Distribution of Global Paleowildfire Events and Controlling Factors from Late Triassic to Early Jurassic Based on Geological Big Data
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摘要: 陆地野火是全球生态系统演化的重要驱动因素之一，研究关键地质历史时期的古野火事件及其控制机制，有助于深入揭示古气候、古环境演变与古野火活动之间的内在联系.基于木炭、惰质组和热解多环芳烃共计268条野火记录，系统分析了晚三叠世至早侏罗世（237~174.7 Ma）全球古野火空间分布及背后的控制因素.研究发现，晚三叠世卡尼期至诺利期‒瑞替期边界古野火集中分布于北半球中低纬度热带、暖温带区域，仅卡尼期古野火在南半球暖温带少量分布；瑞替期至瑞替期‒赫塘期边界（T-J边界），古野火在北半球中纬度多气候带呈均匀分布；早侏罗世野火则集中分布于北半球中纬度暖温带与北热带区域.晚三叠世至早侏罗世全球古野火事件的时空分布，受pCO2、pO2、植被和大型地质事件的共同影响.晚三叠世初期Wrangellia大火成岩省（LIP）活动促进大气pCO2快速升高，叠加植被繁盛与高大气氧含量（pO2），共同促使卡尼期野火高频发生；早诺利期pCO2达峰值后持续下降，伴随pO2降低共同抑制了诺利期野火活动；后续Angayucham LIP与中大西洋大火成岩省（CAMP）火山活动依次促进pCO2跨T-J边界长时间持续回升，该阶段植被群落结构趋于稳定，促使诺利期‒瑞替期边界、瑞替期、瑞替期‒赫塘期边界及赫塘期野火频率呈升高趋势.全球多个T-J典型剖面碳同位素负偏移对主要受CAMP驱动的瑞替期‒赫塘期边界的高频野火事件发生响应；辛涅缪尔期受pO2持续下降与气候转冷影响，野火频率骤降；早侏罗世中晚期pCO2整体处于低位，仅托尔期pO2回升使得野火数量略高于普林斯巴奇期，但野火频率则无明显变化.Abstract: Terrestrial wildfires are among the important driving forces in the evolution of global ecosystems. Studying paleowildfire events and their control mechanisms during key periods in geological history helps reveal the intrinsic connections between climatic and environmental evolution and wildfire activity. A total of 268 paleowildfire records reported worldwide, including records of charcoal, inertinite, and pyrogenic polycyclic aromatic hydrocarbons, were analyzed for the interval from Late Triassic to Early Jurassic (237-174.7 Ma). The study reveals that the spatial distribution of paleowildfires from the Carnian of the Late Triassic to the Norian-Rhaetian boundary was concentrated in tropical and warm-temperate zones at low to mid-latitudes in the Northern Hemisphere, with only a small number of Carnian paleowildfires distributed in the warm-temperate zone of the Southern Hemisphere. From the Rhaetian to the Rhaetian-Hettangian boundary (the Triassic-Jurassic/T-J boundary), paleowildfires were uniformly distributed across multiple climatic belts at mid-latitudes in the Northern Hemisphere. Wildfires in the Early Jurassic were concentrated in the warm-temperate and northern tropical zones at mid-latitudes in the Northern Hemisphere. Global paleowildfire activity from the Late Triassic to the Early Jurassic was controlled by combined effects of pCO2 (10-6; atmospheric CO2 concentration) and pO2 (vol%; atmospheric O2 volume fraction), vegetation change, and major geological events. The volcanic activity of the Wrangellia Large Igneous Province (LIP) in the Early Late Triassic promoted a rapid rise in pCO2. This rise, together with flourishing vegetation and high pO2, collectively drove the high frequency of wildfires during the Carnian. After pCO2 peaked in the Early Norian, it continued to decline, and this decline, together with the decrease in pO2, suppressed wildfire activity during the Norian. Subsequently, volcanic activity associated with the Angayucham LIP and the Central Atlantic Magmatic Province (CAMP) sequentially promoted the long-term recovery in pCO2 across Triassic-Jurassic (T-J) boundary. During this period, the structure of vegetation communities remained relatively stable, which contributed to an increase in wildfire frequency at the Norian-Rhaetian boundary, during the Rhaetian, at the Rhaetian-Hettangian boundary, and during the Hettangian. Negative carbon-isotope excursions recorded in multiple representative T-J boundary sections worldwide are interpreted as responses to the high-frequency wildfire events at the Rhaetian-Hettangian boundary, which were mainly driven by CAMP volcanism. With the continued decline in pO2 and climatic cooling during the Sinemurian, wildfire frequency dropped sharply. In the middle and late stages of the Early Jurassic, pCO2 generally remained at a low level. Only the recovery of pO2 during the Toarcian resulted in a slightly higher number of wildfires than in the Pliensbachian, while wildfire frequency remained almost unchanged.
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图 1 三叠纪‒侏罗纪古野火与古气候相关聚集图谱与发文时间演变图
Fig. 1. Correlation map and temporal trend of publications on Triassic–Jurassic paleowildfire and paleoclimate
图 2 晚三叠世‒早侏罗世不同时期全球古野火事件分布
Fig. 2. Global distribution of Late Triassic–Early Jurassic paleowildfire events through different geological time
图 3 晚三叠世‒早侏罗世全球古野火事件的经纬度分布
Fig. 3. Global distribution of Late Triassic–Early Jurassic paleowildfire events by latitude and longitude
图 4 晚三叠世古野火事件古地理分布
古气候带划分据Boucot et al.（2013）；Wrangellia LIP据Dal Corso et al.（2020）；Angayucham LIP据江海水和陈龑（2025）
Fig. 4. Paleogeographic distribution of Late Triassic paleowildfire events
图 5 晚三叠世‒早侏罗世边界古野火事件与不同区域古地理分布
古气候带划分据Boucot et al.（2013）；CAMP范围据Marzoli et al.（2011，2017）
Fig. 5. Paleowildfire events and paleogeographic distribution across Late Triassic–Early Jurassic boundary
图 6 早侏罗世古野火事件古地理分布
古气候带划分据Boucot et al.（2013）；Karoo-Ferrar LIP据Ivanov et al.（2017）
Fig. 6. Paleogeographic distribution of Early Jurassic paleowildfire events
图 8 晚三叠世‒早侏罗世各个时间段古野火事件记录及相关控制因素模式
大火成岩省喷发体积引自Prokoph et al.（2013）；植物数量引自Cleal and Cascales-Miñana（2014）；pCO2引自Foster et al.（2017）；pO2引自Mills et al.（2023）
Fig. 8. Schematic diagram of paleowildfire event records and associated controlling factors from Late Triassic to Early Jurassic
图 9 全球典型TJB剖面碳同位素负偏移对比（据侯海海等, 2023修改）
Fig. 9. Comparison of negative carbon isotope excursions in globally representative Triassic-Jurassic boundary sections
表 1 本研究中使用的晚三叠世至早侏罗世9个地质历史时间段划分
Table 1. Division of nine geological time intervals from Late Triassic to Early Jurassic
时期 持续时间
（Ma）时间范围
（Ma）托尔期（Toarcian） 9.5 184.2~174.7 普林斯巴奇期（Pliensbachian） 8.7 192.9~184.2 辛涅缪尔期（Sinemurian） 6.6 199.5~192.9 赫塘期（Hettangian） 1.9 201.4~199.5 瑞替期‒赫塘期边界 - 201.4 瑞替期（Rhaetian） 7.1 208.5~201.4 诺利期‒瑞替期边界 - 208.5 诺利期（Norian） 18.5 227~208.5 卡尼期（Carnian） 10.0 237~227 
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