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Article

Synergistic Detrital Zircon U-Pb and REE Analysis for Provenance Discrimination of the Beach-Bar System in the Oligocene Dongying Formation, HHK Depression, Bohai Bay Basin, China

by
Jing Wang
1,
Youbin He
1,*,
Hua Li
1,
Tao Guo
2,
Dayong Guan
2,
Xiaobo Huang
2,
Bin Feng
3,
Zhongxiang Zhao
1 and
Qinghua Chen
4
1
School of Geosciences, Yangtze University, Wuhan 430100, China
2
China National Offshore Oilfield Corporation Limited-Tianjin, Tianjin 300459, China
3
Changqing Division, China Petroleum Logging Co. Ltd., Xi’an 710021, China
4
School of Geosciences, China University of Petroleum (East China), Qingdao 266580, China
*
Author to whom correspondence should be addressed.
J. Mar. Sci. Eng. 2025, 13(7), 1331; https://doi.org/10.3390/jmse13071331
Submission received: 11 June 2025 / Revised: 7 July 2025 / Accepted: 10 July 2025 / Published: 11 July 2025
(This article belongs to the Section Geological Oceanography)
Browse Figures
Versions Notes

Abstract

The Oligocene Dongying Formation beach-bar system, widely distributed in the HHK Depression of the Bohai Bay Basin, constitutes a key target for mid-deep hydrocarbon exploration, though its provenance remains controversial due to complex peripheral source terrains. To address this, we developed an integrated methodology combining LA-ICP-MS zircon U-Pb dating with whole-rock rare earth element (REE) analysis, facilitating provenance studies in areas with limited drilling and heavy mineral data. Analysis of 849 high-concordance zircons (concordance >90%) from 12 samples across 5 wells revealed that Geochemical homogeneity is evidenced by strongly consistent moving-average trendlines of detrital zircon U-Pb ages among the southern/northern provenances and the central uplift zone, complemented by uniform REE patterns characterized by HREE (Gd-Lu) enrichment and LREE depletion; geochemical disparities manifest as dual dominant age peaks (500–1000 Ma and 1800–3100 Ma) in the southern provenance and central uplift samples, contrasting with three distinct peaks (65–135 Ma, 500–1000 Ma, and 1800–3100 Ma) in the northern provenance; spatial quantification via multidimensional scaling (MDS) demonstrates closer affinity between the southern provenance and central uplift (dij = 4.472) than to the northern provenance (dij = 6.708). Collectively, these results confirm a dual (north–south) provenance system for the central uplift beach-bar deposits, with the southern provenance dominant and the northern acting as a subsidiary source. This work establishes a dual-provenance beach-bar model, providing a universal theoretical and technical framework for provenance analysis in hydrocarbon exploration within analogous settings.

1. Introduction

Sediment provenance analysis serves as a critical approach for deciphering regional tectonic evolution, paleogeographic patterns, and crustal material cycling [1,2,3,4]. Current challenges in this field include the mixed superposition effects of multiple source regions, variations in source-to-sink processes under different tectonic settings, and ambiguous sediment supply—all of which significantly constrain research on the formation mechanisms of sedimentary systems [5,6,7]. In recent years, provenance studies have exhibited an interdisciplinary trend, with increasing applications of isotopic dating and geochemical element analysis [8,9]. Detrital zircon U-Pb dating has developed along various technical pathways [10]. Among these, laser ablation–inductively coupled plasma–mass spectrometry (LA-ICP-MS) has emerged as a rapid and cost-effective method for analyzing mineral isotopic information, making it a prevalent technique in the field of zircon U-Pb geochronology [11,12,13].
In provenance analysis, LA-ICP-MS zircon U-Pb dating effectively traces sediment source regions, thereby providing key insights into basin evolution and basin–range coupling processes [14,15,16]. Furthermore, geochemical element characteristics have been shown to possess substantial indicative value in the context of sediment provenance studies [17,18,19]. Sediments, as fundamental components of Earth’s surface environments, serve as repositories of geological information concerning the properties of the underlying rock formations, the processes of weathering, and the mechanisms of transport. This information is inscribed within their elemental composition. Moreover, distribution patterns and quantitative analyses of rare earth elements (REEs), trace elements, and related parameters (e.g., La/Yb and Ce/Eu ratios) can reveal the tectonic settings, material composition, and paleoenvironmental evolution of source regions [20,21]. REE distribution patterns, characteristic ratios (e.g., La/Yb and Ce/Eu), and isotopic compositions (e.g., Sr, Nd) have been extensively applied to discriminate provenance directions and the degree of mixing in terrigenous clastic rocks [22,23,24]. However, sediment geochemical signatures are influenced by multiple factors (e.g., diagenesis, biological activity, post-depositional alteration), which may lead to ambiguous elemental fractionation. Consequently, the employment of integrated methodologies is imperative to enhance the accuracy of provenance tracing. The combined application of LA-ICP-MS zircon U-Pb dating and geochemical element analysis provides high-precision chronological constraints and geochemical fingerprints, enabling confirmation of primary sediment sources and construction of robust sediment supply models [25,26].
The central uplift zone of the HHK Depression, Bohai Bay Basin, China (Figure 1), contains widespread, thin, and continuous Oligocene Dongying Formation beach-bar deposits—primary reservoirs for mid-deep hydrocarbon exploration [27]. However, the complex provenance systems surrounding the depression have obscured sediment sources of these deposits, leading to persistent debate regarding sandbody genesis. Existing literature remains inconclusive: some studies attribute the primary sediment source to braided river delta systems along the northern steep slope [28], while others propose dominant southern gentle-slope provenance systems [29]. A third perspective suggests bidirectional (north–south) sediment supply [30]. Notwithstanding, there are as yet unresolved knowledge gaps regarding provenance directions and supply capacity. Existing studies primarily rely on singular approaches such as stratigraphic thickness analysis [31,32], paleogeomorphic reconstruction, and sedimentary facies comparison [33,34,35]. Given the limitations of traditional provenance methods and the insufficiency of heavy mineral data, this study employs a multifaceted approach that integrates LA-ICP-MS zircon U-Pb dating with comprehensive whole-rock rare earth element (REE) distribution patterns. This multidisciplinary approach systematically analyzes detrital zircon age spectra and REE characteristics of the Dongying Formation within the HHK Depression, aiming to (1) resolve provenance ambiguities of the beach-bar system, (2) clarify source composition and temporal evolution, (3) establish a robust depositional model, and (4) provide insights for provenance studies in analogous basins.

2. Regional Geological Setting

The HHK Depression is situated in the eastern Bohai Bay Basin, China (Figure 1a,b), and is bordered by the Bonan Uplift to the north, the Kendong Uplift to the southwest, the Laibei Uplift to the southeast, and the Miaoxi Depression to the east [36,37]. This depression, which is significant in terms of its hydrocarbon richness, is located within the Bohai Sea area (Figure 1c). The depression primarily features nearly EW-trending extensional fault systems and NNE-trending strike-slip fault systems, forming secondary structural zones including the northern steep slope zone, southern gentle slope zone, central strike-slip zone, and central uplift zone. The internal sub-sags are further subdivided into three distinct categories: the southwestern, northwestern, and eastern sub-depression (Figure 1c).
During the Paleogene rifting–subsidence stage, the Bohai Sea area exhibited a tectonic paleogeomorphology characterized by alternating horsts and grabens. Rifting in this region progressed in an episodic manner and can be subdivided into four extensional phases corresponding to the depositional periods of the Kongdian Formation: fourth member of the Shahejie Formation (E1k-E2s4), third member of the Shahejie Formation (E2s3), second–first members of the Shahejie Formation (E3s2-E3s1), and Dongying Formation (E3d). The HHK Depression preserves a relatively complete Paleogene stratigraphic succession, comprising (in ascending order) the Kongdian Formation (E1k), the fourth to the first member of the Shahejie Formation (E2s4-E3s1), and the third to the first member of the Dongying Formation (E3d3-E3d1). These formations are overlain by the Neogene Guantao (Ng) and Minghuazhen (Nm) formations and Quaternary (Q) deposits [38] (Figure 1d).
The Paleogene initial Rifting Episode I in the Bohai Bay Basin was constrained by low crustal extensional intensity and a dispersed fault depression pattern. The activity rates of basin-controlling faults were generally low (<100 m/Ma), resulting in isolated, restricted distributions of coeval deposits from the Kongdian Formation (E1k) to the fourth member of the Shahejie Formation (E2s4). In contrast, during Rifting Episodes II–III (corresponding to the third member of the Shahejie Formation, E2s3, to the Dongying Formation, E3d), enhanced fault activity (peak rates >300 m/Ma) and lacustrine basin interconnection promoted extensive coverage expansion of sedimentary systems. This led to the development of widely distributed lacustrine to deltaic systems across the entire basin [38,39,40]. Strong tectonic differential activity and significant topographic relief during the Sha-3 Member (E2s3) favored the development of fan-delta and braided-river delta systems. Reduced tectonic activity and subdued topography from the Sha-2 Member (E3s2) to the Sha-1 Member (E3s1) diminished the scale and abundance of fan deltas while increasing the prevalence of braided-river deltas [39]. The Sha-2 Member (E3s2) primarily developed braided-river delta systems with locally mixed beach-bar deposits. The Sha-1 Member (E3s1) inherited the depositional characteristics of the underlying Sha-2 Member (E3s2). However, increased water depth led to a reduction in overall delta scale, thereby shifting the system toward shore-shallow lacustrine deposition with localized beach-bar accumulations [40] (Figure 2a,c).
During the depositional phase of the Dong-3 Member (E3d3), the region experienced fault reactivation and large-scale lacustrine transgression triggered by tectonic activity. These processes resulted in the formation of thick mudstones interbedded with thin sandstones/siltstones, as well as localized braided-river deltas and beach-bar deposits [30]. The Dong-2 Member (E3d2) witnessed attenuated basin subsidence, a shallowing paleo-water depth, and accelerated delta progradation, accompanied by intensified lake-wave reworking. This resulted in expanded beach-bar development, forming braided-river delta–beach-bar depositional systems [41,42]. Late Dongying Formation deposition was accompanied by weakened depression subsidence and rapid delta progradation, leading to lake-basin shrinkage and the dominance of shallow-water deltaic environments [43]. This study focuses on the braided-river delta–beach-bar system of the Dong-3 to Dong-2 Members (E3d3 to E3d2) (Figure 2b,c).

3. Materials and Methods

Samples were collected from Paleogene Dongying Formation sandstones in boreholes within the HHK Depression. Twelve sandstone samples were obtained from five wells: Z1-1, N1-1, N1-2, S1-1, and S1-2 (Figure 1c), yielding 1243 analytical points, of which 849 were valid (concordance >90%), representing a validity rate of 68.3% (Table 1; Supplementary Tables S1–S5). Details of the obtained samples are as follows (Figure 3):
Z1-1 well: Core depths 3420 m, 3450 m, 3470 m, 3490 m, and 3515 m; lithology: siltstone–fine sandstone.
N1-1 well: Core depths 3070 m, 3080 m, 3165 m; lithology: fine sandstone.
N1-2 well: Core depth 3190 m; lithology: siltstone–fine sandstone.
S1-1 well: Core depths 3010 m, 3250 m; lithology: fine sandstone.
S1-2 well: Core depth 3000 m; lithology: medium–coarse sandstone.
Zircon separation, mount preparation, and analyses were conducted at the Bohai Laboratory Center, CNOOC Engineering Technology Branch, under controlled conditions (23 ± 2 °C; 35–50% humidity). Key instrumentation included a laser ablation system (LSX-213 G2+; Serial: 51801) and an inductively coupled plasma-mass spectrometer (Agilent 7800; Serial: SG19253814). For U-Pb dating, zircon domains with clear zoning and no fractures or inclusions were targeted. Laser ablation-inductively coupled plasma mass spectrometry (LA-ICP-MS) was performed using a 30-μm beam diameter. Detrital zircons with 90–100% concordance were assigned 207Pb-based (207Pb/206Pb) corrected ages, while discordant data (<90%) were excluded [44,45,46].
For data processing, external standardization used Plesovice zircon for U-Pb ratio correction (instrumental mass bias), and trace element calibration employed 91,500 zircon along with NIST610-614 glass standards. Isotope and element calculations were performed using the ICP-MS-Data-Cal and Excel 2010 modules, while Isoplot 3.0 was used to generate concordia plots, age probability density functions, and weighted mean ages, following international microbeam U-Pb geochronology standards.
For REE analysis, concentrations were quantified via ICP-MS [47,48] following laser ablation and aerosol nebulization. Normalization used the North American Shale Composite (NASC) for LaN/YbN, δEu, and δCe [47,48,49] (Table 2), which was prioritized over chondrite normalization due to its suitability in hydrocarbon exploration contexts (as opposed to optimization for magmatic differentiation or mantle evolution studies).

4. Results

4.1. LA-ICP-MS Zircon Age Characteristics

Statistical analysis of zircon samples (Table 1; Supplementary Tables S1–S5) revealed zircon counts per well as follows: Z1-1 (118), N1-1 (377), N1-2 (101), S1-1 (139), and S1-2 (56). The Concordia diagram for detrital zircon U-Pb ages from the Dongying Formation in the HHK Depression demonstrates that the majority of analytical points plot on or near the concordia curve (concordance > 90%; Figure 4), indicating closed U-Pb isotopic systems with minimal post-crystallization U/Pb mobility.
Detrital zircon U-Pb ages range from 65 to 3500 Ma, exhibiting three dominant age peaks: 65–135 Ma, 500–1000 Ma, and 1800–3100 Ma (weighted mean ages: 137.3 Ma, 689 Ma, and 2339 Ma, respectively). Age distribution histograms (0–3500 Ma) and stratigraphic column charts (Mesozoic, Paleozoic, Neoproterozoic, Mesoproterozoic/Paleoproterozoic/Neoarchean), along with moving average trend lines, were constructed for the northern and southern source areas as well as the central uplift zone (Table 3; Figure 5).
The relative proportions of zircon ages in the Mesoproterozoic–Neoarchean range are 63% in the central uplift zone, 69% in the southern source area, and 71% in the northern source area. For the Neoproterozoic, the proportions are 20% (central), 18% (south), and 21% (north). Paleozoic zircon populations account for 9% in both the central and southern zones, but only 3% in the north. Mesozoic zircons make up 8% of the central uplift assemblage, 3% of the southern, and 5% of the northern. The moving average trends reveal generally consistent zircon evolution across all wells. However, age spectra (Figure 6) show distinct differences: the N1-1 and N1-2 wells in the north display prominent triple age peaks, while Z1-1, S1-1, and S1-2, representing the central uplift and southern areas, exhibit only dual peaks (500–1000 Ma and 1800–3100 Ma), with the 65–135 Ma peak being relatively weak.

4.2. Whole-Rock REE Abundance Analysis

Fifteen Dongying Formation sandstone samples exhibit high total rare earth element (ΣREE) concentrations, ranging from 616.36 to 1535.31 ppm, and significant light-to-heavy REE fractionation (LREE/HREE = 0.05–0.13; Table 2, Figure 7). North American Shale Composite (NASC)-normalized REE patterns show the following features: Extreme La depletion and Yb enrichment (LaN/YbN = 0.0002–0.0048; mean 0.0011); HREE enrichment (Gd-Lu) with left-leaning patterns (Figure 7); negative Eu anomalies (δEu = 0.43–0.61; mean 0.54); positive Ce anomalies (δCe = 1.69–13.99; mean 6.07) [50,51,52].
Statistical analysis of rare earth element (REE) data reveals significant negative Eu anomalies and positive Ce anomalies. During magmatic differentiation, Eu2+ preferentially partitions into the melt phase due to its geochemical affinity, resulting in Eu depletion within residual solid phases and subsequent magmatic rocks. The relatively consistent δEu values (mean = 0.54) indicate magmatic processes exert dominant control. However, post-magmatic hydrothermal alteration may further modify Eu distribution. Hydrothermally mediated selective dissolution–reprecipitation reactions can remobilize Eu, potentially exacerbating observed Eu depletion in samples [50,51,52].
The broad range of positive Ce anomalies (δCe = 1.69–13.99) reflects multifactorial controls wherein reducing conditions are essential for stabilizing Ce3+, as kinetic hindrance under anoxic/suboxic environments suppresses oxidation of Ce3+ to insoluble Ce4+. This enables persistent aqueous residence and preferential enrichment of Ce3+, thereby generating positive Ce anomalies, while organic matter or specific reductants in sedimentary systems may further enhance Ce3+ stability through complexation reactions to elevate δCe values. Concurrently, the influx of Ce-enriched hydrothermal fluids substantially enhances sedimentary Ce concentrations, with fluid–rock interactions during hydrothermal events facilitating Ce mobilization and precipitation that further enriches Ce within the sedimentary record. These coupled processes—including redox stabilization, hydrothermal influx, and reactive transport—collectively govern the observed broad δCe variability [53,54].

5. Discussion

5.1. Provenance Analysis

Detrital zircon age spectra, histograms, and relative probability curves reveal consistent evolutionary trends with localized variations across the three studied regions (Figure 5). The northern potential source area exhibits three distinct age peaks (65–135 Ma, 500–1000 Ma, 1800–3100 Ma), whereas the central uplift zone and southern potential source area show only two prominent peaks (500–1000 Ma, 1800–3100 Ma), with a weakly developed 65–135 Ma peak. This pattern suggests an altered or diminished sediment supply from the northern source area.
The aforementioned study analyzed sediment supply characteristics from northern and southern potential provenances based on feature similarity, preliminarily revealing a bidirectional (north–south) provenance supply system for the Paleogene Dongying Formation beach-bar system in the HHK Depression. Notably, zircon signatures from the southern provenance exhibit closer affinity with those of the central uplift zone, indicating its dominance within the provenance framework.
To further elucidate supply disparities between these provenances, multidimensional scaling (MDS) was employed to transform detrital zircon age spectra into three-dimensional spatial coordinates [55]. This approach quantifies sediment kinship through spatial distances governed by the core equation:
d i j = ∑ k = 1 p ( x i k − x j k ) 2 ≈ y i − y j
dij—The Bray–Curtis dissimilarity between samples;
yi—3D projection coordinates.
The 3D MDS plot and associated distance matrix quantification demonstrate that the central uplift zone derives sediment bidirectionally from southern and northern provenances, with closer spatial proximity to the southern provenance (dij = 4.472) versus greater separation from the northern provenance (dij = 6.708). This spatial metric confirms the southern provenance as the dominant sediment source, while the northern provenance provides subsidiary inputs (Table 4, Figure 8).
Comparative analysis of whole-rock rare earth element (REE) patterns from the southern potential provenance, northern potential provenance, and central uplift zone in the Dongying Formation of the HHK Depression reveals consistent heavy rare earth element (HREE, Gd-Lu) enrichment and left-leaning curve characteristics in both southern-central (Figure 7a) and northern-central (Figure 7b) profiles [56,57]. This uniformity indicates identical REE distribution modes across all three domains.
Integrated assessment of detrital zircon age distributions, whole-rock REE patterns, and multidimensional scaling (MDS) analysis demonstrates (1) feature homogeneity: moving-average trendlines of detrital zircon U-Pb ages and REE distribution patterns exhibit strong consistency among the southern/northern provenances and central uplift zone; (2) local disparities: zircon spectra from both the southern provenance and central uplift zone display two dominant age peaks, while the northern provenance exhibits three distinct age peaks; (3) MDS spatial quantification: The 3D MDS distance matrix of zircon U-Pb age spectra demonstrates closer spatial proximity between the southern provenance and central uplift zone (dij = 4.472), whereas the northern provenance shows greater separation (dij = 6.708). Synthesizing this evidence, the beach-bar system in the central uplift zone of the HHK Depression derives from a bidirectional (north–south) sediment supply system. Critically, the southern provenance serves as the dominant sediment source, with the northern provenance providing subsidiary inputs.

5.2. Depositional Model

Building upon the established provenance framework and integrating sedimentary environments with tectonic evolution characteristics of the Paleogene HHK Depression [58,59], a dual-provenance-controlled sandbody distribution model has been developed for the Dongying Formation beach-bar system. The Kendong Uplift (south) and Bonan Uplift (north) functioned as regional sediment sources governing delta development along the southern gentle slope and northern steep slope zones, respectively. During Dongying Formation deposition, the basin underwent rift-depression transition, forming braided-river delta–lacustrine systems under the influence of southern (Kendong Uplift) and northern (Bonan Uplift) source-to-sink systems, with beach-bar systems developing in the central uplift zone (Figure 2).
Sands from braided-river deltas along the southern gentle slope and northern steep slope were reworked by lake waves and alongshore currents [60,61,62,63]. These sediments were subsequently redeposited in the central uplift zone—an ‘intra-depression low uplift’ area with attenuated wave energy—forming extensive beach-bar complexes [64,65]. This study confirms the southern provenance as the predominant sediment source, with the southern-slope braided-river delta constituting the primary origin for the central uplift beach-bar system. Conversely, the northern provenance provided subsidiary inputs, with the northern steep-slope delta making relatively minor contributions (Figure 9).

6. Conclusions

(1) The detrital zircon U-Pb age moving average trends of the northern and southern potential provenances and the central uplift belt in the Paleogene Dongying Formation of the HHK Depression are consistent. Whole-rock rare earth element (REE) patterns across all three areas are uniform, characterized by heavy rare earth element (HREE: Gd-Lu) enrichment and a left-leaning REE distribution curve. Detrital zircon age spectra reveal three significant peaks (65–135 Ma, 500–1000 Ma, 1800–3100 Ma) in the northern provenance, whereas the central uplift belt and southern provenance exhibit only two dominant peaks (500–1000 Ma, 1800–3100 Ma) with a weak Mesozoic peak. Multidimensional scaling (MDS) spatial quantification of zircon U-Pb dating indicates significantly closer spatial affinity between the central uplift zone and southern provenance (dij = 4.472) than with the northern provenance (dij = 6.708).
(2) Integrated LA-ICP-MS zircon U-Pb dating and whole-rock REE analyses reveal consistent overall variation patterns among the southern/northern provenances and the central uplift belt. This confirms a dual-provenance system (northern and southern) for the bar-beach system in the central uplift belt of the HHK Sag. Detrital zircon age comparative analysis further indicates differential sediment supply capacities: the southern provenance functions as the primary sediment source, while the northern provenance constitutes a secondary contributor.
(3) A “dual-provenance differential supply model” for the bar-beach system has been established. Under an intra-depression low-uplift tectonic setting, the Kendong Uplift (south) and Bonan Uplift (north) control the development of gentle-slope braided river deltas and steep-slope fan deltas, respectively. Lacustrine waves and coastal currents rework delta-front sands, which are subsequently redeposited in the weak hydrodynamic zone of the central low-uplift belt to form the bar-beach system. This model provides a theoretical basis for predicting deeply buried bar-beach systems and has significant implications for hydrocarbon exploration in similar faulted basins.

Supplementary Materials

The following supporting information can be downloaded at: https://www.mdpi.com/article/10.3390/jmse13071331/s1, Table S1: Zircon LA-ICP-MS U-Pb Age Data of Well Z1-1; Table S2: Zircon LA-ICP-MS U-Pb Age Data of Well N1-1; Table S3: Zircon LA-ICP-MS U-Pb Age Data of Well N1-2; Table S4:Zircon LA-ICP-MS U-Pb Age Data of Well S1-1; Table S5: Zircon LA-ICP-MS U-Pb Age Data of Well S1-2.

Author Contributions

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

Funding

This research was funded by the National Natural Science Foundation of China, grant numbers 42272115 and 42272113 and the National Key Technologies R&D Program of China during the 14th Five-Year Plan Period, grant number CCL2022TJT0NST1867).

Data Availability Statement

The original contributions presented in this study are included in the article/Supplementary Material. Further inquiries can be directed to the corresponding author(s).

Acknowledgments

We would like to extend our gratitude to CNOOC (China) Tianjin Branch Bohai Petroleum Research Institute for their invaluable administrative and technical support, which facilitated the completion of this study. Additionally, we appreciate the kind donations of experimental materials provided by the School of Geosciences, Yangtze University, without which the research would not have been possible.

Conflicts of Interest

Author T.G., D.G., X.H. were employed by the company China National Offshore Oilfield Corporation Limited-Tianjin. Author B.F. was employed by the Changqing Division, China Petroleum Logging Co. Ltd. The remaining authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.

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Jmse 13 01331 g001
Figure 1. Structural location and stratigraphic column of HHK Depression in the Bohai Bay Basin (revised following [20,21]; the tectonic zoning was refined based on fault distribution patterns documented in the literature to ensure its accuracy. The red box in the figure indicates the target layer). (a) Regional location of the Bohai Bay Basin; (b) location of the HHK Depression; (c) the structural division of the HHK Depression; (d) composite stratigraphic column of the Paleogene Shahejie and Dongying formations in the HHK Depression.
Figure 1. Structural location and stratigraphic column of HHK Depression in the Bohai Bay Basin (revised following [20,21]; the tectonic zoning was refined based on fault distribution patterns documented in the literature to ensure its accuracy. The red box in the figure indicates the target layer). (a) Regional location of the Bohai Bay Basin; (b) location of the HHK Depression; (c) the structural division of the HHK Depression; (d) composite stratigraphic column of the Paleogene Shahejie and Dongying formations in the HHK Depression.
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Figure 2. Depositional system characteristics of the Shahejie and Dongying Formations (Paleogene), HHK Depression. (a) Planar distribution of the Shahejie Formation depositional systems; (b) planar distribution of the Dongying Formation depositional systems; (c) profile distribution of sandbody vertical well correlation between the Shahejie and Dongying Formations.
Figure 2. Depositional system characteristics of the Shahejie and Dongying Formations (Paleogene), HHK Depression. (a) Planar distribution of the Shahejie Formation depositional systems; (b) planar distribution of the Dongying Formation depositional systems; (c) profile distribution of sandbody vertical well correlation between the Shahejie and Dongying Formations.
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Figure 3. Lithological histogram of boreholes, physical core photographs, and sampling locations.
Figure 3. Lithological histogram of boreholes, physical core photographs, and sampling locations.
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Figure 4. Concordia diagram of detrital zircon U-Pb ages (concordance > 90%) from Dongying Formation samples in the HHK Depression.
Figure 4. Concordia diagram of detrital zircon U-Pb ages (concordance > 90%) from Dongying Formation samples in the HHK Depression.
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Figure 5. Detrital zircon U-Pb ages obtained from samples of the Dongying Formation samples in the HHK Depression. (a) Samples from Well N1-1. (b) Samples from Well N1-2. (c) Samples from Well Z1-1. (d) Samples from Well S1-2. (e) Samples from Well S1-1.
Figure 5. Detrital zircon U-Pb ages obtained from samples of the Dongying Formation samples in the HHK Depression. (a) Samples from Well N1-1. (b) Samples from Well N1-2. (c) Samples from Well Z1-1. (d) Samples from Well S1-2. (e) Samples from Well S1-1.
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Figure 6. Histogram and moving average trendline of zircon age distribution.
Figure 6. Histogram and moving average trendline of zircon age distribution.
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Figure 7. NASC-normalized REE distribution patterns of the Dongying Formation in the HHK Depression: (a) southern potential provenance and central uplift zone; (b) northern potential provenance and central uplift zone.
Figure 7. NASC-normalized REE distribution patterns of the Dongying Formation in the HHK Depression: (a) southern potential provenance and central uplift zone; (b) northern potential provenance and central uplift zone.
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Figure 8. Three-dimensional MDS diagram of zircon U-Pb age in HHK Depression. The axes are dissimilarities measured between samples.
Figure 8. Three-dimensional MDS diagram of zircon U-Pb age in HHK Depression. The axes are dissimilarities measured between samples.
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Figure 9. Structural and depositional system map showing well location distribution in the HHK Depression.
Figure 9. Structural and depositional system map showing well location distribution in the HHK Depression.
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Table 1. LA-ICP-MS dating sample statistics of detrital zircons from the Dongying Formation in the HHK Depression (detailed data are shown in Tables S1–S5).
Table 1. LA-ICP-MS dating sample statistics of detrital zircons from the Dongying Formation in the HHK Depression (detailed data are shown in Tables S1–S5).
Well NameSampling Depth (m)Number of SpotsValid DataProportion (%)
Z1-13420937581%
3450936166%
3470907684%
34901048582%
35151098073%
N1-130701357556%
3080933437%
3165926773%
N1-2319012310182%
S1-13010966265%
32501077772%
S1-230001085652%
Table 2. REE concentrations (ppm) of detrital rocks from the Dongying Formation in the HHK Depression (REE patterns normalized to NASC).
Table 2. REE concentrations (ppm) of detrital rocks from the Dongying Formation in the HHK Depression (REE patterns normalized to NASC).
Tectonic DivisionSample IDLaCePrNdSmEuGdTbDyHoErTmYbLu∑REELREEHREELREE/HREELaN/
YbN		δEuδCe
Central uplift zoneZ10.280.710.240.291.231.535.611.122138.452.4176.66115.97153.7918.9781.48837.490.10.00240.582.76
Z20.030.420.050.110.921.25.039.9319.2536.1750.2973.14112.51145.77841.242.61798.60.050.00020.5612.3
Z30.050.340.070.110.650.783.426.9413.5426.0136.1456.1190.45114.76643.2335.67607.560.060.00060.525.85
Z40.570.860.450.481.251.355.410.6420.3438.0852.6977.77119.75159.09956.97108.86848.110.130.00480.521.69
Z50.220.520.170.210.880.944.378.9717.3633.245.568.06104.41133.99791.3259.41731.910.080.00210.482.7
Southern gentle slope zoneS10.040.470.060.130.90.994.528.9617.3532.945.2966.82103.34132.16773.7546.99726.760.060.00040.499.55
S20.010.290.030.080.660.643.447.0213.6225.8835.9654.0985.72106.06616.3628.77587.590.050.00020.4313.99
S30.040.410.070.120.851.024.298.6816.8532.244.9366.96104.63137.93769.6742.08727.590.060.00040.537.75
S40.050.480.080.140.871.084.278.6616.8232.4745.4168.35106.77139.6785.5748.21737.360.070.00050.567.07
S50.180.850.250.341.672.258.0814.7833.769.1285.79131.01212.13261.551535.3193.241442.070.060.00090.614.01
S60.050.350.060.120.80.864.087.4413.437.1736.7453.6786.89115.79649.4836.89612.590.060.00060.486.2
Northern steep slope zoneN10.030.350.060.130.961.394.99.3918.1333.8845.8671.03111.35148.52809.6938.84770.850.050.00030.647.58
N20.190.550.20.271.11.265.139.128.0433.3145.4369.97105.34146.74865.8164.57801.240.080.00180.532.88
N30.150.60.180.271.351.676.1611.2823.6442.9761.5290.64142.08183.251060.468.29992.110.070.0010.583.66
N40.210.570.160.221.031.355.6811.1921.9242.1560.4187.62152.01187.261071.864.571007.230.060.00140.563.08
Table 3. Statistical summary of U-Pb geochronology for detrital zircons from the Dongying Formation, HHK Depression.
Table 3. Statistical summary of U-Pb geochronology for detrital zircons from the Dongying Formation, HHK Depression.
Tectonic DivisiononWell NameSampling Depth (m)Zircon Age Range (Ma)Geological Era
MesozoicPaleozoicNeoproterozoicMesoproterozoic/Paleoproterozoic/Neoarchean
Central uplift zoneZ1-1342065–135500–10001800–310012181134
3450—570–10001800–3100001150
3470135–250550–8501800–3100132952
349065–250500–10001800–31006102742
3515—500–10001800–3100051659
Zircon U-Pb age populations (%)0.080.090.20.63
Southern gentle slope zoneS1-1325065–135500–8001800–3100111263
301065–250500–8001800–31005161823
S1-23000 570–10001800–310001649
Zircon U-Pb age populations (%)0.030.090.180.69
Northern steep slope zoneN1-13070——1800–385010371
3080——1800–385000277
316565–250570–10001800–3100351445
N1-2319065–250500–8001800–31001121573
Zircon U-Pb age populations (%)0.050.030.210.71
Table 4. Distance matrix of three-dimensional MDS diagram for zircon U-Pb ages of the Dongying Formation, HHK Depression.
Table 4. Distance matrix of three-dimensional MDS diagram for zircon U-Pb ages of the Dongying Formation, HHK Depression.
Tectonic DivisionCentral Uplift ZoneSouthern Potential
Provenance		Northern Potential
Provenance
Central uplift zone04.4726.708
Southern potential
provenance		4.47206.782
Northern potential
provenance		6.7086.7820
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Wang, J.; He, Y.; Li, H.; Guo, T.; Guan, D.; Huang, X.; Feng, B.; Zhao, Z.; Chen, Q. Synergistic Detrital Zircon U-Pb and REE Analysis for Provenance Discrimination of the Beach-Bar System in the Oligocene Dongying Formation, HHK Depression, Bohai Bay Basin, China. J. Mar. Sci. Eng. 2025, 13, 1331. https://doi.org/10.3390/jmse13071331

AMA Style

Wang J, He Y, Li H, Guo T, Guan D, Huang X, Feng B, Zhao Z, Chen Q. Synergistic Detrital Zircon U-Pb and REE Analysis for Provenance Discrimination of the Beach-Bar System in the Oligocene Dongying Formation, HHK Depression, Bohai Bay Basin, China. Journal of Marine Science and Engineering. 2025; 13(7):1331. https://doi.org/10.3390/jmse13071331

Chicago/Turabian Style

Wang, Jing, Youbin He, Hua Li, Tao Guo, Dayong Guan, Xiaobo Huang, Bin Feng, Zhongxiang Zhao, and Qinghua Chen. 2025. "Synergistic Detrital Zircon U-Pb and REE Analysis for Provenance Discrimination of the Beach-Bar System in the Oligocene Dongying Formation, HHK Depression, Bohai Bay Basin, China" Journal of Marine Science and Engineering 13, no. 7: 1331. https://doi.org/10.3390/jmse13071331

APA Style

Wang, J., He, Y., Li, H., Guo, T., Guan, D., Huang, X., Feng, B., Zhao, Z., & Chen, Q. (2025). Synergistic Detrital Zircon U-Pb and REE Analysis for Provenance Discrimination of the Beach-Bar System in the Oligocene Dongying Formation, HHK Depression, Bohai Bay Basin, China. Journal of Marine Science and Engineering, 13(7), 1331. https://doi.org/10.3390/jmse13071331

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