山东省沂源县螳螂河流域水体氢氧同位素对蒸发效应的指示作用

朱晓燕; 张卓; 黄芬

doi:10.11932/karst20260303

山东省沂源县螳螂河流域水体氢氧同位素对蒸发效应的指示作用

doi: 10.11932/karst20260303

1.
中国地质科学院岩溶地质研究所/自然资源部、广西壮族自治区岩溶动力学重点实验室, 广西桂林 541004
2.
山东省地质调查院, 山东济南 250014

基金项目: 山东省岩溶碳汇调查评价与监测试点项目（鲁勘字[2024]21号）；自然资源部/广西岩溶动力学重点实验室运行（2023009）

详细信息

作者简介:
朱晓燕（1980－），女，硕士，副研究员，主要研究方向为岩溶地质、岩溶碳循环。E-mail：zhuxiaoyan2001@sina.com

中图分类号: P426
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出版历程
- 收稿日期: 2025-11-21
- 录用日期: 2026-04-23
- 修回日期: 2026-04-22
- 刊出日期: 2026-06-25

Indication of evaporation effects by hydrogen and oxygen isotopes in the water bodies of the Tanglanghe River Basin, Yiyuan county, Shandong Province

1.
Institute of Karst Geology, CAGS/Key Laboratory of Karst Dynamics, MNR＆GZAR, Guilin, Guangxi 541004,China
2.
Shandong Institute of Geological Survey, Jinan, Shandong 250014, China

摘要

摘要: 以山东省沂源县螳螂河流域为研究区，基于2024年8月丰水期、2025年4月枯水期地下水与地表水的δD、δ¹⁸O数据，分析水体同位素组成特征，探讨δ¹⁸O与氘盈余（d-excess）对流域蒸发过程的指示意义。结果表明：（1）丰水期各水体δD-δ¹⁸O趋势线接近于全球大气降水线（GMWL），斜率和截距均高于当地大气降水线（LMWL），大气降水为流域主要补给源，螳螂河属雨源型河流；枯水期各水体同位素普遍偏重，蒸发效应显著。（2）地下水δD、δ¹⁸O分布范围窄且季节变化不明显，反映其补径排过程调蓄与时空均化作用强，水文动态稳定；地表水同位素季节差异显著，丰水期偏负而枯水期偏正，按数值均值排序为丰水期：地下水>河流>水库，枯水期：河流>水库>地下水，表明直接受大气降水补给，丰水期径流迅速且滞留时间短，季节信号未被充分混合均化，枯水期水库蒸发强烈。（3）δ¹⁸O与水温呈显著负相关，且相关性优于d-excess。（4）2025年枯水期螳螂河干流蒸发比例为4.62%~19.40%，自上游至下游递增，受地下水补给与河面变化影响。
- 螳螂河 /
- δD /
- δ¹⁸O /
- 蒸发 /
- 水文过程 /
- 流域
Abstract: This study takes the Tanglanghe River Basin in Yiyuan county, Shandong Province as the study area. To investigate the influence of evaporation on the regional water cycle, the stable isotopic compositions of groundwater and surface water samples collected along the Tanglanghe River were systematically measured in August 2024 and April 2025. The analytical results reveal distinct seasonal variations and spatial patterns in the isotopic signatures, highlighting the indicative significance of δ¹⁸O and deuterium excess (d-excess) for evaporation processes in the basin. The major findings are summarized as follows.(1) During the wet period in August 2024, which coincides with the peak of the East Asian Summer Monsoon rainfall, the δD-δ¹⁸O trend line for all water bodies in the basin lies to the Global Meteoric Water Line (GMWL). Notably, both the slope and intercept of the local water line derived from this period are higher than those of the previously established Local Meteoric Water Line (LMWL). This statistical relationship strongly indicates that atmospheric precipitation is the predominant and direct source of recharge for the basin's hydrological system. Therefore, the Tanglanghe River can be definitively classified as a rain-fed fluvial system, with its flow regime primarily dictated by the timing and magnitude of precipitation events within its catchment area. In stark contrast, during the dry period of April 2025, the isotopic compositions of all sampled water bodies exhibited a pronounced enrichment in the heavier isotopes (δ¹⁸O and δD). This systematic shift toward heavier isotopic values directly reflects the dominance of intense evaporation under arid conditions.(2) Building on this temporal contrast, a marked distinction also exists between the isotopic behavior of groundwater and surface water within the Tanglanghe River Basin. Groundwater samples exhibit a notably narrow range of variation in both δD and δ¹⁸O values, and these values demonstrate minimal seasonal fluctuation in samples between the wet and dry periods. This temporal and spatial homogeneity reflects the profound regulatory capacity, storage effect, and mixing homogenization inherent to subsurface flow systems. Conversely, surface water display pronounced seasonal isotopic variability. During the wet period, surface water isotopes are relatively depleted (more negative δ-values), whereas during the dry period, they are significantly enriched (more positive δ-values). Specifically, the isotopic enrichment ranking during the wet period is groundwater > river water > reservoir water (from less negative to more negative), whereas this order reverses dramatically in the dry period to river water > reservoir water > groundwater. This pattern indicates that the water is directly recharged by atmospheric precipitation. During the wet period, runoff is rapid and residence time is short, resulting in inadequate mixing and homogenization of seasonal signals. In the subsequent dry season, the reservoir experiences particularly intense evaporation due to its larger exposed surface area and extended hydraulic retention time, leading to heavy isotope enrichment.(3) Further analysis of environmental controls on isotopic fractionation revealed a significant negative correlation between δ¹⁸O values and water temperature. Notably, this relationship proved statistically stronger than the correlation observed between deuterium excess (d-excess) and temperature, underscoring the greater sensitivity of δ¹⁸O to thermal dynamics during evaporation.(4) Finally, by leveraging the isotopic mass balance approach and the distinct isotopic enrichment observed between the wet and dry periods, the proportion of water loss due to evaporation along the main stem of the Tanglanghe River during the dry period of April 2025 was estimated. The calculated evaporative loss fraction ranges from 4.62% to 19.40%. A distinct spatial trend is evident, with the evaporation ratio progressively increasing from the upstream reaches toward the downstream sections. This downstream increase in evaporative loss is governed by two primary factors. First, the intensity of groundwater recharge, as substantial groundwater inflow, characterized by more depleted and stable isotope signatures, can buffer the evaporation signal. Second, variations in the morphology of the river surface, including wider channel widths and slower flow velocity, increase the exposure time and the surface area available for evaporation flux, thereby accelerating isotope enrichment.
- the Tanglanghe River /
- δD /
- δ¹⁸O /
- evaporation /
- hydrologic process /
- basin

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图 1 2024—2025年沂源县降雨量数据（数据来自淄博水文中心）

Figure 1. Rainfall data of Yiyuan County from 2024 to 2025 (cited from Zibo Hydrological Center)

下载: 全尺寸图片幻灯片

图 2 螳螂河流域地理位置（A）、水文地质条件（B）以及螳螂河水系示意图（C）

注：图B与图C中数字为取样点编号；图C中水系的颜色与宽度仅为示意，不代表实际水量大小。

Figure 2. Geographical location （A）, hydrogeological conditions（B）, and sketch map of the river system（C）of the Tanglanghe River Basin

Note: Numbers in Figures B and C represent sampling site IDs. In Figure C, the color and width of the river system are schematic only and do not reflect actual water volume.

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图 3 螳螂河流域丰水期与枯水期不同水体δ¹⁸O对比

Figure 3. Comparison of δ¹⁸O values of different water bodies in the Tanglang River Basin during the wet period and the dry period

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图 4 螳螂河流域丰水期地表水δ¹⁸O分布

Figure 4. δ¹⁸O distribution of surface water in the Tanglanghe River Basin during the wet period

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图 5 螳螂河流域枯水期地表水δ¹⁸O分布

Figure 5. δ¹⁸O distribution of surface water in the Tanglanghe River Basin during the dry period

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图 6 螳螂河流域丰水期与枯水期不同水体氢氧同位素组成对比

Figure 6. Comparison of hydrogen-oxygen isotope compositions in different water bodies of the Tanglanghe River Basin during the wet period and the dry period

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图 7 螳螂河流域不同水体氧同位素与水温的相关性

Figure 7. Correlation between oxygen isotopes of different water bodies and water temperature in the Tanglanghe River Basin

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图 8 螳螂河流域不同水体氘盈余(d-excess)与水温的相关性

Figure 8. Correlation between deuterium excess (d-excess) of different water bodies and water temperature in the Tanglanghe River Basin

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图 9 枯水期螳螂河δ¹⁸O与蒸发比例沿流程的变化特征

Figure 9. Changes in δ¹⁸O of the Tanglanghe River and the evaporation ratio along the upstream−downstream transect during the dry period

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表 1 螳螂河流域采样点分类

Table 1. Classification of sampling sites in the Tanglanghe River Basin

分类	类型	点位数	点位编号
地表水	河流	11	TL03，TL04，TL05，TL06，TL07， TL11，TL14，TL16，TL18， TL20，TL21
地表水	水库	4	TL08，TL09，TL13，TL19
地下水	泉水	3	TL01，TL10，TL12
	民用井	2	TL02，TL15
	地下河出口	1	TL17

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表 2 螳螂河流域丰水期与枯水期不同水体的δD与δ¹⁸O分析

Table 2. Analysis of δD and δ¹⁸O of different water bodies in the Tanglanghe River Basin during the wet period and the dry period

时期	分类	同位素	总数	均值/‰	标准差	最小值/‰	中位数/‰	最大值/‰
丰水期	河流	δ¹⁸O	9	−10.02	0.60	−10.85	−9.94	−8.74
	河流	δD	9	−70.12	4.83	−75.77	−70.17	−58.77
	水库	δ¹⁸O	4	−11.07	0.42	−11.41	−11.21	−10.45
	水库	δD	4	−79.79	3.82	−83.43	−80.66	−74.41
	地下水	δ¹⁸O	6	−9.84	0.55	−10.40	−9.86	−9.26
	地下水	δD	6	−69.27	3.96	−73.04	−69.61	−64.54
枯水期	河流	δ¹⁸O	11	−7.84	0.49	−8.84	−7.79	−7.07
	河流	δD	11	−55.27	3.00	−61.18	−55.03	−51.19
	水库	δ¹⁸O	4	−8.11	0.55	−8.82	−8.04	−7.53
	水库	δD	4	−60.00	3.34	−64.51	−59.36	−56.79
	地下水	δ¹⁸O	5	−8.94	0.31	−9.33	−8.84	−8.58
	地下水	δD	5	−62.83	2.33	−66.20	−62.67	−60.45

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表 3 螳螂河上游至下游水体δD 和δ¹⁸O 组成

Table 3. Composition of δD and δ¹⁸O along the upstream−downstream transect of the Tanglanghe River

位置	取样点	丰水期		枯水期
位置	取样点	δ¹⁸O/‰	δD/‰	δ¹⁸O/‰	δD/‰
河段A	TL20	−	−	−8.84	−61.18
	TL19	−11.27	−80.48	−8.82	−64.51
	TL14	−10.40	−72.91	−8.03	−54.12
	TL11	−9.94	−69.93	−7.69	−52.56
河段B	TL21	−	−	−8.06	−57.58
	TL07	−9.82	−68.66	−7.79	−55.03
河段C	TL05	−10.06	−70.66	−7.57	−53.60
	TL18	−9.92	−70.14	−7.79	−56.35
	TL03	−8.74	−58.77	−7.16	−51.78
河段D	TL04	−9.85	−70.17	−7.09	−51.19

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表 4 螳螂河流域丰水期与枯水期水温、氢氧同位素与d-excess分析

Table 4. Analysis of water temperature, hydrogen-oxygen isotopes and d-excess in the Tanglanghe River Basin during the wet period and the dry period

时期	参数	总数N	均值	标准差	最小值	中位数	最大值
丰水期	Tw/℃	19	23.00	4.15	14.80	24.16	28.70
	δ¹⁸O/‰	19	−10.18	0.71	−11.41	−10.28	−8.74
	δD/‰	19	−71.89	5.91	−83.43	−72.70	−58.77
	d-excess/‰	19	9.58	0.89	7.81	9.59	11.15
枯水期	Tw/ ℃	20	15.54	2.14	10.60	15.35	19.30
	δ¹⁸O/‰	20	−8.17	0.64	−9.33	−8.04	−7.07
	δD/‰	20	−58.11	4.35	−66.20	−57.60	−51.19
	d-excess/‰	20	7.23	1.99	1.93	7.12	10.10

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表 5 螳螂河干流上游至下游蒸发比例

Table 5. Evaporation ratio from upstream to downstream along the main stem of the Tanglanghe River

取样点	δ¹⁸O/‰	蒸发比例/%
TL20	−8.84	4.62
TL19	−8.82	4.79
TL14	−8.03	11.69
TL11	−7.69	14.49
TL21	−8.06	11.46
TL07	−7.79	13.69
TL05	−7.57	15.45
TL18	−7.79	13.63
TL03	−7.16	18.70
TL04	−7.09	19.40
注：TL07与TL18的δ¹⁸O因保留两位小数而数值相同，实际分别为−7.787‰与−7.794‰，故蒸发比例有差异。

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