Journal of Volcanology and Geothermal Research 383 (2019) 103–111

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Journal of Volcanology and Geothermal Research

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Tephra evidence for the most recent eruption of Laoheishan , volcanic field, northeast

Chunqing Sun a,⁎, Károly Németh b,TaoZhanc,HaitaoYoud, Guoqiang Chu a, Jiaqi Liu a a Key Laboratory of Cenozoic Geology and Environment, Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing 100029, China b Institute of Agriculture and Environment, Massey University, Palmerston North, New Zealand c The Second Hydrogeology and Engineering Geology Prospecting Institute of Heilongjiang Province, Haerbin 150030, China d Key Laboratory of Computational Geodynamics, College of Earth Science, University of Chinese Academy of Sciences, Beijing 100049, China article info abstract

Article history: Wudalianchi volcanic field (WDLC) is one of the youngest intracontinental monogenetic volcanic fields in China. Received 21 June 2017 The 1719–1721 CE Laoheishan-Huoshaoshan eruption, and the 1776 CE Laoheishan eruption are the latest erup- Received in revised form 17 February 2018 tions in WDLC based on the local historical records. However, most of the recent explosive eruptive products Accepted 18 March 2018 around WDLC are attributed to the 1719–1721 CE Laoheishan-Huoshaoshan eruption while less attentions Available online 20 March 2018 were paid on the 1776 CE Laoheishan eruption. There are two types of scoria fall deposits around Laoheishan vol- cano, i.e. the upper light grey high vesicular scoria deposit (US) and below dark low vesicular scoria deposit (BS). Keywords: N b Wudalianchi Most of the glass shards from US exhibit 4% Na2O while BS show 4% Na2O. In addition, US presents two differ- Tephrochronology ent glass composition clusters, indicating a complex magma batch feeding the eruption. Broadly, all of these erup- Laoheishan tive products from WDLC have extreme high potassium (usually N5%) content with trachyandesitic to Nagelaqiushan tephriphonolitic in composition that can be clearly distinguished from those from other nearby volcanic regions, Tephra such as Nuomin (~150 km to Nangelaqiushan lake (NGLQ)), Arxan-Chaihe (~450 km to NGLQ), Longgang (~700 km to NGLQ) and Jingbohu (~550 km to NGLQ). A cryptotephra layer is clearly revealed as a distinct peak in magnetic susceptibility measurements from NGLQ ~ 8 km northwest to Laoheishan volcano. Glass com- position of the cryptotephra layer recorded in NGLQ is similar to the proximal US around Laoheishan volcano. On basis of historical records and field observations, we ascribed US to the 1776 CE Laoheishan eruption and BS to the 1719–1721 CE Laoheishan-Huoshaoshan eruption. Consequently, historical records assigned a precise age (1776 CE) for the tephra recorded in NGLQ, and thus can be used to refine the age model of these lacustrine sediments. © 2018 Elsevier B.V. All rights reserved.

1. Introduction where the mechanisms of volcanism and magmatic sources of related volcanoes have been characterized (Fig. 1) (e.g. Hsu and Chen, 1998; Tephra layers erupted from explosive eruptions are ideal marker Kuritani et al., 2013; Zhang et al., 1995; Zhao et al., 2014; Zou et al., beds to correlate and constrain the ages of Quaternary volcanic events 2003). Tephrochronology is highly beneficial in the estimating of volca- among various depositional archives, and plays a more and more impor- nic risk and establishing eruptive sequences (Larsen and Eiríksson, tant role in the Quaternary and volcanological studies (Blockley et al., 2008; Molloy et al., 2009; Plunkett et al., 2015); in addition chronolog- 2012; Davies, 2015; Lane et al., 2013a; Lowe, 2011; Ponomareva et al., ical uncertainties of sedimentary archives can also be reduced on basis 2015). In addition, tephra layers invisible to naked eyes, known as of tephra layers with well-known ages derived from various sedimen- cryptotephra, have dramatically extended its applications area to tary archives (Barton et al., 2015; Lane et al., 2012). those sites hundreds to thousands of kilometers away from the volcanic In this study, proximal fall deposits around the Laoheishan volcano vents (Jensen et al., 2014; Lane et al., 2013b; Mackay et al., 2016; Sun et were sampled and analyzed (Fig. 1). On the basis of historical records al., 2014). Tephrochronology has been applied across worldwide based and field exposures, we attributed the widespread grey fall deposit on varied sedimentary archives, such as the lake, marine, peat, loess and with highly vesicular to the 1776 CE eruption of Laoheishan volcano, ice cores (Lowe, 2011). However, such studies in China are relative lim- while the dark fall deposits with low vesicular to the 1719–1721 CE ited, and even the Wudalianchi volcanic field (WDLC), northeast China eruption of Laoheishan-Huoshaoshan volcano. In addition, a cryptotephra layer was identified in the lake sediments of ⁎ Corresponding author. Nanagelaqiushan (NGLQ) according to abnormal magnetic susceptibil- E-mail address: [email protected] (C. Sun). ity measurements. The NGLQ cryptotephra layer exhibits similar glass

https://doi.org/10.1016/j.jvolgeores.2018.03.014 0377-0273/© 2018 Elsevier B.V. All rights reserved. 104 C. Sun et al. / Journal of Volcanology and Geothermal Research 383 (2019) 103–111

Fig. 1. Geological map of the Wudalianchi volcanic field (WDLC) showing its position and other related volcanic fields (CBS: Changbaishan, LVF: Longgang, JBH: Jingbohu, ACVF: Arxan- Chaihe, NVF: Nuominhe, EKS: Erkeshan, KL: , ML: Menlu river) in northeast China (modified from Xiao and Wang (2009)). The major Quaternary eruption centers including Laoheishan and Huoshaoshan, the lake of Nangelaqiushan (NGLQ), and proximal sampling sites around Laoheishan were marked in the map. compositions to the 1776 CE and thus have been here correlated; conse- basaltic composition rich in potassium (Chu et al., 2013; Feng and quently, a precise age can be used to refine age model of the NGLQ. Whitford-Stark, 1986; Hsu and Chen, 1998; Kuritani et al., 2013; Zhang et al., 1995; Zou et al., 2003). Some vesicle-filling crustal xeno- 2. Geological background liths can be occasionally found in these volcanic rocks that cover the Lower Cretaceous and Pliocene sandstone and mudstone, and minor The Wudalianchi volcanic field (WDLC: 125°45′–126°30 Long. and Late Mesozoic biotite-granite (McGee et al., 2015). 48°30′–48°50′ Lat.) covers an area of ~800 km2, located at the northwest Volcanic eruptions in WDLC started in the , and the of Heilongjiang Province of China, is one of the major volcanic regions in flows from this stage are widely distributed in the area, such as the northeast China (Fig. 1). Wudalianchi in Chinese means “those five con- Molabushan, Yaoquanshan, and Wohushan (Fig. 1)(Li et al., 1999; Liu, nected pools” (lakes) formed by entering lava flows into Beihe river 1987; Wei et al., 2003; Zhao et al., 2014). Volcanic products erupted damming the river channel. There are about 14 Quaternary volcanic during the Early Holocene can be found at Xilongmenshan and centers with well-preserved cones in this field (Fig. 1), and various Donglongmenshan (Fig. 1)(Xiao and Wang, 2009), and tephra layers well-preserved volcanic landscapes and edifices can also be found, recorded in lacustrine sediments also illustrate early Holocene erup- such as the “fumarolic cones” around Huoshaoshan volcano (Feng and tions (Wang et al., 2015). According to the Qing Dynasty records, the Whitford-Stark, 1986; Gao et al., 2013). The distribution of these volca- youngest eruptive volcanic rocks were formed during the 1719– nic cones in this area usually along northeast direction (Fig. 1), which 1720 CE and 1776 CE at Huoshaoshan and Laoheishan volcanic erup- are controlled by regional faults and older structural elements of the tions (Fig. 1)(Chen et al., 2004; Wei et al., 2003). basement (Xiao and Wang, 2009; Zhao et al., 2014). Usually, the volcanoes in this field started with Hawaiian-style mild 3. Study sites, materials and methods explosive and effusive eruptions that culminated in terminal Strombolian-style explosive eruptions hence most of the volcanoes are 3.1. Proximal tephra samplings covered by texturally diverse multicolor scoriaceous deposits (Xiao and Wang, 2009). The volcanic rocks of the WDLC consist predomi- Laoheishan volcano with a funnel-shaped crater is the highest cone nantly of extensive lava flows, and pyroclastic fall deposits that cover (165.9 m·a.s.l) and deepest crater (145 m·a.s.l) among the 14 volcanic volcanic cones and surrounding areas (Xiao and Wang, 2009; Zhao et centers in the WDLC (Fig. 2A). The latest eruption of Laoheishan and al., 2014). All of these volcanic rocks exhibit homogenous alkaline Huoshaoshan volcanoes during the 1719–1720 CE can be divided into C. Sun et al. / Journal of Volcanology and Geothermal Research 383 (2019) 103–111 105

Fig. 2. Field outcrops around Laoheishan volcano. A is the crater on the top of Laoheishan cone (sample named as LHS-3). B is the general view of the tephra sheet on the southeast side of Laoheishan cone. C and D are the near views of light grey highly vesicular scoria sheet (samples named as LHS-1 and LHS-2 respectively). E is the outcrop of the thick black and reddish low vesicular scoria deposits (BS) below the light grey highly vesicular scoria (US) (sample named as LHS-4). The yellow line marks the boundary between the BS and US, and the yellow arrow indicates ashing of the previous eruptive products by followed eruption.

two stages. The first stage is an explosive eruption from Laoheishan vol- and black low vesicular scoria deposit, and the boundary shows clear cano that produced widespread scoria fall deposits. Later on effusive ashing phenomena just below the upper light grey highly vesicular sco- eruption produced pahoehoe and a'a lava flows outpoured from the ria deposit (US), which suggest that this scoria deposit is older than US Laoheishan and Huoshaoshan volcanoes, and the Wudalianchi was (Fig. 2E). A sample from the lower low vesicular older scoria deposit formed by this effusive eruption (Feng and Whitford-Stark, 1986; Liu, (BS), named as LHS-4 was collected just below the US, near to the site 1997; Xiao and Wang, 2009; Wei et al., 2003). of LHS-2 (Fig. 2E). Laoheishan volcano experienced violent Strombolian eruptions that generated an extensive (~16 km2) and thick scoria fall deposit that can 3.2. Tephra investigations of NGLQ be traced in and around the crater of this volcano. Abundant melted crustal of basement rocks are also hosted in the most recent Nangelaqiushan (126.00° E, 48.74° N), a 149.9 m high volcano with eruptive products (e.g. McGee et al., 2015). Black scoria named LHS-3 an elevation of 596.9 m·a.s.l, is located in the Wudalianchi Global was sampled from the crater of Laoheishan volcano (Fig. 2A). The edifice Geopark (Gao et al., 2013), Heilongjiang Province (Fig. 1). The Heaven of the Huoshaoshan volcano northeast to the Laoheishan volcano (Fig. Lake on the top of Nangelaqiushan is the only crater lake across all the 1) is almost entirely constructed by effusive lava flows with limited cones in the WDLC, and the diameter of this lake is about 400 m. This proximal scoria fall deposits, and no samples were collected from lake has become a swamp now due to pumps for surrounding irriga- Huoshaoshan volcano. tions in the 1970s. Light grey highly vesicular scoria deposit (US) is extensive distrib- Two sedimentary cores (TC1 and TC2) were taken using percussion uted on the south-southwest sides of the Laoheishan scoria cone (Fig. corer in the Nangelaqiushan Lake (NGLQ) in October 2011 and Novem- 2B), and the covering area of this sheet is N16 km2 and thins rapidly in ber 2012. Detailed lithological components and descriptions have been south-southeast direction (Liu, 1997). LHS-1 was collected from this de- presented by Zhou et al. (2016). These two cores share similar litholog- posit in the east side of Laoheishan volcano, and LHS-2 was from its ical units and can be correlated on basis of loss on ignition (LOI) and southeast side (Figs. 1, 2C, D). Below this scoria, there is a thick reddish magnetic susceptibility (Fig. 3 A). 106 C. Sun et al. / Journal of Volcanology and Geothermal Research 383 (2019) 103–111

Fig. 3. A: Magnetic susceptibility of the TC1 and TC2 core of the Lake Nangelaqiu, and the correlation of the two parallel core by the highest of the magnetic susceptibility. B: Bayesian age- depth model for the uppermost 65 cm sequence of Lake Nagelaqiushan core (ages estimates from Zhou et al. (2016)). C: Refined Bayesian age-depth model for the above sequence on the basis of the NGLQ17.5 tephra imported in the appropriate position where the highest magnetic susceptibility was detected.

The TC2 core was subsampled with 5 cm intervals for pollen analysis glass ML3B-G (Jochum et al., 2006) was used to monitor the precision (Zhou et al., 2016), and TC2 core was sampled for tephra separations and accuracy of the data. In order to ensure comparative datasets, and analysis based on the record of magnetic susceptibility. Samples glass compositions for proximal tephra samples from the Laoheishan from peaks of magnetic susceptibility of the TC2 core were treated were also analyzed under the same instrument and analytical with 10% HCl to remove carbonates and with H2O2 to remove organic conditions. materials. After chemical treatments, the samples were sieved, and those particles with a diameter between 30 μm and 100 μm were kept 4. Results and checked for the presence of glass shards under the high-power op- tical microscope. Pure glass shards were mounted and polished to ex- There is a prominent magnetic susceptibility peak at 17.5 cm of Core pose the internal sections for electron microprobe analysis (EPMA). TC2 (named as NGLQ17.5) (Fig. 3A). The NGLQ17.5 is an invisible tephra layer, and the number of glass shards are N3000 shards/0.5 g dry sample 3.3. Geochemical analysis (counting the glass shards under high power microscope). In addition, sam- ple NGLQ18.5 below NGLQ17.5, and NGLQ16.5 and NGLQ15.5 were also EPMA, using a wavelength-dispersive spectrometer (WDS) was per- used to tephra separations and investigations. Glass shards from all of formed on a JEOL JXA 8100 electron microprobe at the State Key Labora- these layers have abundant bubbles and sharp edges illustrating a primary tory of Lithospheric Evolution, Institute of Geology and Geophysics fallout tephra layer (Fig. 4)(Németh, 2010; Shane, 2005). The glass shards (IGGCAS), Chinese Academy of Sciences. Ten major and minor elements of NGLQ tephra have a diameter N 100 um, and exhibit a light brown color (Na, Mg, Al, Si, K, Ca, Fe, Ti, Mn, P) were analyzed with an accelerating and they are rich in microlites (Fig. 4).GlassshardsofUS(LHS-1andLHS-2) voltage of 15 kV, a beam current of 6 nA, and a beam diameter of 10 from Laoheishan volcano also have light brown color with many microlites μm. Peak counting times used were 20 s for all elements except for Na (Fig. 5A, B). The glass shards of the scoria from the crater of Laoheishan vol- (10 s). The measurement of Na content was first made and determined cano (LHS-3) and the BS show dark brown color. Morphology of glass during analysis. Secondary standard glasses from the MPI-DING fused shards correlates the US to the NGLQ tephra better than to the BS.

Fig. 4. Photos of glass shards from NGLQ17.5 tephra recorded in Lake Nangelaqiushan. C. Sun et al. / Journal of Volcanology and Geothermal Research 383 (2019) 103–111 107

Fig. 5. Photos of proximal tephra from Laoheishan volcano. A and B are the photos tephra LHS-1 and LHS-2 respectively (light grey highly vesicular scoria (US)). C is the photo of the LHS-3. D, E and F are the photos of the LHS-4 (thick black and reddish low vesicular scoria deposits (BS)).

Major and minor element data of the glass shards show a relative scoria exhibit a media MgO content between LHS-1 and LHS-2, how- heterogeneous composition. All of glass compositions were normalized ever, the content of N2O is dramatically lower than LHS-1 and LHS-2. to an anhydrous basis in order to compare those data from proximal BS (LHS-4) show a more varied glass composition than the light grey tephra (Pearce et al., 2008, 2014). For the NGLQ17.5 tephra, the SiO2 highly vesicular scoria sheet (LHS-1 and LHS-2) (Tables 1, S1; Figs. 6; varies between 50.52 wt%–55.69 wt%, the MgO between 2.29 wt%– 7), especially the Na2OcontentandK2O/Na2O ratios clearly deviate 4.30 wt%, CaO 4.29 wt%–7.26 wt%, TiO2 2.42 wt%–2.99 wt%, and K2Obe- from those proximal LHS-1 and LHS-2, and NGLQ tephras. tween 5.02 wt%–6.73 wt% (Tables 1, S1; Figs. 6; 7). Other tephra samples Radiocarbon ages and dating procedures for the Nagelaqiushan lake of NGLQ18.5, NGLQ16.5 and NGLQ15.5 also exhibit similar glass compo- sediment cores have been reported previously by Zhou et al. (2016).In sitions. The major element composition of the glass shards from these this study, we have calculated a Bayesian-based age model using the flexi- tephra samples therefore plot mainly in the field of tephriphonolite ble age-depth modeling software Bacon V2.2 (Blaauw and Christen, 2011). and (Fig. 6). Based on this age model, tephra NGLQ17.5 is dated to between 83.8– Glass data of US from Laoheishan volcano fall primarily in the field of 355.3 a cal BP (NGLQ17) and 163.7–409.1 a cal BP (NGLQ18) (Fig. 3B). tephriphonolite and trachyandesite on a total alkali silica diagram (TAS) and the alkali content (usually N9.0 wt%) is similar to those glass shards 5. Discussion from NGLQ tephras (Tables 1, S1; Figs. 6; 7). The LHS-1 and LHS-2 tephras exhibit two different compositional clusters (SiO2 varies be- 5.1. Source and age of the NGLQ tephras tween 53.41 wt%–54.25 wt%, the MgO between 2.77 wt%–3.93 wt%,

CaO 4.81 wt%–6.39 wt%, TiO2 2.49 wt%–2.75 wt%, and K2Obetween During the Holocene, there were extensive explosive eruptions around 5.46 wt%–6.11 wt%, and SiO2 varies between 55.12 wt%–55.71 wt%, the volcanic fields in northeast China, such as the Arxan-Chaihe and the MgO between 2.79 wt%–2.94 wt%, CaO 4.81 wt%–5.12 wt%, TiO2 Nuominhe (~450 km and ~150 km to NGLQ) (Bai et al., 2005; Németh et 2.47 wt%–2.70 wt%, and K2O between 5.94 wt%–6.25 wt% respectively), al., 2017; Sun et al., 2017a; Zhao, 2010), Longgang (~700 km to NGLQ) andlessvariedthanthoseglassdatafromNGLQtephras.TheLHS-3 (Fan et al., 2002; Liu et al., 2009; Sun et al., 2016), Jingbohu (~550 km to 108 C. Sun et al. / Journal of Volcanology and Geothermal Research 383 (2019) 103–111

Table 1 Summary of WDS-EPMA results of glass shards for the tephra from Nangelaqiushan lake (NGLQ15.5-NGLQ18.5) and proximal tephras from Laoheishan bolcano (LHS-1-LHS-4). All the data have been normalized to a hydrous basis with original analytical totals. Secondary standard of MPI-DING glass standard ML3B-G was analyzed to monitor the precision and accuracy of the glass data.

Sample SiO2 TiO2 Al2O3 FeO MnO MgO CaO Na2OK2OP2O5 Analytical total Nangelaqiushan lake NGLQ15.5 (n = 24) 53.89 2.65 15.95 7.24 0.11 3.03 5.50 4.42 6.08 1.13 97.81 Mean 3.66 0.20 1.07 1.27 0.05 0.91 1.58 0.96 0.79 0.20 1.30 2 SD NGLQ16.5 (n = 28) 53.75 2.59 16.13 7.10 0.11 3.09 5.46 4.61 6.03 1.14 98.09 Mean 2.95 0.20 1.20 1.01 0.04 1.17 1.69 0.85 0.89 0.57 2.39 2 SD NGLQ17.5 (n = 40) 53.53 2.67 16.05 7.27 0.11 3.06 5.49 4.60 6.12 1.10 98.02 Mean 2.89 0.25 1.26 1.06 0.05 0.94 1.43 0.92 0.78 0.29 1.84 2 SD NGLQ18.5 (n = 24) 52.71 2.64 16.39 7.37 0.12 2.90 5.37 5.14 6.31 1.05 98.27 Mean 1.86 0.21 1.56 1.18 0.05 1.14 2.02 0.64 0.69 0.36 2.03 2 SD Laoheishan LHS-1 (n = 23) 54.00 2.60 15.61 7.21 0.12 3.43 5.93 4.27 5.70 1.13 97.85 Mean 0.42 0.06 0.17 0.17 0.03 0.22 0.30 0.13 0.13 0.05 0.72 2 SD LHS-2 (n = 16) 55.46 2.60 15.82 6.72 0.10 2.88 4.92 4.35 6.08 1.07 98.41 Mean 0.34 0.12 0.19 0.15 0.03 0.11 0.21 0.29 0.16 0.16 0.97 2 SD LHS-3 (n = 25) 55.53 2.57 15.39 6.75 0.10 3.32 5.53 3.52 6.17 1.13 98.31 Mean 0.63 0.11 0.30 0.39 0.04 0.18 0.31 0.53 0.33 0.08 1.32 2 SD LHS-4 (n = 66) 54.84 2.60 15.53 6.99 0.11 3.33 5.73 3.83 5.96 1.10 98.09 Mean 1.77 0.12 0.78 0.57 0.04 0.73 1.37 0.35 0.70 0.10 1.78 2 SD Secondary standard ML3B-G (n = 15) 51.55 2.13 13.77 10.92 0.17 6.61 10.35 2.35 0.39 0.25 Mean 0.68 0.08 0.22 0.23 0.05 0.14 0.17 0.11 0.04 0.03 2 SD 51.40 2.13 13.60 10.90 0.17 6.59 10.50 2.40 0.39 Preferred value 0.60 0.09 0.20 0.10 0.01 0.08 0.10 0.06 0.00 Uncertainty (95%)

NGLQ) (Chen et al., 2005; Fan et al., 2003; Zhang et al., 2000), Changbaishan the age of the tephra recorded in NGLQ. However, the glass shards (~750 km to NGLQ) (Liu, 1999; Sun et al., 2014, 2015; Wei et al., 2003), and from the tephra of these Changbaishan eruptions are mainly in Wudalianchi (Liu, 1999; Wei et al., 2003). compositions and could not be correlated with the intermediate to Changbaishan volcano is the most noticeable ash-producing volcano basic compositional glass shards of the tephra recorded in NGLQ. in northeast China (Fig. 1), and experienced several major explosive The most recent explosive eruption of Longgang volcanic field was eruptions during the Late Pleistocene to Holocene. For example, the from the 1600 a cal BP eruption of Jinlongdingzi volcano (~700 km to ash from its Millennium eruption was predominantly transported to NGLQ) (Fig. 1)(Liu et al., 2009; Sun et al., 2016). Glass shards from the eastern areas of Changbaishan volcano (Machida and Arai, 1983). this Jinlongdingzi tephra are trachybasaltic to basaltic trachyandesitic However, there were still some historical recorded explosive eruptions in composition, and can be clearly distinguished from the WDLC tephra during the late Holocene, such as the 1903 CE, 1702 CE and 1668 CE highly enriched in potassium (Fig. 6). Radiocarbon 14C dating on the eruptions (Liu, 1999; Wei et al., 2003). The 1903 CE eruption was a charcoal buried in tephra sheet showed that the most recent eruption local affected phreatomagmatic eruption and its products were difficult in Jingbohu occurred at ~5000 a cal BP (Fig. 1)(Fan et al., 2003; Zhang to be transported to more distal areas. The 1702 CE and 1668 CE erup- et al., 2000). What's more, the content of K2O of the Cenozoic tions produced thick fall deposits around the Changbaishan volcanic from Jinbohu is dramatically lower than those from WDLC (Hsu and cone (Sun et al., 2017b), and the ages of these eruptions are similar to Chen, 1998). The WDLC is near to Nuominhe and Arxan-Chaihe volcanic fields, and the latest explosive eruption is the ~2000 a cal BP Gaoshan- Yanshaneruption(Fig. 1)(Bai et al., 2005). However, the trachybasaltic glass compositions of these tephras are clearly separated from the WDLC tephra. The WDLC is also near to some small volcanic areas, such as the Erkeshan, Keluo and Menlu river (Fig. 1)(Zhao et al., 2014), but most of the volcanic rocks from these areas are dated to Late Pleistocene to Early Pleistocene, and no known Holocene eruptions. There are 14 volcanic cones in the Wudalianchi volcanic field, and most of them are formed during Middle Pleistocene (Liu, 1987; Zhao et al., 2014), and there is no clear tephra sheet covered on the surface of these cones ex- cept the Laoheishan volcano. The tephra sheet on the southeast side of Laoheishan volcano was dated to ~270 a BP by thermal luminescence dat- ing method (Ji and Li, 1998), and thus correlated to the historical records of the 1719–1721 CE Laoheishan-Huoshaoshan eruption. The most noticeable recent eruption in Wudalianchi volcanic field is the 1719–1721 CE Laoheishan-Huoshaoshan eruption due to it was linked to the formation of these two volcanoes, but another recorded eruptive event could not be ignored, i.e. the 1776 CE eruption (Chen et al., 2004). As for the 1719–1721 CE eruption, the Ninggutalveji written by Zhenchen Wu from Qing Dynasty recorded: “During June to July, 59th year of Kangxi Emperor Qing Dynasty (i.e. AD 1720), at around the site (i.e. Laoheishan) 50 km northeast to Dedu, the Fig. 6. TAS diagram (Le Maitre et al., 1989) for comparing the glass data from the tephra fire and smog were ejected into sky, and the sounds like thunder which recorded in Nagelaqiushan Lake (NGLQ15.5-NGLQ18.5) and proximal tephras from can be heard within 5–6km. Sulfur and black rocks were ejected, such Laoheishan volcano (LHS-1-LHS-4) against the whole rock data from Nuominhe, glass phenomena last about one year, and finally a hill was formed.” data from Arxan-Chaihe (Moon lake and Gaoshan), and glass data from Longgang volcanic fields. Whole rock compositions from Nuominhe volcanic field are from Zhao (2010), glass data from Arxan-Chaihe are from Sun et al. (2017a), and glass data from The Heilongjiangwaiji written by Qing Xi from Qing Dynasty Longgang volcanic field are from Sun et al. (2016). recorded: C. Sun et al. / Journal of Volcanology and Geothermal Research 383 (2019) 103–111 109

Fig. 7. Major element compositions of glass shards from NGLQ tephras and proximal Laoheishan tephra. The grey shadow line (4% Na2O) in the diagram of MgO vs. Na2O indicates that most of glass shards from LHS-3 and LHS4 can be distinguished from those from NGLQ, LHS-1 and LHS-2 tephras.

“58th year of Kangxi Emperor Qing Dynasty (i.e. AD 1719), at around All of these historical records showed that the formations of the site (i.e. Laoheishan direction) southeast to Moergen, one day, fire Laoheishan volcano and Huoshaoshan volcano as well as the formation was suddenly erupted from earth surface and went out several days of the five connected lakes of this region were around 1719–1721 CE. later, rocks were ejected, sounds were loudly, and ponds were formed And the lava flows were also described in the local government docu- (i.e. the five connected lakes of Wudalianchi).” ments of Qing Dynasty (Chen et al., 2004). 110 C. Sun et al. / Journal of Volcanology and Geothermal Research 383 (2019) 103–111

Based on the historical documents of Heilongjiang translated by these tephra layers, and thus we could not determine the relative ages Tang Heer (Chen et al., 2004), local citizens recorded that there were between LHS-1 and LHS-2. Finally, we can conclude that the 1776 CE also explosive eruptions after the 1719–1721 CE eruption, i.e. 1776 CE: eruption had different eruptive phases, and tephra from these phases have been transported to those reverse directional sites N8kmaway “There was an earthquake at AD 1776, and large rocks and ash were from Laoheishan volcano. Although the Laoheishan volcano and ejected from the direction of Laoheishan volcano, and the sun could Huoshaoshan volcano were formed during the violent 1719–1721 CE not be seen for about three days. Local citizens moved to western direc- eruption, the dispersal of scoria deposits from these eruptions are tions due to the tephra fallouts.” more limited than the tephra from 1776 CE eruption. For example, no – fi Such descriptions in line with the tephra dispersal of US around the tephra layer sourced from 1719 1721 CE eruption was identi ed in Laoheishan volcano (i.e. covered on its east-southeast sides). Therefore, NGLQ. there was an explosive eruption at 1776 CE and the widespread US was from this eruption. The US is more likely to be transported to and thus 5.2. Bayesian age modeling covered much wider areas (Liu, 1997). There are ashing phenomena on the boundary between the US (LHS-1 and LHS-2) and BS (LHS-4) The tephra layer recorded in NGLQ has been served as a marker layer (Fig. 2E). Although there is no sufficient evidence to testify the eruptive to link and correlate different cores from this lake (Zhou et al., 2016), gap between these two kinds of scoria deposits, at least, proximal out- and the known 1719–1721 CE was used to as the age of this tephra crops at Laoheishan volcano suggest that the BS were from a relative layer. On the basis of the radiocarbon datings from Zhou et al. (2016) older eruption than the eruption corresponded to US. Consequently, and Bayesian age-depth modeling by Bacon software, the age range taking into account of historical records, the widespread US should be for the depth of 17 cm is 83.8–355.3 a cal BP, and 18 cm is 163.7– correlated with the 1776 CE eruption, and the relative BS might be 409.1 a cal BP, which overlaps with the historical recorded eruptions from the formation stage of Laoheishan volcano, i.e. the 1719–1721 CE of 1719–1721 CE eruption and 1776 CE eruption (Fig. 3). However, eruption. due to low resolution and dating uncertainties, it is difficult to correlate Broadly, the scoria deposits and the tephra around the Laoheishan this tephra to a precise eruption based on this modeling result. How- volcano share similar glass major element compositions (Figs. 6, 7), ever, correlations of between NGLQ tephras and proximal Laoheishan but the BS present a relative lower content of Na2O than the US (Fig. tephras, tephra dispersal descriptions of historical documents, field ev- 7). The LHS-1 and LHS-2 exhibit two different clusters of glass major el- idence from this study indicate that 1776 CE should be the actual age of ement compositions, which implies that they might be from different this tephra layer. For example, the scoria deposits from 1719–1721 CE eruptive phases during the 1776 CE eruption. eruption can be clearly distinguished from the NGLQ tephras and the The NGLQ tephra presents more varied glass major element compo- light grey scoria from 1776 CE eruption (Figs.6,7). sitions than the proximal scoria and tephra deposits around the Using above ages and related depths, 1776 CE was imported for the Laoheishan volcano (Figs. 6, 7). Overall, the NGLQ tephra layers show age of NGLQ17.5 tephra at the depth of 17.5 cm of TC2 core (~9.5 cm in a closer affinity to the US around the Laoheishan volcano, i.e. LHS-1 TC1 core). The results of the modeling exercise show that the ages over and LHS-2, and the BS (LHS-4) and LHS-3 can be excluded as a source last 1000 years are highly improved (Fig. 3C). We could not precisely as- candidate for the NGLQ tephra when considering the content of Na2O. sess the relative impacts from 1719–1721 CE eruption and 1776 CE Four continuous tephra layers as NGLQ18.5, NGLQ17.5, NGLQ16.5, and eruption due to the low resolution sampling of present pollen analysis NGLQ15.5 were sampled and analyzed for comparisons. However, (Fig. 8). But, this precise age-assigned tephra layer provides a maker there no any heterogeneous glass compositions can be detected within bed for future paleo-climatic studies.

Fig. 8. Pollen and charcoal percentage of Lake Nangelaqiushan TC1 core (uppermost 30 cm, Zhou et al., 2016). The dark grey line at 9.5 cm marks the position of NGLQ17.5 tephra. C. Sun et al. / Journal of Volcanology and Geothermal Research 383 (2019) 103–111 111

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