丽江黑龙潭地下河系统的水均衡分析与预测评价

任世川; 杨晓艳; 杨颖彬; 刘海峰; 杨帆

doi:10.11932/karst20230604

丽江黑龙潭地下河系统的水均衡分析与预测评价

doi: 10.11932/karst20230604

任世川^{1, 2, 3,},
杨晓艳^{1, 2, 3},
杨颖彬^{1, 2, 3},
刘海峰^{1, 2, 3},
杨帆^{1, 2, 3}

1.
自然资源部高原山地地质灾害预报预警与生态修复重点实验室, 云南昆明 650216
2.
云南省高原山地地质灾害预报预警与生态修复重点实验室, 云南昆明 650216
3.
云南省地质环境监测院, 云南昆明 650216

详细信息

作者简介:
任世川（1979－），男，工程硕士，正高级工程师，主要从事水工环地质方面的调查研究工作。E-mail：56926747@qq.com

中图分类号: P641.134
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出版历程
- 收稿日期: 2023-01-01
- 网络出版日期: 2023-12-28
- 刊出日期: 2023-12-01

Equilibrium analysis and prediction evaluation of the Heilongtan groundwater system in Lijiang of northwestern Yunnan Province

REN Shichuan^{1, 2, 3
,},
YANG Xiaoyan^{1, 2, 3},
YANG Yingbin^{1, 2, 3},
LIU Haifeng^{1, 2, 3},
YANG Fan^{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

摘要

摘要: 滇西北丽江黑龙潭流量大幅减少、间歇式断流问题日趋频繁，已成为地方经济社会发展的重要制约因素。在对丽江盆地区域水文地质条件和黑龙潭地下水系统动态调查的基础上，考虑社会经济发展过程中人类工程活动的影响，以近70年的数据为基础，采用水均衡法定量分析黑龙潭地下水系统流量的动态变化及其影响因素，得出不同时段黑龙潭断流的主要原因，并根据近年黑龙潭断流的影响因素及变化趋势，预测未来黑龙潭流量的变化趋势，2021—2030年，黑龙潭将成为季节性泉水，2030年之后，黑龙潭泉群将长期处于断流状态。该认识可为黑龙潭的地下水动态恢复和丽江城区地下水水资源开发及环境保护提供依据。
- 地下水系统 /
- 水均衡分析 /
- 黑龙潭断流 /
- 丽江市
Abstract: The karst water system is a dynamic system controlled by the degree of karst development and the underlying geological conditions. It constantly evolves with changes in climate, human activities, and many other factors. As one of the main driving forces of environmental change, human activities have caused the change at the rate and intensity far exceeding that of natural succession in a short period of time. The environmental effects and induced hydrogeological problems resulting from human activities are extremely difficult to distinguish and quantify, and hence have been the working focus of local governments and scholars at home and abroad. The Lijiang basin is a typical covered and semi-covered karst water system developed in the strong uplift zone of the late Cenozoic crust, which has given birth to the Heilongtan spring, the Xiguanlongtan spring, the Jiudinglongtan spring and other karst springs (spring groups). These springs are not only important water sources for Lijiang City, but also the city's highlights of tourism resources. Among them, the Heilongtan groundwater system is the most important karst water subsystem in the groundwater system of the Lijiang basin. However, the primary discharge point of this system, the Heilongtan spring, has currently experienced a significant reduction in flow and increasing intermittent drying up, which have become important factors restricting local economic and social development. Based on the comprehensive analysis of data over the past 70 years, the investigation of hydrogeological conditions in the Lijiang basin area, and the dynamic monitoring of the Heilongtan groundwater system, we quantitatively evaluated the dynamic flow change of and its influencing factors on the Heilongtan groundwater system with the method of water equilibrium. Fully considering the impact of human engineering activities in socioeconomic development, we summarized factors for the drying-up of the Heilongtan groundwater system as follows. (1) From 1951 to 1990, human engineering activities that replaced and reduced regional vegetation increased natural evaporation capacity and continuously increased evaporative discharge by 10,827,400 m³, accounting for 87.00% of the total decrease in the resources of the Heilongtan groundwater system (12,445,400 m³). This is the main reason for the drying-up probability and the increasing span of Heilongtan spring. (2) From 1991 to 2018, with the recovery of vegetation, the evaporative discharge continuously decreased by 18,303,400 m³, compared with that in the 1980s, which was beneficial to the recovery of Heilongtan spring. However, the factors such as human mining, leakage from the surface river system, and urban development and rereconstruction have caused a total decrease of groundwater resources by 50,586,900 m³, which is unfavorable to the recovery of the Heilongtan spring and is also the cause for its drying up. Among these causes, urbanization and human groundwater extraction reduced groundwater resources by 45,805,200 m³, which accounted for 90.54% of the overall decrease and was another primary cause of the drying-up. According to the change of influencing factors of the Heilongtan spring in recent years, the future changes of its flow predicted by the method of water equilibrium shows that: (1) From 2021 to 2030, the Heilongtan spring will change into a seasonal spring and become drying up during median water year and low flow year. (2) After 2030, the Heilongtan spring groups will remain drying up for a considerable amount of time with a very slim chance of reproduction. This study research can serve as a foundation for the dynamic recovery of Heilongtan groundwater, and the development and environmental protection of the groundwater resources in the urban area of Lijiang.
- groundwater system /
- water equilibrium analysis /
- the drying-up of the Heilongtan spring /
- Lijiang City

HTML

图 1 丽江盆地水文地质及地下水系统关系图

Figure 1. Relationship between hydrogeology and groundwater system in the Lijiang basin

下载: 全尺寸图片幻灯片

图 2 黑龙潭历史断流情况变化趋势曲线图

Figure 2. Trend curve of the historical drying-up of the Heilongtan spring

下载: 全尺寸图片幻灯片

图 3 丽江站与九子海站2001年至2017年降水关系曲线图

Figure 3. Precipitation relationship between Lijiang station and Jiuzihai station from 2001 to 2017

下载: 全尺寸图片幻灯片

表 1 丽江盆地社会经济发展和地下水环境变化情况统计表

Table 1. Statistics of socioeconomic development and groundwater environment change in the Lijiang basin

变化因素			1940s	1950s	1960s	1970s	1980s	1990s	2000s	2010s	备注
丽江县（古城区和玉龙县）国民生产总值/亿元			0.3	0.6	0.7	1.2	3.3		42.5	194.2	收集数据极值
丽江城人口/万人							3.90	6.91	14.62	22.70	收集数据极值
城市建成区面积/km²			1.70	2.10			3.22	7.55	30.58	48.90	收集数据极值
公路里程/km			0	15			33		51	335.95
内耕地面积/km²						129.09		89.05		77.44
水利工程蓄水量/万m³			0				3 000		11 483
城市供水规模/万m³			0	0		71.4	80.5		876	3 504	收集数据极值
地下水开采量/万m³			0	37	37	37	37	51.05	589.83	1 412.36
丽江市植被覆盖率/%			47.20			30.40	27.30	43.6	61.10	70.34	收集数据极值
九子海站	年平均降水量/mm		1 289.7	1 199.4	1 256.5	1 218.5	1 215.1	1 319.9	1 274.3	1 108.8
九子海站	极值差/mm		507	229	446	441	518	523	489	777
年平均蒸发量/mm				2 003.6	2 118.1	2 178.5	2 240.3	2 079.8	1 551.6	1 528.4
年平均气温/℃				12.5	12.6	12.6	12.7	12.8	13.3	13.7
年平均日照数/h				2 453.3	2 572.8	2 518.8	2 450.5	2 420.9	2 366.7	2 403.6
玉龙雪山		冰雪面积/km²				155.63	97.40	85.34	113.84	17.97	收集数据极值
玉龙雪山		冰川面积/km²		11.61				8.50	5.30	3.98	收集数据极值

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表 2 1953—2017年黑龙潭地下水系统补给量和排泄量10年平均值变化统计表

Table 2. Statistics of the 10-year average value change of replenishment and discharge of the groundwater in the Heilongtan spring from 1952 to 2017

	年代	20世纪					21世纪		多年平均
	年代	53—60	61—70	71—80	81—90	91—00	01—10	11—17	多年平均
降水入渗补给量 /万m³		8 129.73	8 494.85	8 238.22	8 214.88	8 923.72	8 615.18	6 998.36	8 230.71
黑龙潭泉群	水量 /万m³	4 448.27	4 544.82	4 081.52	3 633.94	4 298.41	3 854.67	239.22	3 585.84
黑龙潭泉群	占补给量 /%	54.72	53.50	49.54	44.24	48.17	44.74	3.42	42.62
侧向排泄量	水量 /万m³	3 412.47	3 668.96	3 884.13	4 309.13	4 330.06	4 475.46	6 533.48	4 373.38
侧向排泄量	占补给量 /%	41.98	43.19	47.15	52.46	48.52	51.95	93.36	54.09
其它排泄	水量 /万m³	268.99	281.07	272.57	271.81	295.25	285.05	225.66	271.49
其它排泄	占补给量 /%	3.31	3.31	3.31	3.31	3.31	3.31	3.22	3.30

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表 3 黑龙潭及丽江城地下水系统的水资源量变化统计表

Table 3. Statistics of the quantity change in groundwater resource of the Heilongtan spring and Lijiang City

年代	变化
年代	变化因素	降水（浮动）	蒸发	灌溉水	人工开采	地表河系渗漏	盆地入渗面积变化	城市化其它影响	合计
1951—1990	变化量/万m³	599	−1 082.74	−50.05	−37.00	0	−74.75	0	−1 244.54
1951—1990	等价降水量/mm	599	−160	−7.5	−5.5	0	−11	0	−184
1991—2018	变化量/万m³	777	+1 830.34	−243.63	−1 300.70	−234.54	−279.82	−3 000.00	−3 228.35
1991—2018	等价降水量/mm	777	+270	−36	−187	−36	−41	−459	−489

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表 4 不同年份黑龙潭地下水系统排泄量变化一览表

Table 4. Discharge changes of the Heilongtan groundwater system in different years

时间节点/年份	水位/m (井口为0 m)	降水量/mm·a⁻¹	入渗补给量/万m³·a⁻¹	黑龙潭排泄量/万m³·a⁻¹	其它泉水排泄量/万m³·a⁻¹	侧向排泄量/万m³·a⁻¹	断流次数 /次
1989—1992	无	1 318.4	8 913.21	5 179.79	294.91	3 438.51	0
1993—1997	−1.04~−0.94	1 237.9	8 369.37	2 657.01	276.92	5 435.44	2
2006—2010	−1.75~−1.57	1 300.3	8 790.89	2 061.14	290.86	6 438.89	4

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