云南泸西皮家寨大泉壅水水位变化特征研究

周翠琼; 柴金龙; 张贵; 王宇; 何绕生; 王劲; 李继红

doi:10.11932/karst20240606

云南泸西皮家寨大泉壅水水位变化特征研究

doi: 10.11932/karst20240606

周翠琼^{1, 2, 3,},
柴金龙⁴,
张贵^{1, 2, 3, ,},
王宇^{1, 2, 4},
何绕生^{1, 2, 3},
王劲^{1, 2, 3},
李继红^{1, 2, 3}

1.
自然资源部高原山地地质灾害预报预警与生态保护修复重点实验室, 云南昆明 650216
2.
云南省高原山地地质灾害预报预警与生态保护修复重点实验室(筹), 云南昆明 650216
3.
云南省地质环境监测院, 云南昆明 650216
4.
云南省地质调查局, 云南昆明 650051

基金项目: 国家重点研发计划专项( 2016YFC0502502 )

详细信息

作者简介:
周翠琼（1972－），女，高级工程师，主要从事水工环地质调查研究工作。E-mail：407528806@qq.com

通讯作者:
张贵（1964－），男，正高级工程师，主要从事水工环地质调查研究工作。E-mail：ynsghszg@163.com。

中图分类号: P641.73
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出版历程
- 收稿日期: 2024-02-10
- 网络出版日期: 2025-03-21
- 刊出日期: 2024-12-25

Study on the variation characteristics of backwater levels of the Pijiazhai karst spring in Luxi county, Yunnan

ZHOU Cuiqiong^{1, 2, 3
,},
CHAI Jinlong⁴,
ZHANG Gui^{1, 2, 3
, ,},
WANG Yu^{1, 2, 4},
HE Raosheng^{1, 2, 3},
WANG Jin^{1, 2, 3},
LI Jihong^{1, 2, 3}

1.
Key Laboratory of Geohazard Forecast and Geoecological Restoration in Plateau Mountainous Area, MNR, Kunming, Yunnan 650216, China
2.
Yunnan Key Laboratory of Geohazard Forecast and Geoecological Restoration in Plateau Mountainous Area, Kunming, Yunnan 650216, China
3.
Yunnan Institute of Geo-Environment Monitoring, Kunming, Yunnan 650216, China
4.
Yunnan Geological Survey, Kunming, Yunnan 650051, China

摘要

摘要: 皮家寨岩溶大泉位于泸西盆地上游盆地底部边缘，泉流量1 072~1 957 L·s⁻¹，动态较稳定。采用钻探、物探、壅水试验等方法对皮家寨大泉水位开展研究，结果表明：泸西盆地边缘的皮家寨大泉具一定的承压性；泉口壅水时周边水位升幅、响应时间与距离无直接关系，而受岩溶发育及连通程度控制，各向异性明显；泉口上游含水介质结构以溶隙−管道结构为主，壅水时水位升幅较大、响应较快，初期会形成2~3 h的地下水“涌浪”现象，多表现为初期水位快速上升而达到最大值，随后出现短时下降，之后再逐渐上升达到稳定值的“双峰型”；泉口下游含水介质结构以溶隙网络结构为主，壅水时水位升幅一般较小，响应较慢，多表现为较均匀上升的“直线型”。泉口壅水高度控制在一定范围内时，不会引起流量明显减小。工程实践结果，泉口水头抬升4.4 m时流量未减小。
- 岩溶水 /
- 大泉 /
- 壅水 /
- 水位动态分析 /
- 云南泸西
Abstract: The Pijiazhai karst spring is located at the edge of the upstream Luxi basin, where the terrain shifts from steep to gentle slopes. The spring's recharge area covers 115 km², where the recharge runoff area is the white water karst trough valley in the upper reaches of the basin and the peak-cluster depression area at the edge of the basin. There are more springs in the white water karst trough valley but the dynamic is unstable. The main aquifer formations in the spring are dolomite and limestone of the Triassic Gejiu Formation. Although karst development is strong, it is uneven, leading to significant variability in hydraulic properties. Besides precipitation recharge, leakage from the Baishuitang reservoir is a crucial source of recharge. The hydraulic gradient, from the Baishuitang reservoir to the spring outlet, ranges from 1.43% to 1.62%, with groundwater flow velocities between 144.82 and 176.45 m·h⁻¹. The spring discharge varies from 1,072 to 1,957 L·s⁻¹ and remains relatively stable. By means of drilling, geophysical exploration and backwater test, the water levels of the Pijiazhai karst spring are studied. A total of 16 boreholes were drilled near the spring outlet, with depths ranging from 15.1 to 45.1 meters, and the maximum rise in backwater level reached 0.66 meter.Results indicate that, despite the intense karst development near the Pijiazhai karst spring, the distribution of this development is spatially uneven. Horizontally, the analysis of joint fissures reveals four major karst development zones composed of densely distributed caves and solution fissures. Additionally, at varying depths, these dense zones of caves and solution fissures are also present vertically. To the north of the spring outlet, karst development is intense but uneven, predominantly featuring solution fissures and caves, with some caves diameters reaching 4.7 meters. Downstream of the spring, karst development is relatively weaker and more uniform, primarily consisting of solution fissures, with fewer and smaller caves, the largest being 0.6 meters in diameter. At the eastern side of the spring outlet, a significant karst development zone is dominated by solution fissures, which generally exceed 70 meters in thickness, and are widely distributed. Overall, at the area near the spring outlet, a complex and interconnected network of fissures and conduits have been developed. The Pijiazhai karst spring exhibits a certain degree of pressure resistance. Prior to the backwater at the spring outlet, the water levels in 15 nearby observation boreholes, with the exception of the upstream Borehole zk1, are consistently 0.3 to 3.0 meters lower than the water levels at the spring outlet. After backwater, the water levels at the spring outlet remains elevated compared to the levels in the other observation boreholes. The increase in water levels around the spring outlet during the backwater process, as well as the response time and distance, do not exhibit a direct relationship; rather, they are influenced by the development and connectivity of the karst system, demonstrating significant anisotropy. Notably, the spring outlet experiences the most substantial rise in water levels, while the northern upstream area shows a relatively larger increase. In contrast, the southern downstream area exhibits a rapid decline in the amplitude of the rise, and the eastern region experiences a smaller and slower increase. Upstream of the spring outlet, the aquifer structure is mainly characterized by fissure-conduit systems, which show substantial and rapid water level rises during backwater. This often results in a 2–3 hours of groundwater "surge" phenomenon, initially marked by a rapid rise to a peak, and then a brief decline, followed by a gradual rise to a stable level, forming a "double-peak" pattern. Downstream, the aquifer structure is primarily a fissure network, leading to smaller and slower rises of water levels during backwater, typically showing a more uniform "linear" rise, with occasional short-term anomalies of water level decrease before rising. When the backwater height at the spring outlet maintains within a specific range, short-term fluctuations in groundwater levels may cause the spring water to become turbid; however, this does not result in a significant decrease in discharge. Engineering practice confirms that a rise of 4.4 meters in spring head does not lead to a noticeable reduction in discharge.
- karst water /
- karst spring /
- backwater /
- dynamic analysis of water level /
- Luxi county of Yunnan

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图 1 皮家寨大泉水文地质图

1.个旧组d段白云岩 2.个旧组a段、c段灰岩 3.个旧组b段砂泥岩 4.飞仙关组砂泥岩 5.第四系松散岩 6.地层产状 7.断层、推测断层 8.上升、下降泉，右为流量（L·s⁻¹） 9.消水、涌水洞，右为流量（L·s⁻¹） 10.落水洞 11.地下水流向 12.推测岩溶管道 13.系统边界 14.水库、季节性水体

Figure 1. Hydrogeologic map of the Pijiazhai karst spring

1. dolomite at Section D of the Gejiu Formation 2. limestone at sections A and C of the Gejiu Formation 3. sand shale at Section B of the Gejiu Formation 4. sand shale of the Feixianguan Formation 5. loose sedimentary rocks of the Quaternary System; 6. attitude of stratum 7. fault and supposed fault 8. upwelling and downwelling springs, and flow rate (L·s⁻¹) on the right 9. sinkhole and water gushing hole, and flow rate (L·s⁻¹) on the right 10. ponor 11. direction of groundwater flow 12. supposed karst conduit 13. system boundary 14. reservoir and seasonal water body

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图 2 皮家寨大泉钻孔水位等水位线图

1.皮家寨大泉及流量（L·s⁻¹） 2.等水头线标高（m） 3.水头升幅等值线（m） 4.地下水流向 5.岩溶强发育带 6.观测钻孔，上为编号，下为孔深（m） 7.个旧组灰岩与第四系分界线

Figure 2. Contour map of water levels of boreholes of the Pijiazhai karst spring

1. the Pijiazhai karst spring and its flow (L·s⁻¹) 2. elevation of iso-head line (m) 3. contour of head increase (m) 4. direction of groundwater flow 5. zone with strong karst development 6. observation borehole (The number is on the top, and the hole depth is at the bottom.) (m) 7. boundary line between the limestone of the Gejiu Formation and the Quaternary System

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图 3 皮家寨大泉出口段水位变化概化图

1.填土 2.黏土 3.灰岩 4.溶隙 5.溶隙密集带或小溶洞 6.溶洞管道流 7.裂隙流 8.承压水位线 9.地下水流速（长短表示相对大小）10.涡流

Figure 3. Schematic diagram of variations in water levels at the outlet of the Pijiazhai karst spring

1. earth fill; 2. clay 3. limestone 4. solution fissure 5. zone with intensive solution fissures or small karst cave 6. flow of cave conduits 7. fissure flow 8. level of the hydraulic pressure 9. flow rate of groundwater (indicated by the length of line) 10. vortex

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图 4 观测点水位响应过程曲线图

Figure 4. Curve of response to water level in observation points

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