Study on the distribution of uranium content in cave stalagmites in china and its influencing factors
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摘要: 石笋铀含量是石笋年代学研究的重要指标，关系到年代学的准度和精度。但石笋的铀含量受什么因素控制，目前认识仍有限。文章旨在探究中国洞穴石笋铀含量的时空分布特征及关键影响因素，为同行筛选合适铀含量的石笋样品提供参考，进而减少石笋资源的浪费。文章收集并分析了国内已发表的114个洞穴石笋样品的数据，通过分析石笋样品的空间分布格局以及铀含量的时间演变特征，探讨了区域地质构造背景、洞穴围岩岩性、石笋矿物相以及石笋发育的水文气候条件等因素对石笋铀含量的影响。分析结果表明：（1）中国已发表的石笋记录，铀含量主要分布在0.5×10−6~10×10−6之间，其中1×10−6~10×10−6高铀含量的石笋主要分布在黔渝鄂湘交界中生代及之前的石灰岩地层中的岩溶洞穴内；（2）当石笋矿物相为方解石时，发育在白云岩中的石笋铀含量比灰岩中的铀含量要高；（3）围岩或地层中含有一定的白云岩是高铀含量的文石石笋易出现的重要因素；（4）石笋铀含量与区域水文气候条件存在显著相关性，且与石笋生长速率成正相关关系，即温暖湿润的气候条件下，石笋铀含量较高，寒冷干旱的气候条件下铀含量较低；（5）特殊地质结构，如含煤、围岩侵入等是造成部分洞穴石笋高铀含量的原因。研究进一步深化了对石笋铀含量变化规律的认识，为今后筛选高铀含量石笋样品提供了理论依据和实践指导。Abstract:
The uranium content of stalagmites is the foundation of stalagmite chronology research. It directly determines whether a stalagmite sample is suitable for paleoclimate research and affects the accuracy and precision of stalagmite dating results. Currently, two uranium-series dating techniques are commonly used for stalagmites: U-Th dating and U-Pb dating. The U-Th method can date samples up to approximately 690,000 years old, while the U-Pb method extends the dating range to the Paleozoic or even earlier geological periods. However, the reliability of both methods is highly dependent on the uranium concentration in the stalagmites. Stalagmite samples with low uranium content often result in large age uncertainties, which can lead to significant misinterpretations of the timing and duration of past abrupt climatic events, thereby compromising the accuracy of paleoclimate reconstructions. Therefore, investigating the factors that influence uranium concentrations in stalagmites is of great significance both theoretically and practically. Such understanding can help identify high-uranium stalagmite samples, enhance dating precision, and ultimately support the establishment of more robust chronological frameworks. Nevertheless, current knowledge of the mechanisms controlling uranium content in stalagmites remains limited. Most existing studies focus on the climatic significance of uranium concentration and initial (234U/238U) ratios in stalagmites. Previous studies have shown that the uranium content in stalagmites is influenced by factors such as soil, surrounding rock, the infiltration path of karst water, and the duration of water-rock interaction; While, systematic large-scale studies that integrate these factors are still lacking. In China, karst landscapes are widely distributed, and stalagmite records have played a vital role in high-resolution paleoclimate studies. However, there are relatively few comprehensive analyses on the temporal and spatial distribution characteristics of uranium content in cave stalagmites, as well as the influencing factors. This study aims to explore the temporal and spatial distribution characteristics of uranium content in cave stalagmites in China and the key influencing factors. The goal is to provide a scientific basis for selecting suitable stalagmite samples with adequate uranium concentrations, thereby minimizing unnecessary use and waste of valuable stalagmite resources. This study collects and analyzes the data from 114 published cave stalagmite samples in China. By examining the spatial distribution and temporal evolution of uranium concentrations, the study explores the roles of regional tectonic background, host rock lithology, mineralogy of the stalagmite, and the hydroclimatic conditions under which the stalagmites formed. The main research objectives are: (1) Clarifying the spatial distribution pattern and temporal variation characteristics of uranium content in Chinese stalagmites; (2) Identifying the primary controlling factors, including geological settings, mineral composition, and environmental parameters; (3) Providing scientific criteria for selecting suitable samples for uranium-series dating, thereby avoiding unnecessary waste of stalagmite resources. The analysis of the research results indicates: (1) The spatial distribution of karst caves in China is regionally distinct. Although they are widely distributed, most caves develop on the second geomorphic step and in tectonically active zones such as the Qinling-Dabie orogenic belt and the monsoon-affected regions east of the Hu Line. The warm and humid climate conditions are conducive to the development of karst caves; (2) Based on published Chinese stalagmite records, uranium concentrations typically range from 0.5×10−6 to 10×10−6. High-uranium stalagmites (1×10−6 to 10×10−6) are mainly found in karst caves developed in Mesozoic or older limestone formations located in the junction regions of Guizhou, Chongqing, Hubei, and Hunan; (3) The lithology of host rocks is a critical factor influencing uranium enrichment. When stalagmites are composed of calcite, those formed in dolomite tend to have higher uranium contents than those formed in limestone. This may be attributed to differences in rock weathering processes, inter-crystalline porosity, and water-rock interaction time; (4) The presence of dolomite within the host rock or geological strata appears to be an important contributor to elevated uranium levels in aragonite stalagmites; (5) Uranium concentrations are significantly correlated with regional hydroclimate conditions. There is a positive relationship between uranium content and stalagmite growth rate: stalagmites formed under warm and humid conditions generally contain higher uranium levels, whereas those formed under cold and arid conditions tend to have lower uranium concentrations; (6) In general geological settings, the primary source of uranium in sedimentary strata is ancient seawater, thus creating a link between uranium content in stalagmites and that in paleo-seawater. However, in certain specialized geological environments,such as coal-bearing formations or areas with magmatic intrusions,localized uranium enrichment in bedrock can lead to abnormally high uranium levels in stalagmites. This study enhances our understanding of the variability and controlling mechanisms of uranium concentration in stalagmites under different lithological, stratigraphic, and climatic conditions. The findings provide both theoretical insights and practical guidelines for selecting high-uranium stalagmite samples, thereby supporting the continued advancement of stalagmite-based paleoclimate reconstructions. -
图 4 北半球夏季太阳辐射[88]（a）,海平面[89]（b），靖远黄土磁化率[90]（c），东亚夏季降水[91]（d），全球古温度[92]（e），湖北三宝洞石笋平均生长速率[83,93]（f）与湖北三宝洞石笋铀含量[3,9,14−26]（g）
Figure 4. Insolation in July at 65°N[88] (a); sea level[89] (b); loess magnetic susceptiblility record from Jingyuan, Gansu[90] (c); East Asian Summer Precipitation[91] (d); Global Paleotemperature[92] (e); average growth rate of stalagmites[83−93] in Sabao Cave, Hubei (f); and uranium content of stalagmites[3,9,14−26] in Sanbao Cave,Hubei (g)
表 1 石笋铀含量及洞穴相关数据（表中数据参考文献见中国知网增强出版附件1）
Table 1. Stalagmite Uranium Content and Cave-Related Data (Data References in Appendix 1)
石笋采样洞穴 经度 纬度 U含量/×10−6 地层 矿物相 岩性 北京苦栗树 115.650 39.683 0.454 元古界 方解石 次纯碳酸岩盐 北京石花洞 115.642 39.985 0.285 奥陶 方解石 白云岩 云南乃古石林区 103.436 24.761 0.033 二叠 方解石 灰岩 云南小白龙洞 103.350 24.200 0.642 三叠 方解石 灰岩–白云岩 云南葫芦洞 101.167 26.533 0.294 元古界 方解石 次纯碳酸盐岩层 云南仙人洞 103.500 25.849 0.188 二叠 方解石 灰岩 云南赤土仙人洞 99.633 27.767 0.663 三叠 方解石 灰岩 云南省司岗里洞 99.549 23.533 0.203 二叠 方解石 灰岩 云南宜良九乡蝙蝠洞 103.053 24.610 4.727 元古界 文石 灰岩–白云岩 云南硝洞 104.933 26.033 2.043 石炭 方解石 灰岩 辽宁暖和洞 124.933 41.317 0.120 石炭 方解石 不纯碳酸盐岩层 辽宁本溪水洞 124.071 41.297 0.182 奥陶 方解石 灰岩 辽宁庙洞 125.300 41.092 0.185 寒武 方解石 灰岩 辽宁王家葳洞 124.383 41.217 0.105 侏罗 方解石 灰岩 山东临沂地下画廊 118.417 35.683 13.397 寒武 方解石 灰岩 山东开元洞 118.034 36.406 0.364 奥陶 方解石 灰岩 山东黄巢洞 118.333 36.617 0.398 奥陶 方解石 灰岩 山东上小峰洞 118.017 36.350 0.374 奥陶 方解石 灰岩 福建玉华洞 117.533 26.767 0.463 侏罗 方解石 灰岩 福建仙云洞 117.266 25.561 18.777 二叠 方解石 灰岩 贵州董哥洞 108.082 25.033 0.621 石炭 方解石 灰岩 贵州三星洞 107.183 27.367 2.231 二叠 方解石 白云岩 贵州石膏洞 107.208 28.200 1.073 寒武 方解石 白云岩 贵州雾露洞 105.089 26.067 2.624 三叠 方解石 灰岩 贵州衙门洞 107.900 25.483 0.074 石炭 方解石 灰岩 贵州黑洞 106.167 27.200 0.652 三叠 方解石 灰岩 贵州竹磂坪洞 104.958 26.017 0.107 石炭 方解石 灰岩 贵州水西洞 106.398 27.061 0.791 三叠 方解石 灰岩 贵州七星洞 107.251 25.983 1.831 石炭 方解石 灰岩 贵州石将军洞 106.065 26.284 14.690 三叠 方解石 白云岩 贵州白骨洞 106.495 26.224 0.140 泥盆 方解石 灰岩 贵州山王洞 107.300 28.233 7.294 奥陶 方解石 白云岩 贵州郑家洞 106.030 26.279 0.430 三叠 文石-方解石 白云岩 贵州道观洞 105.090 26.064 0.044 三叠 方解石 灰岩 贵州夜郎洞 105.736 26.041 0.030 三叠 方解石 灰岩–白云岩 贵州龙泉洞 107.914 25.483 0.205 二叠 方解石 灰岩 贵州飞龙洞 104.882 24.970 0.171 三叠 方解石 灰岩–白云岩 贵州Poya洞 108.967 27.883 0.327 寒武 方解石 白云岩 贵州红岩洞 109.150 28.100 0.139 寒武 方解石 白云岩 贵州织金洞 105.683 26.661 0.018 三叠 方解石 灰岩 江苏宜兴茗岭洞 119.700 31.183 0.052 志留 方解石 灰岩 青藏高原东部黄龙洞 103.817 32.717 0.190 三叠 方解石 灰岩 陕西佛爷洞 109.167 33.567 0.569 奥陶 方解石 灰岩 陕西九仙洞 109.100 33.567 0.379 奥陶 方解石 不纯碳酸盐岩层 陕西大鱼洞 106.321 33.099 16.913 二叠 文石 不纯碳酸盐岩层 陕西祥龙洞 106.328 32.948 0.179 寒武 方解石 次纯碳酸盐岩层 陕西汉中地洞河溶洞 106.540 32.679 1.146 二叠 方解石 次纯碳酸盐岩层 陕西白云洞 113.467 36.633 0.753 奥陶 方解石 灰岩–白云岩 山西龙洞 113.342 38.700 0.808 奥陶 方解石 白云岩 山西龙凤洞 113.550 38.680 0.114 奥陶 方解石 灰岩 山西莲花洞 113.717 38.167 0.218 奥陶 方解石 白云岩 湖北神农架三宝洞 110.433 31.667 0.732 元古界 方解石 白云岩 湖北神农架永兴洞 111.233 31.567 0.627 志留 方解石 灰岩 湖北神农架青天洞 110.367 31.500 1.755 元古界 方解石 次纯碳酸盐岩层 湖北豪猪洞 109.983 30.683 0.144 三叠 方解石 灰岩 湖北落水洞 109.101 29.717 1.431 二叠 方解石 灰岩 湖北大石包洞 105.050 26.083 0.323 二叠 方解石 不纯碳酸盐岩层 湖北牛洞 110.267 31.700 0.793 志留 方解石 灰岩-白云岩 湖北天鹅洞 110.633 31.700 0.230 元古界 方解石 灰岩 湖北犀牛洞 110.420 31.679 1.491 寒武 方解石 灰岩 湖北黑龙洞 110.433 31.667 7.985 元古界 方解石 白云岩 湖北林渚洞 110.317 31.517 0.298 元古界 方解石 次纯碳酸盐岩层 湖北龙腑宫洞 110.775 31.692 5.798 元古界 方解石 灰岩 湖北海落洞 109.983 30.753 2.763 二叠 方解石 灰岩 湖北和尚洞 110.419 30.446 0.650 寒武 方解石 灰岩–白云岩 湖北黄龙洞 110.218 33.134 0.184 元古界 方解石 灰岩 甘肃武都万象洞 105.000 33.283 3.590 石炭 方解石 类型不明的碳酸盐岩层 甘肃乌鸦洞 105.426 33.821 0.458 泥盆 方解石 类型不明的碳酸盐岩层 甘肃黄爷洞 105.117 33.603 0.537 石炭 方解石 灰岩 西藏昌都崩勒溶洞 96.515 31.218 0.126 三叠 方解石 灰岩 西藏天门洞 90.033 30.875 0.385 二叠 方解石 灰岩 西藏香格里拉市石卡雪山高原 99.594 27.803 0.382 石炭 方解石 灰岩 重庆新崖洞 109.467 30.750 0.126 三叠 方解石 灰岩 重庆水鸣洞 107.833 29.750 1.118 三叠 方解石 灰岩 重庆羊子洞 107.375 29.267 0.186 三叠 方解石 灰岩 重庆羊口洞 107.183 29.033 7.405 二叠 方解石 白云岩 重庆芙蓉洞 107.900 29.217 2.236 寒武 文石 灰岩 重庆金佛洞 107.183 29.033 19.110 二叠 方解石 白云岩 重庆粱天湾洞 107.033 28.833 12.469 二叠 方解石 灰岩 重庆黑风洞 117.517 26.750 4.407 二叠 方解石 灰岩 重庆天坑洞 108.776 28.735 1.597 奥陶 方解石 灰岩 重庆XSY洞 108.369 29.707 0.130 三叠 方解石 灰岩 河南老母洞 111.567 33.767 0.805 白垩 方解石 灰岩 河南马沟洞 113.383 34.317 0.366 奥陶 方解石 灰岩 河南东石崖洞 111.567 33.783 0.158 元古界 方解石 灰岩 河南伏牛山南坡南阳洞 111.533 33.433 0.915 元古界 方解石 大理岩 四川诺水河溶洞群 107.167 32.425 0.372 二叠 方解石 灰岩 四川仙人洞 107.167 32.422 0.180 二叠 方解石 灰岩 四川神奇洞 103.100 28.933 5.127 三叠 方解石 次纯碳酸盐岩层 四川宋家洞 107.179 32.421 0.327 二叠 方解石 灰岩 四川梭子洞 107.167 32.433 0.260 二叠 方解石 灰岩 湖南水源洞 112.807 25.300 4.829 二叠 文石 灰岩 湖南石马洞 119.036 32.531 0.227 侏罗 方解石 不纯碳酸盐岩层 湖南莲花洞 109.528 29.133 3.832 奥陶 文石-方解石 灰岩 湖南惹迷洞 109.178 28.930 1.462 奥陶 文石 灰岩 湖南金滩湾洞 109.600 29.483 2.873 寒武 方解石 灰岩–白云岩 湖南玲珑洞 111.567 27.483 0.316 泥盆 方解石 灰岩 湖南要坝洞 109.833 28.800 0.195 奥陶 方解石 灰岩–白云岩 新疆科桑洞 81.689 42.744 0.589 志留 方解石 灰岩 新疆巴鲁克洞 84.733 42.433 0.860 泥盆 方解石 灰岩–白云岩 江西神农洞 117.364 28.683 2.356 石炭 文石 灰岩 河北珍珠洞 113.720 38.260 0.168 奥陶 方解石 灰岩 河北兴隆洞 117.450 40.483 0.199 元古界 方解石 白云岩 河北黄金洞 118.658 40.225 1.007 元古界 方解石 白云岩 南京葫芦洞 119.033 32.050 0.268 奥陶 方解石 不纯碳酸盐岩层 南京汤山洞 119.045 32.058 0.150 奥陶 方解石 灰岩 南京猿人洞 119.000 32.003 0.223 奥陶 方解石 次纯碳酸盐岩层 台湾涧飞洞 121.054 22.848 3.033 古近系 方解石 灰岩 桂林丰鱼岩 110.317 24.417 0.035 泥盆 方解石 灰岩 桂林响水洞 110.917 25.244 0.269 泥盆 方解石 灰岩 桂林水南洞 110.312 25.283 0.042 泥盆 方解石 灰岩 桂林九罗岩 109.772 25.127 7.920 泥盆 文石 灰岩–白云岩 广西盘龙洞 110.355 24.961 0.045 泥盆 方解石 灰岩 广东牛鼻洞 112.580 24.252 34.025 石炭 文石 灰岩 
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