不同地质背景下北方岩溶作用强度研究

刘文; 徐聪聪; 于令芹; 李海翔; 卢茜茜; 朱钦锋; 柳浩然

doi:10.11932/karst20230502

不同地质背景下北方岩溶作用强度研究

doi: 10.11932/karst20230502

刘文^{1, 2, 3,},
徐聪聪^{1, 2, 3},
于令芹^{1, 2, 3},
李海翔^{1, 2, 3},
卢茜茜^{1, 2, 3},
朱钦锋^{1, 2, 3},
柳浩然^{1, 2, 3, ,}

1.
山东省地质矿产勘查开发局八〇一水文地质工程地质大队(山东省地矿工程勘察院) , 山东济南 250014
2.
山东省地下水环境保护与修复工程技术研究中心, 山东济南 250014
3.
山东省地质矿产勘查开发局地下水资源与环境重点实验室, 山东济南 250014

基金项目: 山东省地矿局八〇一队科技创新项目：鲁中南岩溶区 “碳中和”潜力调查及关键技术研究(2022JBGS801-13)；国家自然科学基金面上项目：多级次地下水流系统对北方岩溶大泉动态的影响机制42272288)；山东省地矿局地质勘查与科技创新项目：北方岩溶关键带监测基地建设项目(HJ202110)

详细信息

作者简介:
刘文(1985－)，男，博士，高级工程师，主要从事岩溶地质相关调查研究工作。E-mail：liuwen37801@163.com

通讯作者:
柳浩然（1986－），男，硕士，工程师，从事地下水环境监测研究。E-mail：lhr801@126.com

中图分类号: P642.25
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出版历程
- 收稿日期: 2023-04-17
- 录用日期: 2023-08-21
- 修回日期: 2023-08-18
- 网络出版日期: 2023-10-20
- 刊出日期: 2023-10-01

Study on the intensity of boreal karstification under different geological conditions: A case study at the recharge area of Baotu Spring drainage area, Jinan, Northern China

LIU Wen^{1, 2, 3
,},
XU Congcong^{1, 2, 3},
YU Lingqin^{1, 2, 3},
LI Haixiang^{1, 2, 3},
LU Qianqian^{1, 2, 3},
ZHU Qinfeng^{1, 2, 3},
LIU Haoran^{1, 2, 3
, ,}

1.
801 Institute of Hydrogeology and Engineering Geology, Shandong Provincial Bureau of Geology & Mineral Resources (Shandong Provincial Geo-mineral Engineering Exploration Institute), Jinan, Shandong 250014, China
2.
Shandong Engineering Research Center for Environmental Protection and Remediation on Groundwater, Jinan, Shandong 250014, China
3.
Key Laboratory of Groundwater Resources and Environment, Shandong Provincial Bureau of Geology & Mineral Resources, Jinan, Shandong 250014, China

摘要

摘要: 岩溶作用过程可形成碳汇是不争的事实，为进一步探索不同地质背景对岩溶作用的影响机制，选取典型北方岩溶泉域−济南趵突泉泉域补给区为研究区，采用标准溶蚀试片法进行野外现场试验。结果表明，下伏岩性为花岗岩、碳酸盐岩、黄土、页岩的各试点平均溶蚀速率分别为：3.49、0.26、0.11、0.09 mg·cm⁻²·a⁻¹；碳酸盐岩、黄土、页岩分布区溶蚀速率大气 > 地表 > 壤中，且壤中部分呈随深度增加而降低的趋势，而在花岗岩分布区则呈完全相反。分析发现，土壤水与溶蚀速率相关性远高于CO₂，是北方岩溶区岩溶作用进行的限制因子。本研究结果有助于认识半湿润气候条件下岩溶碳汇机制，为北方其他岩溶区乃至整个同类型岩溶区相关研究的开展积累了经验。
- 标准溶蚀试片法 /
- 岩性 /
- 岩溶作用 /
- 北方岩溶 /
- 济南趵突泉泉域
Abstract: It is an indisputable fact that the process of karstification can form carbon sink, and the research on this process is in the ascendant. However, the factors affecting karstification process are very complicated, and the geological background is one of the most important aspects. The effect mechanism of different geological backgrounds on karstification and the data of dissolution rate under different geological backgrounds can provide a basis for understanding the karst process and its mechanism under sub-humid climate and improving the estimation accuracy of karst carbon sink. The recharge area of Baotu Spring area in Jinan, a typical boreal karst spring area, is selected as the research area, and the standard dissolution tablet test of carbonate rock is used for field measurement.At the northern edge of the mountainous region in central Shandong, the research area is located in the Baotu Spring area of Jinan, bordering Mount Tai in the south and the Yellow River in the north (116°40'30"-117°14'10"E; 36°14'50"-36°46'10"N). The spring area borders the Mashan fault and Dongwu fault to the west and east, respectively. These two faults are permeable in the north and weakly permeable in the south. The southern boundary is the ridgeline of Mount Tai, and the igneous body in the north is called "Jinan Rock". Constrained by the special topography and geological structure, precipitation infiltration in the southern mountainous area recharges the Cambrian-Ordovician karst aquifer which presents strong karst development, and then moves from south to north. According to the statistics of Jinan Meteorological Bureau, Jinan City is characterized by a warm temperate continental climate with four distinct seasons at an annual average temperature of 14.7 ℃. Its average precipitation per year is 647.9 mm, more than 70% of which is concentrated in July, August and September with less from December to March. During the four-year test, pH values of precipitation in Jinan (Guishan) National Basic Meteorological Station averaged between 6.96 and 7.61, which means there was no acid rain in this period.The standard dissolution tablet method is widely used in the study of karstification process because of its advantages such as short-term monitoring, simple preparation of sampling, mature embedding method and the condition closer to the natural state than that in a laboratory. The study area is located in the low mountainous but hilly area of the north wing of Mount Tai and the southern Jinan far away from the urban area, which is also the recharge area of Baotu Spring area. The area is forest and shrub land with less interference from human activities. We buried standard dissolution carbonate tablets around the end of November 2017, and retrieved them around the end of November 2021, with a total test period of four years. When burying these tablets, we selected test sites with different basement lithology in the same small watershed where the meteorological conditions are not significantly different, to ensure the relative consistency of test backgrounds such as precipitation and temperature. Meanwhile, we collected layered soil samples for testing physical and chemical indexes, atmospheric and soil CO₂, soil water content, etc. Results show that the average dissolution rates of granite, carbonate, loess and shale are 3.49 mg·cm⁻²·a⁻¹, 0.26 mg·cm⁻²·a⁻¹, 0.11 mg·cm⁻²·a⁻¹ and 0.09 mg·cm⁻²·a⁻¹, respectively. In other words, the influence of basement lithology on dissolution rate is significant. The dissolution rate of granite area is much larger than that of the other ones. The dissolution rate of carbonate area is larger than that of loess and shale, and the lowest in shale area. From a vertical profile perspective, the dissolution rate of carbonate rock area, loess area and shale area is atmospheric>surface>soil, and the rate in soil decreases with the increase of depth, while the dissolution rate in granite area shows a completely opposite trend.It is found that there is no obvious correlation between soil CO₂ and dissolution rate. The variation trend of soil organic matter content in the profiles of carbonate rock, loess and shale is consistent with that of dissolution rate, indicating that the former may have a direct effect on the latter, but the consistency does not show in the granite area. There is an exponential correlation between soil pH and dissolution rate at all sites, and the dissolution rate decreased significantly with the increase of pH. Soil water content has an obvious linear relationship with the dissolution rate, and is the limiting factor of karstification process in boreal karst area compared with soil CO₂.This study is a useful exploration in the boreal karst area, the results of which help to deepen the understanding of the karstification process under the semi-humid and semi-arid climate conditions, and provide a comparative example for other karst areas in the north and even the whole karst area of the same type.
- standard dissolution tablet method /
- lithology /
- karstification /
- boreal karst /
- Baotu Spring area in Jinan

HTML

图 1 考虑水−岩−气−生相互作用的碳酸盐风化碳汇模式图^{[17- 18]}

Figure 1. Conceptual model for carbonate weathering related carbon sink

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图 2 研究区地理位置及水文地质略图

Figure 2. Overview map of geographical location and hydrogeology of the study area

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图 3 试片埋设深度与溶蚀速率的关系

Figure 3. Relationship between the burial depth of test tablet and its dissolution rate

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图 4 碳酸盐岩分布区土壤水分含量与溶蚀速率的关系

Figure 4. Relationship between water content of soil and dissolution rate in the carbonate rock area

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图 5 碳酸盐岩分布区土壤CO₂与溶蚀速率的关系

Figure 5. Relationship between CO₂ content of soil and dissolution rate in the carbonate rock area

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图 6 土壤有机质含量/×10⁻³

Figure 6. Organic matter content of soil/×10⁻³

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图 7 土壤无机碳含量

Figure 7. Inorganic carbon content of soil

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图 8 pH与溶蚀速率的关系

Figure 8. Relationship between pH and dissolution rate

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表 1 标准溶蚀试验点位概况

Table 1. Overview of the test sites of standard dissolution

编号	埋放日期	取回日期	埋放天数	土地利用类型	优势植被	伴生植被	基底岩性	地貌部位	坡向/视坡度
LB01	2017年11月25日	2021年11月26日	1 462	林地	槐树	构树、灌丛	碳酸盐岩	山坡	135°/20°
LB02	2017年11月28日	2021年11月25日	1 458	林地	柏树	黄荆	花岗岩	山坡	95°/10°
LB03	2017年11月28日	2021年11月26日	1 459	林地	槐树	杂草	花岗岩	近山顶山坡	90°/60°
LY01	2017年11月15日	2021年12月8日	1 484	林地、灌丛	杨树	黄荆、杂草	页岩	山坡	0°/3°
LY02	2017年11月16日	2021年12月6日	1 481	林地	柏树	黄荆、杂草	页岩	山坡	345°/30°
LY03	2017年11月16日	2021年12月7日	1 482	林地	柏树	黄荆、杂草	花岗岩	山坡	270°/8°
LY04	2017年11月17日	2021年12月3日	1 477	林地	柏树	黄荆	碳酸盐岩	近山顶山坡	315°/45°
XY01	2017年11月21日	2021年12月2日	1 472	园地	核桃树	山楂	黄土	山谷河漫滩	180°/1°
XY02	2017年11月23日	2021年12月1日	1 469	园地	苹果树	杂草	页岩	山谷尾端	0°/3°
XY03	2017年11月23日	2021年12月1日	1 469	园地	苹果树	杂草	页岩	山谷尾端	0°/3°
XY04	2017年11月24日	2021年12月1日	1 468	林地	柏树	黄荆	碳酸盐岩	山坡	90°/45°
XY05	2017年11月24日	2021年12月2日	1 469	未利用地	灌草丛		碳酸盐岩	山坡	225°/30°
ZG01	2017年11月25日	2021年11月28日	1 464	林地	柏树		碳酸盐岩	山坡	180°/15°
ZG02	2017年11月29日	2021年11月29日	1 461	林地	柏树	杂草	碳酸盐岩	山坡	190°/10°

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表 2 按基底岩性分层溶蚀速率表/mg·cm⁻²·a⁻¹

Table 2. Layered dissolution rate of different basement lithology/mg·cm⁻²·a⁻¹

层位	碳酸盐岩	页岩	花岗岩	黄土
大气	0.791 7	0.832 5	0.829 0	0.761 9
表层	0.473 5	0.222 4	1.294 8	0.328 6
中间层		0.047 2	2.672 4	0.040 6
底层	0.051 1	0.018 4	6.504 1	0.011 6
壤中平均	0.262 3	0.093 8	3.490 4	0.105 4

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表 3 平均溶蚀速率、土壤CO₂含量及含水率

Table 3. Average dissolution rate, CO₂ and water content in soil

点位	平均溶蚀速率/ mg·cm⁻²·a⁻¹	平均CO₂含量/ ×10⁻⁶	含水率/ %
LB02	5.708 6	2 733.33	16.17
LB03	1.556 2	2 750.00	9.08
LY03	3.206 5	2 783.33	17.22
LY01	0.073 5	1 760.00	22.52
LY02	0.046 8	4 514.29	29.22
XY02	0.065 7	2 100.00	37.12
XY03	0.189 0	5 200.00	33.70
LY04	0.194 4	1 991.67	17.47
XY04	0.448 5	4 587.50	21.60
XY05	0.461 7	3 016.67	23.77
ZG01	0.233 9	3 333.33	22.63
ZG02	0.056 5	4 016.67	15.86
LB01	0.178 8	4 225.00	11.85
XY01	0.105 4	1 960.00	35.81
注：含水率基于试片埋设和取回时测量的结果进行平均。 Note: Water content is averaged based on the results measured when the test tablet is buried and retrieved

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表 4 不同深度土壤CO₂含量/×10⁻⁶

Table 4. CO₂ content of soil in different depths/×10⁻⁶

点位	测试层位/cm
点位	0	10	20	30	40	50	60	80	壤中平均
LB02	389		2 000	3 200	3 000				2 733.33
LB03	378			2 500		3 000			2 750
LY03	388	2 400		3 300		2 650			2 783
LY01	385	1 100	1 400		2 100		2 200	2 000	1 760
LY02	385	3 800	3 000	6 800		4 700		5 000	4 660
XY02	378	2 200	1 800		2 300				2 100
XY03	378	5 200		5 400	5 000				5 200
LB01	385	2 900	5 200	4 000	4 800				4 225
LY04	381	1 600	2 100	2 800	2 000				2 125
XY04	381	2 550	4 600	4 600		6 600			4 588
XY05	381	3 800	3 300	1 950					3 017
ZG01	388	3 800		4 400	1 800				3 333
ZG02	375	3 600	4 760	3 920	5 200				4 370
XY01	378	2 450	2 200		2 000		1 650	1 500	1 960
平均值	382	2 950	3 036	3 897	3 133	4 238	1 925	2 833	3 257

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