, exhibits distinct geochemical characteristics, belonging to the low-K tholeiitic series but peraluminous (A/CNK = 1.833–1.893), with SiO2 = 51.8%–52.8%. It has comparable Fe2O3T and MgO contents (7.2%–7.6%, 8.2%–8.5%) to hornblende gabbro, higher Al2O3 (14.3%–14.9%), and lower CaO (∼3.4%). Notably, gabbro has exceptionally high MnO contents (9.9%–10.2%), distinguishing it from hornblende gabbro. REE contents are high (132.8–134.2 ppm) with a “right-dipping” pattern (LaN/YbN = 4.9–5.2; Figure 8E,F). N-MORB-normalized diagrams show significant depletion in K, Ba, P, and Ti, and positive anomalies in Sr, U, Pb, and weak Nd.
Diorite samples belong to the low-K tholeiitic and calc-alkaline series, metaluminous (A/CNK = 0.841–1.022), with SiO2 = 58.1%–61.7%. It has lower Fe2O3T (5.3%–6.0%) and MgO (1.6%–3.4%), low CaO (5.0%–5.9%), high Al2O3 (16.1%–18.2%), and elevated Na2O (1.7%–4.7%). Although in diorite sample plots within the monzonite field, it is located near the boundary between monzonite and diorite. Based on its microscopic characteristics and field occurrence, this rock should still be classified as diorite. REE contents are high (115.9–215.9 ppm) with steep “right-dipping” patterns (LaN/YbN = 19.7–19.8). N-MORB-normalized diagrams show depletion in K, Ce, Pr, P, and Ti, and strong positive anomalies in La, Pb, Sr, and Nd (Figure 8G,H).

4.3. Sr-Nd Isotopes of the Whole Rock

Whole-rock Sr-Nd isotope testing was performed on selected hornblendite, hornblende gabbro, diorite, and troctolite samples from the Weiyuanpu intrusion. The calculated ages were derived from the zircon U-Pb dating results of corresponding lithologies reported in this study. The whole-rock Sr-Nd isotope data are presented in Supplementary Table S4.
All lithologies exhibit slightly enriched Sr isotopes, with Nd isotopes ranging from weakly depleted to weakly enriched. Troctolite shows the most depleted Nd isotope signature (ISr = 0.7047, εNd(t) = −0.71). Hornblendite, together with troctolite as the most mafic components of the Weiyuanpu intrusion, has the lowest Sr isotope values (ISr 0.7043–0.7049, εNd(t)= +0.31–+0.41). Hornblende gabbro displays a broader range of Nd isotopes (ISr = 0.7053~0.7055, εNd(t) = (−0.10~+0.66), possibly indicating that its formation spanned the entire evolution of the intrusion. Diorite has the most enriched Nd isotopes (ISr = 0.7051, εNd(t) = +0.9197; Figure 9).

5. Discussion

5.1. Petrogenesis

The Beidalazi pluton exposed in Weiyuanpu Town, Kaiyuan, northern Liaoning, and the hornblendite, troctolite, hornblende gabbro, gabbro, anorthosite, and diorite in the Zhaojiatai intrusion share nearly identical zircon U-Pb ages and similar geochemical and Sr-Nd isotopic characteristics. This indicates that they originated from the same parental magma and belong to a single magmatic event, collectively referred to as the Weiyuanpu pluton.
The mafic–ultramafic components (hornblendite, troctolite, hornblende gabbro, gabbro, and anorthosite) in the Weiyuanpu pluton exhibit distinct layered cumulate textures, conforming to the cumulate rock characteristics defined by Wager in 1960 [46]. Transitional contacts are observed between different lithologies. Microscopically, troctolite—the most mafic lithology—shows hornblende, pyroxene, and olivine arranged in a cumulate texture, with anhedral plagioclase filling interstices. Small pyroxene and hornblende xenocrysts are visible in plagioclase, along with occasional pressure cracks. Biotite, mostly anhedral, wraps around olivine, and some biotite contains plagioclase with harbor-shaped dissolution edges. Hornblendite features dense cumulate textures of hornblende with accretionary cumulate structures: large hornblende grains (partially altered to chlorite and clay) and rare alteration in small grains confirm two-stage cumulation. Pyroxene xenocrysts with harbor-shaped dissolution edges and magnetite xenocrysts within hornblende indicate hornblende formed after pyroxene and magnetite. Pyroxene grains show evenly distributed magnetite exsolution lamellae. In hornblende gabbro, subhedral hornblende and pyroxene are compactly arranged in a cumulate texture, with anhedral plagioclase filling intercumulate spaces. Anorthosite’s cumulate plagioclase occasionally contains magnetite xenocrysts, with anhedral magnetite and biotite filling interstices. The consistent cumulate textures across lithologies indicate a cumulate origin for the Weiyuanpu intrusion. Microscopic observations suggest the main mineral crystallization sequence: olivine → pyroxene → magnetite → hornblende, with plagioclase crystallizing throughout the process.
Trace-element characteristics further support the cumulate origin. Some hornblendites (low-SiO2 type) exhibit “up-convex” REE patterns with peaks at Sm or Eu, similar to REE partitioning in cumulate minerals, indicating control by cumulate processes and typical cumulate rock features (Figure 8C) [47]. Heavy rare-earth elements (HREE) are relatively flat, and anorthosite, hornblende gabbro, and troctolite show varying degrees of positive Eu anomalies, indicative of plagioclase crystallization. Nearly parallel trace and REE patterns among end members suggest that the fractional crystallization of the mafic parent magma dominated the magmatic process, with minor assimilation–contamination. In Harker diagrams (Figure 10), CaO, FeO, Fe2O3, MgO, TiO2, Cr, Co, and V decrease with increasing SiO2, reflecting the fractional crystallization of mafic minerals (e.g., hornblende and pyroxene), while Al2O3 and Na2O show increasing trends. Since V is a compatible element in hornblende and Al2O3/Na2O mainly reside in plagioclase, this linear trend indicates a gradual increase in plagioclase proportion during magmatic evolution, consistent with the cumulate origin [48].

5.2. Source Characteristics

Cumulate-origin rocks are generally products of early magmatic evolution. The abundant occurrence of hornblende indicates that hornblende was a mineral close to the liquidus during diagenesis. Experiments show that hornblende crystallizes from the melt at 400 MPa with ~5 wt% water or 960 MPa with 7–9 wt% water content [49,50]. Therefore, the presence of hornblendite and hornblende gabbro with abundant hornblende suggests the early magmatic evolution stage contained a certain amount of water.
The N-MORB-normalized multi-element diagram (normalization values after [41]) effectively constrains the pluton’s subduction-related origin. As illustrated in Figure 8, pronounced positive anomalies in fluid-mobile elements (Rb, Cs, U, Pb, and K) coupled with marked negative anomalies in high-field-strength elements (Nb, Ta) collectively indicate fluid-related metasomatism within this magmatic system.
Nb and Th are high-field-strength elements (HFSE), generally insoluble in fluids but showing different incompatibilities in melts. Th is more incompatible than Nb, and thus enriches earlier during partial melting. Zr, also an HFSE with low mobility, is a reference element [51,52]. Th preferentially enters the melt during low-degree partial melting, significantly increasing Th/Zr, while Nb/Zr increases moderately. If fluids carry Th (e.g., Th-rich hydrothermal activity), source-region Th/Zr may rise; however, Nb and Zr are less affected by fluids, leading to limited ratio changes and trends distinct from melting [26,53]. Rb, a large-ion lithophile element (LILE), is highly soluble in fluids and incompatible in melting. Y, a middle rare-earth element (MREE), is firmly retained in residual garnet during melting, causing Y depletion in the melt [54]. Nb is controlled by residual rutile—Nb depletion occurs in the melt if rutile remains. High Rb/Y reflects garnet retention (Y depletion), and low Nb/Y indicates rutile retention (Nb depletion), typical of high-pressure melting environments (e.g., subduction zones). Fluids carrying Rb may increase Rb/Y, but without mineral residue control, Nb/Y changes little, differing from melting trends. Melt-dominated processes show significant increases in Th/Zr and Rb/Y, accompanied by decreasing Nb/Y, reflecting melting mineral control. Fluid involvement causes local Th/Zr increases and Rb/Y increases without synchronous Nb/Y decreases, indicating the fluid enrichment of LILE. Plotting all lithologies on Nb/Zr vs. Th/Zr and Rb/Y vs. Nb/Y diagrams (Figure 11) shows that the Weiyuanpu pluton exhibits low Nb/Zr and Nb/Y ratios, consistent with fluid-enriched trends.
Melts derived from the partial melting of mantle peridotite with residual garnet have low Yb contents and high LREE (e.g., La, Sm)/Yb ratios, whereas the melting of spinel lherzolite sources produces relatively flat trends. In the Sm/Yb vs. Sm diagram (Figure 12A), mafic–ultramafic rocks show higher Sm/Yb ratios than spinel lherzolite, more similar to garnet lherzolite. In the (La/Sm)N vs. (Tb/Yb)N diagram (Figure 12B), data from the Weiyuanpu pluton fall near the boundary between spinel and garnet peridotite, closer to garnet peridotite, consistent with the Sm/Yb-Sm diagram. All of these indicate that the Weiyuanpu pluton formed from a moderate degree (10%–50%) of the melting of a garnet (with minor spinel) lherzolite mantle containing phlogopite.
The main hydrous minerals in mantle rocks are hornblende and phlogopite. Melting experiments show that phlogopite-bearing mantle-derived magmas have higher Rb/Sr and lower Ba/Rb ratios than hornblende-bearing magmas [30]. Samples from the Weiyuanpu pluton generally exhibit high Rb/Sr and low Ba/Rb ratios (Figure 13), indicating the dominant hydrous mineral in the mantle source was phlogopite rather than hornblende. Suppose a phlogopite-rich mantle is metasomatized by slab-derived fluids from subducted oceanic crust. In that case, this process may introduce significant Ca, Al, and H2O, favoring the formation of amphibole over phlogopite. Consequently, amphibole-rich lithologies can develop within the mantle wedge above subduction zones. The formation of phlogopite in the mantle wedge is likely related to subduction-zone fluid metasomatism, suggesting the Weiyuanpu pluton originated from garnet (with minor spinel) lherzolite metasomatized by subduction-related fluids, forming phlogopite-bearing lherzolite.

5.3. Jurassic Tectonic Evolution of the Eastern Segment of the Northern Margin of the North China Craton

The lithospheric mantle of the NCC is generally considered to have enriched characteristics, a mainstream view in current research [48,62]. The 87Sr/86Sr ratios (0.70425–0.70545) of the Weiyuanpu pluton are slightly higher than typical depleted mantle (DMM: 0.702–0.704) but much lower than continental crust (>0.710), indicating mild enrichment in the source region. εNd(t) values (−0.7 to +0.9), close to the chondritic uniform reservoir (CHUR, εNd(t) = 0), fall between depleted mantle (εNd(t) > +8) [63] and enriched mantle (εNd(t) < 0). The variation in whole-rock Sr-Nd isotopes from slight depletion to slight enrichment suggests the plutons formed from a transitional mantle source region, potentially involving lithospheric mantle melting, subducted material recycling, or crustal contamination [64]. The significantly positive εHf(t) values suggest a dominant depleted mantle source, possibly indicating the intrusion originated from the partial melting of lithospheric mantle triggered by upwelling asthenospheric mantle, with the mixing of enriched components (subduction-related metasomatic products) and depleted asthenosphere. The Sr-Nd isotopes of the Weiyuanpu pluton exhibit decoupling, manifested as elevated εNd(t) values, a feature that often indicates the addition of subducted components [65].
The timing of the Paleo-Pacific Ocean subduction remains controversial. Zircon geochronological analyses of the Weiyuanpu pluton indicate its formation at 170 Ma, while geochemical data suggest a back-arc extensional setting, implying that the subduction of the Paleo-Pacific Ocean might have initiated by this time. Additionally, extensive Jurassic magmatic activities have been documented in the eastern segment of the northern margin of the NCC. The geochronological data are presented in Table S6, which summarizes the Late Triassic to Middle Jurassic magmatic activity in Kaiyuan and surrounding areas. Early Jurassic magmatism was dominated by granodiorite and diorite (Figure 14), such as the Dadingzi (200 ± 3 Ma) and Qishiergedingzi (200 ± 1 Ma) intrusions [10], characterized by high-K calc-alkaline affinities, enriched LREE and LILE, and depleted HFSE features typical of subduction-related arc magmatism. The Middle Jurassic marked the peak of magmatism, with widespread monzogranite, granodiorite, and minor diorite (e.g., Tiangang (175 ± 3 Ma), Dalinggou (176 ± 1 Ma), and Qingniushan syenogranite (178 ± 2 Ma) intrusions [66,67]). These rocks show high SiO2, low MgO, and elevated Sr/Y and (La/Yb)N ratios in some adakitic rocks, indicating the melting of thickened lower crust. Starting in the early Jurassic, magmatism along the northeastern NCC margin became increasingly frequent, peaking in the late Early Jurassic before declining. Most Jurassic magmatic rocks exhibit active continental margin characteristics. In the Early Jurassic, a large number of porphyry-type molybdenum deposits associated with porphyry bodies developed in the Xiaoxing’anling–Zhangguangcailing area [68]. The intrusion and eruption of Early Jurassic intermediate–acid magmas provided heat sources, material sources, and ore-hosting spaces for the formation of porphyry-type molybdenum deposits. Most porphyry-type molybdenum deposits occur in or are controlled by intermediate–acid meso-epizonal intrusive rocks or subvolcanic rocks, such as the Daheishan molybdenum deposit. They are characterized by active continental margin tectonics, particularly developing near paleosuture zones or faults [69]. The formation of the continental margin transcurrent fault system including the Dunhua–Mishan Fault and the occurrence of large-scale sinistral strike-slip events [70,71], combined with the aforementioned evidence of magmatic activity in the region, indicate that the subduction of the Paleo-Pacific Ocean had already commenced in the Middle Jurassic.
Back-arc basin basalts (BABB) typically exhibit a pronounced Th positive anomaly, meaning their Th/N-MORB ratios are significantly greater than 1 (usually >2, and often even higher). This reflects the influence of metasomatism by subduction zone-derived fluids on the source region, originating from the preferential extraction of high-field-strength elements (HFSE) like Nb-Ta by subducting slab fluids/melts. Samples from a back-arc extensional setting generally do not display a strong Nb negative anomaly (i.e., their Nb/N-MORB ratios are close to or slightly below 1). In the back-arc extensional environment, while subduction influence is present, the extensional process leads to a higher degree of decompression melting, and the source region may be closer to a depleted mantle source less modified by subduction [72]. In Figure 15, the geochemical characteristics of the Weiyuanbao rock bodies exhibit strong BABB signatures, indicating their derivation from a subduction-induced back-arc extensional setting.
During the Late Jurassic (~170 Ma), the Paleo-Pacific Ocean initiated low-angle subduction beneath the East Asian continental margin, a process considered the initial dynamic trigger for the destruction of the NCC [19]. At this time, the subducted slab likely underthrusts the NCC in a flat-slab manner, leading to intense metasomatism of the lithospheric mantle caused by hydrous fluids released from the slab. These slab-derived fluids caused the replacement of refractory cratonic mantle by hydrous oceanic mantle components, resulting in lithospheric thinning from >200 km to <80 km [73]. The partial melting of such a metasomatically enriched lithospheric mantle is likely caused by the upwelling of asthenospheric mantle [74]. Such fluid metasomatism significantly lowered the mantle melting point, promoting partial melting and generating hydrous mafic–ultramafic magmatic source regions. The Yanshan Movement played a crucial role in the deconcratonization of the NCC, causing significant crustal deformation of the NCC [75,76]. Between 170 and 165 Ma, regional angular unconformity can be seen from beneath ancient strata with folding deformation [77]; strata above the unconformity may have been deposited in a general extensional environment. Integrating regional magmatic characteristics with the above analysis, the Weiyuanpu pluton is inferred to have formed during Jurassic subduction of the Paleo-Pacific Ocean beneath Eurasia, which triggered back-arc extension, mantle melting, and asthenospheric upwelling associated with cratonic thinning, ultimately producing hydrous mafic–ultramafic magmas.

6. Conclusions

Based on petrological, chronological, mineralogical, geochemical, and isotopic studies of the mafic–ultramafic (hornblende-rich plutonic) rocks in Weiyuanpu, Kaiyuan, northern Liaoning, the following conclusions are drawn:
  • The Weiyuanpu mafic–ultramafic intrusions consist of hornblendite, troctolite, hornblende gabbro, gabbro, diorite, and anorthosite. Zircon age dating suggests that they are Middle Jurassic (~170 Ma) mafic–ultramafic complex along the northern margin of the NCC.
  • Hornblendite, troctolite, hornblende gabbro, gabbro, and anorthosite in the Weiyuanpu pluton are of cumulate origin, while diorite represents residual components. The main mineral crystallization sequence is olivine → pyroxene → magnetite → hornblende, with plagioclase forming throughout the process.
  • The Weiyuanpu pluton originated from garnet (with minor spinel) lherzolite in the mantle wedge, which was metasomatized by subduction-related fluids, forming phlogopite-bearing lherzolite.
  • The Weiyuanpu cumulates likely formed during Middle Jurassic subduction of the Paleo-Pacific Ocean beneath Eurasia. This process induced back-arc extension, NCC lithospheric thinning and mantle melting, generating water-rich mafic–ultramafic magmas.

Supplementary Materials

The following supporting information can be downloaded at: https://www.mdpi.com/article/10.3390/min15060651/s1, Table S1: Zircon U-Pb data for hornblendite, hornblende gabbro, and diorite.; Table S2: In situ zircon Lu-Hf isotopic compositions of hornblendite, hornblende gabbro, and diorite in Weiyuanpu. Table S3: Whole-rock major-element compositions (wt.%) and trace-element concentrations (×10−6) of various lithologies in Weiyuanpu; Table S4: Whole-rock Sr-Nd isotopic compositions of norite, hornblende gabbro, hornblendite, and diorite in Weiyuanpu; Table S5: Measured vs. recommended values of Certified Reference Materials (CRMs) in all experiments; Table S6: Late Triassic–Middle Jurassic magmatic activity in Kaiyuan and adjacent areas [78,79,80,81,82].

Author Contributions

Conceptualization, Y.Z. (Yifan Zhang); methodology, Y.Z. (Yifan Zhang); software, Y.Z. (Yi Zhang) and Y.L.; formal analysis, J.C. and Y.Z. (Yi Zhang); investigation, Y.M.; writing—original draft preparation, Y.Z. (Yifan Zhang) and X.M.; writing—review and editing, Y.Z. (Yifan Zhang), J.C. and X.M.; funding acquisition, X.M. All authors have read and agreed to the published version of the manuscript.

Funding

This work was supported by the Liaoning Provincial Natural Science Foundation of China [2024-MSLH-505] and the funding project of Northeast Geological S&T Innovation Center of China Geological Survey [QCJJ2023-27].

Data Availability Statement

The authors confirm that all data are presented in the paper.

Acknowledgments

We appreciate Mingyao Qu, Hao Chen for their contributions to this article. We specifically extend our gratitude to Falak (Postdoctoral Researcher) from the research team for the professional language polishing of this manuscript, which significantly enhanced the clarity of scientific communication.

Conflicts of Interest

The authors declare no conflicts of interest.

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Figure 2. Geological map and sampling points of the study area.
Figure 2. Geological map and sampling points of the study area.
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Figure 3. Field images of Weiyuanpu pluton. (A) Hornblende gabbro intrudes into Triassic gneiss, with augen K-feldspar enclaves observed in the hornblende gabbro; (B,C) hornblendite with layered cumulate texture; (D) hornblende gabbro with cumulate texture; (E) gabbro with cumulate texture; (F) anorthosite and troctolite; (G) hornblende gabbro; (H) hornblende gabbro and anorthosite.
Figure 3. Field images of Weiyuanpu pluton. (A) Hornblende gabbro intrudes into Triassic gneiss, with augen K-feldspar enclaves observed in the hornblende gabbro; (B,C) hornblendite with layered cumulate texture; (D) hornblende gabbro with cumulate texture; (E) gabbro with cumulate texture; (F) anorthosite and troctolite; (G) hornblende gabbro; (H) hornblende gabbro and anorthosite.
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Figure 4. Photomicrographs of Weiyuanpu pluton (Am—Amphibole; Aug—Augite; Mag—Magnetite; Pl—Plagioclase; Qtz—Quartz; Ol—Olivine; Bt—Biotite). (A–H) Photomicrographs of Beidalazi pluton showing major minerals; (I–L) photomicrographs of Zhaojiataicun pluton showing major minerals.
Figure 4. Photomicrographs of Weiyuanpu pluton (Am—Amphibole; Aug—Augite; Mag—Magnetite; Pl—Plagioclase; Qtz—Quartz; Ol—Olivine; Bt—Biotite). (A–H) Photomicrographs of Beidalazi pluton showing major minerals; (I–L) photomicrographs of Zhaojiataicun pluton showing major minerals.
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Figure 5. Age concordance diagram, weighted average diagram. and cathodoluminescence diagram of representative zircon grains from the Weiyuanpu pluton. (A) Zircon U-Pb ages of hornblendite samples; (B,C) Zircon U-Pb ages of hornblende gabbro samples; (D) Zircon U-Pb ages of diorite samples.
Figure 5. Age concordance diagram, weighted average diagram. and cathodoluminescence diagram of representative zircon grains from the Weiyuanpu pluton. (A) Zircon U-Pb ages of hornblendite samples; (B,C) Zircon U-Pb ages of hornblende gabbro samples; (D) Zircon U-Pb ages of diorite samples.
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Figure 6. εHf(t) versus age plot for samples. (after [35,37,38]).
Figure 6. εHf(t) versus age plot for samples. (after [35,37,38]).
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Figure 7. (A) K2O-SiO2 diagram (after [39]). (B) TAS diagram of igneous rocks (after [40]) 1—olivine gabsite; 2a—alkaline gabbro; 2b—subalkaline gabbro; 3—gabbro diorite; 4—diorite; 5—granodiorite; 6—granite; 7—silicolite; 8—II gaprogabbro; 9—monzonite; 10—monzonite; 11—quartz monzonite; 12—syenite; 13—parafalite; 14—parasfeldspar monzondiorite; 15—feldspathoid monobasic syenite; 16—sublong syenite; 17—sublong pluton; 18—aegirine sodium/phosphorous nepheline/coarse garnet.
Figure 7. (A) K2O-SiO2 diagram (after [39]). (B) TAS diagram of igneous rocks (after [40]) 1—olivine gabsite; 2a—alkaline gabbro; 2b—subalkaline gabbro; 3—gabbro diorite; 4—diorite; 5—granodiorite; 6—granite; 7—silicolite; 8—II gaprogabbro; 9—monzonite; 10—monzonite; 11—quartz monzonite; 12—syenite; 13—parafalite; 14—parasfeldspar monzondiorite; 15—feldspathoid monobasic syenite; 16—sublong syenite; 17—sublong pluton; 18—aegirine sodium/phosphorous nepheline/coarse garnet.
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Figure 8. Chondrite-normalized rare earth element patterns and N-MORB–normalized trace-element spider diagrams for the magmatic rocks studied. Normalizing data for the chondrite and N-MORB are from [41]. (A) REE distribution patterns of anorthosite and troctolite; (B) N-MORB normalized trace element spider diagrams of anorthosite and troctolite; (C) REE distribution patterns of hornblendite (low-SiO2 and high-SiO2); (D) N-MORB normalized trace element spider diagrams of hornblendite (low-SiO2 and high-SiO2); (E) REE distribution patterns of hornblende gabbro and gabbro; (F) N-MORB normalized trace element spider diagrams of hornblende gabbro and gabbro; (G) REE distribution patterns of diorite; (H) N-MORB normalized trace element spider diagrams of diorite.
Figure 8. Chondrite-normalized rare earth element patterns and N-MORB–normalized trace-element spider diagrams for the magmatic rocks studied. Normalizing data for the chondrite and N-MORB are from [41]. (A) REE distribution patterns of anorthosite and troctolite; (B) N-MORB normalized trace element spider diagrams of anorthosite and troctolite; (C) REE distribution patterns of hornblendite (low-SiO2 and high-SiO2); (D) N-MORB normalized trace element spider diagrams of hornblendite (low-SiO2 and high-SiO2); (E) REE distribution patterns of hornblende gabbro and gabbro; (F) N-MORB normalized trace element spider diagrams of hornblende gabbro and gabbro; (G) REE distribution patterns of diorite; (H) N-MORB normalized trace element spider diagrams of diorite.
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Figure 9. An illustration of the correlation of Sr-Nd isotopes (after [42,43,44,45]).
Figure 9. An illustration of the correlation of Sr-Nd isotopes (after [42,43,44,45]).
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Figure 10. Harker diagram of Weiyuanpu pluton. (A) Fe2O3 versus SiO2 plot for samples; (B) FeO versus SiO2 plot for samples; (C) MgO versus SiO2 plot for samples; (D) CaO versus SiO2 plot for samples; (E) Al2O3 versus SiO2 plot for samples; (F) K2O versus SiO2 plot for samples; (G) Na2O + K2O versus SiO2 plot for samples; (H) V versus SiO2 plot for samples; (I) Ba versus SiO2 plot for samples; (J) Cr versus SiO2 plot for samples; (K) TiO2 versus SiO2 plot for samples; (L) Ni versus SiO2 plot for samples;.
Figure 10. Harker diagram of Weiyuanpu pluton. (A) Fe2O3 versus SiO2 plot for samples; (B) FeO versus SiO2 plot for samples; (C) MgO versus SiO2 plot for samples; (D) CaO versus SiO2 plot for samples; (E) Al2O3 versus SiO2 plot for samples; (F) K2O versus SiO2 plot for samples; (G) Na2O + K2O versus SiO2 plot for samples; (H) V versus SiO2 plot for samples; (I) Ba versus SiO2 plot for samples; (J) Cr versus SiO2 plot for samples; (K) TiO2 versus SiO2 plot for samples; (L) Ni versus SiO2 plot for samples;.
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Figure 11. Petrogenetic discrimination plots of the Weiyuanpu pluton studied: (A) Nb/Zr versus Th\Zr (after [55]). (B) Rb/Y versus Nb/Y (after [56]).
Figure 11. Petrogenetic discrimination plots of the Weiyuanpu pluton studied: (A) Nb/Zr versus Th\Zr (after [55]). (B) Rb/Y versus Nb/Y (after [56]).
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Figure 12. Petrogenetic discrimination plots of the Weiyuanpu pluton studied: (A) Sm/Yb versus Sm; the melting curves correspond to spinel lherzolite (modal and melt modes: ol 0.530 + opx 0.270 + cpx 0.170 + sp 0.030, and ol 0.060 + opx 0.280 + cpx 0.670 + sp 0.110) (after [57]) and garnet lherzolite (modal and melt modes: ol 0.600 + opx 0.200 + cpx 0.100 + gt 0.100, and ol 0.030 + opx 0.160 + cpx 0.880 + gt 0.090) (after [58]). Mineral/matrix partition coefficients and DMM (Depleted MORB Mantle) values are from [59,60]. Primitive Mantle (PM), N-MORB, and E-MORB compositions are cited from [41]. The numbers along each curve indicate the degree of partial melting for the given mantle source regions. (B) (La/Sm)N versus (Tb/Yb)N.
Figure 12. Petrogenetic discrimination plots of the Weiyuanpu pluton studied: (A) Sm/Yb versus Sm; the melting curves correspond to spinel lherzolite (modal and melt modes: ol 0.530 + opx 0.270 + cpx 0.170 + sp 0.030, and ol 0.060 + opx 0.280 + cpx 0.670 + sp 0.110) (after [57]) and garnet lherzolite (modal and melt modes: ol 0.600 + opx 0.200 + cpx 0.100 + gt 0.100, and ol 0.030 + opx 0.160 + cpx 0.880 + gt 0.090) (after [58]). Mineral/matrix partition coefficients and DMM (Depleted MORB Mantle) values are from [59,60]. Primitive Mantle (PM), N-MORB, and E-MORB compositions are cited from [41]. The numbers along each curve indicate the degree of partial melting for the given mantle source regions. (B) (La/Sm)N versus (Tb/Yb)N.
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Figure 13. Diagram of Ba/Rb-Rb/Sr of the Weiyuanpu pluton [61].
Figure 13. Diagram of Ba/Rb-Rb/Sr of the Weiyuanpu pluton [61].
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Figure 14. (A) Simplified tectonic map of Northeast China. (B) Distribution map of Late Triassic–Middle Jurassic magmatic activity in Kaiyuan and adjacent areas [13] (Chronological data are presented in Table S6).
Figure 14. (A) Simplified tectonic map of Northeast China. (B) Distribution map of Late Triassic–Middle Jurassic magmatic activity in Kaiyuan and adjacent areas [13] (Chronological data are presented in Table S6).
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Figure 15. Tectonic interpretation based on ThN-NbN systematics [72].
Figure 15. Tectonic interpretation based on ThN-NbN systematics [72].
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Zhang, Y.; Ma, X.; Chen, J.; Liu, Y.; Zhang, Y.; Ma, Y. Petrogenesis and Tectonic Significance of Middle Jurassic Mafic–Ultramafic Cumulate Rocks in Weiyuanpu, Northern Liaoning, China: Insights from Zircon Geochronology and Isotope Geochemistry. Minerals 2025, 15, 651. https://doi.org/10.3390/min15060651

AMA Style

Zhang Y, Ma X, Chen J, Liu Y, Zhang Y, Ma Y. Petrogenesis and Tectonic Significance of Middle Jurassic Mafic–Ultramafic Cumulate Rocks in Weiyuanpu, Northern Liaoning, China: Insights from Zircon Geochronology and Isotope Geochemistry. Minerals. 2025; 15(6):651. https://doi.org/10.3390/min15060651

Chicago/Turabian Style

Zhang, Yifan, Xu Ma, Jiafu Chen, Yuqi Liu, Yi Zhang, and Yongwei Ma. 2025. "Petrogenesis and Tectonic Significance of Middle Jurassic Mafic–Ultramafic Cumulate Rocks in Weiyuanpu, Northern Liaoning, China: Insights from Zircon Geochronology and Isotope Geochemistry" Minerals 15, no. 6: 651. https://doi.org/10.3390/min15060651

APA Style

Zhang, Y., Ma, X., Chen, J., Liu, Y., Zhang, Y., & Ma, Y. (2025). Petrogenesis and Tectonic Significance of Middle Jurassic Mafic–Ultramafic Cumulate Rocks in Weiyuanpu, Northern Liaoning, China: Insights from Zircon Geochronology and Isotope Geochemistry. Minerals, 15(6), 651. https://doi.org/10.3390/min15060651

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