Jian-Qiang Liu

Saskia Erdmann

Li-Hui Chen

Hui-Li Zhang

Bin Wu

Gang Zeng

Xiao-Jun Wang

Zhu-Liang Lei

Xun Yu

Petrological evidence for magma recharge and mixing beneath the Ma'anshan monogenetic volcano of Xiaogulihe in Northeast China

Keywords: Northeast China, ultrapotassic rocks, Ma'anshan monogenetic volcano, fractional crystallization, magma recharge and mixing

Geochemical compositions of rocks from monogenetic volcanoes in intraplate settings are commonly used to constrain their mantle source and melting processes; however, the subsequent magmatic evolution of such small-volume volcanic systems is commonly ignored. Here we present petrographic observations, mineral chemistry, whole-rock major and trace element data, and thermodynamic modeling for Quaternary ultrapotassic rocks from the Ma'anshan monogenetic volcano of Xiaogulihe in Northeast China. We use these data to evaluate the crystallization conditions and recharge and mixing processes that the magmas have experienced within the crust. The Ma'anshan volcanic products are predominantly phonotephrite and tephriphonolite. These rocks have small variations in geochemical composition with moderate SiO 2 (47.29-49.4 wt.%), high total alkali contents (K 2 O + Na 2 O = 9.85-11.87 wt.%), and high K 2 O/Na 2 O ratios (3.18-4.21). Two types of assemblages were identified in these ultrapotassic rocks: Type-1 antecrysts (olivine and leucite) and hybrid crystals (clinopyroxene, formed by incongruent replacement of antecrysts) and type-2 autocrysts (olivine and leucite). For the type-2, normally zoned olivines, Ni decreases and Mn increases more rapidly with decreasing %Fo than for oceanic basalts, which can be explained by abundant olivine and leucite fractionation in strongly alkaline melts at shallow crustal levels (<200 MPa). The type-1 olivines are reversely zoned and their cores have lower Fo, CaO, and Ni, and higher Mn, than their rims. The type-1 leucites are sieve-textured, partially resorbed, and rimmed by type-1 olivines. The type-1 clinopyroxenes have diopsidic compositions, forming J o u r n a l P r e -p r o o f Journal Pre-proof monomineralic crystal clusters. Although the type-1 antecrystic and hybrid crystals are rare, their presence provides robust evidence for magma recharge and mixing beneath the Ma'anshan monogenetic volcano. This study shows that magmas erupted in monogenetic volcanic fields may experience complex processes within the crust despite their small volumes and relatively uniform compositions, which is important to consider in the interpretation of the construction, evolution, and longevity of their magma plumbing systems.

Introduction

Monogenetic volcanic fields (also termed -small-scale basaltic systems‖) are characterized by clusters of scattered and mostly small (<2 km 2 ) volcanoes [START_REF] Mcgee | Interpreting chemical compositions of small-scale basaltic systems: A review[END_REF][START_REF] Németh | Monogenetic volcanism: personal views and J o u r n a l P r e -p r o o f discussion[END_REF][START_REF] Smith | Source to surface model of monogenetic volcanism: a critical review[END_REF][START_REF] Walker | Basaltic-volcano systems[END_REF]. Such volcanic fields are the most widespread form of volcanism on Earth and occur in a variety of different tectonic settings, including intraplate, extensional, and subduction-related environments [START_REF] Cañón-Tapia | Reappraisal of the significance of volcanic fields[END_REF]. Due to their small eruptive volumes and entrainment of mantle xenoliths, it is generally considered that magmas erupted in monogenetic volcanic fields have not been significantly modified by magmatic evolution processes (i.e., assimilation and fractional crystallization, or magma recharge and mixing) during their ascent from source to surface [START_REF] Mcgee | Interpreting chemical compositions of small-scale basaltic systems: A review[END_REF][START_REF] Smith | Source to surface model of monogenetic volcanism: a critical review[END_REF]. Many geochemical studies have therefore focused on using whole-rock compositions from monogenetic volcanoes to infer the nature of their mantle source(s) and/or degrees of mantle melting [START_REF] Mcgee | The J o u r n a l P r e -p r o o f inception and progression of melting in a monogenetic eruption: Motukorea Volcano, the Auckland Volcanic Field[END_REF][START_REF] Mcgee | Asthenospheric Control of Melting Processes in a Monogenetic Basaltic System: a Case Study of the Auckland Volcanic Field, New Zealand[END_REF](McGee et al., , 2015a;;[START_REF] Rasoazanamparany | Temporal and compositional evolution of Jorullo volcano, Mexico: Implications for magmatic processes associated with a monogenetic eruption[END_REF][START_REF] Reiners | Temporal-compositional trends in intraplate basalt eruptions: Implications for mantle heterogeneity and melting processes[END_REF]. Marked correlations have been observed between the volume of individual monogenetic volcanoes and their chemical composition in the Auckland volcanic field, New Zealand, which have been explained by different degrees of melting of a heterogeneous mantle source [START_REF] Mcgee | Asthenospheric Control of Melting Processes in a Monogenetic Basaltic System: a Case Study of the Auckland Volcanic Field, New Zealand[END_REF](McGee et al., , 2015a)). In the Auckland volcanic field, nepheline-bearing melts are considered to have originated from a deep, carbonated, garnet peridotite source, whereas less alkalic melts are the products of shallower melting of depleted spinel peridotite (McGee et al., 2015a). However, the bulk composition of erupted rocks J o u r n a l P r e -p r o o f commonly obscures the real details of magmatic evolution, representing the resultant composition of mixed magmas that have experienced different processes and that may comprise different source components. By contrast, high-resolution, mineral-scale textural and chemical investigations can help to unravel the complexity of the magmatic systems feeding monogenetic basaltic volcanoes [START_REF] Coote | Olivine phenocryst origins and mantle magma sources for monogenetic basalt volcanoes in northern New Zealand from textural, geochemical and δ18O isotope data[END_REF][START_REF] Jankovics | Olivine major and trace element compositions coupled with spinel chemistry to unravel the magmatic systems feeding monogenetic basaltic volcanoes[END_REF][START_REF] Morgado | Transient shallow reservoirs beneath small eruptive centres: Constraints from Mg-Fe interdiffusion in olivine[END_REF]. A complex set of open-and closed-system processes (including magma stalling, storage, fractionation, mixing, replenishment, cumulate formation and remobilization, incorporation of fragments and crystals from the wall rocks) have been proposed to explain, for example, the various types of olivines and significant compositional variation of olivine-hosted spinel inclusions hosted by the eruptive products of the Fekete-hegy volcanic complex in the intracontinental monogenetic Bakony-Balaton Highland Volcanic Field [START_REF] Jankovics | Olivine major and trace element compositions coupled with spinel chemistry to unravel the magmatic systems feeding monogenetic basaltic volcanoes[END_REF]. Magma residence times in shallow reservoirs obtained via Mg-Fe diffusion modelling in olivine phenocrysts are inferred to vary from a few days to dozens of days for the Caburgua cones of the Andean Southern Volcanic Zone, which indicates the existence of a transient reservoir beneath the small eruptive centers [START_REF] Morgado | Transient shallow reservoirs beneath small eruptive centres: Constraints from Mg-Fe interdiffusion in olivine[END_REF]. Numerous geochemical and some petrological studies have been undertaken on Cenozoic volcanic rocks in eastern China that were erupted as monogenetic fields in an intraplate tectonic setting (Fig. 1a), in order to evaluate their mantle source. Five potassium-rich monogenetic volcanic fields (Wudalianchi, Erkeshan, Keluo, Nuominhe, and Xiaogulihe) that are located at the boundary between the northwestern

J o u r n a l P r e -p r o o f

Journal Pre-proof margin of the Songliao Basin and the Greater Khingan Range (Fig. 1b; [START_REF] Liu | Lithospheric thickness controlled compositional variations in potassic basalts of Northeast China by melt-rock interactions[END_REF]Liu et al., , 2017a;;[START_REF] Zhang | Nature of the lithospheric mantle beneath NE China: evidence from potassic volcanic rocks and mantle xenoliths[END_REF] have been interpreted to derive from metasomatized lithospheric mantle [START_REF] Chu | Source of highly potassic basalts in northeast China: Evidence from Re-Os, Sr -Nd-Hf isotopes and PGE geochemistry[END_REF][START_REF] Sun | Geochemistry of ultrapotassic volcanic rocks in Xiaogulihe NE China: Implications for the role of ancient subducted sediments[END_REF][START_REF] Zhang | Potassic volcanic rocks in NE China: geochemical constraints on mantle source and magma genesis[END_REF][START_REF] Zou | Constraints on the origin of historic potassic basalts from northeast China by U-Th disequilibrium data[END_REF] or from recycled ancient sediments from the mantle transition zone [START_REF] Kuritani | Transition zone origin of potassic basalts from Wudalianchi volcano, northeast China[END_REF]Wang et al., 2017). Previous studies have established that crustal assimilation had played little or no role in their evolution (McGee et al., 2015b;[START_REF] Zou | Constraints on the origin of historic potassic basalts from northeast China by U-Th disequilibrium data[END_REF], while the importance of fractionation or magma recharge and mixing remains unconstrained. High-resolution seismic imaging and magnetotelluric studies have identified a significant low-velocity and high-conductivity anomaly at a depth of ~7-13 km below the Weishan volcano of Wudalianchi volcanic field, which is interpreted to delineate a shallow magma storage zone that comprises crystal-rich magma with liquid-rich magma pockets (Li et al., 2016;[START_REF] Zhang | Integrated study on the geological and geophysical survey in the Wudalainchi Volcano Field[END_REF]. Recently, three-dimensional magnetotelluric imaging further identified a low-resistivity body of 0.3-3.0 Ω•m at depths of ~2-4 km and down to ~15 km beneath the Weishan volcano in the Wudalianchi volcanic field, which corresponds to a magma storage zone in the upper and middle crust. The Weishan volcano is thus likely in an active stage undergoing magma recharge [START_REF] Gao | Magma recharging beneath the Weishan volcano of the intraplate Wudalianchi volcanic field, northeast China, implied from 3-D magnetotelluric imaging[END_REF]. This raises the question as to if and under which conditions magmas may have intermittently stalled and evolved at shallow crustal depths beneath K-rich monogenetic volcanoes in Northeast China. The Ma'anshan volcano of Xiaogulihe [START_REF] Shao | Discovery of Xiaogulihe perpotassic basic and ultrabasic volcanic rock in the north-west Heilongjiang province, China[END_REF] is spatially associated with the Weishan volcano of the Wudalianchi volcanic field (Zhao et al., 2014a) (Fig. 1b).

Both volcanoes are characteristic examples of monogenetic volcanoes in Northeast

J o u r n a l P r e -p r o o f China that have erupted potassium-rich magmas in the Quaternary [START_REF] Zhang | Potassic volcanic rocks in NE China: geochemical constraints on mantle source and magma genesis[END_REF]. In this study, we present detailed petrographic observations, mineral chemical data, whole-rock major and trace element data, and thermodynamic and compositional modelling for Cenozoic ultrapotassic lavas that were erupted at the Ma'anshan monogenetic volcano of Xiaogulihe in Northeast China (Fig. 1c). We use these observations, data, and models to evaluate magma evolution processes in the volcano's crustal magmatic plumbing system.

Geological Background

Cenozoic continental intraplate volcanic rocks are widespread in Northeast China, covering an area of ~5000 km 2 (Fig. 1b; [START_REF] Basu | Major element, REE, and Pb, Nd and Sr isotopic geochemistry of Cenozoic volcanic rocks of eastern China: implications for their origin from suboceanic-type mantle reservoirs[END_REF][START_REF] Liu | Cenozoic episodic volcanism and continental rifting in northeast China and possible link to Japan Sea development as revealed from K-Ar geochronology[END_REF][START_REF] Zhang | Potassic volcanic rocks in NE China: geochemical constraints on mantle source and magma genesis[END_REF]. These volcanic rocks are mainly exposed along the flanks of the Songliao Basin with the Greater Khingan Range in the west, the Lesser Khingan Range in the north, and the Changbaishan Mountains in the east (Fig. 1b; [START_REF] He | Light Mg isotopic composition in the mantle beyond the Big Mantle Wedge beneath eastern Asia[END_REF]. The Songliao Basin and the Greater Khingan Range are part of the Xing'an-Mongolia Orogenic Belt (XMOB; Fig. 1a), which in turn is the eastern part of the Paleozoic Central Asian Orogenic Belt, which formed during subduction and the collision between the North China Craton and Siberian Plate [START_REF] Jahn | Granitoids of the Central Asian Orogenic Belt and continental growth in the Phanerozoic[END_REF][START_REF] Sengör | Evolution of the Altaid tectonic collage and Palaeozoic crustal growth in Eurasia[END_REF]. Cenozoic volcanic rocks in Northeast China can be subdivided into ultrapotassic, potassic, and sodic series according to their K 2 O contents and K 2 O/Na 2 O ratios [START_REF] Liu | Lithospheric thickness controlled compositional variations in potassic basalts of Northeast China by melt-rock interactions[END_REF](Liu et al., , 2017a)). The potassic (and ultrapotassic) volcanic rocks form about 60 monogenetic volcanoes that are associated with outflows of aa J o u r n a l P r e -p r o o f lavas, which cover an area of >3000 km 2 (Fig. 1b) (Zhao et al., 2014a(Zhao et al., , 2014b)). Based on K-Ar dating, field characteristics and stratigraphy, the volcanic rocks were erupted in three main episodes: in the middle-late Miocene (16.5-7.0 Ma), the late Pliocene to Pleistocene (2.3-0.13 Ma), and the Recent (up to 1721 AD) [START_REF] Zhang | Nature of the lithospheric mantle beneath NE China: evidence from potassic volcanic rocks and mantle xenoliths[END_REF].

Sample description

The Ma'anshan monogenetic volcano of Xiaogulihe is located in the northernmost part of the potassic volcanic rock belt in Northeast China (Fig. 1b).

Rocks erupted from the Ma'anshan cover an area of about 13.8 km 2 (Fig. 1c).

Previous K-Ar dating (0.30-0.19 Ma; [START_REF] Zhang | Source's characteristics of ultra-potassium basaltic rocks from northeast China and research on regional mantle geochemistry[END_REF] has shown that the Ma'anshan volcano erupted in the Quaternary, near the end of the second main eruptive episode.

In this study, twelve fresh samples were collected from the lava flows of Ma'anshan volcano. The collected samples are porphyritic, massive to vesicular, comprising olivine, leucite, and rare clinopyroxene phenocrysts embedded in a microgranular matrix consisting of leucite, nepheline, sodalite, feldspar, phlogopite, and Fe-Ti oxides (Fig. 2). More detailed petrographic characteristics and mineral chemistry data are presented in the following sections. No mantle-derived xenoliths or xenocrysts were found or have been previously reported in the Xiaogulihe volcanic rocks [START_REF] Zhang | Nature of the J o u r n a l P r e -p r o o f lithospheric mantle beneath the eastern part of the Central Asian fold belt: mantle xenolith evidence[END_REF].

Analytical Methods

The samples were cut into thin slabs and the fresh central parts were powdered to J o u r n a l P r e -p r o o f ~200 mesh for whole-rock geochemical analysis. Whole-rock major element compositions were determined using a Thermo Scientific ARL 9900 X-ray fluorescence (XRF) spectrometer at the State Key Laboratory for Mineral Deposits Research in Nanjing University, Nanjing, China. Based on measured values for standard rock reference materials (BCR-2 and BHVO-2; Wilson, 1997a[START_REF] Wilson | Data compilation for USGS reference material BHVO-2, Hawaiian Basalt[END_REF], the analytical accuracy was ±1% for elements with concentrations of >1.0 wt.% and ±10% for elements with concentrations of <1.0 wt.%. Measurements of whole-rock trace element concentrations were undertaken at the Department of Geology, Northwest University, Xi'an, China. Trace elements were determined using an ELAN 6100DRC inductively coupled plasma mass spectrometer (ICP-MS) after acid digestion (HF + HNO 3 ) of samples in Teflon bombs. Analyses of USGS standards (BHVO-2, AGV-2, and BCR-2; Wilson, 1997a[START_REF] Wilson | Data compilation for USGS reference material BHVO-2, Hawaiian Basalt[END_REF][START_REF] Wilson | Data compilation and statistical analysis of intralaboratory results for AGV-2[END_REF] indicate the precision and accuracy are better than ±5% for Li, Sc, V, Cr, Co, Ni, Cu, Zn, Rb, Sr, Y, Zr, Nb, Ba, Th, and the rare earth elements (REEs), and better than ±10% for Hf, Ta, Pb, and U. Whole-rock major and trace element compositions of twelve Xiaogulihe ultrapotassic rocks and the standard reference materials during the analyses are listed in Table 1 andTable S1 respectively.

We prepared polished thin-sections to characterize the mineral assemblages and textures. Furthermore, several samples were crushed to handpick crystals using a binocular microscope to provide us with a large number of phenocrysts for micro-chemical characterization. Inclusion-rich leucite and clinopyroxene crystals fractured in the process and crucial textural information was lost, and we therefore J o u r n a l P r e -p r o o f Journal Pre-proof exclusively handpicked olivine phenocrysts. Selected olivine grains were mounted in epoxy resin, polished to 0.1 μm, cleaned ultrasonically in ethanol and distilled water, and finally carbon-coated. Major (SiO 2 , MgO, and FeO) and minor element (CaO, NiO, and MnO) contents of 441 olivine crystals were acquired in a total of >490 analyses, including core-rim compositions. Major and minor element compositions of 39 leucite and 10 clinopyroxene crystals in thin-sections were also analyzed. All these analyses were undertaken with an electron microprobe (EMP) using a JEOL JXA-8230 Superprobe at the State Key Laboratory of Nuclear Resources and Environment, East China Institute of Technology, Nanchang, China. The beam size was set to 2 μm, and an acceleration voltage of 15 kV and a current of 20 nA were used for all analyses. Calibration standards for the olivine analyses were rhodonite (Si and Mn), magnetite (Fe), olivine (Mg), diopside (Ca), and pentlandite (Ni). Peak counting times were 20 s for major elements (Si, Mg, and Fe), 60 s for minor elements (Ca and Mn), and 90 s for Ni. Background counting times were 5 s on each side of the peaks. To monitor instrumental drift, an internal olivine standard (MongOl; [START_REF] Batanova | New Olivine Reference Material for In Situ Microanalysis[END_REF] was analyzed as an unknown after every five analyses. Seventy-eight analyses of the MongOl olivine showed that the analytical uncertainty was better than ±2% for SiO 2 , FeO, and MgO, ±4% for NiO, and ±7% for MnO and CaO. Calibration standards used during the leucite analyses were biotite (Si), rutile (Ti), jadeite (Al and Na), and kaersutite (Fe and K), while those used during the clinopyroxene analyses were almandine garnet (Si), rutile (Ti), jadeite (Al and Na), magnetite (Fe), bustamite (Mn), diopside (Ca, Mg, and Cr), and pentlandite (Ni). Peak counting times were 10 s J o u r n a l P r e -p r o o f and the background counting times were 5 s on each side of the peaks. Analytical uncertainties were <±1% for major elements and <±5% for trace elements.

Back-scattered electron (BSE) imaging and electron microprobe X-ray mapping were used to characterize chemical zoning of the minerals. The compositional data for the Xiaogulihe olivines and MongOl olivine standard are provided in Tables S2 andS3 respectively. Major and trace element data for leucite and clinopyroxene are listed in Tables S4 andS5 respectively.

Results

Whole-rock major and trace element compositions

The Xiaogulihe volcanic rocks collected from the Ma'anshan volcano have low SiO 2 (47.29-49.40 wt.%) and high total alkali (K 2 O + Na 2 O = 9.85-11.87 wt.%) contents, and are mostly phonotephrites and tephriphonolites (Le [START_REF] Bas | A chemical classification of volcanic rocks based on the total alkali-silica diagram[END_REF] (Fig. 3a). The rocks have high K 2 O contents (7.83-9.08 wt.%) and K 2 O/Na 2 O ratios (3.18-4.21), and plot in the field for ultrapotassic rocks (Fig. 3b).

Chondrite-normalized rare earth element (REE) patterns reveal that the Xiaogulihe ultrapotassic rocks are enriched in light rare earth elements (LREEs) over heavy rare earth elements (HREEs) (Fig. 4), which are somewhat similar to other potassium-rich rocks from Northeast China.

Phenocryst textures and compositions

Phenocrysts in the Xiaogulihe ultrapotassic rocks are olivine (10-15 vol.%), J o u r n a l P r e -p r o o f leucite (25 vol.%), and minor clinopyroxene (≤1-2 vol.%) (Fig. 2 and Fig. 5). Based on textures and compositions, we identified two types of phenocryst assemblages (Fig. 5, Fig . 6 and Fig. 7). The type-1 assemblages must have crystallized earlier, while the type-2 ones formed later from the magmatic plumbing system. The type-1 olivines (≤ 1-2 vol.% of all olivine crystals) are subhedral to slightly skeletal, and occur as single crystals that are up to ~500 m in size (Fig. 5a and Fig. 6). The olivines have cores that exhibit irregular resorption surfaces, but the rims are defined by euhedral crystal surfaces (Fig. 6). The type-1 olivines are reversely zoned with cores having lower Fo (76-81), Ni (39-786 ppm), and Ca (1229-1908 ppm), and higher Mn (2726-3516 ppm), than the rims (Fo = 82-87; Ni = 794-1367 ppm; Ca = 1822-2787 ppm; Mn = 1843-2532 ppm; Fig. 5b and Fig. 6). Considering Fe 2+ -Mg partitioning (K D (Fe-Mg) ol-liq =0.27 ± 0.03; [START_REF] Draper | P-T phase relations of silicic, alkaline, aluminous liquids: New results and applications to mantle melting and metasomatism[END_REF], the type-1 olivine core compositions appear to be out of equilibrium with potential host melts, i.e., a melt with a composition equivalent to the bulk rocks (Fig. 8a), and Ni-Ca contents increase and Mn contents decrease with increasing Fo values from core to rim (Fig. 9). The type-2 olivines (>98 vol. % of all olivine crystals) are euhedral-subhedral, up to ~500 m in size, and occur as single crystals (Fig. 5c and Fig. 7) or crystal clusters (not shown). These olivines are normally zoned and have cores with slightly higher Fo (87-88) and significantly higher Ni (1815-2153 ppm), but lower Ca (1844-2080 ppm) and Mn (1518-1897 ppm) than their rims (Fo = 85-87; Ni = 1037-1391 ppm; Ca = 2151-2887 ppm; Mn = 1758-2440 ppm; Fig. 5d and Fig. 7). Considering Fe 2+ -Mg partitioning, their core compositions appear to be in equilibrium with a melt J o u r n a l P r e -p r o o f composition that approximates the whole-rock composition (Fig. 8). The more evolved rims of the type-2 crystals appear to have been in equilibrium with the melt that has crystallized to the matrix of the rocks (Fig. 8a). Nickel contents decrease and Ca-Mn contents increase with decreasing Fo content for the type-2 olivines (Fig. 9). However, Ni and Mn contents show a more pronounced decrease and increase with Fo values, respectively, than olivines from Koolau (Hawaii) basalts, mid-ocean ridge basalts (MORB), and high-μ (high 238 U/ 204 Pb, HIMU) ocean island basalts (Fig. 9).

The type-2 olivines have compositions and compositional trends that differ entirely from the type-1 crystals, but have similar rim compositions as the type-1 olivines (Fo ~ 86; Fig. 8a and Fig. 9).

The type-1 leucites ( ≤ 1-2 vol. % of all leucite crystals) are subhedral, sieve-textured, and up to ~500 m in size (Fig. 5e). The sieve-textured crystals are filled by fine-grained matrix minerals (ilmenite, clinopyroxene, and apatite), while rimmed by type-1 olivine (Fig. 5e). The type-2 leucites (>98 vol.% of all leucite crystals) are euhedral-subhedral and typically 50-100 m in size (Fig. 5f). These leucites have relatively homogeneous chemical compositions with ~54.9-57.1 wt.% SiO 2 , ~20.0-21.2 wt.% Al 2 O 3 and ~21.0-21.9 wt.% K 2 O (Table S4). Clinopyroxene phenocrysts (≤1-2 vol.%) in the Ma'anshan volcanic rocks are euhedral-subhedral, up to ~300 m in size, and form clusters of crystals (Fig. 5g), which we classify as type-1 crystals. They have low Al 2 O 3 contents (< 1 wt.%) and Mg# number (83.7-89.2) (Table S5) and plot below the Fe-Mg equilibrium field (Fig. 8b). They are classified as diopside in terms of the nomenclature of [START_REF] Morimoto | Nomenclature of pyroxenes[END_REF] (Fig. 5h), and J o u r n a l P r e -p r o o f commonly do not show resorption textures or significant compositional zoning (Fig. 5g).

Discussion

Phenocryst origins

Phenocrysts in volcanic rocks can have a variety of origins [START_REF] Davidson | Microsampling and Isotopic Analysis of Igneous Rocks: Implications for the Study of Magmatic Systems[END_REF][START_REF] Coote | Olivine phenocryst origins and mantle magma sources for monogenetic basalt volcanoes in northern New Zealand from textural, geochemical and δ18O isotope data[END_REF]. The type-1 and type-2 olivine, leucite, and clinopyroxene phenocrysts may be: [START_REF] Gleeson | Crustal controls on apparent mantle pyroxenite signals in ocean-island basalts[END_REF] Autocrysts that crystallized from and are in equilibrium with the host magma; (2) antecrysts derived from previously crystallized magma pulses in the magmatic plumbing system [START_REF] Davidson | Microsampling and Isotopic Analysis of Igneous Rocks: Implications for the Study of Magmatic Systems[END_REF]; (3) xenocrysts from crustal or mantle wall-rocks; or (4) hybrid crystals that formed in reactions between the magma and xenocrysts, antecrysts, or autocrysts [START_REF] Beard | Reactive bulk assimilation: A model for crust-mantle mixing in silicic magmas[END_REF][START_REF] Couch | Mineral disequilibrium in lavas explained by convective self-mixing in open magma chambers[END_REF][START_REF] Erdmann | Textures of Peritectic Crystals as Guides to Reactive Minerals in Magmatic Systems: New Insights from Melting Experiments[END_REF]. Crystal textures, zoning, and mineral and host melt compositions are typically used to infer their different origins. All olivine crystals have Fo (76-90%) and NiO (0.005-0.431 wt.%) yet elevated CaO (0.121-0.404 wt.%) contents (Table S2 and Fig. 9), which are unlike those of typical mantle xenocrysts [START_REF] Foley | Minor and trace elements in olivines as probes into early igneous and mantle melting processes[END_REF][START_REF] Thompson | Transient high temperatures in mantle plume heads inferred from magnesian olivines in Phanerozoic picrites[END_REF], and clinopyroxene has Al 2 O 3 contents of <1.0 wt.% and Mg# < 90 (Table S5), which suggest that none of the crystals are mantle xenocrysts. The euhedral-subhedral morphology and lack of evidence for resorption of the type-2 olivine and leucite crystals (Fig. 5c, Fig. 5f and Fig. 7) indicate an autocrystic origin. Moreover, the cores (~Fo 90) of the type-2 olivine crystals are in Fe-Mg equilibrium with the bulk-rock compositions (Fig. 8a) as J o u r n a l P r e -p r o o f expected for early, near-liquidus crystallization, while the more evolved crystal rims (~Fo 86) are in equilibrium with a melt equivalent to the matrix composition, which is expected for late, pre-or syn-eruptive crystallization, providing further evidence for an autocrystic origin.

In contrast to the type-2 crystals, the type-1 olivine, leucite, and clinopyroxene show clear evidence for textural and/or compositional disequilibrium, indicating an antecrystic, xenocrystic or hybrid origin. The type-1 olivine and leucite occur as single crystals that show evidence for partial resorption (Fig. 5a, Fig. 5e and Fig. 6), which we therefore interpret as antecrysts or crustal xenocrysts. The cores of the type-1 olivines have lower Fo (76-80%) values and NiO (0.005-0.1 wt.%) contents and high MnO (0.352-0.454 wt.%) contents (Fig. 5b and Fig. 6), which are not in equilibrium with their host rock compositions (Fig. 8a). Their compositions are, however, consistent with compositions predicted by fractional crystallization modeling from an initial magma composition equivalent to that of primitive Ma'anshan volcanic rocks (Fig. 9), following extensive crystallization of olivine-leucite-clinopyroxene. We take this as evidence for an antecrystic origin, i.e.

we infer that the type-1 crystals formed from a magma batch that crystallized prior to the main Xiaogulihe magmas, and that this early magma batch crystallized to a significant degree. Leucite is rare in crustal rocks, yet it occurred as partially resorbed crystals in the Ma'anshan ultrapotassic magmas, which further argues for an antecrystic and against a crustal xenocrystic origin.

The type-1 clinopyroxenes form monomineralic clusters of relatively small J o u r n a l P r e -p r o o f crystals (Fig. 5g). We rule out that the clinopyroxenes are glomerocrysts (i.e. autocrysts formed by heterogeneous nucleation) or that they formed in a reaction between autocrysts and host melt, as they are out of compositional equilibrium with their host melt (i.e. the composition of the bulk rocks; Fig. 8b). The clinopyroxene crystals could represent antecrysts, e.g. derived from a crystal mush, or they could be hybrid crystals that have formed in a reaction between antecrysts or xenocrysts and host melts [START_REF] Beard | Reactive bulk assimilation: A model for crust-mantle mixing in silicic magmas[END_REF][START_REF] Couch | Mineral disequilibrium in lavas explained by convective self-mixing in open magma chambers[END_REF][START_REF] Erdmann | Textures of Peritectic Crystals as Guides to Reactive Minerals in Magmatic Systems: New Insights from Melting Experiments[END_REF]. We cannot entirely rule out that the clinopyroxene crystals formed after crustal xenocrysts, but we found no evidence for crustal xenocrysts or micro-xenoliths. If the clinopyroxene crystals represented a cluster of antecrysts, we would expect textures indicating partial resorption (as for olivine and leucite), which we do not observe. We favor the interpretation that they have formed in an incongruent reaction between antecrysts and host melt, given that antecrystic olivine and leucite are present (Fig. 5a, 5e and Fig. 6).

Hybrid crystals formed in incongruent reactions between antecrysts and melt typically

show mono-or poly-mineralic clusters of small, randomly oriented crystals.

Fractional crystallization in the magmatic plumbing system

We have identified two crystal populations in the Ma'anshan volcanic rocks: [START_REF] Gleeson | Crustal controls on apparent mantle pyroxenite signals in ocean-island basalts[END_REF] Type-1 antecrysts (olivine and leucite) and hybrid crystals (clinopyroxene) that crystallized from previous magma pulses in the magmatic plumbing system; and (2) type-2 autocrysts (olivine and leucite) that crystallized from the main Xiaogulihe magmas. Investigation of the textures and compositions of the various phenocryst J o u r n a l P r e -p r o o f phases can provide conclusive evidence for open-system evolution within the magmatic plumbing system.

For the type-2 olivines, the Ni contents decrease rapidly while the Mn contents increase markedly with decreasing Fo values (Fig. 9). [START_REF] Zhang | Variation of olivine composition in the volcanic rocks in the Songliao basin, NE China: lithosphere control on the origin of the K-rich intraplate mafic lavas[END_REF] reported similar trends for Ni and Mn versus Fo for olivines from the Xiaogulihe volcanic rocks (Fig. 9), and proposed that such compositional trends record variable degrees of mechanical stirring and mixing between different batches of primary melts. However, mixing between relatively Ni-rich and -poor magmas and their olivine populations should produce variably zoned crystals (i.e., abundant crystals that show steep core-rim increases and decreases in Ni), which is not the case. It has been demonstrated experimentally that the olivine/melt partition coefficients for Ni and Mn in strongly alkaline melts (D Ni Ol/Liq = 62-95 and D Mn Ol/Liq = 1.4-2.6) are higher than those in basaltic systems (D Ni Ol/Liq = 2-20 and D Mn Ol/Liq = 0.4-1.8) [START_REF] Foley | Trace element partitioning in lamproitic magmas -the Gaussberg olivine leucitite[END_REF]. Furthermore, Mn is highly incompatible, and Ni is moderately incompatible in leucite (D Mn Lc/Liq = 0.016 and D Ni Lc/Liq = 0.249) in potassic and ultrapotassic melts [START_REF] Foley | Trace element partitioning in lamproitic magmas -the Gaussberg olivine leucitite[END_REF]. Thus, fractional crystallization of olivine and leucite from alkaline melts can result in rapid depletion of Ni, but rapid enrichment of Mn, in residual melts [START_REF] Foley | Trace element partitioning in lamproitic magmas -the Gaussberg olivine leucitite[END_REF][START_REF] Foley | Minor and trace elements in olivines as probes into early igneous and mantle melting processes[END_REF]. Olivine phenocrysts that crystallized from such residual melts would have lower Ni and higher Mn contents, which can explain the steep Xiaogulihe olivine Fo-Ni and Fo-Mn compositional trends (Fig. 9). To test if fractional crystallization of olivine ± clinopyroxene ± leucite could reproduce the observed Ni-Mn-Ca compositional trends (Fig. 9a-c), we J o u r n a l P r e -p r o o f modeled crystallization at 200 MPa using the rhyolite-MELTS software [START_REF] Gualda | Rhyolite-MELTS: a modified calibration of MELTS optimized for silica-rich, fluid-bearing magmatic systems[END_REF][START_REF] J O U R N A L P R E -P R O O F Gualda | MELTS_Excel: AMicrosoft Excel-based MELTS interface for research and teaching of magma properties and evolution[END_REF], with the Ni and Mn partition coefficients of [START_REF] Foley | Trace element partitioning in lamproitic magmas -the Gaussberg olivine leucitite[END_REF] and Ca partition coefficient of Herzberg and O'Hara (2002). The modeling results show that the type-2 olivine Ni-Mn-Ca compositions fall on the olivine-leucite liquid line of descent with up to ~13 wt.% olivine and ~25 wt.% leucite crystallization (i.e., at proportions that closely match the observed abundances of type-2 olivine and leucite of 10-15 and ~25 vol.%, respectively; Fig. 9).

As mentioned above, the composition and compositional trends of the Xiaogulihe type-2 olivines differ from those of olivines from oceanic basalts (HIMU, MORBs and Koolau; Fig. 9), which have been interpreted to record extensive fractional crystallization of olivine and leucite in strongly alkaline melts. The difference of absolute Ni, Mn, and Ca contents of olivines at a given Fo value is interpreted to reflect diverse primary magma compositions derived from variably peridotite-or pyroxeneite-rich and variably carbonated mantle sources [START_REF] Herzberg | Identification of Source Lithology in the Hawaiian and Canary Islands: Implications for Origins[END_REF][START_REF] Ruprecht | Feeding andesitic eruptions with a high-speed connection from the mantle[END_REF][START_REF] J O U R N A L P R E -P R O O F Sobolev | An olivine-free mantle source of Hawaiian shield basalts[END_REF][START_REF] Sobolev | The amount of recycled crust in sources of mantle-derived melts[END_REF]. The steep Ni versus Fo compositional trend that is characteristic for the type-2 olivines of Xiaogulihe closely resembles that of Koolau olivines with >Fo89, thus indicating crystallization of similar assemblages and partitioning conditions (for relatively alkali-rich magmas). HIMU olivine to our type-2 olivine compositional trend, which we infer to reflect an increase in the proportion of co-crystallizing minerals in which Mn is incompatible (i.e. leucite in the Xiaogulihe ultrapotassic rocks).

Thermodynamic model constraints on phase relations and compositions

To further characterize the phase relations and constrain the crystallization conditions (temperature, pressure, and melt H 2 O contents) of the Xiaogulihe ultrapotassic rocks, we undertook thermodynamic modeling using the rhyolite-MELTS software [START_REF] Gualda | Rhyolite-MELTS: a modified calibration of MELTS optimized for silica-rich, fluid-bearing magmatic systems[END_REF][START_REF] J O U R N A L P R E -P R O O F Gualda | MELTS_Excel: AMicrosoft Excel-based MELTS interface for research and teaching of magma properties and evolution[END_REF] using the composition of our most primitive Xiaogulihe sample (16XLGH06; MgO = 8.85 wt.%). A range of modeled pressures (50-1200 MPa) and temperatures (900°C-1500°C) were chosen to examine the conditions at crustal depths. Low initial melt H 2 O contents (0.5 and 1.0 wt.%) [START_REF] Chen | Water content of the Xiaogulihe ultrapotassic volcanic rocks, NE China: implications for the source of the potassium-rich component[END_REF] and relatively oxidizing conditions (QFM+1) were used as such conditions have previously been inferred for J o u r n a l P r e -p r o o f spatially and temporally associated magma systems (e.g., the Wuchagou, Xunke, and Menluhe volcanic systems; Erdmann et al., 2019; Fig. 1) but also for potassic to ultrapotassic basalts from Eastern China [START_REF] Hong | Recycled carbonate-induced oxidization of the convective mantle beneath Jiaodong, Eastern China[END_REF].

The modeling results indicate that olivine is always the liquidus phase, and crystallizes at ≥1350°C (Fig. 10a,b), which is consistent with the large phenocryst size of type-2 olivine as compared with type-2 leucite (Fig. 5c,5f). Near-liquidus olivine is modeled to have Fo ~ 89, which matches the observed type-2 olivine core compositions (Fig. 8). For an initial melt H 2 O content of 0.5 wt.% and an oxygen fugacity of QFM+1, leucite crystallization is predicted to follow olivine crystallization at 1275°C-1175°C and at pressures of <500-700 MPa (Fig. 10a). At pressures of >500-700 MPa, clinopyroxene is modeled to crystallize after olivine at 1250°C-1175°C, followed by leucite (Fig. 10a). The assemblage of 11-17 vol.% olivine and 16-24 vol.% leucite predicted in the model simulating crystallization at <200 MPa, with an initial melt H 2 O content of 0.5 wt.%, provides the best match to the observed phase assemblage and abundance. At higher pressures or melt H 2 O contents, olivine, and clinopyroxene become dominant over leucite (Fig. 10a and10b), which is inconsistent with the mineral proportions observed in the natural samples.

Therefore, the co-crystallization of abundant type-2 olivine and leucite, and the absence of autocrystic type-2 clinopyroxene in the Xiaogulihe ultrapotassic rocks, reflect shallow crystallization from a relatively H 2 O-poor magma (≤0.5 wt.%) at an oxygen fugacity of ~QFM+1. These constraints suggest that the erupted Xiaogulihe magmas were temporarily stored and partially crystallized at a depth of ~6-7 km, J o u r n a l P r e -p r o o f which is consistent with shallow magma storage that has been imaged geophysically below the Wudalianchi volcanic field (~7-13 km) [START_REF] Gao | Magma recharging beneath the Weishan volcano of the intraplate Wudalianchi volcanic field, northeast China, implied from 3-D magnetotelluric imaging[END_REF]Li et al., 2016).

Compared with the Xiaogulihe whole-rock compositional trends, the modeled liquid compositions significantly diverge toward higher SiO 2 , Al 2 O 3 , and TiO 2 , and lower MgO and FeO contents (Fig. 10c-10f), indicating that simple fractional crystallization of olivine and leucite alone cannot account for the compositional variation of the Xiaogulihe magmas. Other processes (i.e. magma recharge and mixing) in the magmatic plumbing system may have affected the erupted compositions of the Xiaogulihe magmas.

Magma recharge and mixing beneath the Xiaogulihe monogenetic volcano

The presence of reversely zoned olivine is commonly taken as evidence for magma recharge and mixing or contamination and partial assimilation of mantle or crustal rocks [START_REF] Erdmann | Characteristic Textures of Recrystallized, Peritectic, and Primary Magmatic Olivine in Experimental Samples and Natural Volcanic Rocks[END_REF][START_REF] Gleeson | Crustal controls on apparent mantle pyroxenite signals in ocean-island basalts[END_REF][START_REF] Herzberg | Phantom Archean crust in Mangaia hotspot lavas and the meaning of heterogeneous mantle[END_REF][START_REF] Thornber | Olivine-liquid relations of lava erupted by Kilauea volcano from 1994 to 1998: implications for shallow magmatic processes associated with the ongoing East-Rift-Zone eruption[END_REF]. Magma recharge and mixing between rift-stored and summit-derived basaltic magmas has been proposed to explain the presence of reversely zoned olivine from Kilauea volcano [START_REF] Thornber | Olivine-liquid relations of lava erupted by Kilauea volcano from 1994 to 1998: implications for shallow magmatic processes associated with the ongoing East-Rift-Zone eruption[END_REF]. Large (>2 mm) reversely zoned olivine crystals in eastern Galápagos basalts have cores with lower Fo contents as compared with their rims, which indicates they record magma recharge and mixing [START_REF] Gleeson | Crustal controls on apparent mantle pyroxenite signals in ocean-island basalts[END_REF]. The cores of type-1 olivines in the Ma'anshan rocks have irregular resorption surfaces, but their rims have planar crystal surfaces and/or euhedral-subhedral crystal habits (Fig. 5a and Fig. 6), which indicate J o u r n a l P r e -p r o o f resorption followed by crystallization. The cores have low Fo (76-80%) and NiO (0.005-0.1 wt.%) contents, and high MnO (0.352-0.454 wt.%) contents (Fig. 9), indicating crystallization from a relatively evolved melt. Our modeling indicates that crystallization of significant amounts of leucite (~40 vol.%), clinopyroxene (~35 vol.%), and olivine (~20 vol.%) at ~200 MPa produces olivine with Ni-Mn-Ca-Fo compositions similar to the type-1 olivine cores (Fig. 9). The core-rim increase in Fo%, Ni, and Ca, and decrease in Mn in the type-1 olivines (Fig. 9) record magma recharge and mixing with a more primitive and/or hotter magma. Thermodynamic modeling (Fig. 9) highlights that the magmas from which the type-1 and type-2 olivine crystallized must have had similar compositions, and that the melt in equilibrium with type-2 olivine was significantly more primitive and hotter than that in equilibrium with type-1 olivine cores. Given that the primitive rims of the type-1

olivines have a relatively narrow width (< 30 m) compared to the size of the type-2 olivines (Fig. 5a and Fig. 5c), we presume that the type-1 crystals were entrained relatively late during the evolution of the main Ma'anshan magmas (producing only relatively narrow overgrowth zones) when most of the type-2 olivine had already crystallized.

The magma recharge and mixing processes beneath the Ma'anshan monogenetic volcano of Xiaogulihe are further evidenced by the type-1 antecrystic leucite and by the hybrid clinopyroxene crystals. The type-1 leucites are sieve-textured, partially resorbed, and survived as skeletal crystals (Fig. 5f), which indicates that they were at some point not in equilibrium with their host melt. Decompression of J o u r n a l P r e -p r o o f H 2 O-undersaturated magmas may cause partial resorption of their crystal cargo and thus lead to the formation of skeletal crystals [START_REF] Humphreys | Magma evolution and open-system processes at Shiveluch Volcano: Insights from phenocryst zoning[END_REF], but leucite is not predicted to crystallize at large depth (e.g. our model results) and it has also been shown experimentally to be a low-pressure phase [START_REF] Shea | Leucite crystals: Surviving witnesses of magmatic processes preceding the 79AD eruption at Vesuvius, Italy[END_REF]. Furthermore, the type-1 leucites are commonly rimmed by type-2 olivines, which provides evidence for magma recharge and mixing with a more primitive melt. Clinopyroxene clusters in the Xiaogulihe ultrapotassic rocks are interpreted as the hybrid, reaction products between melt and antecrysts or xenocrysts. We favor the interpretation that they formed by reaction between antecrysts and melt, i.e. we suggest that crystal mush fragments were entrained into the hotter recharged magma.

Figure 11 shows a magma recharge and mixing model that can account for the phenocrysts with distinct textures and compositions in the Xiaogulihe ultrapotassic rocks. We suggest that an early shallow magma storage zone existed beneath the Ma'anshan volcano, in which magmas experienced extensive crystallization and formed a crystal-rich mush containing the type-1, low-Fo olivine, leucite, and clinopyroxene (Fig. 11a). Subsequently, this crystal-rich mush was recharged and mixed with a hotter and more primitive magma (Fig. 11b). During this process, the type-1 olivines were partially resorbed, but their planar crystal surfaces and euhedral-subhedral crystal shapes record crystallization of type-2 olivine. The type-1 leucite was also partially resorbed and then overgrown by type-2 olivine. Any clinopyroxene present in the crystal mush (which should have co-existed with the Fo-poor type-1 olivine composition; Fig. 11a) melted during this process, as we have J o u r n a l P r e -p r o o f not identified any antecrystic clinopyroxene crystals. We speculate that the antecrystic clinopyroxene may have been replaced by the hybrid clinopyroxene crystal clusters.

Typically, melting of antecrystic clinopyroxenes produces skeletal crystals (e.g. common for plagioclase, where anorthite-rich skeletons partially replace more albite-rich cores, but also observed for other minerals) (Streck, 2008;[START_REF] Erdmann | Characteristic Textures of Recrystallized, Peritectic, and Primary Magmatic Olivine in Experimental Samples and Natural Volcanic Rocks[END_REF]. However, fast dissolution of crystals at conditions outside their stability field (e.g. as for clinopyroxene in the Xiaogulihe magmas, which did not crystallize type-2 autocrysts) could result in complete dissolution of the original crystal(s). During further cooling or decompression of the magmas, they would be supersaturated in nuclei and form new crystals/crystal clusters. Shallow crustal magma storage is inferred to be relatively rare in the plumbing systems beneath monogenetic volcanoes [START_REF] Mcgee | Interpreting chemical compositions of small-scale basaltic systems: A review[END_REF]. However, geophysical surveys have suggested that crystal-rich magma mush is present in reservoirs beneath the youngest monogenetic volcanoes of the Wudalianchi volcanic field and that mush-rich zones have completely crystallized beneath older volcanoes at depths of ~3-5 and ~8-15 km [START_REF] Gao | Magma recharging beneath the Weishan volcano of the intraplate Wudalianchi volcanic field, northeast China, implied from 3-D magnetotelluric imaging[END_REF]Li et al., 2016). Our study provides the first direct petrological evidence for the existence of a shallow magma storage zone beneath a K-rich monogenetic volcano in Northeast China. Though petrological studies cannot constrain the architecture of magma plumbing systems as geophysical surveys can, they are crucial for the interpretation of many geological surveys (e.g., by verifying if crustal magma storage zones do indeed exist or if geophysical anomalies correspond to fluid-rich zones) and they are also crucial for their hazard assessment.

J o u r n a l P r e -p r o o f

Conclusions

We used mineral textures, whole-rock, mineral chemical compositions and thermodynamic modeling to investigate the magmatic evolution in the crustal The classification of ultrapotassic, potassic, and sodic series volcanic rocks in K 2 O/Na 2 O compositional space follows that of [START_REF] Foley | The ultrapotassic rocks: characteristics, classification, and constraints for petrogenetic models[END_REF]. Literature data for the Xiaogulihe ultrapotassic rocks (while squares) are from [START_REF] Sun | Geochemistry of ultrapotassic volcanic rocks in Xiaogulihe NE China: Implications for the role of ancient subducted sediments[END_REF] and [START_REF] Zhang | Variation of olivine composition in the volcanic rocks in the Songliao basin, NE China: lithosphere control on the origin of the K-rich intraplate mafic lavas[END_REF]. Literature data for the Wudalianchi-Erkeshan-Keluo-Nuominhe J o u r n a l P r e -p r o o f potassic rocks (grey triangles) are from [START_REF] Basu | Major element, REE, and Pb, Nd and Sr isotopic geochemistry of Cenozoic volcanic rocks of eastern China: implications for their origin from suboceanic-type mantle reservoirs[END_REF], [START_REF] Chen | Geochemistry of Cenozoic basalts and mantle xenoliths in Northeast China[END_REF], [START_REF] Chu | Source of highly potassic basalts in northeast China: Evidence from Re-Os, Sr -Nd-Hf isotopes and PGE geochemistry[END_REF], [START_REF] Fan | The Cenozoic basaltic rocks of eastern China: petrology and chemical composition[END_REF], [START_REF] Hsu | Geochemistry of late Cenozoic basalts from Wudalianchi and Jingpohu areas, Heilongjiang Province, northeast China[END_REF], [START_REF] Kuritani | Transition zone origin of potassic basalts from Wudalianchi volcano, northeast China[END_REF], [START_REF] Liu | Major-and trace-element compositions of Cenozoic basalts in eastern China: Petrogenesis and mantle source[END_REF], Liu et al. (2017a), Wang et al. (2017), [START_REF] Zhang | Potassic volcanic rocks in NE China: geochemical constraints on mantle source and magma genesis[END_REF], Zhao et al. (2014), and[START_REF] Zou | Constraints on the origin of historic potassic basalts from northeast China by U-Th disequilibrium data[END_REF]. et al. (2003). Normalized value of the chondrite is from [START_REF] Anders | Abundances of the elements: Meteoritic and solar[END_REF]. coefficient between clinopyroxene and basaltic melt falls from 0.27 [START_REF] Putirka | Clinopyroxene+ liquid equilibria to 100 kbar and 2450 K[END_REF] to 0.23 [START_REF] Toplis | An experimental study of the influence of oxygen fugacity on Fe-Ti oxide stability, phase relations, and mineral-melt equilibria in ferro-basaltic systems[END_REF]. [START_REF] Zhang | Variation of olivine composition in the volcanic rocks in the Songliao basin, NE China: lithosphere control on the origin of the K-rich intraplate mafic lavas[END_REF], olivine compositions from MORBs, Koolau [START_REF] Sobolev | The amount of recycled crust in sources of mantle-derived melts[END_REF], and HIMU basalts [START_REF] Weiss | Key new pieces of the HIMU puzzle from olivines and diamond inclusions[END_REF]. Black solid fields represent calculated Ni, Ca, and Mn contents for olivines crystallized from primary melts derived from a fertile peridotite source [START_REF] Herzberg | Identification of Source Lithology in the Hawaiian and Canary Islands: Implications for Origins[END_REF]. Dotted black curves delineate compositional trends for modeled olivines along a possible liquid line of descent (LLD) from sample 16XGLH06 at 200 MPa. We calculated the LLD for the K-rich magma system using the rhyolite-MELTS software of [START_REF] J O U R N A L P R E -P R O O F Gualda | MELTS_Excel: AMicrosoft Excel-based MELTS interface for research and teaching of magma properties and evolution[END_REF] for crystallization at relatively oxidizing conditions (QFM+1) and at low H 2 O content (0.5 wt.%). The composition of olivines that crystallized along the LLD were calculated using partition coefficients reported by [START_REF] Foley | Trace element partitioning in lamproitic magmas -the Gaussberg olivine leucitite[END_REF] did not survive this process, but may have reacted with the liquid of the main magma to form hybrid crystal clusters with a relatively Mg-rich composition, in near-equilibrium with the host melt.

J o u r n a l P r e -p r o o f b LOI=Loss on ignition.

c Mg#=Mg 2+ /(Mg 2+ +Fe 2+ ), assuming Fe 3+ /Fe total = 0.1, cation ratio.

J o u r n a l P r e -p r o o f

Journal Pre-proof

  The shallower Ni versus Fo trend of olivine from MORBs likely reflects the partitioning of Ni between olivine and alkali-poor host melt, as compared to the more alkali-rich Koolau and Xiaogulihe systems. The extensive, shallow Ni versus Fo fractionation trends for olivines from Koolau, HIMU and MORBs with <Fo89 are J o u r n a l P r e -p r o o f characteristic for co-crystallization of olivine, clinopyroxene, and plagioclase[START_REF] Ruprecht | Feeding andesitic eruptions with a high-speed connection from the mantle[END_REF], as also highlighted by our modelling (which predicts abrupt shallowing of the compositional trend when clinopyroxene joins the crystallizing assemblage; Fig.9a). The overall relatively flat Ca compositional trends for olivines from Koolau and MORB or the decrease in Ca versus Fo for olivines from HIMU basalts (Fig.9b) are consistent with extensive plagioclase and/or clinopyroxene co-crystallization, which is characteristic for these rock suites. The steepness of trends of olivine Mn versus Fo increases from MORB over Koolau and

  magmatic plumbing system beneath the Ma'anshan volcano in Northeast China. In combination, we interpret our observations and data to indicate that a crystal-rich mush that contained type-1 olivine, leucite, and clinopyroxene had crystallized at shallow level (~200 MPa). The main Xiaogulihe ultrapotassic magmas, which crystallized normally zoned, high-Ni, low-Mn olivine and leucite (type-2) from a low-H 2 O melt, recharged and partially mixed with the crystal-rich mush (i.e. a resident magma). The steep decrease in Ni and increase in Mn contents with Fo values of the type-2 olivine record fractional crystallization from alkali-rich melts in which olivine-melt Ni-Mn partition coefficients were high. The presence of some reversely zoned olivines, hybrid clinopyroxene clusters, and partially resorbed leucites overgrown by olivine indicates that the main Xiaogulihe magmas entrained minor volumes (<5 vol.%) of the crystal-rich magma mush. Despite their small eruptive volume and relatively uniform geochemical compositions, magmas erupted in monogenetic volcanic fields may undergo complex magmatic processes in the crust, as shown here for the Xiaogulihe system.

Figure Captions Figure 1 .

 Captions1 Figure Captions

Figure 2 .

 2 Figure 2. Representative photomicrographs of the Xiaogulihe ultrapotassic rocks. (a)

Figure 3 .

 3 Figure 3. Plots of (a) Na 2 O + K 2 O versus SiO 2 (Le Bas et al., 1986), and (b) K 2 O

Figure 4 .

 4 Figure 4. Chondrite-normalized rare earth element (REE) pattern for the Xiaogulihe

Figure 5 .

 5 Figure 5. (a) Back-scattered electron (BSE) image and (b) compositional traverses for

Figure 6 .

 6 Figure 6. (a) BSE image, (b-c) compositional traverses A-A' and B-B', and (d-f)

Figure 7 .

 7 Figure 7. (a) BSE image, (b) compositional traverses A-A', and (c-f) X-ray elemental

Figure 8 .

 8 Figure 8. (a) Plot of whole-rock Mg number (Mg#) versus olivine Fo content for the

Figure 9 .

 9 Figure 9. Plots of (a) Ni, (b) Ca, and (c) Mn versus Fo values for the type-1 and -2

  (Ni and Mn) andHerzberg and O'Hara (2002) (Ca). Gray dotted lines indicate the compositional trends inferred to record recharge and mixing between magmas containing the type-1 and type-2 olivines.

Figure 10 .

 10 Figure 10. Summary of selected thermodynamic model results for sample

Figure 11 .

 11 Figure 11. Schematic diagrams showing our magma recharge and mixing model

Table 1

 1 Whole-rock major element (wt.%) and trace element compositions (ppm) of Xiaogulihe ultrapotassic rocks in N

	Sample 16XGLH01 16XGLH02 16XGLH03 16XGLH04	16XGLH05	16XGLH06	16XGLH07	16XGLH08	16XGLH09
			N50°44′50.6″		N 50°44′49.6″	N 50°44′44.5″	N 50°44′34.9″	N 50°43′28.3″	N 50°42′46.5″
			E 124°47′50.9″		E 124°47′32.3″	E 124°47′21″	E 124°47′9.03″	E 124°46′26.9″	E 124°44′38.3″
	SiO2	48.39	48.38	49.40	47.66	48.00	47.36	48.04	48.26	49.01
	TiO2	2.90	2.96	3.01	2.92	2.91	2.82	2.86	3.02	3.03
	Al2O3	11.10	11.17	11.56	11.17	11.30	11.29	11.26	11.40	11.59
	Fe2O3t a	7.60	7.66	7.80	7.60	7.70	7.94	7.91	7.74	7.47
	MnO	0.11	0.11	0.12	0.11	0.11	0.11	0.11	0.12	0.11
	MgO	8.23	8.29	8.34	8.33	8.40	8.85	8.97	8.13	7.61
	CaO	6.12	6.05	6.33	6.39	6.33	6.67	6.46	6.15	5.60
	Na2O	2.02	2.51	2.42	2.22	2.60	2.40	2.01	1.97	2.56
	K2O P2O5 LOI b Total Mg# c Li Be Sc V Cr Co Ni Cu Zn Ga Ge Rb Sr Y Zr	8.50 1.12 2.55 98.64 70.45 6.84 7.46 18.1 122 240 34.1 202 38.9 98.8 25.3 1.75 152 1175 26.0 904	8.50 1.22 1.88 98.73 70.44 7.27 7.75 18.6 113 245 34.4 205 36.9 100.6 25.9 1.78 152 1243 26.2 925 J o u r n a l P r e -p r o o f 8.57 8.05 8.26 7.85 1.72 1.64 1.67 1.72 1.60 2.60 1.39 1.55 100.86 98.70 98.67 98.55 70.18 70.70 70.60 71.05 7.15 7.18 7.33 6.72 7.65 7.53 7.48 6.29 18.5 18.2 18.4 18.0 149 154 153 158 241 238 250 269 33.4 33.5 34.4 37.5 193 199 197 213 34.3 35.1 36.5 37.9 99.1 97.6 98.7 96.9 25.8 25.1 25.1 23.6 1.75 1.72 1.68 1.59 159 163 147 140 1461 1593 1565 1622 26.6 25.9 26.4 24.5 916 900 884 749	7.98 1.17 1.79 98.56 71.40 7.45 6.80 18.2 172 267 36.6 213 37.5 97.8 24.3 1.66 144 1249 25.2 817	7.88 1.72 2.17 98.56 69.81 6.68 7.69 18.4 159 232 32.7 191 32.3 99.1 25.6 1.75 176 1481 26.5 915	8.91 1.43 1.37 98.69 69.16 7.41 7.02 17.6 146 217 31.2 187 34.8 98.6 25.6 1.74 156 1267 25.4 844
	Nb	70.7	72.6	72.1	70.5	70.7	69.1	71.3	70.6	69.0
	Cs	1.39	1.40	1.42	1.39	1.36	1.30	1.35	1.46	1.36
	Ba	3568	3835	2106	3182	3259	3131	3739	2322	2912
	La	154	157	158	154	156	137	145	156	152
	Ce	311	316	317	307	309	273	285	316	305
	Pr	34.0	34.7	35.0	33.9	34.2	30.0	31.5	35.1	33.9
	Nd	126	130	130	127	127	112	118	129	126
	Sm	17.5	17.9	18.0	17.5	17.7	15.7	16.4	18.1	17.4
	Eu	4.45	4.57	4.47	4.44	4.48	4.05	4.27	4.51	4.39
	Gd	12.9	13.1	13.2	12.9	13.1	11.7	12.3	13.2	12.8
	Tb	1.35	1.38	1.39	1.35	1.38	1.26	1.30	1.38	1.33
	Dy	6.21	6.31	6.37	6.21	6.33	5.85	6.03	6.39	6.13

Acknowledgements

We are grateful to Wenli Xie and Ye Liu for their assistance with the major-and J o u r n a l P r e -p r o o f

trace-element analyses of the bulk rocks. We also thank Lei Wu for her assistance in mounting olivine in the epoxy targets. We thank Ian E M Smith and two anonymous reviewers for their constructive comments on an earlier version of this manuscript. J o u r n a l P r e -p r o o f

Declaration of interests

☒ The authors declare that they have no known competing financial interests or personal relationships that could have appeared to influence the work reported in this paper.

☐The authors declare the following financial interests/personal relationships which may be considered as potential competing interests:

J o u r n a l P r e -p r o o f