The Discovery and Geochemical Characteristics of an Eocene Peridotite Xenolith-Bearing Mafic Volcanic Neck in Coastal Southeast China

1 Introduction

Continental lithosphere is an important component of the Earth, and peridotite xenoliths captured by rapidly ascending basaltic magmas produced in some tectonic environments can provide direct samples of the upper mantle or lower crust of continental lithosphere. Such xenoliths also provide evidence of the nature and evolution of the mantle, the composition of the mantle, and the tectonic setting of the basaltic magmatism that captured the xenoliths. There are two main models for the petrogenesis of peridotite xenoliths: 1) they represent the refractory residue of the upper mantle after partial melting that generated basaltic magmas (Wang and Yang, 1987a; Wang and Yang., 1987b; Deng et al., 1988; Cong et al., 1996; Yan et al., 2007), or 2) they represent rock fragments of the upper mantle that were captured by ascending basaltic magma as accidental enclaves, meaning they played no direct role in the formation of the basaltic magmas (Tatsumoto et al., 1992; C. ; Liu et al., 1995; T. ; Li and Ma, 2002).

Southeastern China has a complex geological history that includes late Mesozoic to Cenozoic lithospheric thinning and extensive basaltic magmatism. This magmatism peaked in coastal SE China after the late Mesozoic and has been the focus of many studies (Cui et al., 2011; C. ; Liu et al., 1995; Tang et al., 2010; G. ; Xie et al., 2005; Xing et al., 1999; J. ; Yan et al., 2005a; Zhou et al., 2006), including a large body of research devoted to the nature of the mantle during this magmatism (D. Chen et al., 1997; C. Chen et al., 2008; C. Dong C. W. et al., 2006; C. Dong Y. X. et al., 2006; He and Xu, 2011; Li, 2000; Z. Li and Li, 2007; X. Li et al., 2007; J. Liu and Yan, 2007; Shen et al., 1999; D. Y. Wang et al., 2002; D.Z. Wang and Shen, 2003; Xiao et al., 2006; X. Xu et al., 2008; W. Zhang and Fang, 2014; Zhi and Qin, 2004; Zhi et al., 1994). This previous research focused on the Late Cretaceous and Miocene mantle in this area and was based on mantle xenoliths obtained mainly from late Neogene basaltic rocks. Peridotite xenoliths also occur within post-Neogene alkaline basalts that have been used to characterize the Cenozoic evolution of the mantle beneath SE China (Bodinier and Garrido, 2008; C. ; Dong et al., 1997; Z. ; Dong et al., 1999; X. ; Wang et al., 2012).

However, the Paleogene (and especially the Eocene) evolution of the mantle in this area is poorly known, primarily due to the rarity of basic rocks hosting mantle xenoliths that formed at this time, meaning that the characteristics and the evolution of the Cretaceous to Neogene mantle beneath coastal SE China are uncertain.

Rare peridotite xenoliths are present within Mesozoic and Paleogene basalts in coastal SE in China (Figure 1), including peridotite xenoliths within Mesozoic basalts of the Fuxin area of Liaoning Province, the Daoxian area in Hunan Province, and the Daxizhuang area of eastern Shandong Province (Guo et al., 2013a; Guo et al., 2013b; Pei et al., 2004; D. Y. ; Wang et al., 2002; Xia et al., 2010; W. ; Xu et al., 2013; J. ; Yan et al., 2005a; G. ; Yang et al., 2012; J. ; Ying et al., 2010; J. ; Ying et al., 2013; X. ; Yang et al., 2008; Zheng et al., 1999; Q.J. ; Zhou et al., 2013). Previous research on this Mesozoic mantle has been based on inference, meaning the characteristics of this mantle source region are poorly constrained.

FIGURE 1

FIGURE 1. Temporal and spatial distribution of late Mesozoic–Cenozoic basalts in SE China (revised after Xu and Xie, 2005). (A) Temporal and spatial distribution of late Mesozoic basalts in SE China; (B) Temporal and spatial distribution of Cenozoic basalts in SE China.

A mafic volcanic neck located in the Fuding area of coastal SE China, within the southern section of the Cretaceous Fuding volcanic basin, is associated with a Mesozoic tectono-magmatic belt that is controlled by the NE–SW striking Fuding–Fuqing Fault. The Fuding basalts were erupted onto volcanic rocks of the lower Shimaoshan Formation (Figure 2), contain peridotite xenoliths, and were assigned by L. Li et al. (2011) to the late Oligocene to middle Pleistocene Fotan Group.

FIGURE 2

FIGURE 2. Tectonic and geological maps of the Fuding area, Fujian province (adapted from Dai and Chen, 2008).

Here, we present new whole-rock Ar–Ar ages and geochemical data for mafic rocks from the Fuding mafic volcanic neck. These data constrain the formation age and tectonic setting of the Fuding mafic rocks, which contain peridotite xenoliths that provide clues to the characteristics of the Eocene mantle and to the post late-Mesozoic evolution of the mantle in coastal SE China.

2 Geological Background and Petrological Characteristics

The Fuding mafic volcanic neck is oval shaped and has a long axis that trends NW–SW, with a length of 790 m, a width of 420 m (Figure 2), and with clearly developed columnar joints. The neck is divided into three facies: an outermost eruption facies basaltic breccia volcano, an intermediate effusive facies basalt, and an innermost central neck facies volcano containing olivine-bearing gabbro–diabase rocks (Figure 3A). The neck contains basaltic volcanic breccias, basalts, gabbros, and diabasic rocks. The lithofacies within the neck are heterogeneously distributed, with a columnar jointed cumulate gabbro section located above the diabase (Figures 3B,C). The geological characteristics of the neck are as follows.

FIGURE 3

FIGURE 3. Photographs showing typical characteristics of the Fuding mafic volcanic neck. (A) Contact between basalts and units of the Shimaoshan Group, showing a maroon baked margin, (B) columnar-jointed gabbro and diabase, (C) general characteristics of the cumulate-textured Fuding gabbro, (D) rounded peridotite xenoliths within the layered basalt.

2.1 Volcanic Breccia

The volcanic breccias are gray–black, are brecciated and massive, and are dominated by breccias and crystals in a basaltic matrix. The rocks comprise angular–subangular breccia (60%–70% of the rock mass), and crystals (10%) of olivine, clinopyroxene, spinel, and others (Figure 4A) in a basaltic matrix (20%) containing skeletal crystals.

FIGURE 4

FIGURE 4. Representative photomicrographs showing typical petrographic features of the Fuding mafic volcanic neck. (A) Typical basaltic breccia, (B) olivine and clinopyroxene phenocrysts within basalt, (C) olivine phenocrysts within vesicular basalt, (D) clinopyroxene phenocrysts overprinting olivine within cumulate-textured gabbro, (E) zoned clinopyroxene phenocrysts within cumulate-textured gabbro, (F) diabasic textured diabase, (G) diabasic and intersertal textured diabase, (H) diabasic textured diabase, (I) diabasic textured diabase containing twinned clinopyroxene, (J) granular mosaic textured and zoned clinopyroxene phenocrysts, (K) peridotite xenoliths with small olivines enclosed by clinopyroxene, (L): peridotite xenoliths and olivines containing visible kink banding.

2.2 Basalt

The basalt is gray–black, porphyritic, and has an almond-shaped structure. These rocks contain olivine (0.3–3 mm in size), clinopyroxene, and plagioclase phenocrysts that form 10%–20% of the rock. The amygdales in the basalt are filled with zeolite (Figures 4B,C), and both amygdales and phenocrysts are hosted by an intergranular matrix that contains clinopyroxene (50%–55%), olivine (5%), feldspar (12%–15%), basaltic glass (15%), and minor ilmenite. The presence of basaltic glass indicates that the basaltic magma underwent rapid cooling to form a rock with minor amounts of iddingsite and chlorite alteration.

These basalts contain many rounded peridotite xenoliths (Figure 3D) that are generally 3–15 cm across (largest, 20 cm). The xenoliths are spinel lherzolites with a subhedral granular texture (Figures 4J–L) and they contain olivine (95%) with minor amounts of spinel, clinopyroxene, and orthopyroxene (<5%).

2.3 Gabbro

The gabbro is dark–gray, medium-grained, and has a cumulate gabbroic texture. The largest phenocrysts are ∼15 mm in diameter and the rock contains 60%–80% phenocrysts, mainly plagioclase, clinopyroxene, and olivine with minor and localized alkali feldspar. The clinopyroxenes are subhedral, columnar (Figures 4D,E), zoned, and make up 15%–20% of the rock, whereas the plagioclase (25%–30%) is euhedral–subhedral and columnar, 0.2–6 mm in size, has clear polysynthetic twinning. The olivine gabbro is subhedral–subhedral, granular, and overprinted by the development of clinopyroxene megacrysts, with some of the olivine being visibly corroded. The olivines have diameters of 0.2–2 mm and make up 10%–20% of the rock. The alkali feldspars are platy and make up 5%–10% of the rock. These minerals occur in a fine-grained matrix of clinopyroxene, olivine, and plagioclase that forms 20%–35% of the rock. The gabbros also contain minor amounts of magnetite, ilmenite, zircon, apatite, and other accessory minerals, and the overall phenocryst abundance within the gabbro unit decreases from top to bottom.

2.4 Diabase

Diabase occurs beneath the gabbro and has a diabasic texture and a partly visible intersertal texture (Figures 4F,G). Some of the clinopyroxenes within the diabase are twinned (Figures 4H,I), and this unit has a similar mineralogy to the gabbros described above.

3 Analytical Methods

3.1 Whole-Rock Ar–Ar Analytical Procedures

The basalts dated during this study contain peridotite xenoliths and phenocrysts that were removed before analysis. Two basalt samples were dated by whole-rock Ar–Ar methods. The samples were crushed into small chips (≤5 mm) that were hand-picked under a binocular microscope to remove phenocrysts. The ⁴⁰Ar/³⁹Ar dating was carried out using a GV5400 mass spectrometer at the State Key Laboratory of Lithospheric Evolution, Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing, China, using the analytical procedures described by H. Qiu and Jiang (2007). All errors are reported at 2σ values and argon gas was extracted from the sample by step-heating using a MIR10 CO₂ laser. The released gases were purified using two Zr/Al getter pumps operated for 5–8 min at room temperature and ∼450°C, respectively. The background signal prior to analysis was <2 mV and the signal derived from the sample generally fluctuated between 40 and 200 mV. The dating results were calculated and plotted using ArArCALC software (Koppers, 2002), with a J-value of 0.00955 as determined using ZBH-2506 biotite (132 Ma) flux monitors. The results of these Ar–Ar analyses are given in Tables 1 and 2.

TABLE 1

TABLE 1. Results of ⁴⁰Ar/³⁹Ar dating of Fuding basalt sample TMS2-2.

TABLE 2

TABLE 2. Results of ⁴⁰Ar/³⁹Ar dating of Fuding basalt sample TMS2-1.

3.2 Whole-Rock Geochemical Analyses

Bulk-rock major, trace, and rare earth element (REE) concentrations were determined using X-ray fluorescence (XRF) and inductively coupled plasma–mass spectrometry (IC–MS) at the National Research Center for Geoanalysis, Chinese Academy of Geological Sciences (CAGS), Beijing, China. Major element concentrations were determined by XRF and yielded analytical uncertainties better than 5%. Trace and REE concentrations were determined by ICP–MS, with the REE separated using cation exchange techniques. Analytical uncertainties during ICP–MS analysis were 10% for elements with concentrations of <10 ppm and ∼5% for those with concentrations of >10 ppm (Zeng et al., 2012). The results of these analyses are listed in Table 3.

TABLE 3

TABLE 3. Major (wt.%) and trace (ppm) compositions of mafic volcanic samples from the northeast of Fujian Province.

3.3 Whole-Rock Sr–Nd Isotopic Analyses

Whole-rock Sr and Nd isotope ratios were determined by thermal ionization mass spectrometry (TIMS) using a Finnigan MAT-262 instrument at the CAS Key Laboratory of Crust–Mantle Materials and Environments, University of Science and Technology of China (USTC), Hefei, China. Analytical precision for these isotope ratio measurements is given as ± 2σ (standard error). Sr isotopic ratios were corrected for mass fractionation relative to a ⁸⁶Sr/⁸⁸Sr value of 0.1194, and analysis of the NBS987 standard yielded a measured ⁸⁷Sr/⁸⁶Sr ratio of 0.710298 ± 20 with a precision of ∼0.002%. Measured ¹⁴³Nd/¹⁴⁴Nd ratios were normalized to a ¹⁴⁶Nd/¹⁴⁴Nd value of 0.7219, and analysis of the La Jolla Nd standard yielded a measured ¹⁴³Nd/¹⁴⁴Nd ratio of 0.511851 ± 45. Single-stage Nd model ages (T_DM1) are calculated relative to the depleted mantle reservoir (Depaolo, 1988), and two-stage Nd model ages (T_DM2) are calculated for different ages of magmatism relative to average continental crustal values with a ¹⁴⁷Sm/¹⁴⁴Nd ratio of 0.118 (Jahn and Condie, 1995).

4 Analytical Results

4.1 Ar–Ar Geochronology

The Funding basalt samples (TMS2-2 and TMS2-1) from the Fotan volcanic succession dated by the ⁴⁰Ar/³⁹Ar method yielded apparent ages that were determined using age spectra and isotope correlation (³⁶Ar/⁴⁰Ar vs. ³⁹Ar/⁴⁰Ar) diagrams (Figures 5, 6; Tables 1,2). The latter provides a quantitative measure of the initial argon composition and allows the identification of excess argon that has ⁴⁰Ar/³⁶Ar ratios greater than the present day atmospheric value of 295.5. The data in Table 1 and Figure 2 indicate that little excess argon was present in the basalt samples.

FIGURE 5

FIGURE 5. Plateau and isochron Ar–Ar ages for sample TMS2-2. (A) and isochron Ar‐Ar age (B) for sample TMS2-2.

FIGURE 6

FIGURE 6. Plateau Ar–Ar age for sample TMS2-1.

The plateau age for sample TMS2-2 is 38.5 ± 1.2 Ma (Figure 5A), a date that is within error of the isochron age for this sample (38.5 ± 2.3 Ma; Figure 5B). The second sample (TMS2-1) was collected from the basal section of the Fuding area and yielded an older plateau age (42.3 ± 2 Ma; Figure 6). As such, we interpret the plateau ages for these samples to represent the volcanism that formed the Fuding basalts, indicating that the final eruption of the Fotan Formation occurred at 42.3–38.5 Ma. Hence, the eruption of the Fuding basalt occurred at 42.3–38.5 Ma, during the Eocene.

4.2 Whole-Rock Geochemical Characteristics

4.2.1 Gabbro and Diabase

The gabbro and diabase samples from the Fuding area have restricted ranges of SiO₂ (46.54–47.03 wt.%), total Fe expressed as FeO (FeO_T; 11.34–12.32 wt.%), CaO (8.92–10.07 wt.%), and Al₂O₃ (12.12–14.23 wt.%) concentrations, but a wide range of MgO concentrations (8.64–10.17 wt.%). Plotting these samples on a total alkali versus silica (TAS; SiO₂ versus Na₂O + K₂O) classification diagram indicates the majority are trachybasalts with a few basalts, although all of the samples plot above the alkaline curve in this diagram (Figure 7A). These samples have K₂O and K₂O + Na₂O concentrations of 1.99–2.35 and 4.67–5.65 wt.%, respectively, yielding high K₂O/Na₂O ratios (0.65–0.82) that indicate these samples are alkaline basaltic rocks (Figures 7B,C,D).

FIGURE 7

FIGURE 7. Geochemical classification diagrams showing variations in the compositions of samples from the Fuding mafic volcanic neck. (A) Total alkali versus silica (TAS) diagram (after Middlemost, 1994); (B) SiO₂ vs. K₂O + Na₂O diagram (after LeMaitre et al., 1989); (C) AFM diagram; and (D) Zr/TiO₂ versus Nb/Y diagram (after Pearce, 1996).

Plotting data of the gabbro and diabase samples on Harker diagrams yields negative correlations between SiO₂ and CaO, FeOT, and MgO concentrations, and positive correlations between SiO₂ and Na₂O, K₂O, and Al₂O₃ concentrations (Figure 8).

FIGURE 8

FIGURE 8. Harker-type diagrams showing variations in the geochemical compositions of mafic rocks from the Fuding volcanic neck.

All of the gabbro and diabase samples have high total REE (ΣREE) values (201.2–221.29 ppm; average of 212.91 ppm) and they are light REE (LREE) enriched, with total LREE to total heavy REE (HREE; ΣLREE/ΣHREE) ratios of 10.21–11.32 (average of 10.76). These samples have (La/Yb)_N (where _N denotes normalization to the chondrite ratio of Sun and McDonough, 1989) ratios of 18.26–20.46 (average of 19.41), reflecting the degree of fractionation of the LREE from the HREE. These samples show (La/Sm)_N values from 3.82 to 4.27 (average of 4.09) and (Gd/Yb)_N values from 2.88 to 3.16 (average of 3.09). They are free of significant Eu anomalies (Eu/Eu* = 1.00–1.05, average of 1.02) and have smooth chondrite-normalized REE patterns (Figure 9A). All of the samples are enriched in the large ion lithophile elements (LILE), have differentiated high field strength element (HFSE) concentrations, and are slightly depleted in Ti and Y (Figure 9C). They have chondrite-normalized REE and primitive-mantle-normalized multi-element variation patterns that are similar to those of typical OIB compositions but differ from typical N- or E-type mid-ocean-ridge basalt (MORB) compositions.

FIGURE 9

FIGURE 9. Chondrite-normalized REE and primitive-mantle-normalized multi-element diagrams for samples from the Fuding mafic volcanic neck. Diagrams are normalized to the chondrite and primitive mantle compositions of Sun and McDonough (1989). (A) and (C) for gabbro and diabase samples; (B) and (D) for basalt samples.

4.2.2 Basalts

The basalts analyzed during this study contain higher concentrations of MgO (10.75–11.12 wt.%) than the gabbro and diabase samples, with both basalt samples classified as tephrites or basanites and both plotting above the alkaline curve (Figure 7A), indicating that both of these basalts are alkaline basaltic rocks (Figures 7B,D).

Both of the basalt samples contain higher ΣREE concentrations (314.10–332.08 ppm; average of 323.09 ppm) than the gabbro and diabase samples, although the basalts are similar to these other samples in that they have OIB-type REE and multi-element variation diagram characteristics that contrast with typical N- or E-type MORB compositions (Figures 9B,D).

4.3 Whole-Rock Sr–Nd Characteristics

The isotopic Rb–Sr and Sm–Nd ratios of the whole-rock samples are given in Table 4. The gabbro, diabase, and basalt samples have uniform initial εNd(t) (3.05–4.56, average of 3.90) and initial ⁸⁷Sr/⁸⁶Sr (0.703794–0.703911, average of 0.703865) values. They have two-stage Nd model (T_DM2) ages than range from 0.61 to 0.73 Ga (average of 0.67 Ga).

TABLE 4

TABLE 4. Rb–Sr and Sm–Nd isotopic compositions of mafic volcanics from the northeast of Northeast Fujian Province.

5 Discussion

5.1 Petrogenetic Evolution

5.1.1 Basalts

The basalts from the Fuding mafic volcanic neck are enriched in the REE and have highly differentiated HFSE compositions that are apparent in their OIB-type primitive-mantle-normalized multi-element diagrams (Figures 9B,D; Edwards et al., 1994; Sun and McDonough, 1989; Zhao and Zhou, 2007). Both of these samples are classified as within-plate alkali basalts in the Nb–Zr–Y diagram of Meschede ,1986; Figure 10A). These basalts have Ti/V ratios between 75 and 80 that are much higher than those of arc basalts, and they plot in the OIB field on a modified Ti versus V diagram (Figure 10B; Shervais, 1982). Both samples plot in the OIB field on a Nb/Yb versus Th/Yb diagram (Figure 10C; J. Pearce and Peate, 1995). They yield high Mg# values (= 100*MgO/(MgO + 0.85*Fe₂O₃T) and contain low concentrations of SiO₂, suggesting that they originated from a parental magma that was derived from an OIB-like mantle source in a continental rift environment, without any crustal input.

FIGURE 10

FIGURE 10. (A) Nb-Zr-Y, (B) Ti versus V (after Shervais, 1982) and (C) Th/Yb–Nb/Yb (after Pearce & Peate, 1995) diagrams for samples from the study area. Average N-MORB, E-MORB, and OIB compositions are from Sun and McDonough (1989), and SSZ-, N-MORB-, E-MORB-, and OIB-type fields are from Mahe et al., 2004, Saccani and Photiades (2005), and Aldanmaz et al., 2008.

5.1.2 Gabbro and Diabase

The gabbro and diabase samples from the Fuding area have similar REE and HFSE characteristics as the basalt samples, again indicating that these units have an OIB-type affinity (Figures 9A,C, Figures 10A–C; Edwards et al., 1994; Sun and McDonough, 1989; Zhao and Zhou, 2007). However, the gabbro and diabase units have Mg# values of 63.96–66.58, suggesting that they record the minor differentiation of olivine and pyroxene. This fractionation is also evidenced by a negative correlation between SiO₂ and MgO concentrations (Figure 8). In addition, the positive correlation between Fe₂O₃T and MgO concentrations shown by the gabbro samples is indicative of the fractionation of olivine (Figure 11A), whereas the positive correlation between CaO and MgO concentrations in these samples is evidence of the fractionation of clinopyroxene (Figure 11B). This conclusion is also supported by the presence of positive correlations between Cr, Ni, and MgO concentrations (Figures 11C,D).

FIGURE 11

FIGURE 11. Harker-type diagrams showing variations in the Fe₂O₃T, CaO, Cr, and Ni concentrations of samples from the Fuding area relative to MgO. (A), CaO (B), Cr (C), and Ni (D) concentrations of samples from the Fuding area relative to MgO.

The lack of any significant Eu anomalies (Eu/Eu* = 1.00–1.05; Figure 9A) indicates that the gabbro and diabase units do not record any plagioclase fractionation. However, crustal contamination can modify the composition of mantle-derived magmatic rocks. Crustal materials are enriched in the LILE, K₂O, and Na₂O, and are depleted in P₂O₅ and TiO₂. The gabbro and diabase units within the Fuding area contain low and invariant concentrations of K₂O and Na₂O, suggesting that they record minimal amounts of crustal contamination. Crustal contamination can also produce negative Nb and Ta, and positive Zr and Hf anomalies relative to the LILE and LREE (Sun and McDonough, 1989; Zhao and Zhou, 2007); however, these anomalies are absent in the primitive-mantle-normalized multi-element diagrams for the gabbro and diabase samples from the study area (Figure 9C), again suggesting that these units record minimal crustal contamination. All of the samples show low initial ⁸⁷Sr/⁸⁶Sr values (average of 0.703865) and high εNd(t) values (3.05–4.56, average of 3.90). These data indicate that the basalt, gabbro, and diabase units in the Fuding area were derived from an OIB-type mantle source, with the gabbro and diabase units recording minor amounts of crustal contamination.

5.2 Implications of Ar–Ar Dating

The basalts from the Fuding mafic volcanic neck in coastal SE China are generally alkaline (average Na₂O + K₂O = 5.77 wt.%) and are enriched in TiO₂ (average TiO₂ = 2.15 wt.%), whereas Neogene basalts in this area are largely subalkaline (average Na₂O + K₂O = 2.79 wt.%) and contain lower concentrations of TiO₂ (average TiO₂₌<1.5 wt.%; Lu et al., 2000), indicating significant geochemical differences between these basalts.

The trace and REE compositions of the Fuding mafic volcanic neck are different from those of the Neogene basalts of coastal SE China. The basalts from the former contain higher Rb (average of 87 ppm), Sr (average of 984 ppm), Ba (average of 807 ppm), and total REE (average of 243 ppm) concentrations and have higher light REE/heavy REE (LREE/HREE) ratios (average of 11.93) than the Neogene basalts of coastal SE China (average Rb, Sr, Ba, and total REE concentrations of 17.5, 339, 201, and 112 ppm, respectively, with an average LREE/HREE ratio of 4.22; Lu et al., 2000; J. Qiu et al., 1999; S. Wang, 1998; X. Wang et al., 2012; J. Zhang and Lu, 1997; Zouet al, 2000).

L. Li et al. (2011) reported that the Taimushan granite formed at 96.16 ± 1.6 Ma and suggested that the Fuding basalts formed part of the late Oligocene to middle Pleistocene Fotan Group. Our unpublished zircon U–Pb laser ablation (LA)–ICP–MS analyses yielded a Late Cretaceous age of 88.2 ± 1.0 Ma for these basalts, although these ages may be unreliable. The two basalt samples from the Fuding mafic volcanic neck yield similar Ar–Ar ages of 38.5 ± 1.2 and 42.3 ± 2 Ma, indicating that the basalts within both the neck and within the Fotan Group were emplaced during the Eocene.

5.3 Implications of the Presence of Peridotite Xenoliths

Cretaceous basalts in coastal SE China are usually associated with other contemporaneous bimodal volcanic rocks. The basalts in this area crop out over a much smaller area than associated acidic volcanic rocks and are thought to have been derived from either an enriched region of mantle, from a depleted region of the mantle and then either assimilated crustal material or underwent magma mixing, or were derived from the crust–mantle transition zone (C. Chen et al., 2008; Cui et al., 2011; He and Xu, 2011; Z. Li and Li, 2007; X. Li et al., 2007; H. Li et al., 1995; Tang et al., 2010; Xing et al., 1999; G. Xie et al., 2005; X. Xu et al., 2008; J. Yan et al., 2005b; Yu et al., 1993).

As mentioned above, both the petrogenesis of the basalts in coastal SE China and the nature of the mantle beneath this region remain uncertain. The main cause of this uncertainty is the lack of mantle rocks in this area; however, peridotite xenoliths within the Fuding basalts can be used to determine the characteristics of the Eocene mantle in this area, including the post late-Mesozoic evolution of the mantle beneath coastal SE China.

The nature of the late Mesozoic mantle in coastal SE China remains debated. Several different models have been proposed, including 1) enriched lithospheric mantle beneath Fujian and Zhenjiang provinces (Cui et al., 2011; Tang et al., 2010; G. ; Xie et al., 2005; J. ; Yan et al., 2003; J. ; Yan et al., 2005a; Yan et al., 2005b; Z. ; Yang et al., 1999; B. ; Zhang et al., 2004), 2) enriched mantle that mixed with both depleted and EMII type enriched mantle material (X. Xie et al., 2001), 3) local areas of weakly enriched mantle that is compositionally similar to EMII-type enriched mantle (H. Zhang et al., 2005), and 4) depleted asthenospheric mantle (Q. Zhou et al., 2010).

Both the late Mesozoic basalts and acidic volcanic rocks in coastal SE China have isotopic characteristics similar to those of enriched mantle (C. Dong C. W. et al., 2006; Y. Dong Y. X. et al., 2006; C. Dong et al., 2007; Z. Yang et al., 1999; Xing et al., 1999; Xue et al., 1996; J. Zhou and Chen, 2001), suggesting that the Cretaceous upper mantle in this region was relatively stable but also weakly enriched.

The Paleocene basalts in coastal SE China generally crop out in the northern parts of the Jiangsu and Hefei basins, as well as in the Mingguang and Fushan areas (Qian and Li, 1996; Z. ; Yang et al., 1999). These basalts contain abundant peridotite xenoliths, were emplaced at 64–56 Ma, have the characteristics of typical continental basalts, and were derived from weakly enriched mantle (D. Chen, 1992; Cong et al., 1996; Z. Yang et al., 1999; X. Zhou, 1992).

Eocene basalts are sporadically exposed within coastal SE China and have been reported from the Sanshui Basin in Guangdong Province (Y. Dong Y. X. et al., 2006; Hu et al., 2013; Xiao et al., 2006; X. Zhang et al., 1993; W. Zhang and Fang, 2014; Zhu et al., 1991). X. Zhang et al. (1993) reported K–Ar ages of 45–55 Ma for these basalts, and Y. Dong Y. X. et al. (2006) obtained a zircon U–Pb age of 46–45 Ma for basaltic rocks in the Sanshui Basin. The latter basalts are thought to have been generated by partial melting of a depleted region of the mantle that generated continental rift-type magmatic rocks (Y. Dong Y. X. et al., 2006; W. Zhang and Fang, 2014), or partial melting of an enriched region of the mantle within a continental rift setting (Hu et al., 2013). The Sanshui basalts yield recalculated εNd(t) values of −0.77 to +1.23 (mean age 50 Ma) (Zhu et al., 1991) that reflect the weakly depleted nature of the Eocene mantle in coastal SE China. The basalt, gabbro, and diabase units within the Fuding area have OIB-type geochemical affinities with low initial ⁸⁷Sr/⁸⁶Sr ratios (average of 0.703865) and high εNd(t) values (average of 3.90) which similar with the depleted mantle. Its OIB type geochemical characteristics may be inherited from crustal materials with similar characteristics. Meanwhile, the widespread Neogene basalts in coastal SE China are exposed in the Xinchang area of Zhejiang Province, the Jiashan area of Anhui province, the Fangshan area of Jiangsu province, and the Sanshui Basin in Guangdong Province, and all of these Neogene basalts were derived from a depleted region of the mantle (R. Wang and Yang, 1987a, Wang and Yang, 1987b; Zhi et al., 1994). Thus, the mantle beneath coastal SE China evolved between the Cretaceous and the Neogene from enriched to depleted, and this change occurred during the Eocene.

6 Conclusion

Whole-rock Ar–Ar analyses of two basalt samples from the Fuding mafic volcanic neck yield ages of 38.5 ± 1.2 and 42.3 ± 2 Ma, indicating that the basalts were erupted at 42.3–38.5 Ma.

The basalt, gabbro, and diabase units within the Fuding area have OIB-type geochemical affinities with low initial ⁸⁷Sr/⁸⁶Sr ratios (average of 0.703865) and high εNd(t) values (average of 3.90). Both gabbro and diabase units record minor amounts of crustal contamination.

Peridotite xenoliths within the Fuding basalt provide evidence of the nature of the Eocene mantle in this area, especially the post late-Mesozoic evolution of the mantle beneath coastal SE China. The mantle beneath coastal SE China evolved from enriched to depleted between the Cretaceous and the Neogene, with this change occurring during the Eocene.

Data Availability Statement

The original contributions presented in the study are included in the article/supplementary material, further inquiries can be directed to the corresponding author.

Author Contributions

XZ designed the study. CL wrote the first draft. YJ analyzed the geochemical data. GX drew some of the figures. MY and ZD completed the geochemical experimental analysis. All authors discussed the results and contributed to the preparation of the manuscript.

Funding

This work was supported by Geological Survey projects (DD20221633) of the China Geological Survey, National key research and development program (No 2016YFC0600205) and Geological Survey projects (Nos 121201008000150002, 1212011121098, 121201008000150002, and 12120113070800) of the China Geological Survey.

Conflict of Interest

The 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.

Publisher’s Note

All claims expressed in this article are solely those of the authors and do not necessarily represent those of their affiliated organizations, or those of the publisher, the editors and the reviewers. Any product that may be evaluated in this article, or claim that may be made by its manufacturer, is not guaranteed or endorsed by the publisher.

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