Next Article in Journal
Taxonomic Diversity: Importance, Threats, and Status of Diatoms from Lowland Urban Springs (Northeast Poland)
Previous Article in Journal
Assessing Climate Change Impacts on Groundwater Recharge and Storage Using MODFLOW in the Akhangaran River Alluvial Aquifer, Eastern Uzbekistan
Previous Article in Special Issue
Groundwater Vulnerability and Environmental Impact Assessment of Urban Underground Rail Transportation in Karst Region: Case Study of Modified COPK Method
 
 
Search for Articles:
Title / Keyword
Author / Affiliation / Email
Journal
Article Type
 
 
Advanced Search
 
Section
Special Issue
Volume
Issue
Number
Page
 
Journals
Water
Volume 17
Issue 15
10.3390/w17152292
water-logo
Submit to this Journal Review for this Journal Propose a Special Issue
► Article Menu

Article Menu

share Share announcement Help format_quote Cite
first_page
settings
Order Article Reprints
Font Type:
Arial Georgia Verdana
Font Size:
Aa Aa Aa
Line Spacing:
Column Width:
Background:
Review

Recharge Sources and Flow Pathways of Karst Groundwater in the Yuquan Mountain Spring Catchment Area, Beijing: A Synthesis Based on Isotope, Tracers, and Geophysical Evidence

by
Yuejia Sun
1,2,
Liheng Wang
1,2,*,
Qian Zhang
1,2 and
Yanhui Dong
1,2
1
Key Laboratory of Deep Petroleum Intelligent Exploration and Development, Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing 100029, China
2
College of Earth and Planetary Sciences, University of Chinese Academy of Sciences, Beijing 100049, China
*
Author to whom correspondence should be addressed.
Water 2025, 17(15), 2292; https://doi.org/10.3390/w17152292 (registering DOI)
Submission received: 30 June 2025 / Revised: 30 July 2025 / Accepted: 31 July 2025 / Published: 1 August 2025
(This article belongs to the Special Issue Contaminant Transport, Risk Assessment, and Ecological Impacts in Karst)
Browse Figures
Versions Notes

Abstract

Karst groundwater systems are critical to water supply and ecological sustainability in northern China, yet their heterogeneity poses challenges for flow characterization. The Yuquan Mountain (YM) Spring, historically a major karst spring in western Beijing, has experienced persistent drying, raising concerns about its recharge and flow mechanisms. This study integrates published isotope data, spatial distributions of Na+ and Cl− as hydrochemical tracers, groundwater age estimates, and geophysical survey results to assess the recharge sources and flow pathways within the YM Spring catchment area. The analysis identifies two major recharge zones: the Tanzhesi area, primarily recharged by direct infiltration of precipitation through exposed carbonate rocks, and the Junzhuang area, which receives mixed recharge from rainfall and Yongding River seepage. Three potential flow pathways are proposed, including shallow flow along faults and strata, and a deeper, speculative route through the Jiulongshan-Xiangyu syncline. The synthesis of multiple lines of evidence leads to a refined conceptual model that illustrates how geological structures govern recharge, flow, and discharge processes in this karst system. These findings not only enhance the understanding of subsurface hydrodynamics in complex geological settings but also provide a scientific basis for future spring restoration planning and groundwater management strategies in the regions.

1. Introduction

Karst aquifers play a vital role in global freshwater supply, serving as crucial sources of drinking water for approximately one-quarter of the world’s population [1,2,3]. Due to their unique hydrogeological properties, including high permeability, dual porosity, and strong heterogeneity, karst systems can store and transmit large quantities of groundwater through both diffuse and conduit flow mechanisms. Globally, approximately 15.2% of the ice-free land surface is underlain by carbonate rocks, with karst regions most extensive in China, which has both the largest absolute karst area (2.54 million km2) and the highest national percentage (26.5%) among major countries [3,4,5,6]. However, the same complex structure that makes karst aquifers efficient water suppliers also poses significant challenges for understanding their hydrodynamics. Subsurface heterogeneity, rapid and localized recharge events, and poorly constrained flow paths often make it difficult to characterize the recharge, flow, and discharge processes within these systems [7,8,9]. As a result, the scientific community still faces considerable uncertainty in modeling and managing karst groundwater resources, particularly under conditions of increasing anthropogenic stress and climate variability [4,10,11].
Numerous methods have been developed to investigate karst groundwater systems, reflecting their inherent complexity and heterogeneity [12,13,14,15,16]. At the foundational level, conventional hydrogeological techniques are widely applied, including monitoring groundwater level fluctuations, conducting pumping tests, performing water balance calculations, and analyzing karst spring discharge responses to precipitation [17,18,19]. While these approaches are effective for identifying fundamental hydrological relationships and characterizing the temporal dynamics of groundwater systems, they largely remain at the stage of empirical observation and phenomenological description.
To progress from empirical observation to a process-based understanding of the hydrological cycle, isotopic and geochemical tracers are now widely employed. Stable isotopes (δ2H, δ18O) delineate recharge sources and quantify mixing between water masses [20,21,22], whereas radiogenic strontium ratios (87Sr/86Sr) elucidate water–rock interaction and the evolution of flow paths [23,24]. Radioactive tracers such as 3H and 14C provide groundwater residence times [25,26], thereby constraining potential flow pathways. Collectively, these methods have greatly advanced the mechanistic understanding of karst aquifers, allowing researchers to resolve flow connectivity, residence times, and recharge processes with enhanced precision. In parallel, a suite of non-invasive techniques is now employed to resolve the internal architecture of karst media. These techniques, including electrical resistivity tomography, seismic imaging [27], distributed temperature sensing [28], and hydraulic tomography [29], have been employed to explore the internal hydraulic architecture of karst systems. These techniques are especially valuable in delineating preferential flow paths, identifying conduit networks, and estimating permeability heterogeneity, thus providing a spatially resolved picture of subsurface hydrological structure.
Building on this foundation, numerical modeling has become an essential tool for the quantitative analysis of karst groundwater systems. Depending on the complexity of the conceptual model and data availability, researchers may employ equivalent porous media models [30], dual-porosity or dual-permeability approaches, and discrete fracture or conduit flow models [31,32]. These models integrate multi-source observations and allow for scenario testing under changing environmental or anthropogenic conditions. Despite these methodological advances, the comprehensive and systematic characterization of karst groundwater systems remains a formidable challenge. The intrinsic spatial heterogeneity and dynamic behavior of karst environments demand integrative, multi-method frameworks that combine observation, process inference, structural imaging, and predictive modeling [16].
The Yuquan Mountain (YM) karst groundwater system, located in the western part of Beijing, China, represents a typical karst system with both scientific significance and practical importance. Historically, the YM Spring was one of the most important natural springs in Beijing, supplying high-quality water to urban residents and supporting local ecosystems. As early as the Qing Dynasty, the spring was incorporated into imperial garden designs [33], and throughout the 20th century, it contributed meaningfully to municipal water use. However, since 1975, the spring has experienced complete flow cessation due to intensive groundwater extraction and declining recharge, and has not naturally resumed flow since then [34]. The disappearance of the spring has had negative consequences for local ecological conservation, urban water security, and public heritage values. Moreover, the lack of a comprehensive understanding of the hydrogeological framework and groundwater flow dynamics in the region limits the potential for scientifically informed management or possible spring recovery strategies. Given the importance of the spring to both the Beijing metropolitan area and the broader ecological function of the Beijing–Tianjin–Hebei region (North China), there is an urgent need to systematically integrate existing knowledge and identify knowledge gaps.
This paper aims to provide a comprehensive review of hydrogeological studies conducted in the YM karst groundwater system, with the goal of synthesizing current knowledge on recharge sources, groundwater flow patterns, and subsurface structure. By reviewing published data from water balance analysis, stable and radiogenic isotopes, major ion chemistry, geophysical surveys, and groundwater age studies, we propose an updated conceptual model of groundwater flow in the region. Furthermore, we critically assess the limitations of existing investigations and highlight key directions for future research, including the need for integrated monitoring networks, advanced modeling approaches, and consideration of artificial recharge scenarios. This review not only deepens scientific understanding of the YM Spring system and lays a foundation for subsequent hydrogeological and ecological restoration efforts, but also advances a transferable framework for studying and managing large karst springs elsewhere in northern China and analogous karst systems worldwide.

2. Study Area

2.1. General Setting

This study focuses on the YM Karst Spring System, which is situated within the broader Western Mountains Karst Groundwater System in Beijing, the capital of China. While the Cambrian and Ordovician carbonate aquifer represents the primary hydrogeological unit of interest, the study area also includes Carboniferous, Permian, and Jurassic clastic formations (e.g., sandstones and mudstones) with relatively low permeability and porosity, resulting in poor water yield capacity. These non-karst lithologies form part of the structural framework and influence the spatial distribution of recharge and flow paths. Defined by its own recharge, flow, and discharge boundaries, the spring catchment area represents an independent groundwater system embedded within a structurally and topographically complex region [35]. Geographically, the spring catchment area is located in the mountainous western suburbs of Beijing. It is bounded to the east and south by major fault systems, while the western and northern boundaries generally follow the surface water divides, demarcating the limits of natural recharge (Figure 1).
Topographically, the region exhibits a general gradient from northwest to southeast. The western portion consists of the northern extensions of the Taihang Mountains, featuring low mountains and hills with elevations ranging from 200 to 700 m above sea level (Figure 1a). In contrast, the eastern part transitions into a broad alluvial and diluvial plain, forming a low-lying outlet zone for both surface and subsurface flow. The total surface area of the study region is approximately 1319 km2 (Figure 1b).
Climatically, the study area falls within a typical semi-arid, temperate continental monsoon climate zone. The precipitation and temperature are highly synchronized seasonally, with warm, wet summers and cold, dry winters. The multi-year average annual precipitation is approximately 600 mm, but its temporal distribution is markedly uneven [36]. Over 85% of the total annual precipitation occurs during the summer monsoon season between July and September. The Yongding River, the principal river in the study area, enters from the northwest near the Yanchi Hydrological Station and exits in the southeast at the Lugouqiao Hydrological Station, traversing the spring domain longitudinally [37]. Since the 1960s, the Beijing section of the Yongding River has experienced progressive flow reduction, transforming into a seasonal river. However, since the implementation of ecological water replenishment measures in 2019, full-channel flow was reestablished by 2021 [36,38].

2.2. Geological and Hydrogeological Framework

The study area is situated along the northern margin of the North China Craton, within the Yanshan Fold Belt, a tectonically active region dominated by northeast–southwest (NE–SW) trending structures [39]. The central structural feature controlling the study area is the Jiulongshan–Xiangyu syncline (S1, Figure 1b), which defines the regional geological framework and plays a key role in influencing groundwater occurrence and flow dynamics. Along the southeastern boundary of the YM spring catchment area, the Babaoshan Fault (F3, Figure 1b) and the Huangzhuang–Gaoliying Fault (F2, Figure 1b) serve as major tectonic limits. The former is a compressive-shear fault, and the latter is a normal-slip fault. In addition to the dominant NE–SW structures, northwest–southeast (NW–SE)-oriented faults are also well developed. Among them, the Nankou–Sunhe Fault (F1, Figure 1b), a sinistral strike-slip fault at the northeastern edge of the area, marks an important boundary, while the central Yongding River Fault (F4, Figure 1b) may act as a major subsurface pathway for groundwater movement [23].
The stratigraphy of the region spans from the Proterozoic Changcheng Group to the Quaternary, with older units primarily exposed in the mountainous western and central parts, and younger deposits dominating the eastern plain. Tectonic deformation has caused localized exposures of older formations near fault zones. Of particular hydrogeological importance are the carbonate formations of Cambrian and Ordovician age, consisting predominantly of limestone and dolomitic limestone, which exhibit strong karst development and serve as the primary aquifer units in the region.
Hydrogeologically, the YM spring catchment area represents a fault-controlled karst aquifer system characterized by dual recharge mechanisms. Direct recharge occurs through infiltration of precipitation over exposed carbonate outcrops, while indirect recharge is facilitated by leakage from surface water bodies, especially the Yongding River. Groundwater flows predominantly from the higher elevations in the northwest toward lower-lying discharge zones in the southeast, including the historical discharge point of the YM Spring, which ceased flowing in the 1970s [23]. Despite extensive historical use, the detailed groundwater flow regime remains poorly understood due to the complex interplay among lithological heterogeneity, structural controls, and anthropogenic impacts.
Groundwater in the area is mainly stored in two types of aquifers: the unconsolidated Quaternary alluvial–diluvial deposits and the fractured and karstified carbonate formations. The karst groundwater system can be further classified into three hydrogeological types based on the overburden conditions:
(1)
Exposed-type karst aquifers, such as those in Junzhuang and Tanzhesi (Figure 1b, Figure 2), where Ordovician carbonates are directly exposed at the surface and receive direct rainfall infiltration;
(2)
Covered-type aquifers, like those beneath the Quaternary sediments in Wenquan and Dongxiaokou towns (Figure 1b and Figure 2), where the karstified carbonates are overlain by unconsolidated deposits;
(3)
Confined or buried karst systems, located in the central part of the study area, controlled structurally by the Jiulongshan–Xiangyu syncline (S1, Figure 1b) and overlain by Carboniferous–Jurassic strata.
In addition to the karstified carbonate aquifers, the study area includes significant exposures of Carboniferous, Permian, and Jurassic clastic formations, such as sandstone, mudstone, and siltstone (Figure 1b). These lithologies generally have low primary permeability and exhibit limited groundwater storage and transmission capacity. From a hydrogeological perspective, they act primarily as aquitards or aquicludes, restricting vertical and lateral flow, and locally influencing the direction and compartmentalization of groundwater movement. The spatial distribution of these non-karst units, particularly where they overlie or border carbonate aquifers, plays an important role in shaping the groundwater flow field by constraining recharge areas and guiding flow along structural discontinuities such as faults and synclines.
Both local precipitation and the water of the Yongding River are critical recharge sources to these karst systems. In areas where the Ordovician limestone is exposed, such as Junzhuang and Tanzhesi, direct infiltration is significant. Additionally, leakage from the Yongding River is likely to recharge the aquifer system, particularly in areas near its course. Regionally, the general flow direction of karst groundwater follows a southwest–northeast trend, nearly parallel to the dominant structural grain. Discharge pathways include lateral outflow, upward leakage into the overlying Quaternary aquifer, artificial abstraction, and historical spring discharge.
Water 17 02292 g002
Figure 2. (a) Hydrogeological cross-section from Junzhuang to Lugou Bridge (A–B; see Figure 1b for location; adapted from Tang et al. [40]); (b) hydrogeological cross-section from Tanzhesi to YM Spring (C–D; see Figure 1b for location; adapted from Qin et al. [23]). Legend items 1–9 are consistent with those in Figure 1.
Figure 2. (a) Hydrogeological cross-section from Junzhuang to Lugou Bridge (A–B; see Figure 1b for location; adapted from Tang et al. [40]); (b) hydrogeological cross-section from Tanzhesi to YM Spring (C–D; see Figure 1b for location; adapted from Qin et al. [23]). Legend items 1–9 are consistent with those in Figure 1.
Water 17 02292 g002

3. Recharge Mechanisms of Karst Groundwater

Understanding the recharge mechanisms of karst groundwater systems is essential for accurately characterizing aquifer dynamics and managing water resources. A variety of approaches have been developed to investigate recharge processes, ranging from conventional water balance calculations to advanced geochemical and isotopic tracing methods [41,42]. The water balance approach estimates the quantitative contribution of various potential recharge sources—such as precipitation, river infiltration, and lateral inflow—by analyzing input-output relationships across defined hydrological boundaries. In parallel, hydrochemical and isotopic indicators offer powerful tools to identify and distinguish recharge sources, assess recharge pathways, and constrain residence times within the aquifer system. Therefore, it is valuable to combine these methodological perspectives in order to evaluate the key recharge sources that sustain the YM karst groundwater system.

3.1. Quantifying Recharge from Precipitation and River Leakage via Water Balance Calculations

The YM karst groundwater system encompasses several stratigraphic aquifer units, including the Jixian, Cambrian, and Ordovician formations [23]. Among these, the Ordovician limestone formations are widely exposed in areas such as Tanzhesi and Junzhuang (Figure 1), where well-developed karst fractures and conduits offer favorable conditions for the infiltration of local precipitation and Yongding River water. A comparative analysis of groundwater level fluctuations in observation wells and local precipitation records in these exposed zones reveals a clear hydraulic linkage. Wang et al. [43] reported that peak groundwater levels in the Ordovician aquifer typically lag behind peak rainfall events by approximately 40 days. This relatively short delay highlights a significant recharge response, indicating that direct infiltration of precipitation is a major contributor to groundwater recharge in the exposed limestone areas of Tanzhesi and Junzhuang (Figure 1).
To quantify the contribution of these exposed limestone zones to the recharge of the YM karst aquifer system, a preliminary estimation was conducted using the infiltration coefficient method. This approach integrates spatial data on exposed karst areas, long-term precipitation statistics, and site-specific infiltration coefficients to assess annual recharge volumes. Unlike traditional empirical estimates that assign infiltration values based solely on lithological categories, this method accounts for surface conditions, offering a more accurate assessment of precipitation infiltration. Based on these calculations (Table 1), the estimated recharge from exposed karst areas ranges from approximately 48.03 × 106 m3/year to 63.67 × 106 m3/year.
In addition to direct recharge from precipitation, the Yongding River plays a crucial role in supplying water to the YM spring domain through seepage losses along its course. The river enters the study area at the Yanchi hydrological station and exits at the Lugouqiao station (Figure 1b), flowing from northwest to southeast. As noted earlier, extensive outcrops of Cambrian and Ordovician limestone are present near Junzhuang. These carbonate formations are strongly influenced by the Jiulongshan–Xiangyu syncline and the Yongding River Fault, which together control the structural configuration and hydraulic connectivity of the aquifer system. In this area, the karst aquifers exhibit highly developed dissolution features such as conduits and fractures, resulting in high permeability. Additionally, the riverbed in this segment is characterized by good infiltration capacity, creating favorable conditions for direct recharge from the river into the underlying karst aquifers.
Historical discharge records from hydrological stations support the mechanism of river leakage contributing to the karst aquifer system. Between 2000 and 2014, monitored streamflow data indicated that the river experienced significant seepage losses near the Junzhuang area, with an estimated total leakage of approximately 72.77 × 106 m3. More recent estimates based on water balance calculations reveal a substantial increase in seepage volumes, likely driven by the ecological flow restoration projects initiated in 2019 for the Yongding River. Specifically, leakage losses within the study area were estimated at approximately 1.72 × 108 m3 in 2020, 1.81 × 108 m3 in 2021, and 2.58 × 108 m3 in 2022. This increasing trend highlights the growing role of river leakage as a recharge source for the YM karst groundwater system, especially in the context of ongoing ecological enhancement efforts.
In summary, both direct infiltration from precipitation over exposed carbonate rocks and seepage losses from the Yongding River represent two major sources of recharge to the YM karst groundwater system. Water balance calculations indicate that the annual recharge from exposed limestone areas ranges between 48.03 × 106 and 63.67 × 106 m3, while river leakage has shown a significant upward trend in recent years, reaching up to 2.58 × 108 m3 in 2022. These findings underscore the critical hydrological connectivity between surface water and the underlying karst aquifer and provide a quantitative foundation for further tracer-based investigations of recharge mechanisms.

3.2. Tracing Recharge Sources Using Stable Isotopes (δ2H or δD and δ18O)

Stable isotopes of hydrogen and oxygen (δD and δ18O) are widely used in hydrogeological studies to identify the origin and recharge processes of groundwater. Because these isotopes are integral components of the water molecule, they are highly conservative during subsurface transport and reflect the climatic and hydrological conditions at the time of recharge. In karst systems, where mixing of multiple recharge sources is common and flow pathways are often complex and heterogeneous, stable isotopes provide a powerful tool to distinguish between inputs from precipitation, river leakage, and other potential contributors.
Atmospheric precipitation is typically one of the most important recharge sources for groundwater. However, since δD and δ18O values in precipitation are subject to significant fractionation influenced by geographical and climatic factors, accurate interpretation of groundwater isotopic signatures requires the establishment of a reliable local meteoric water line (LMWL) based on year-round precipitation sampling. Unlike regions with long-term monitoring sites under the IAEA/WMO Global Network for Isotopes in Precipitation (GNIP), the Beijing area lacks such international and long-term stations. To address this limitation, previous studies have established regional LMWLs based on locally collected precipitation data in Beijing. In particular, Hao et al. [44] conducted systematic sampling from July 2011 to July 2012 at the Western Mountain region of Beijing, which is geographically closer to the study area than earlier work by Zhai et al. [45] in the eastern plain of Beijing. Their results showed that δD ranged from −119.46‰ to −13.96‰ with an average of −61.86‰, while δ18O ranged from −15.47‰ to −1.84‰ with an average of −8.87‰. Based on this dataset, the LMWL for the Western Mountain region was defined as δD = 7.17 δ18O + 1.46 (n = 39, R2 = 0.9342) [44]. Compared to the Global Meteoric Water Line (GMWL: δD = 8 δ18O + 10, [46]), the lower slope and intercept of the local line indicate that regional precipitation is influenced not only by oceanic moisture but also by arid climatic conditions and localized vapor recycling processes (Figure 3).
The δD values of karst groundwater in the study area range from −84.00‰ to −50.30‰, with an average of −64.15‰, while δ18O values vary from −11.29‰ to −5.75‰, averaging −8.58‰. These values fall entirely within the isotopic envelope of local precipitation, confirming that atmospheric rainfall is a major recharge source for the karst aquifer. As shown in Figure 3, a subset of the groundwater samples plots closely along the LMWL, whereas others deviate toward the lower right, away from the LMWL. A linear regression of the karst groundwater isotopic data yields the equation δD = 5.21 δ18O − 19.43, which features a significantly lower slope and intercept than the LMWL. This regression line can be interpreted as an evaporation water line (EWL, Figure 3), indicating that, following meteoric recharge, the groundwater may have been influenced by additional sources or subject to evaporation.
Water 17 02292 g003
Figure 3. Comparison of δ2H and δ18O values of karst groundwater and Yongding River water in the study area with meteoric water lines. The Local Meteoric Water Line (LMWL) is based on the work of Hao et al. [44], while the Global Meteoric Water Line (GMWL) follows Craig [46]. EWL stands for Evaporation Water Line. KG-1 represents karst groundwater data from Qin et al. [23], while KG-2 and Yongding River water data are sourced from Li [47]. Blue-shaded areas (δ18O < −9.00‰) indicate groundwater primarily recharged by precipitation; green-shaded areas (δ18O > −9.00‰) indicate groundwater recharged by a mixture of precipitation and Yongding River water.
Figure 3. Comparison of δ2H and δ18O values of karst groundwater and Yongding River water in the study area with meteoric water lines. The Local Meteoric Water Line (LMWL) is based on the work of Hao et al. [44], while the Global Meteoric Water Line (GMWL) follows Craig [46]. EWL stands for Evaporation Water Line. KG-1 represents karst groundwater data from Qin et al. [23], while KG-2 and Yongding River water data are sourced from Li [47]. Blue-shaded areas (δ18O < −9.00‰) indicate groundwater primarily recharged by precipitation; green-shaded areas (δ18O > −9.00‰) indicate groundwater recharged by a mixture of precipitation and Yongding River water.
Water 17 02292 g003
The Yongding River water exhibits δD values ranging from −61.91‰ to −36.00‰, with an average of −50.30‰, and δ18O values from −7.52‰ to −2.65‰, with a mean of −5.86‰ [23,47]. These isotopic compositions are more enriched relative to the karst groundwater and also lie to the right of the LMWL, consistent with evaporative modification. Notably, most of the river water samples align with the same regression line defined by the groundwater samples, indicating a strong isotopic correlation between the two and implying hydrological connectivity.
Further analysis shows that groundwater samples with δ18O values less than −9.00‰ tend to cluster tightly along the LMWL, consistent with recharge primarily from direct precipitation. In contrast, karst groundwater samples with δ18O values greater than −9.00‰ generally align with the linear regression line of karst groundwater (previously defined in this section, representing an evaporation-influenced trend), and many of them overlap with river water samples. According to the δ18O contour map of the study area derived from Li’s dataset [47], these isotopically enriched groundwater samples are predominantly distributed along the banks of the Yongding River. This spatial distribution further supports the interpretation that river leakage significantly contributes to the recharge of the local karst groundwater system.
A similar pattern was observed by Tang et al. [48] in their study of the Niangziguan karst spring, a representative large karst spring system in northern China located in Shanxi Province. Using δD and δ18O analyses, they identified a dual recharge mechanism involving both direct infiltration of meteoric precipitation and river leakage. Specifically, isotopically depleted karst groundwater, characterized by more negative isotopic values, was associated with direct recharge from local precipitation and showed weak or negligible hydraulic connectivity with surface water. In contrast, groundwater that received substantial input from river leakage showed isotopic enrichment and overlapped significantly with the isotopic signatures of river water.
In the context of the present study, a similar differentiation is evident. Karst groundwater that is primarily recharged by atmospheric precipitation tends to display more negative isotopic values and is mainly distributed in the Tanzhesi area (Figure 1). Conversely, groundwater with mixed recharge from both precipitation and river seepage exhibits more enriched isotopic signatures, aligning closely with those of the Yongding River. These enriched groundwater samples are predominantly found in the Junzhuang area (Figure 1) and along the course of the river itself. This spatial and isotopic pattern underscores the importance of both recharge sources and highlights the significant role of river leakage in shaping the hydrogeochemical characteristics of the YM karst system.

3.3. Tracing Groundwater Sources Using Strontium Isotopes

Strontium isotopes have emerged as a robust tool for investigating groundwater provenance, water–rock interactions, and mixing processes in complex hydrogeological systems [49]. In natural settings, strontium (Sr) is primarily hosted in minerals such as strontianite (SrCO3), celestite (SrSO4), plagioclase feldspars, and apatite. Among the four naturally occurring isotopes of strontium—84Sr, 86Sr, 87Sr, and 88Sr—the 87Sr/86Sr ratio is widely employed as a geochemical tracer because 8787Sr is radiogenic (produced by the decay of 87Rb), while 86Sr is stable and non-radiogenic. This isotopic ratio is sensitive to the lithology through which water has interacted, thus providing valuable insights into groundwater flow paths and source contributions [50,51].
Typical 87Sr/86Sr values vary with rock type and can serve as diagnostic end-members in mixing models. Marine carbonates such as Ordovician limestone generally exhibit low 87Sr/86Sr values, consistent with the composition of ancient seawater during that period, ranging from 0.707840 to 0.709100 [52,53]. Dolomites tend to display slightly higher ratios (~0.711), while silicate-rich rocks—especially granitic or metamorphic terrains—can exceed 0.715 due to prolonged radiogenic accumulation from Rb-rich minerals [54].
Atmospheric precipitation in the Beijing region shows 87Sr/86Sr values ranging from 0.709118 to 0.710357 [55], while water samples from the Yongding River have reported values around 0.710331 [23]. These benchmarks provide essential reference points for interpreting strontium isotope signatures in local karst groundwater.
Plotting 87Sr/86Sr ratios against the molar ratio of Mg2+/(Mg2+ + Ca2+) for groundwater, precipitation, and river water samples in the study area reveals important patterns (Figure 4). Most karst groundwater samples fall within a narrow range of 87Sr/86Sr values between 0.708 and 0.710 and Mg2+/(Mg2+ + Ca2+) values between 0.226 and 0.562, consistent with extensive interaction with carbonate lithologies, particularly limestone [23]. This isotopic signature is indicative of waters that have undergone dissolution processes typical of flow through Ordovician limestone formations.
The spatial distribution of 87Sr/86Sr ratios and Mg2+/(Mg2+ + Ca2+) values across the study area provides further insights into groundwater recharge pathways and lithological controls (Figure 4). Karst groundwater samples from the Tanzhesi area (KG-T) cluster closely with local rainwater, exhibiting 87Sr/86Sr ratios below 0.710 and relatively low Mg2+/(Mg2+ + Ca2+) values. This geochemical similarity indicates that these waters are primarily recharged by local precipitation, with minimal influence from other geological sources. In contrast, groundwater samples from the Junzhuang area (KG-J) also plot near the rainwater field but show a slight shift toward higher Mg2+/(Mg2+ + Ca2+) ratios. This shift suggests enhanced water–rock interaction or partial mixing with Yongding River water, which is characterized by a distinct isotopic signature. Together, these observations support the interpretation that karst groundwater in the Junzhuang area receives mixed recharge from both atmospheric input and river seepage.
Notably, buried karst groundwater near the YM Spring shows significantly higher 87Sr/86Sr ratios (>0.712, Figure 4). These values suggest either interaction with silicate-rich rocks, greater residence times, or mixing with Quaternary porous aquifer waters that have undergone prolonged water–rock interaction. Their separation from the main limestone cluster indicates a different recharge history or deeper flow path.
Water 17 02292 g004
Figure 4. Relationship between 87Sr/86Sr and Mg2+/(Mg2+ + Ca2+) ratios for precipitation, karst groundwater, and Yongding River water in the study area. Rainwater data are from Xu and Han [55], while all other data are sourced from Qin et al. [23]. KG represents karst groundwater in the study area; KG-T and KG-J refer to samples from the Tanzhesi and Junzhuang areas, respectively.
Figure 4. Relationship between 87Sr/86Sr and Mg2+/(Mg2+ + Ca2+) ratios for precipitation, karst groundwater, and Yongding River water in the study area. Rainwater data are from Xu and Han [55], while all other data are sourced from Qin et al. [23]. KG represents karst groundwater in the study area; KG-T and KG-J refer to samples from the Tanzhesi and Junzhuang areas, respectively.
Water 17 02292 g004

3.4. Tracing Recharge Using Na+ and Cl− Concentrations

Sodium (Na+) and chloride (Cl−) are widely regarded as conservative tracers in hydrogeological studies due to their low reactivity and minimal participation in most geochemical processes. These ions are commonly used to identify mixing processes between different water bodies and to trace the sources of salinity. In coastal aquifers, elevated concentrations of Na+ and Cl− often indicate seawater intrusion. In inland systems, however, their variations can reflect water–rock interactions, evaporation effects, or contributions from anthropogenic or surface water sources.
In the YM karst system, notable differences in Na+ and Cl− concentrations exist between river water and karst groundwater, making them useful indicators of recharge pathways and mixing processes. Previous studies [23] have shown that Yongding River water, which flows through the study area, is characterized by relatively high concentrations of Na+ and Cl−, likely due to upstream anthropogenic inputs and longer surface residence time. In contrast, karst groundwater flowing through carbonate formations typically contains lower concentrations of these ions, as carbonates contribute minimally to Na+ and Cl− loads during dissolution.
Precipitation in the Beijing region exhibits significantly lower concentrations of both Na+ and Cl−, with values ranging from 0.09 to 4.14 mg/L for Na+ and 3.02 to 7.68 mg/L for Cl−. This reinforces the interpretation that rainwater may serve as a dilute end-member for both karst groundwater and river water.
A comparative analysis of Na+ and Cl− concentrations in the study area reveals that karst groundwater samples collected along the Yongding River corridor exhibit significantly elevated Na+ (5.3~95.7 mg/L) and Cl− (8.2~104 mg/L) concentrations relative to other karst groundwater sites [23]. This spatial trend aligns well with the hypothesis that river water contributes to the recharge of the karst aquifer, especially in the vicinity of the riverbed. The enrichment in Na+ and Cl− can thus be attributed to seepage from the Yongding River into the underlying carbonate aquifer system, reinforcing conclusions drawn from isotopic evidence in previous sections (Figure 5).
Water 17 02292 g005
Figure 5. Spatial Distribution of Na+ (a) and Cl− (b) in karst groundwater and their relationship with the Yongding River in the study area. Contour map derived from Qin et al. and Tang et al. [23,40].
Figure 5. Spatial Distribution of Na+ (a) and Cl− (b) in karst groundwater and their relationship with the Yongding River in the study area. Contour map derived from Qin et al. and Tang et al. [23,40].
Water 17 02292 g005
Overall, the spatial correspondence between elevated Na+ and Cl− levels in groundwater and proximity to the river channel supports the existence of a hydraulic connection between the Yongding River and the karst groundwater system, particularly in areas where geological conditions enhance vertical permeability.

4. Flow Patterns of Karst Groundwater

While multi-isotope and hydrochemical analyses provide valuable insights into the recharge sources and mechanisms of karst groundwater, a full understanding of the subsurface flow regime requires further investigation of flow pathways and residence times. In this section, we build on the recharge findings by integrating results from previous geophysical surveys and groundwater age data. Together, these datasets allow us to delineate preferential flow channels, infer flow patterns at depth, and ultimately construct a conceptual model of karst groundwater flow in the study area.

4.1. Preferential Flow Pathways Identified by Geophysical Methods

Due to the highly heterogeneous nature of karst media, it is often difficult and economically prohibitive to characterize subsurface permeability structures solely through drilling. In this context, geophysical methods offer a cost-effective and non-invasive alternative for identifying preferential groundwater flow pathways.
To investigate the structural controls on groundwater flow within the YM Spring catchment area, Tang et al. [40] conducted a 16 km-long geophysical survey along the Yongding River from Junzhuang downstream, combining magnetotelluric (MT) and controlled-source audio-frequency magnetotelluric (CSAMT) methods. Their results revealed five distinct low-resistivity zones, interpreted as concealed fractured fault zones based on their linear geometry and absence of surface outcrops; this includes the concealed segment of the Yongdinghe Fault. These hidden fault zones are interpreted to potentially function as preferential flow pathways for karst groundwater, serving as subsurface conduits in certain segments. However, their hydraulic role may vary spatially, with some faults potentially acting as barriers or confining structures under different geological conditions. Additionally, the MT and CSAMT profiles confirmed that the core of the Jiulongshan–Xiangyu syncline (S1 in Figure 1), composed of Cambrian and Ordovician carbonate rocks, is buried to depths exceeding 2000 m. This finding challenges the deep circulation model proposed by Chen et al. [56], who suggested that Yongding River leakage recharges groundwater at Junzhuang, forming a confined aquifer system that flows southeastward through the ultra-deep carbonate core of the syncline. However, such deep circulation would be expected to produce elevated TDS and temperature anomalies, neither of which is supported by the current hydrochemical and thermal observations. These results, instead, support a model in which precipitation and river seepage recharge the system at Junzhuang, followed by shallow subsurface flow through Yongding River alluvial deposits and fractured zones toward the southeast (Figure 6).
To further refine the understanding of karst groundwater pathways, Li et al. [57] carried out an integrated geophysical investigation focused on delineating the runoff pathways of karst groundwater feeding the YM Spring. Using gravity surveys, CSAMT profiles, and microtremor measurements, they characterized the bedrock topography and structural fabric between the western flank of the spring and the Yongding River. A total of 10 potential fault structures were interpreted, most of which are normal faults that likely serve dual roles as both aquifer boundaries and conduits. Their interpretation identified a dominant karst flow path characterized by high-permeability fractured zones, extending along the Yongding River fault zone from Junzhuang and turning northeastward near the Babaoshan fault (Figure 6). This newly recognized preferential flow path provides a scientific basis for understanding and potentially restoring discharge at the YM Spring.

4.2. Karst Groundwater Residence Time Distribution

Groundwater age, also referred to as groundwater residence time, denotes the time elapsed since water entered the subsurface system through recharge until it exits via discharge [58,59]. This parameter is critical for understanding groundwater renewability and the dynamics of its interaction with surrounding geological media. Groundwater age exerts strong control on the evolution of hydrochemical and isotopic characteristics, including solute concentrations, temperature, and isotopic signatures, and serves as a key indicator of flow velocity, circulation depth, and hydrologic connectivity in aquifer systems.
In the YM Spring catchment area, groundwater residence times were estimated by Li [47] using a combination of radioactive isotopes (3H, 14C) and chlorofluorocarbon (CFC) tracers. The results show that the karst groundwater in this area is generally young, with 86.7% of samples having residence times of less than 30 years, and only 8.9% exceeding 50 years. This indicates a predominantly active and rapid circulation system with strong renewal capacity. Spatially, the typical recharge zones at Tanzhesi and Junzhuang are characterized by shallow groundwater ages ranging from 3 to 21 years, attributed to well-developed karst fissures and rapid infiltration of precipitation. In contrast, groundwater in the downstream discharge area of the YM Spring exhibits older ages between 17 and 29 years, reflecting cumulative travel times along the flow paths.
The analysis of groundwater age data along the main flow paths toward the YM Spring provides further insights into the regional flow dynamics. Groundwater recharged in the Junzhuang area flows southeastward along the Yongding River fault zone (F4, Figure 1b), where residence times remain relatively stable between 18 and 21 years. This consistency suggests a high-permeability flow path, where the fault zone facilitates rapid lateral transport of river-derived recharge. However, upon approaching the intersection with the Huangzhuang–Gaoliying Fault (F3, Figure 1b), residence times gradually increase from 18 to 27 years as groundwater continues toward the spring outlet. This pattern suggests a transition to slower flow velocities or enhanced mixing with older water, potentially due to structural barriers or compartmentalization introduced by fault interactions. The observed spatial trends in groundwater age thus emphasize how faults of varying nature contribute to shaping both the flow patterns and residence times of karst groundwater.

4.3. Integrated Conceptual Model of Karst Groundwater Recharge and Flow Pathways

A synthesis of the hydrogeochemical, isotopic, and geophysical evidence reveals a comprehensive understanding of the karst groundwater flow system in the study area. The YM Spring catchment area receives recharge from multiple sources, including direct infiltration of local precipitation, seepage from surface water (notably the Yongding River from Yanchi to Junzhuang), and lateral inflow from adjacent recharge zones. Groundwater movement is strongly influenced by the orientation of geological structures, the spatial distribution of carbonate aquifers, and the overall morphology of the stratigraphy. Groundwater discharge in the system primarily occurs through artificial extraction, lateral outflow, and natural spring discharge.
Two main recharge zones have been identified: the exposed Ordovician limestones in the Tanzhesi and Junzhuang areas. In the Tanzhesi area, precipitation infiltrates directly into fractured carbonate rocks, forming groundwater that flows along the strike of the Ordovician strata from the southwest to the northeast, ultimately discharging at the YM Spring or contributing to downstream lateral outflow (Figure 7).
In contrast, the Junzhuang area receives not only precipitation recharge but also significant seepage input from the Yongding River. The resulting karst groundwater flows along three primary pathways (Figure 7):
  • Shallow Riverbed Flow path: Part of the river-infiltrated groundwater flows along the Yongding River fault and alluvial sediments at shallow depths, crossing the Jiulongshan–Xiangyu syncline from northwest to southeast. It eventually re-enters the carbonate aquifer near the Bajiao area (Figure 1b) through fractured zones, where it merges with groundwater from Tanzhesi. The combined flow then turns northeast and discharges at the YM Spring.
  • Deep Syncline Flow path: Another portion of groundwater recharged at Junzhuang follows the northwest limb of the Jiulongshan–Xiangyu syncline, moving downgradient through Ordovician carbonates into the deeper core of the syncline. It then resurfaces along the southeast limb and discharges at the YM Spring. Due to the lack of supporting hydrochemical, isotopic, and temperature data, this deep flowpath remains a subject of debate.
  • Direct Lateral Flow: Some groundwater continues laterally to the downstream regions via inter-aquifer flow or transitions into the overlying Quaternary porous aquifer system via upward leakage or baseflow interaction.
In addition, the presence and distribution of cave points, as shown in Figure 1b, provide further evidence for identifying major karst flow pathways. These caves are typically formed along zones of enhanced dissolution and represent locations where groundwater has actively contributed to the development of subsurface conduits. The alignment of cave points with inferred fault zones and zones of low resistivity supports the interpretation that these features function as preferential flow channels within the karst system. Therefore, the spatial distribution of caves is not only indicative of the intensity of karstification but also provides important clues for delineating recharge routes and dominant subsurface flow paths.
Discharge from the karst system occurs through the YM Spring, lateral flow toward the southeast, evapotranspiration, and hydraulic contributions to adjacent Quaternary porous aquifers. The integration of recharge mechanisms, structural controls, and hydrogeological data supports the construction of a conceptual model that highlights the complexity and multi-scale nature of karst groundwater circulation within the YM Spring domain.

4.4. Limitations and Future Research Directions

While this study presents a comprehensive characterization of recharge mechanisms and flow dynamics in the YM karst groundwater system using hydrogeochemical, isotopic, and geophysical evidence, several methodological and conceptual limitations remain. Addressing these limitations is essential for advancing our understanding of structurally complex karst aquifers, particularly in rapidly urbanizing and tectonically active regions like western Beijing. Future research should consider the following key priorities.

4.4.1. Expand the Spatial and Temporal Coverage of Groundwater Monitoring and Sampling

Despite the integration of multiple hydrogeological datasets, the current spatial and temporal distribution of groundwater samples remains limited, particularly in deeper carbonate formations and synclinal cores. This restricts our ability to validate conceptual models of deep flow paths. The scarcity of deep boreholes and the absence of long-term observational wells hinder assessments of subsurface connectivity and flow persistence. Furthermore, geothermal or hot spring water samples, which could provide valuable constraints on circulation depth and groundwater residence time, were not included in the current study. Establishing a multi-depth, long-term monitoring network that includes deep carbonate units is critical for improving sample representativeness and temporal resolution.

4.4.2. Apply a Broader Range of Isotopic Tracers to Reduce Source Uncertainty and Track Geochemical Evolution

The current analysis primarily utilizes δD, δ18O, and 87Sr/86Sr isotopes to infer recharge sources and mixing processes. While these tracers offer robust insights, their application in this study is largely restricted to a single hydrological period. The lack of multi-year or event-scale isotopic data limits our ability to evaluate seasonal dynamics or extreme recharge events. Future research should incorporate long-term isotope monitoring across multiple hydrological years, particularly during high-precipitation or drought periods. In addition, integrating additional geochemical and isotopic tracers could significantly enhance source attribution and improve understanding of geochemical evolution in both shallow and deep flow systems. For instance, the application of additional tracers, such as boron (δ11B), calcium (δ44/40Ca), magnesium (δ26Mg), and lithium (δ7Li), and noble gases could improve our understanding of water–rock interactions, ion exchange, and groundwater residence time, especially in deeper zones [60,61,62].

4.4.3. Enhance Subsurface Structural Characterization Through Integration of Geophysical and Fiber-Optic Temperature Sensing Techniques

Although MT and CSAMT surveys successfully identified low-resistivity anomalies interpreted as preferential flow zones, these methods have limited resolution in capturing fine-scale conduit geometries or hydraulic connectivity. Future studies should incorporate high-resolution electrical resistivity tomography (ERT), borehole logging, hydraulic tomography (HT), and possibly cross-hole tomography to better resolve the structure and properties of conduit networks [29,63]. Furthermore, distributed temperature sensing (DTS) using fiber-optic cables represents a promising complementary approach [64]. DTS can detect subtle temperature anomalies caused by groundwater flow and, when combined with ERT, can help distinguish between conductive and resistive pathways. This integrated strategy could significantly improve our ability to assess the hydrologic function of faults (e.g., conduits vs. barriers) and map the spatial configuration of karst features and their connectivity with recharge sources [65,66].

4.4.4. Integrate Multi-Source Datasets Through Advanced Fusion Techniques for Improved Flow Modeling

Given the inherent heterogeneity and data sparsity of karst systems, future research should prioritize the development of data-driven fusion frameworks capable of integrating multi-scale hydrogeological datasets. Probabilistic models, Bayesian networks, and machine learning algorithms can accommodate uncertainties while synthesizing disparate data sources, including structural, geophysical, isotopic, and hydrochemical information [67,68,69]. These approaches have the potential to enhance our ability to delineate recharge zones, simulate flow pathways, and predict discharge behaviors under varying climatic and anthropogenic scenarios [70]. Coupling such data-driven tools with process-based numerical models and refined conceptual frameworks will be essential for quantifying the dynamics of karst aquifers and improving resource management in similar fractured terrains.

5. Conclusions

Karst groundwater systems are of critical importance for maintaining ecological balance, ensuring drinking water security, and sustaining river baseflow, especially in water-scarce regions of northern China. The YM Spring, historically among the largest karst springs in western Beijing, has long served as an important indicator of regional groundwater dynamics in the capital city of China. However, the spring has ceased discharging for years, reflecting both environmental degradation and the intensifying pressure on Beijing’s urban water supply. In this context, improving the understanding of the hydrological processes governing karst groundwater recharge, flow, and discharge in the YM Spring catchment area is not only of academic interest but also essential for water resource management and spring restoration efforts.
This study integrates hydrochemical, isotopic, and geophysical data to refine the conceptual understanding of recharge mechanisms and flow pathways in the YM karst system. The results suggest that the main recharge zones are located in the Tanzhesi and Junzhuang areas, with groundwater predominantly following stratigraphic dip and structural controls toward discharge points such as YM Springs. Two principal flow pathways are proposed: one shallow and fault-guided, and the other potentially deep and structurally controlled beneath the Jiulongshan–Xiangyu syncline. However, the existence of the deep pathway remains speculative due to limited corroborative data.
Future work should address the following priorities: (1) Expand vertically resolved monitoring across multiple depths to obtain head, chemistry, temperature, and age data, especially in deep carbonate units and fault zones; (2) apply multi-isotope and non-traditional tracer techniques to better constrain recharge sources, geochemical evolution, and groundwater residence time; (3) integrate high-resolution geophysical methods, such as ERT and DTS, to delineate conduit networks and assess fault-zone permeability, particularly in structurally complex areas like Junzhuang; and (4) develop coupled, data-driven and process-based models that assimilate structural, geophysical, hydrochemical, and isotopic data to simulate recharge–discharge dynamics under varying climatic and anthropogenic pressures.
These strategies not only enhance the scientific understanding of karst aquifer behavior in tectonically complex settings but also inform practical measures for spring protection and potential restoration. Specifically, delineating key recharge areas and verifying dominant flow pathways will facilitate ecological zoning, targeted conservation efforts, and artificial recharge interventions, all critical to the long-term sustainability of karst groundwater resources in the Beijing region. Moreover, the conceptual framework developed in this study offers a transferable foundation for groundwater management in other karst systems.

Author Contributions

Conceptualization, L.W.; methodology, L.W.; software, Y.S. and Q.Z.; validation, Y.D.; formal analysis, L.W.; investigation, Y.S. and Q.Z.; resources, L.W.; data curation, L.W. and Y.S.; writing—original draft preparation, Y.S.; writing—review and editing, L.W., Q.Z. and Y.D.; visualization, Q.Z. and Y.S.; supervision, L.W.; project administration, L.W.; funding acquisition, L.W. All authors have read and agreed to the published version of the manuscript.

Funding

This research was supported by the Beijing Natural Science Foundation, grant number 8232049.

Data Availability Statement

The data in this study are explained in the article. For detailed data, please contact the corresponding author.

Conflicts of Interest

The authors declare no conflicts of interest.

References

  1. Hartmann, A.; Goldscheider, N.; Wagener, T.; Lange, J.; Weiler, M. Karst water resources in a changing world: Review of hydrological modeling approaches. Rev. Geophys. 2014, 52, 218–242. [Google Scholar] [CrossRef]
  2. Bakalowicz, M. Karst and karst groundwater resources in the Mediterranean. Environ. Earth Sci. 2015, 74, 5–14. [Google Scholar] [CrossRef]
  3. Stevanović, Z. Karst waters in potable water supply: A global scale overview. Environ. Earth Sci. 2019, 78, 662. [Google Scholar] [CrossRef]
  4. Goldscheider, N.; Chen, Z.; Auler, A.S.; Bakalowicz, M.; Broda, S.; Drew, D.; Hartmann, J.; Jiang, G.; Moosdorf, N.; Stevanovic, Z.; et al. Global distribution of carbonate rocks and karst water resources. Hydrogeol. J. 2020, 28, 1661–1677. [Google Scholar] [CrossRef]
  5. Ford, D.; Williams, P.D. Karst Hydrogeology and Geomorphology; John Wiley & Sons: Hoboken, NJ, USA, 2007; p. 576. [Google Scholar]
  6. Chen, Z.; Auler, A.S.; Bakalowicz, M.; Drew, D.; Griger, F.; Hartmann, J.; Jiang, G.; Moosdorf, N.; Richts, A.; Stevanovic, Z.; et al. The World Karst Aquifer Mapping project: Concept, mapping procedure and map of Europe. Hydrogeol. J. 2017, 25, 771–785. [Google Scholar] [CrossRef]
  7. Bakalowicz, M. Karst groundwater: A challenge for new resources. Hydrogeol. J. 2005, 13, 148–160. [Google Scholar] [CrossRef]
  8. Healy, R.W. Estimating Groundwater Recharge; Cambridge University Press: Cambridge, UK, 2010. [Google Scholar]
  9. Joji, V.S.; Viswanathan, S.; Sebastian, S. A Textbook of Managed Aquifer Recharge: Managed Aquifer Recharge; Scholars’ Press: Chisinau, Moldova, 2021. [Google Scholar]
  10. Wang, W.; Fan, Y.; Li, K.; Wang, X.; Kang, J. Challenges of Spring Protection and Groundwater Development in Urban Subway Construction: A Case Study in the Jinan Karst Area, China. Water 2022, 14, 1521. [Google Scholar] [CrossRef]
  11. Dillon, P.; Escalante, E.F.; Megdal, S.B. Managed Aquifer Recharge for Water Resilience; MDPI Books: Basel, Switzerland, 2021. [Google Scholar]
  12. Kresic, N.; Panday, S. Modeling of groundwater flow and transport in coastal karst aquifers. Hydrogeol. J. 2021, 29, 249–258. [Google Scholar] [CrossRef]
  13. Eisenlohr, L.; Király, L.; Bouzelboudjen, M.; Rossier, Y. Numerical simulation as a tool for checking the interpretation of karst spring hydrographs. J. Hydrol. 1997, 193, 306–315. [Google Scholar] [CrossRef]
  14. Kaufmann, G.; Braun, J. Karst Aquifer evolution in fractured, porous rocks. Water Resour. Res. 2000, 36, 1381–1391. [Google Scholar] [CrossRef]
  15. Li, S.; Kang, Z.; Feng, X.-T.; Pan, Z.; Huang, X.; Zhang, D. Three-Dimensional Hydrochemical Model for Dissolutional Growth of Fractures in Karst Aquifers. Water Resour. Res. 2020, 56, e2019WR025631. [Google Scholar] [CrossRef]
  16. Dong, Y.; Duan, R.; Li, Z.; Lü, X.; Cai, C.; Liu, J.; Wang, L. Quantitative evaluation of hydrothermal fluids and their impact on diagenesis of deep carbonate reservoirs: Insights from geochemical modeling. Mar. Pet. Geol. 2021, 124, 104797. [Google Scholar] [CrossRef]
  17. Meng, Q.; Xing, L.; Liu, L.; Xing, X.; Zhao, Z.; Zhang, F.; Li, C. Time-lag characteristics of the response of karst springs to precipitation in the northern China. Environ. Earth Sci. 2021, 80, 348. [Google Scholar] [CrossRef]
  18. Song, X.; Hao, H.; Liu, W.; Wang, Q.; An, L.; Jim Yeh, T.-C.; Hao, Y. Spatial-temporal behavior of precipitation driven karst spring discharge in a mountain terrain. J. Hydrol. 2022, 612, 128116. [Google Scholar] [CrossRef]
  19. Fiorillo, F.; Leone, G.; Pagnozzi, M.; Esposito, L. Long-term trends in karst spring discharge and relation to climate factors and changes. Hydrogeol. J. 2021, 29, 347–377. [Google Scholar] [CrossRef]
  20. Rusjan, S.; Sapač, K.; Petrič, M.; Lojen, S.; Bezak, N. Identifying the hydrological behavior of a complex karst system using stable isotopes. J. Hydrol. 2019, 577, 123956. [Google Scholar] [CrossRef]
  21. Barbieri, M.; Boschetti, T.; Petitta, M.; Tallini, M. Stable isotope (2H, 18O and 87Sr/86Sr) and hydrochemistry monitoring for groundwater hydrodynamics analysis in a karst aquifer (Gran Sasso, Central Italy). Appl. Geochem. 2005, 20, 2063–2081. [Google Scholar] [CrossRef]
  22. Dar, F.A.; Jeelani, G.; Perrin, J.; Ahmed, S. Groundwater recharge in semi-arid karst context using chloride and stable water isotopes. Groundw. Sustain. Dev. 2021, 14, 100634. [Google Scholar] [CrossRef]
  23. Qin, D.; Zhao, Z.; Guo, Y.; Liu, W.; Haji, M.; Wang, X.; Xin, B.; Li, Y.; Yang, Y. Using hydrochemical, stable isotope, and river water recharge data to identify groundwater flow paths in a deeply buried karst system. Hydrol. Process. 2017, 31, 4297–4314. [Google Scholar] [CrossRef]
  24. Török, A.I.; Moldovan, A.; Tănăselia, C.; Kovacs, E.; Mirea, I.C.; Moldovan, O.T.; Levei, E.A. Sr Isotope, Major, and Trace Element Signatures in Karst Groundwaters. Water 2023, 15, 1431. [Google Scholar] [CrossRef]
  25. Musgrove, M.; Jurgens, B.C.; Opsahl, S.P. Karst Groundwater Vulnerability Determined by Modeled Age and Residence Time Tracers. Geophys. Res. Lett. 2023, 50, e2023GL102853. [Google Scholar] [CrossRef]
  26. Jiang, G.; Guo, F.; Tang, C. Groundwater systems in bare and covered karst aquifers: Evidence from tracer tests, hydrochemistry, and groundwater ages. Environ. Earth Sci. 2019, 78, 608. [Google Scholar] [CrossRef]
  27. Chalikakis, K.; Plagnes, V.; Guerin, R.; Valois, R.; Bosch, F.P. Contribution of geophysical methods to karst-system exploration: An overview. Hydrogeol. J. 2011, 19, 1169–1180. [Google Scholar] [CrossRef]
  28. Munn, J.D.; Maldaner, C.H.; Coleman, T.I.; Parker, B.L. Measuring Fracture Flow Changes in a Bedrock Aquifer Due to Open Hole and Pumped Conditions Using Active Distributed Temperature Sensing. Water Resour. Res. 2020, 56, e2020WR027229. [Google Scholar] [CrossRef]
  29. Dong, Y.; Fu, Y.; Wang, L. Enhanced Characterization of Fractured Zones in Bedrock Using Hydraulic Tomography through Joint Inversion of Hydraulic Head and Flux Data. Hydrology 2024, 11, 122. [Google Scholar] [CrossRef]
  30. Song, X.; Cen, C.; Liu, K.; Zhang, C.; Zhou, A.; Wang, Y.; Peng, Q.; Na, J. Numerical Simulation Analysis of the Impact of Tunnel Construction on Aquifers in the Karst Regions of Southwestern China. Water 2025, 17, 619. [Google Scholar] [CrossRef]
  31. Zheng, X.; Yang, Z.; Wang, S.; Chen, Y.-F.; Hu, R.; Zhao, X.-J.; Wu, X.-L.; Yang, X.-L. Evaluation of hydrogeological impact of tunnel engineering in a karst aquifer by coupled discrete-continuum numerical simulations. J. Hydrol. 2021, 597, 125765. [Google Scholar] [CrossRef]
  32. Zheng, X.; Yang, Z.; Zhan, S.; Du, X.; Chen, Y.; Hu, R.; Chen, Y.-F. Numerical simulation of tracer breakthrough curves in karst aquifers by a coupled discrete-continuum model. J. Hydrol. 2024, 645, 132147. [Google Scholar] [CrossRef]
  33. Zhao, L. The formation of the river systems in the area of Three Hills and Five Gardens in the Qing Dynasty. J. Beijing Union Univ. 2015, 13, 16–21, (In Chinese with English Abstract). [Google Scholar]
  34. Dong, D.; Ma, R.; Li, Y.; Lin, J. Predictive analysis of conditions and schemes for Yuquan Mountain spring water recovery in western suburbs of Beijing. Urban Geol. 2021, 16, 139–146, (In Chinese with English Abstract). [Google Scholar]
  35. Bonacci, O.; Andrić, I. Karst spring catchment: An example from Dinaric karst. Environ. Earth Sci. 2015, 74, 6211–6223. [Google Scholar] [CrossRef]
  36. Xu, C.; Sun, Y.; Shi, B.; Wang, X.; Li, R.; Li, M.; Xi, B.; Feng, C. Study on the Processes Influencing and Importance of Ecological Water Replenishment for Groundwater Resources: A Case Study in Yongding River. Water 2022, 14, 828. [Google Scholar] [CrossRef]
  37. Ji, Z.; Cui, Y.; Zhang, S.; Chao, W.; Shao, J. Evaluation of the Impact of Ecological Water Supplement on Groundwater Restoration Based on Numerical Simulation: A Case Study in the Section of Yongding River, Beijing Plain. Water 2021, 13, 3059. [Google Scholar] [CrossRef]
  38. Liu, S.; Zhou, Y.; Zang, Y.; McClain, M.E.; Wang, X.-S. Effects of downstream environmental flow release on enhancing the groundwater recharge and restoring the groundwater/surface-water connectivity in Yongding River, Beijing, China. Hydrogeol. J. 2023, 31, 1795–1811. [Google Scholar] [CrossRef]
  39. Wang, Y.; Zhou, L.; Li, J. Intracontinental superimposed tectonics—A case study in the Western Hills of Beijing, eastern China. Bulletin 2011, 123, 1033–1055. [Google Scholar] [CrossRef]
  40. Tang, C.; Liang, Y.; Han, K.; Ji, Y.; Wang, W.; Zhao, C.; Shen, H. Hydrogeological significance of the Jiulongshan-Xiangyu syncline at Yuquan Mountain spring. Carsologica Sin. 2015, 34, 431–437, (In Chinese with English Abstract). [Google Scholar]
  41. Željković, I.; Kadić, A. Groundwater balance estimation in karst by using simple conceptual rainfall–runoff model. Environ. Earth Sci. 2015, 74, 6001–6015. [Google Scholar] [CrossRef]
  42. Zhao, M.; Hu, Y.; Zeng, C.; Liu, Z.; Yang, R.; Chen, B. Effects of land cover on variations in stable hydrogen and oxygen isotopes in karst groundwater: A comparative study of three karst catchments in Guizhou Province, Southwest China. J. Hydrol. 2018, 565, 374–385. [Google Scholar] [CrossRef]
  43. Wang, L.; Zhang, Y.; Gong, H.; Yang, G.; Liu, J.; Sun, Y. A study on recovery condition of Yuquan Mountain spring in Beijing. Hydrogeol. & Eng. Geol. 2016, 43, 22–28, (In Chinese with English Abstract). [Google Scholar]
  44. Hao, Y.; Yu, X.; Deng, W.; Jia, G.; Lou, Y.; Bai, Y. The Variations of Hydrogen and Oxygen Compositions and Moisture Sources in the Precipitation in Western Mountain Areas of Beijing. J. Nat. Resour. 2016, 31, 1211–1221. [Google Scholar]
  45. Zhai, Y.; Wang, J.; Teng, Y.; Zuo, R. Hydrogeochemical and isotopic evidence of groundwater evolution and recharge in aquifers in Beijing Plain, China. Environ. Earth Sci. 2013, 69, 2167–2177. [Google Scholar] [CrossRef]
  46. Craig, H. Isotopic Variations in Meteoric Waters. Science 1961, 133, 1702–1703. [Google Scholar] [CrossRef] [PubMed]
  47. Li, X. Characteristics of the Circulation and Renewability of the Karst Water System in Xishan Area, Beijing; China University of Geosciences: Beijing, China, 2017. (In Chinese) [Google Scholar]
  48. Tang, C.; Jin, H.; Liang, Y. Using Isotopic and Hydrochemical Indicators to Identify Sources of Sulfate in Karst Groundwater of the Niangziguan Spring Field, China. Water 2021, 13, 390. [Google Scholar] [CrossRef]
  49. Barbieri, M. Isotopes in Hydrology and Hydrogeology. Water 2019, 11, 291. [Google Scholar] [CrossRef]
  50. Négrel, P.; Petelet-Giraud, E.; Widory, D. Strontium isotope geochemistry of alluvial groundwater: A tracer for groundwater resources characterisation. Hydrol. Earth Syst. Sci. 2004, 8, 959–972. [Google Scholar] [CrossRef]
  51. Pu, J.; Yuan, D.; Zhang, C.; Zhao, H. Tracing the sources of strontium in karst groundwater in Chongqing, China: A combined hydrogeochemical approach and strontium isotope. Environ. Earth Sci. 2012, 67, 2371–2381. [Google Scholar] [CrossRef]
  52. Veizer, J.; Ala, D.; Azmy, K.; Bruckschen, P.; Buhl, D.; Bruhn, F.; Carden, G.A.F.; Diener, A.; Ebneth, S.; Godderis, Y.; et al. 87Sr/86Sr, δ13C and δ18O evolution of Phanerozoic seawater. Chem. Geol. 1999, 161, 59–88. [Google Scholar] [CrossRef]
  53. Burke, W.H.; Denison, R.E.; Hetherington, E.A.; Koepnick, R.B.; Nelson, H.F.; Otto, J.B. Variation of seawater 87Sr/86Sr throughout Phanerozoic time. Geology 1982, 10, 516–519. [Google Scholar] [CrossRef]
  54. Han, G.; Liu, C.-Q. Water geochemistry controlled by carbonate dissolution: A study of the river waters draining karst-dominated terrain, Guizhou Province, China. Chem. Geol. 2004, 204, 1–21. [Google Scholar] [CrossRef]
  55. Xu, Z.; Han, G. Chemical and strontium isotope characterization of rainwater in Beijing, China. Atmos. Environ. 2009, 43, 1954–1961. [Google Scholar] [CrossRef]
  56. Chen, Y.-S.; Ma, Y.-L. On the Recharge of Ground-water in Beijing by the Yongding River through Western Hills. J. Hydraul. Eng. 1981, 3, 10–18, (In Chinese with English Abstract). [Google Scholar]
  57. Li, Q.; Lei, X.; Yang, Y.; Quanhe, Y.; Chen, L.; Wei, G.; Jiefu, S. A study of flow path in Yuquan Mountian area of western Beijing based on integrated geophysical technology. Geol. China 2019, 46, 346–358, (In Chinese with English Abstract). [Google Scholar]
  58. Bethke, C.M.; Johnson, T.M. Groundwater Age and Groundwater Age Dating. Annu. Rev. Earth Planet. Sci. 2008, 36, 121–152. [Google Scholar] [CrossRef]
  59. Ferguson, G.; Cuthbert, M.O.; Befus, K.; Gleeson, T.; McIntosh, J.C. Rethinking groundwater age. Nat. Geosci. 2020, 13, 592–594. [Google Scholar] [CrossRef]
  60. Mayfield, K.K.; Eisenhauer, A.; Santiago Ramos, D.P.; Higgins, J.A.; Horner, T.J.; Auro, M.; Magna, T.; Moosdorf, N.; Charette, M.A.; Gonneea, M.E.; et al. Groundwater discharge impacts marine isotope budgets of Li, Mg, Ca, Sr, and Ba. Nat. Commun. 2021, 12, 148. [Google Scholar] [CrossRef]
  61. Bagard, M.-L.; West, A.J.; Newman, K.; Basu, A.R. Lithium isotope fractionation in the Ganges–Brahmaputra floodplain and implications for groundwater impact on seawater isotopic composition. Earth Planet. Sci. Lett. 2015, 432, 404–414. [Google Scholar] [CrossRef]
  62. Jiang, W.; Sheng, Y.; Wang, G.; Shi, Z.; Liu, F.; Zhang, J.; Chen, D. Cl, Br, B, Li, and noble gases isotopes to study the origin and evolution of deep groundwater in sedimentary basins: A review. Environ. Chem. Lett. 2022, 20, 1497–1528. [Google Scholar] [CrossRef]
  63. Ma, L.; Sun, X.; Qian, J.; Wang, W.; Deng, Y.; Fang, Y. Identification of high-permeability and water-rich zones in a fractured karst water source area based on the hydraulic tomography method. J. Hydrol. 2024, 629, 130648. [Google Scholar] [CrossRef]
  64. Furlanetto, D.; Camporese, M.; Schenato, L.; Costa, L.; Salandin, P. Fiber optics passive monitoring of groundwater temperature reveals three-dimensional structures in heterogeneous aquifers. Sci. Rep. 2024, 14, 8430. [Google Scholar] [CrossRef]
  65. Dong, Y.; Fu, Y.; Yeh, T.-C.J.; Wang, Y.-L.; Zha, Y.; Wang, L.; Hao, Y. Equivalence of Discrete Fracture Network and Porous Media Models by Hydraulic Tomography. Water Resour. Res. 2019, 55, 3234–3247. [Google Scholar] [CrossRef]
  66. Fu, Y.; Dong, Y.; Wang, L.; Bour, O.; Klepikova, M.V.; Zong, Z.; Xu, Z.; Zhou, Z. Characteristics of hydraulic conductivity in mountain block systems and its effects on mountain block recharge: Insights from field investigation and numerical modeling. J. Hydrol. 2022, 612, 128184. [Google Scholar] [CrossRef]
  67. Namous, M.; Hssaisoune, M.; Pradhan, B.; Lee, C.-W.; Alamri, A.; Elaloui, A.; Edahbi, M.; Krimissa, S.; Eloudi, H.; Ouayah, M.; et al. Spatial Prediction of Groundwater Potentiality in Large Semi-Arid and Karstic Mountainous Region Using Machine Learning Models. Water 2021, 13, 2273. [Google Scholar] [CrossRef]
  68. Basu, B.; Morrissey, P.; Gill, L.W. Application of Nonlinear Time Series and Machine Learning Algorithms for Forecasting Groundwater Flooding in a Lowland Karst Area. Water Resour. Res. 2022, 58, e2021WR029576. [Google Scholar] [CrossRef]
  69. Banusch, S.; Somogyvári, M.; Sauter, M.; Renard, P.; Engelhardt, I. Stochastic Modeling Approach to Identify Uncertainties of Karst Conduit Networks in Carbonate Aquifers. Water Resour. Res. 2022, 58, e2021WR031710. [Google Scholar] [CrossRef]
  70. Ma, J.; Li, T.; Li, X.; Zhou, S.; Ma, C.; Wei, D.; Dai, K. A probability prediction method for the classification of surrounding rock quality of tunnels with incomplete data using Bayesian networks. Sci. Rep. 2022, 12, 19846. [Google Scholar] [CrossRef]
Water 17 02292 g001
Figure 1. (a) Location map of the study area; (b) simplified hydrogeological map of the study area. 1—Quaternary unconsolidated porous aquifers; 2—Jixian System carbonate aquifer; 3—Cambrian carbonate aquifer; 4—Ordovician carbonate aquifer; 5—Carboniferous–Permian–Jurassic clastic porous-fractured aquifers; 6—Groundwater flow direction; 7—Faults or synclinal structures; 8—Karst caves; 9—Spring; 10—Yongding River; 11—Major towns/hydrological station; 12—Guanting Reservoir. A–B and C–D—Locations of hydrogeological cross-sections shown in Figure 2.
Figure 1. (a) Location map of the study area; (b) simplified hydrogeological map of the study area. 1—Quaternary unconsolidated porous aquifers; 2—Jixian System carbonate aquifer; 3—Cambrian carbonate aquifer; 4—Ordovician carbonate aquifer; 5—Carboniferous–Permian–Jurassic clastic porous-fractured aquifers; 6—Groundwater flow direction; 7—Faults or synclinal structures; 8—Karst caves; 9—Spring; 10—Yongding River; 11—Major towns/hydrological station; 12—Guanting Reservoir. A–B and C–D—Locations of hydrogeological cross-sections shown in Figure 2.
Water 17 02292 g001
Water 17 02292 g006
Figure 6. Schematic map of the spatial distribution of preferential groundwater flow paths in the YM Spring catchment area.
Figure 6. Schematic map of the spatial distribution of preferential groundwater flow paths in the YM Spring catchment area.
Water 17 02292 g006
Water 17 02292 g007
Figure 7. Conceptual model of karst groundwater flow pattern and circulation processes in the YM Spring catchment area. Subsurface stratigraphy and hydrogeological units follow the legend provided in Figure 2.
Figure 7. Conceptual model of karst groundwater flow pattern and circulation processes in the YM Spring catchment area. Subsurface stratigraphy and hydrogeological units follow the legend provided in Figure 2.
Water 17 02292 g007
Table 1. Calculation results of local precipitation infiltration in the exposed karst areas of the study area.
Table 1. Calculation results of local precipitation infiltration in the exposed karst areas of the study area.
No.Region 1Area of Exposed Karst Region (km2)Precipitation (mm/year) 2Infiltration CoefficientRecharge Volume (×106 m3)
1J-O25.18622.570.25~0.353.92~5.49
2J-C20.990.20~0.252.61~3.27
3T-O104.98682.600.35~0.4825.08~34.40
4T-C120.230.20~0.2516.41~20.52
Total 271.38 48.03~63.67
Notes: 1 J-O and J-C refer to the Ordovician and Cambrian exposed karst areas in Junzhuang, respectively, and T-O and T-C refer to the Ordovician and Cambrian exposed karst areas in Tanzhesi, respectively. 2 Precipitation data were obtained from meteorological stations located near exposed karst areas for the period 2020–2022.
Disclaimer/Publisher’s Note: The statements, opinions and data contained in all publications are solely those of the individual author(s) and contributor(s) and not of MDPI and/or the editor(s). MDPI and/or the editor(s) disclaim responsibility for any injury to people or property resulting from any ideas, methods, instructions or products referred to in the content.

Share and Cite

MDPI and ACS Style

Sun, Y.; Wang, L.; Zhang, Q.; Dong, Y. Recharge Sources and Flow Pathways of Karst Groundwater in the Yuquan Mountain Spring Catchment Area, Beijing: A Synthesis Based on Isotope, Tracers, and Geophysical Evidence. Water 2025, 17, 2292. https://doi.org/10.3390/w17152292

AMA Style

Sun Y, Wang L, Zhang Q, Dong Y. Recharge Sources and Flow Pathways of Karst Groundwater in the Yuquan Mountain Spring Catchment Area, Beijing: A Synthesis Based on Isotope, Tracers, and Geophysical Evidence. Water. 2025; 17(15):2292. https://doi.org/10.3390/w17152292

Chicago/Turabian Style

Sun, Yuejia, Liheng Wang, Qian Zhang, and Yanhui Dong. 2025. "Recharge Sources and Flow Pathways of Karst Groundwater in the Yuquan Mountain Spring Catchment Area, Beijing: A Synthesis Based on Isotope, Tracers, and Geophysical Evidence" Water 17, no. 15: 2292. https://doi.org/10.3390/w17152292

APA Style

Sun, Y., Wang, L., Zhang, Q., & Dong, Y. (2025). Recharge Sources and Flow Pathways of Karst Groundwater in the Yuquan Mountain Spring Catchment Area, Beijing: A Synthesis Based on Isotope, Tracers, and Geophysical Evidence. Water, 17(15), 2292. https://doi.org/10.3390/w17152292

Note that from the first issue of 2016, this journal uses article numbers instead of page numbers. See further details here.

Article Metrics

Back to TopTop