**1. Introduction**

Lava flows in every volcanic field represent the major volcanic events and significant phases of volcanism [1]. The most distinctive characteristics of lava flows are their surface morphology. Such surface "shapes and patterns" not only represent the interests of tourism and scientific exhibitions but also reveal great value for

interpretations of how volcanism occurred, potential indicators of petrogenesis, shifting of eruption phases, eruptive magnitudes (volumes and ejection pressures), and geochronology of how long an eruption last. In general, two types of the morphology of lava flows have been described in the literature: ʻaʻā type and pāhoehoe [1]. pāhoehoe lava flows commonly emerge during events of Strombolian style eruptions with low viscosity and high-temperature basaltic eruptions [2, 3]. This type of lava flow is usually known for its smooth surfaces and gentle undulations, with occasional hummocky surfaces and tumuli. In general, pāhoehoe lava flows can extend tens of kilometers in distance from their sources [3]. Small outflows alternatively emerge from the chilled crust of the surface and can feed small "toes", which are approximately no more than few dm thick, several m long, and dm-to-m wide. Pāhoehoe lava flows are associated with low outflux velocity; this means the volumetric flow rates are about 2–5 m3 /s and slow flow front velocities are approximately 1–10 m/hr. [3]. These behaviors of the emplacement are shown by the low flux velocity profile allowing the flows to develop a chilled crust keeping the melt able to move. Thus, the forehead of flows commonly proceeds moving slower than the lateral partitions of the flow body; this indicates not only the flow can maintain undisrupted with smooth and intact surfaces but also preserve "toe" structures while the flows keep moving. Like its counterpart, aa-type lava flows commonly present as extremely rough surfaces with spikes and swarmed gullies [1]. ʻaʻā lava type generally has denser inner parts. The emplacement behavior shows that the flows commonly have a thick (1–2 m) chilled shield surrounding the main lava body. The forehead of rough surfaces with clinkers can be broken while the flow moves [4–6]. The fallen part will eventually be buried by the bottom of the flows. Topography can affect significantly how the flow moves, and facilitate ponding or cascading effects in steep steps or behind obstacles or valleys. Pāhoehoe lava can also become rubble where chilled crusts can be broken apart and carried rapidly further. In this case, morphotypes could work better to describe the flows (e.g., [7]).

Following the regional tectonic trends, fissure eruptions always generate large volumes of lava, which form the continental flood basaltic lava provinces [8, 9]. Commonly, the lava provinces can stretch into hundreds to thousands of km2 areas. Due to the volumes of the lava that ejected, a basaltic flood lava province usually was formed over long time, extreme in a period of 1 to 2 million years [10, 11]. The fissure eruptions generally are related to the continental rift zones, such as East African Great Rift [12]. The stretching or rifting property usually produces large lava volumes These geological settings are usually defined by monogenetic volcanic fields. They are defined by tens to hundreds of small vents formed due to mainly two eruptive styles, such as Strombolian, Hawaiian, and phreatomagmatic types [13]. Those small vents usually swarm and confine in a large region (e.g., thousands of km2 ). The occurrences of monogenetic volcanic fields are commonly shown by the linear trend of vents, clustering, or randomly distributed all strongly influenced by the crustal structure of the region where they erupted [14, 15]. In old continental crusts inherited structural elements commonly influence the vent distribution of monogenetic volcanic fields and can be controlled by the regional fracture zones, which could subsequently form fissure-aligned volcanic systems [14].

The products of monogenetic volcanism are commonly revealed as scoria cones, cinder cones, tuff cones, tuff rings, lava flows, and pyroclastic materials (formations of ashes and density currents). Those straight-generated and primitive volcanic products can be easily affected by the local environments and climates; in other words, the surface processes (Kereszturi et al. 2011). When the surface processes

*Eruption Scenario Builder Based on the most Recent Fissure-Feed Lava-Producing Eruptions… DOI: http://dx.doi.org/10.5772/intechopen.109908*

influenced the young volcanism, it could vastly change the outlines of the topography and landforms [16]. Also, the pre-existed landforms play an important role in forming subsequent volcanic landforms, such as hydrogeology-controlled lowlands and complexities of country rocks.

Modeling for lava flow emplacement is one of the interests of interpretations of lava eruptions in some ways that are beyond human records. Long lava flow commonly indicates flows extending approximately more than 100 km from their sources [17] (Stephenson et al. 1998). In general, long flows can generate rapid and insulated emplacements. The rapid model can expect lava flows exceeding 100 km from sources [17], with less than 0.5°C/km of chilling stages under the transporting velocity of approximately 2–15 m/s. The insulated models prefer flows outfluxing under low velocities [3, 12, 17], for example, 0.1–1.4 m/s. Also, insulated emplacements can be expected the thickness of flows to be no more than 23 m at the maximum, with effusive rates at about 8–7100 m3 /s [3]. Slope datasets are the essence of all the above-mentioned assessments. The flows that were emplaced by rapid aspect should be distinguished by the channel-fed structures, for example, lava channels on the surfaces of ʻaʻā type, and expected as generated from short-lived lava fountaining. On the other hand, the insulated aspect can be expected to produce a range of inflated tube-feeding, and sheet pāhoehoe flows within a long distance from their sources/ vents. Such flows are also marked as an indicator of a long-lived ponding system [3].

Volcanic eruptions commonly reveal themselves as multi-phases and prolonged event during the syn-eruptive stages. Also, building a range of eruption scenarios can allow researchers to have a better view of the complexities of volcanic eruptions and volcanic uncertainties [18]. In general, the eruption scenarios contain four major aspects: eruption locations, types of eruptive phases, duration of a single phase, and occurrence and frequency of hazards. Eruption locations indicate short-lived and small vents with their distributions and a single large composite volcano, which produces long-lived and complex volcanic events. The transitions between different eruptive types show that the diversities of volcanism are the current and future preceding states of volcanoes. Durations of eruptive phases analyze the potential magnitudes of local volcanism and are considered either discrete or prolonged eruptions. Hazards' frequencies and occurrence are considered as the influences of erupted gas, blast styles, pyroclastic density current-triggered syn-eruptive disasters, and post-eruptive lahar events.

In NE China, numerous mafic monogenetic volcanic fields formed through the Cenozoic. Among these fields, there are volcanic fields that had historic volcanic eruptions including lava effusions such as those known from Wudalianchi [19, 20] and the Arxan-Chaihe Volcanic Fields [21]. Two young volcanoes located in the southeast part of the Arxan-Chaihe Volcanic Field (ACVF), that is, Yanshan-the "triple vent" and Gaoshan (eastern side of YS), have been dated under the C14 method, which revealed the ages of those two vents about 1900–1990 cal a BP [21, 22].

The major aim of this research is to focus on providing the best possible eruption model to understand the potential impact of a similar eruption in the future based on the youngest eruptive event in the region that occurred approximately 2000 years ago in ACVF. To constrain this, we employed satellite images that show the surface successions of lava flows as a range of typical indicators of how to build the possible chronicle of the vent onset events and the subsequent ponding processes in the volcanic histories of ACVF. Thus we propose that the youngest eruption in the region took place along fissure-dominated vents. As the ACVF is part of the UNESCO Global Geopark network [23], volcanic hazard needs to be treated seriously and this work

provides valuable geology-based information and lava flow simulation to envision the likely eruption scenario the region may face in a future volcanic eruption.
