Paleoproterozoic Plate Tectonics Recorded in the Northern Margin Orogen, North China Craton

The occurrence of plate tectonic processes on Earth during the Paleoproterozoic is supported by ca. 2.2–1.8 Ga subduction‐collision orogens associated with the assembly of the Columbia‐Nuna supercontinent. Subsequent supercontinent breakup is evidence by global ca. 1.8–1.6 Ga large igneous provinces. The North China craton is notable for containing Paleoproterozoic orogens along its margins, herein named the Northern Margin orogen, yet the nature and timing of orogenic and extensional processes of these orogens and their role in the supercontinent cycle remain unclear. In this contribution, we present new field observations, U‐Pb zircon and baddeleyite geochronology dates, and major/trace‐element and isotope geochemical analyses from the northern margin of the North China craton that detail its Paleoproterozoic tectonic and magmatic history. Specifically, we record the occurrence of ca. 2.2–2.0 Ga magmatic arc rocks, ca. 1.9–1.88 Ga tectonic mélange and mylonitic shear zones, and folded lower Paleoproterozoic strata. These rocks were affected by ca. 1.9–1.8 Ga granulite‐facies metamorphism and ca. 1.87–1.78 Ga post‐collisional, extension‐related magmatism along the cratonal northern margin. We interpret that the generation and emplacement of these rocks, and the coupled metamorphic and magmatic processes, were related to oceanic subduction and subsequent continent‐continent collision during the Paleoproterozoic. The occurrence of ca. 1.77–1.73 Ga mafic dykes and ca. 1.75 Ga mylonitic shear zones along the northern margin of the North China craton may have been related to a regional mantle plume event. Our results are consistent with modern style plate tectonics, including oceanic subduction‐related plate convergence and continent‐continent collision, operating in the Paleoproterozoic.

occurrence of an Archean paired metamorphic belt, a fundamental characteristic of asymmetric convergent plate boundaries, indicating westward-directed subduction beneath an intra-oceanic arc along a ∼1,600-km-long belt of accretionary mélange (e.g., T. M. Kusky et al., 2016;J. P. Wang et al., , 2019Wu, Wang, et al., 2022;Zhong et al., 2021Zhong et al., , 2022. Alternative to interpretations of modern-style plate tectonic events, researchers have proposed that vertical plume-related tectonics involving crustal delamination and volcanic resurfacing are evidenced in the Archean-Paleoproterozoic rock record. For example, Peng et al. (2022) proposed that large igneous provinces across portions of the extinct Columbia-Nuna supercontinent reflect the occurrence of a ca. 1.8 Ga pulsating plume that was responsible for ancient plate motion.
The North China craton together with the Siberian, Baltica, Laurentian, North Australian, and Indian cratons likely formed the core of the Proterozoic Columbia-Nuna supercontinent (e.g., Meert, 2012;Rogers & Santosh, 2002;Zhao et al., 2002). The configuration of cratons forming the supercontinent remains debated, which is partially due to an inadequate understanding of the Paleoproterozoic rocks that form the margins of the cratons and their tectonic histories (Figure 1a). This problem is exemplified by the disagreement regarding the Paleoproterozoic tectonic history of the North China cratonal margins. One proposed end-member model for the tectonic development of the Paleoproterozoic North China orogen includes the formation of the southwest-trending Trans-North China orogen during the collision between the Eastern and Western blocks (e.g., Faure et al., 2007;Kröner et al., 2005Kröner et al., , 2006Trap et al., 2009Trap et al., , 2012S. H. Zhang et al., 2007;Zhao et al., 2005). In this model, the Western block comprises both the Yinshan block of the northern North China margin and the Ordos block that collided with the Khondalite series at ca. 1.92 Ga. A second end-member model involves the tectonic development of the Paleoproterozoic east-trending North Margin orogen from the collision between  Wu et al. (2018). The North China craton is divided into the Eastern and Western blocks, Central Orogenic belt, and Northern Margin orogen. (b) Simplified geological map of the northern margin of the North China craton, based on our field observations and modified from Wu, Wang, et al. (2022). The locations of detailed geological maps are shown.

Geological Setting
The North China craton is bounded by the early Paleozoic Qilian orogen to the southwest, the late Paleozoic Central Asian Orogenic System to the north, and the Mesozoic Qinling-Dabie Shan orogen to the south (Figure 1a) (e.g., Zuza & Yin, 2017). The craton consists of Archean-Paleoproterozoic metamorphic basement rocks and unmetamorphosed to weakly metamorphosed Meso-and Neoproterozoic cover successions (e.g., T. M. Kusky et al., 2016;Zhai & Santosh, 2011;Zhao et al., 2005;Zhao & Zhai, 2013). The North China craton is traditionally divided into the Archean Eastern and Western blocks that are separated by the ∼1,600-km-long, northeast-trending Neoarchean Central Orogenic Belt (e.g., T. M. Kusky & Li, 2003; T. M. Kusky et al., 2007;J. P. Wang et al., , 2019Wu et al., 2018;Wu, Li et al., 2022;Wu, Wang et al., 2022) (Figure 1a). The Central Orogenic Belt is also referred to as the Paleoproterozoic Trans-North China Orogen in the tectonic model of Zhao et al. (2001Zhao et al. ( , 2005, Trap et al. (2012), and subsequent papers. It has been proposed that the Eastern Block comprises the Langrim and Lonngang blocks, which are sutured along the Paleoproterozoic Jiao-Liao-Ji orogen (e.g., Tam et al., 2011;Zhao et al., 2005). The Jiao-Liao-Ji orogen consists of ca. 3.8-2.6 Ga tonalitetrondhjemite-granodiorite gneisses (TTGs) and greenstone belts overlain by ca. 2.6-2.5 Ga metasedimentary cover rocks. However, T. M. Kusky et al. (2016) suggested that the Jiao-Liao Ji tectonic unit is a possible deformed retroarc basin and these blocks are poorly defined, much older accreted arcs. Zhao et al. (2005) suggested that the Western Block consists of the Ordos and Yinshan blocks that are sutured along the Paleoproterozoic "Khondalite belt" orogen. However, some researchers proposed that the northern margin of the North China craton is formed by the Paleoproterozoic Northern Margin orogen (e.g., B. Wu et al., 2018, Wu, Wang et al., 2022, also known as the Inner Mongolia-Northern Hebei orogen of T. M. Kusky et al. (2016). The Paleoproterozoic Northern Margin orogen includes the ca. 1.90-1.88 Ga Bayan Obo mélange, the Yinshan Block, and the northern "Khondalite series" (e.g., T. M. Kusky et al., 2016;Wu et al., 2018). The western continuation of the Northern Margin orogen is the Alxa block. In this context, we regard the Yinshan Block as a ribbon-shaped microcontinent comprising a Paleoproterozoic arc sequence developed upon the TTGs and metasedimentary rocks that was incorporated into the Northern Margin orogen. Furthermore, some researchers interpreted that the Archean North China craton formed via the amalgamation of at least six microcontinents along Neoarchean greenstone belts (e.g., Zhai, 2011Zhai, , 2014Zhai et al., 2021;Zhai & Santosh, 2011).

Paleoproterozoic Donggouzi Ultramafic-Mafic Complex
The northeast-trending Donggouzi ultramafic-mafic complex is elliptical in shape (∼700 m long and ∼200-300 m wide) and contains peridotite with internal blocks of amphibole pyroxenite and websterite (Han et al., 2020) (Figures 4a and 4b). The peridotite, amphibole pyroxenite, and websterite have been metamorphosed to amphibolite and granulite facies (Han et al., 2020). The Donggouzi ultramafic-mafic complex was cut by the syenite and mafic dykes with chilled intrusion margins (Figures 4c and 4d). The wall rocks of the ultramafic-mafic complex include TTG gneisses, high-pressure granulites, and metamorphosed Fengzhen Group supracrustal rocks. The Donggouzi ultramafic-mafic rocks and an alkali granite intrude Paleoproterozoic high-pressure granulites, all of which are unconformably overlain by Cenozoic basalts (Figure 4a). Han et al. (2020) determined the age of the Donggouzi ultramafic-mafic complex to be between ca. 1.849-1.845 Ga. They suggested that emplacement of the ultramafic-mafic complex occurred in a post-orogenic extensional setting, possibly associated with continent-continent collision along the northern margin of the North China craton at ca. 1.90-1.88 Ga. In this study, a diabase dyke sample (sample DGZ) was collected for U-Pb baddeleyite geochronology (Figure 4d).

Paleoproterozoic Wuchuan Ductile Shear Zones
The Wuchuan mylonitic shear zones occur in several lithologic units in the mapping area and contain at least two generations of shear foliation (Wu, Wang et al., 2022) (Figure 5). The older ductile shear foliation occurs in Neoarchean felsic mylonite, dolomitic marble, Neoarchean ultramafic-mafic rocks, and Paleoproterzoic gneissic granite/diorite and dykes ( Figure 5). This older foliation observed in ca. 1.98 Ga diorite are crosscut by a ca. 1.87 Ga gabbro dyke. Wu, Wang, et al. (2022) interpreted that this older foliation formed via ca. 1.98-1.87 Ga left-slip ductile shear. The younger shear foliation is folded in biotite plagioclase gneiss ( Figure 6a) and quartzite (sample 19-WC-06d) ( Figure 6b) and occurs in marble ( Figure 6c) and Paleoproterozoic granodiorite (sample 19-WC-06c). The Paleoproterozoic granodiorite is intruded by undeformed plagioclase amphibolite (sample 19-WC-06a) and diorite (sample 19-WC-06b) (Figures 6d and 6e). We used this intrusional contact to constrain the age of the ductile shear associated with the younger foliation. The presence of shear folds within the quartzite, mineral stretching lineation and rotated porphyroclast in mylonitized marble are interpreted to have formed during a regional extensional event.

Paleoproterozoic Bayan Obo Mélange and Yongli Carbonatite
The Bayan Obo mélange, one of the oldest documented sedimentary mélanges on Earth, contains a structurally complex tectonic mixture of metapelites, metapsammites, and mica-quartz schist matrix. These rocks are mixed with exotic blocks of ultramafic and metagabbroic rocks and metabasalts that locally include possible relict pillow structures, plagiogranite, amphibolite, carbonatite, alkaline granulite, and TT gneisses. Zircon 207 Pb/ 206 Pb ages of various blocks in the Bayan Obo mélange demonstrate that the formation and associated deformation of age of 10.1029/2022GC010662 6 of 31 the mélange is ca. 1.9 Ga . Rocks of the Bayan Obo mélange were deposited near the subduction trench, based on the mixing of upper and lower plate volcanic rocks and textural relationships within the mélange . The ∼300-400-m-wide and ∼1-km-long, northwest-southeast-elongated Yongli carbonatite pluton intrudes Hongqiyingzi Group metamorphic rocks and is itself intruded by syenogranite. Subvertical, northwest-striking fluorite veins within the carbonatite pluton are ∼10-50 cm wide. Numerous subangular and subelliptical xenoliths of amphibolite and pyroxene biotite plagioclase gneiss occur within the carbonatite and range in width from >10 m to ∼5-10 cm. The long axes of the xenoliths are oriented northwest-southeast, mirroring the shape of the larger host carbonatite pluton. Wu, Wang, et al. (2022) reported a protolith age of ca. 1.862 Ga for the Yongli carbonatite pluton. Geochemistry results of Yongli carbonatite show ocean island basalt-like characteristics, which may be indicative of within-plate magmatism (Wu, Wang, et al., 2022).

U-Pb Zircon Geochronology
Zircon grains used for U-Pb geochronology were separated from eight samples using traditional methods involving crushing, sieving, and magnetic and density separations. Individual zircon grains were picked under a binocular microscope and mounted in epoxy with standard zircon grains. Cathodoluminescence images of zircon grains were collected using a JXA-880 electron microscope with operating conditions of 20 kV and 20 nA at the Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing. Zircon grains were analyzed   via inductively coupled plasma mass spectrometry (ICP-MS) using an Agilent 7500a instrument coupled with a New Wave Research UP193FX Excimer Laser Ablation System at the Key Laboratory of Continental Collision and Plateau Uplift, Institute of Tibetan Plateau Research, Chinese Academy of Sciences, Beijing. Common Pb corrections were performed assuming an initial Pb composition from Stacey and Kramers (1975). The primary standard used was GJ1 (Jackson et al., 2004). Secondary standards included 91,500 ( 238 U/ 206 Pb age of 1,065 Wiedenbeck et al., 1995) and Plesovice ( 238 U/ 206 Pb age of 337 Sláma et al., 2008). Reported U-Pb ages are 206 Pb*/ 207 Pb* ages for grains older than 1,000 Ma and 206 Pb*/ 238 U* ages for grains younger than 1,000 Ma. Crystallization ages are interpreted from analyses with <10% discordance. Concordia diagrams and weighted mean U-Pb ages were processed using Isoplot v.3 (Ludwig, 2003). Age data and concordia plots are reported with 2σ error. Uncertainties of weighted mean ages are presented at the 95% confidence level (Figure 8). Sample   Table 1 for sample  locations and Table S1 in Supporting Information S1 for details of analyses. locations and U-Pb zircon geochronology results are shown in Table 1. Details of geochronology analyses are shown in Table S1 of Supporting Information S1.  (Figure 8h), which we interpret is the maximum depositional age of the quartzite sample. This quartzite sample has two major zircon populations with two peaks at ca. 1.95 and ca. 2.14 Ga. A minor age population occurs at ca. 2.48 Ga (Figure 8h).

U-Pb Baddeleyite Geochronology
U-Pb baddeleyite analyses were conducted via laser ablation ICP-MS at the Beijing Geo-Analysis Laboratory. Detailed operating conditions for laser ablation using the ICP-MS instrument and data reduction follow those of Xie et al. (2008). Laser ablation was performed using a NWR193 system with a 193-nm excimer laser source. An Agilent 7500 ICP-MS instrument was used to acquire ion signal intensities. He was applied as a carrier gas. Note. MSWD, mean square weighted deviation; MDA, maximum depositional age.

Table 1 Summary of Sample Locations and Geochronology Results From This Study
Ar was used as the make-up gas and mixed with He via a T-connector before entering the ICP-MS instrument. Each analysis incorporated a background acquisition of approximately 15 seconds (gas blank) followed by 45 s of data acquisition from the sample. Off-line raw data selection and integration of background, analytical signals, time-drift correction, and quantitative calibration for U-Pb dating were performed using ICPMSDataCal. All measurements were performed using the Phalaborwa baddeleyite with a 207 Pb/ 206 Pb age of 2,059.8 ± 0.8 Ma (Heaman & LeCheminant, 1993) as the external standard and monitoring sample. The geochronologic data were processed using Isoplot v.3 (Ludwig, 2003). Sample locations and U-Pb baddeleyite geochronology results are shown in Table 1. Details of geochronologic analyses are shown in Table S2 of Supporting Information S1.   Table 1 for sample locations and Table S2 in Supporting Information S1 for details of analyses.

Whole-Rock Geochemistry and Sr-Nd-Pb-Hf Isotope
Three granulite and seven diabase samples were analyzed for their whole-rock major oxide, trace elements, and Sr-Nd-Pb-Hf isotope compositions at the Wuhan Sample Solution Analytical Technology Co., Ltd. in Hubei, China to determine the setting of their petrogenesis. Prior to analysis, weathered surfaces were removed from whole-rock samples. Samples were then crushed and ground into powder (>200 mesh) using a ball mill. Major element compositions were determined via X-ray fluorescence spectrometry with analytical accuracy better than 2%. Trace element compositions were measured via ICP-MS with analytical accuracy better than 5%. Sr-Nd-Pb-Hf isotopes were measured using a Neptune Plus multi-collector ICP-MS with spectral analysis accuracy better than 0.002%. Prior to isotope analysis, sample dissolution was performed using acid digestion (HF + HCLO4 + HNO3). Background isotope measurements were conducted within the error range. Aliquots of NIST SRM 987, JNDI-1, and JMC international standard solutions were regularly used for evaluating the reproducibility and accuracy of the instrument.  (Figure 10a). In primitive mantle-normalized spider diagrams, the three lamprophyre samples are enriched in large-ion lithophile elements (LILES; e.g., Th, U, Ba, K) and depleted in high-field strength elements (HFSEs; e.g., Nb, Ta, Ti) ( Figure 10b).  (Figure 10a). In primitive mantle-normalized spider diagrams, the three samples are enriched in large-ion lithophile elements (LILES; e.g., Th, U, K) and depleted in high-field strength elements (HFSEs; e.g., Nb, Ta and Ti) (Figure 10b).  (Figure 10a). In primitive mantle-normalized spider diagrams, the three samples are depleted in large-ion lithophile elements (LILES; e.g., Th, U, K) and enriched in high-field strength elements (HFSEs; e.g., Nb, Ta and Ti) (Figure 10b).

Paleoproterozoic Granulites and Dykes of the Northern North China Craton
Crystallization ages of the Yanggao granulites in the northern North China craton based on our U-Pb zircon geochronology define three groups: (a) ca. 1,838 ± 6 Ma hornblende hypersthene plagioclase granulite; (b) ca. 1,807 ± 7 Ma hypersthene plagioclase granulite; and (c) ca. 1,782 ± 6 Ma plagioclase pyroxene granulite. The U-Pb baddeleyite age of the hypersthene plagioclase granulite of ca. 1,802 ± 16 Ma is similar to its zircon crystallization age. In this section, we use the U-Pb baddeleyite age of ca. 1.802 Ga for the crystallization age of the hypersthene plagioclase granulite for the purpose of discussion, because the slight younger baddeleyite age is closer to the magmatism. Geochemistry results of the ca. 1.802 Ga Yanggao granulite samples show E-MORB characteristics, which may be indicative of petrogenesis in a back-arc extensional setting. Sr-Nd-Pb-Hf isotope compositions also support the interpretation of petrogenesis in a post-collisional, continental magmatic arc setting during the Paleoproterozoic, possibly sourced from a partially melted, subducted oceanic slab. We observed that the ca. 1.802 Ga hypersthene plagioclase granulite body was cut by the ca. 1.782 Ga plagioclase pyroxene granulite intrusion. We also observed that the ca.  Zhang et al., 2022), which were interpreted to be related to continent-continent collision. The occurrence of (ultra-)high-temperature granulites along the northern margin of the North China craton was initially reported by Jin (1989). Santosh, Tsunogae, et al. (2007) and Santosh, Wilde, et al. (2007) reported the timing of the peak metamorphism to be ca. 1.92 Ga. Based on field relationships and geochronological data, researchers have interpreted that the (ultra-)high-temperature metamorphism was cogenetic with the emplacement of ca. 1.93-1.91 Ga, mantle-derived gabbro dykes possibly related to subduction of a spreading ridge (e.g., Guo et al., 2012;Peng et al., 2010 Kusky et al., 2007Kusky et al., , 2016Peng et al., 2014;Wei et al., 2019;Wu et al., 2018;Wu, Wang, et al., 2022;D. Xiao et al., 2021) (Figure 11).
We observed that ca.  (Han et al., 2020). Geochemical  compositions of the Yanggao and Donggouzi diabase dykes show OIB characteristics, which may be indicative of petrogenesis in an intraplate extensional setting. Sr-Nd-Pb-Hf isotope compositions of the dykes suggest an enriched mantle source, possibly derived from an upwelling mantle plume that interacted with the lithosphere. This interpretation is supported by the geochemical composition of the Yanggao diabase that shows strong fractionation, possibly related to partial melting of enriched lithospheric mantle. Major oxide, trace element, and Sr-Nd-Pb-Hf isotope geochemical compositions of the ca. 1.767-1.778 Ga Yanggao and Donggouzi diabase and gabbro dykes suggest that they were generated from a late Paleoproterozoic mantle plume within the North China craton. From these results, we interpret that magmatism and deformation related to continent-continent collision to form the Northern Margin orogen terminated by ca. 1.78 Ga.

Detrital Zircon Ages and Isotope Concentrations From the Northern North China Craton
Few Neoarchean and Paleoproterozoic magmatic and metamorphic rocks are exposed in the North China craton due to multiple phases of Phanerozoic overprinting (e.g., Zuza & Yin, 2017). To mitigate this issue, we compiled detrital zircon crystallization ages and isotope concentrations to constrain the Neoarchean-Paleoproterozoic magmatic and metamorphic history of the Northern Margin orogen. Previous studies of the North China craton have focused on the central orogen between the Eastern and Western blocks.

Paleoproterozoic Tectonic Evolution of the Northern North China Craton
Paleoproterozoic magmatism in the North China craton initiated at ca. 2.2 Ga in the Northern Margin orogen and Central Orogenic Belt. Previous studies suggested that a subduction-related continental arc was present from ca. 2.2-2.0 Ga, whereas several contemporaneous, extension-related A-type granitoids and mafic dykes have been reported in the central portion of the craton (Figure 14). Recent researchers suggest that prior to continent-continent collision, significant extension occurred in the upper plate during Andean-type subduction along the cratonal margin (e.g., Gün et al., 2021). Also, the major oxide, trace element, and isotope geochemical compositions of the A-type granitoids suggest that they were associated with differentiation of contemporaneous mafic rocks (J. . Therefore, we propose that the ca. 2.2-2.0 Ga magmatic arc was related to the subduction event between the northern margin of the North China craton and another craton within the Columbia-Nuna supercontinent along the Bayan Obo mélange   (Figures 14a and 14b). This interpretation is consistent with igneous zircon age populations with a ca. 1.95 Ga peak along the northern margin of the North China craton. Detrital zircon ages show that the maximum depositional age estimate of the Paleoproterozoic Hongqiyingzi Group quartzite is ca. 1.93 Ga. We observed the Hongqiyingzi Group quartzite to be folded due to ductile shear (Figure 14b). The ca. 1.93-1.80 Ga clockwise metamorphic P-T paths of high-pressure granulites of the northern North China craton margin are interpreted to be related to continent-continent collision and crustal thickening along the northern North China craton margin. In addition, ca. 1.87-1.80 Ga, post-collisional granitoids, mafic dykes, and carbonatites intrude Neoarchean ultramafic-mafic rocks and TTG gneiss (Figure 14c). The comparable ca. 1.90-1.85 Ga, post-collisional granitoids and dykes also occur along the southern margin of the North China craton, which reflects reworking by continent-continent collision of the northern and southern cratonal margins with outboard cratons of the Columbia-Nuna supercontinent during that time. This interpretation is consistent with the metamorphic age population with a peak at ca. 1.85 Ga for the northern North China craton margin. Lastly, the ca. 1.78 Ga Yanggao plagioclase pyroxene granulite and ca. 1.77 Ga lamprophyre dykes are key evidence that continent-continent collision likely terminated by at least ca. 1.78 Ga (Figure 14c).
The Wuchuan mylonitic shear zones exposed along the northern margin of the North China craton contain at least two generations of ductile shearing. Wu, Wang, et al. (2022) interpreted that the earlier generation of shear foliation was associated with ca.  Peng et al. (2022) further proposed that the Xiong'er large igneous province represents the mantle plume center of the oldest hotspot track since ca. 1.8 Ga. They also interpret that the ca. 1.73 Ga Miyun large igneous province developed along the northern cratonal margin, which is consistent with the timing of the younger generation of ductile shear in Wuchuan ( Figure 14d). The crust above the impinged mantle plume head may have experienced ductile or brittle-ductile deformation during broadscale extension (e.g., Birhanu et al., 2016;Gerya, 2014;Koptev et al., 2018) and/or along the flanks of thermally dirven buoyant upwellings in the crust (e.g., B. He et al., 2009;Roberts & Tikoff, 2021;J. Zuo et al., 2021;Zuza et al., 2022) (Figure 14d). The whole-rock concentrations of our ca. 1.77-1.76 Ga mafic dikes show lithospheric affinity, for example, depletion in Nb and Ta, but enriched in Th, U, and large ion lithophile elements such as Rb and La and enriched light rare earth elements. The negative εNd(t) varies from −7.4 to −21.3 and εHf(t) values range from −5.76 to −15.49; whereas their 206 Pb/ 204 Pbt and 207 Pb/ 204 Pbt vary between 16.8-17.5 and 15.4-15.5, respectively. In this scenario, crust affected by the mantle plume would experience voluminous dyke/sill intrusions, rapid uplift, heating and weakening of the mid-lower crust, the formation of progressively widening rifts (e.g., Buck, 1991;Campbell, 2005;Ernst & Buchan, 2003;Koptev et al., 2018;Morgan, 1971) coupled with possible crust scale buoyant upwellings driven by the partial melting of the lower crust. The occurrence of these processes in the North China craton is supported by the record of late Paleoproterozoic granulite-to amphibolite-facies metamorphism, widespread ca. 1.78-1.63 Ga mafic dyke/sills, and the Zha'ertai-Bayan Obo-Huade and Xiong'er rift zones along the northern and south margins of the craton (e.g., C. H. Peng, 2015;Peng et al., 2022;Zhai et al., 2000Zhai et al., , 2015S. H. Zhang et al., 2017;Zhou et al., 2018). In addition, detrital zircon ages for sedimentary rocks within the Zha'ertai-Bayan Obo-Huade rift along the northern cratonal margin show three major Neoarchean-Paleoproterozoic age populations of ca. 2.56-2.47 Ga, ca. 1.96-1.86 Ga, and ca. 1.78-1.62 Ga (e.g., C. H. Zhou et al., 2018), which are associated tectono-magmatic events that formed the Central Orogenic Belt, Northern Margin orogen, and large igneous provinces in the craton.
Ultimately, the Archean-Paleoproterozoic unique geologic history may have generated the thickened cratonic mantle keel to stabilize the North China craton. Cratonization may occur during repeated orogenesis (e.g., McKenzie & Priestley, 2016;Pearson et al., 2021) or mantle plume impingement (J. X. Xu et al., 2021). The two main phases of orogeny (e.g., 2.5 and 1.8 Ga) could have thickened the mantle lithosphere during progressive shortening. The subsequent ca. 1.8-1.6 Ga mantle plume event could have dehydrated and melt-depleted the continental mantle, and crustal heating and melting may have homogenized the composite North China crust. North China remained a relatively stable craton from the Paleoproterozoic until its destruction starting in the Mesozoic (e.g., Wu, Wang, et al., 2022).
The present-day Himalayan-Tibetan orogen and Tibetan Plateau contains records of preceding arc magmatism, ocean closure and major collisions, anatexis and leucogranite formation, granulite grade metamorphism, and a wide distributed zone of intra-plate deformation, Specifically, the eroded records of the modern Himalayan-Tibetan orogen would reveal phases of subduction-arc magmatism (e.g., initial subduction of the Meso-Tethys ocean) and subsequent collisional orogeny for longer than ∼200 Myr over an area with a north-south width >2,000 km (e.g., Kapp & DeCelles, 2019;Zuza et al., 2020). Therefore, tectonic reconstructions should consider that some of these major orogens, including the Northern Margin orogen, are not spatially restricted to narrow belts in time and space, but rather they likely persisted as broad, long-lived orogenic cycles that exist well within the intraplate continental interior. The hotter temperatures of Proterozoic orogens should have caused orogens to more laterally expansive but with more limited crustal thickening (Spencer et al., 2021). Here we have provided more support for the assertion that the Paleoproterozoic Northern Margin orogen stretched north-south over a distance of ∼200 km across the North China. In addition, we suggest that the western extent of Paleoproterozoic Northern Margin orogen may at least continue to the Longshou Shan of the western Alax block in the North China craton (Wu et al., 2021;Wu, Li et al., 2022), defining a west-east width of ∼1,600 km. These refined dimensions should be considered in attempts to restore the configuration of Archean-Paleoproterozoic cratons within supercontinents.

Conclusions
The Archean-Paleoproterozoic North China craton experienced two major arc magmatic and collisional events in the Neoarchean (ca. 2.5 Ga) and Paleoproterozoic (ca. 1.9 Ga), respectively, which are recorded in rocks exposed along the Northern Margin orogen. We present new field observations and results of zircon and baddeleyite U-Pb geochronology (11 samples), whole-rock major oxide and trace element geochemistry (12 samples), Sr-Nd-Pb-Hf isotope geochemistry (10 samples). In addition, we compiled detrital zircon ages and zircon Hf isotope data from across the Neoarchean Central Orogenic Belt and Paleoproterozoic Northern Margin orogen. Results including the occurrence of the ca. 1.84-1.78 Ga Yanggao granulite and 1.78 Ga lamprophyre intrusion led to interpretations, that a possible Himalayan-style continent-continent collision, with widespread intracontinental Figure 15. Global distribution of Paleoproterozoic (ca. 2.1-1.8 Ga) orogens that contain Paleoproterozoic carbonatites, granulites, and eclogites. Map is compiled from Zhao et al. (2002), C. Xu et al. (2018), and A. Yin et al. (2020). We propose that the east-trending Paleoproterozoic Northern Margin orogen developed as part of the North China craton. deforma tion, formed as a result of the Northern Margin orogen and terminated by 1.78 Ga. Ca. 1.77 Ga mafic dykes and ca. 1.75 Ga mylonitic shear zones exposed along the northern margin of the North China craton are possibly associated with a regional mantle plume event. Our results of arc magmatism, continental collision, and widely distributed intracontinental deformation are consistent that modern-style plate tectonics was operative by at least the late Paleoproterozoic.

Data Availability Statement
There are no restrictions on data usage. Zircon and baddeleyite analyses are archived at https://doi.org/10.26022/ IEDA/112688, and our geochemical data are archived at https://doi.org/10.26022/IEDA/112689. mous reviewers for their constructive comments that have led to significant improvements of the original draft of this manuscript. This research was supported by Grants from the Basic Science Center for Tibetan Plateau Earth System (CTPES, Grant 41988101), the Second Tibetan Plateau Scientific Expedition and Research Program (Grant 2019QZKK0708), National Science Foundation of China (Grants 41772227 and 41702232), Tectonics Program of the National Science Foundation of U.S.A. (EAR 1914503 and EAR 1914501), and the Inner Mongolia Mapping Programs (Project Numbers 1212010811001, 1212011120700, DD20160045, and 1212010510506) administered by the Institute of Geological Survey, China University of Geosciences (Beijing). We thank Dr. Yahui Yue assistance in ICP-MS analyses. All data supporting the interpretations and conclusions of this study can be found in the manuscript text, the Supporting Information file, and specifically Tables S1 and S2 in Supporting Information S1.