Stable Isotope Analysis of Mammalian Enamel From the Early Pleistocene Site of Madigou, Nihewan Basin: Implications for Reconstructing Hominin Paleoenvironmental Adaptations in North China

Introduction

Understanding the impact of paleoenvironmental variability on hominin behavioral adaptations is a key area of research in human evolution (deMenocal, 1995; Ambrose, 2001; Behrensmeyer, 2006), and is of crucial relevance for understanding the initial dispersal of humans from Africa into Eurasia (Gabunia et al., 2000; Bar-Yosef and Belfer-Cohen, 2001; Van der Made, 2011) and hominin behavioral adaptations during the Middle Pleistocene Climate Transition (MPT) at ∼ 1.25–0.7 Ma, which is marked by a progressive increase in the amplitude of climate oscillations (Ruddiman et al., 1986; Mudelsee and Schulz, 1997; Clark et al., 2006; Wang et al., 2017). It has been hypothesized that the MPT triggered substantial hominin dispersals from Africa to Eurasia (Larick and Ciochon, 1996; Wu and Liu, 2001; Deng et al., 2007; Abbate and Sagri, 2012), and it may be linked to a more sustained settlement by Homo erectus in northern latitudes of East Asia. A more continuous occupation of northern latitudes would be aided by a diversity of adaptive behaviors, following patterns observed elsewhere (deMenocal, 2011; Grove, 2012; Potts, 2012, 2013; Potts and Faith, 2015), in which human biological evolution and lithic technological innovations were coupled with a high frequency of climatic fluctuation cycles.

The Nihewan Basin (Figure 1) in North China is well known for its abundance of archaeological sites through the Lower and Upper Pleistocene (Schick et al., 1991; Zhu et al., 2001, 2004; Deng et al., 2006, 2007; Ao et al., 2010, 2013; Zuo et al., 2011). Nihewan paleoenvironments have been reconstructed through the analysis of sedimentary features and mammalian enamel stable isotopes (Deng et al., 2001; An et al., 2005; Ding et al., 2005; Pei et al., 2009), pollen (Li et al., 1996; Wu et al., 2007; Pei et al., 2009), magnetic susceptibility (Deng et al., 2007; Pei et al., 2009, 2019), iron oxides (Pei et al., 2009), soluble salts (Li et al., 2010), and site formation processes (Jia et al., 2019). Recent archaeological studies (Pei et al., 2017, 2019; Yang et al., 2017, 2020, 2021) have discussed the links between climatic variability and human adaptations, suggesting that changes in lithic technological strategies occurred at the beginning of the MPT. Such changes would be evidenced by the flexibility in raw material procurement, diversification of flaking techniques, a refinement of retouching techniques, and an increase of tool types. However, the environmental context in which such new technological patterns emerged has not yet been properly ascertained.

FIGURE 1

FIGURE 1. (A–C) Location of the Nihewan Basin in China and the distribution of key Pleistocene sites in the Cenjiawan Platform. (D) Trenches at the MDG site complex, viewed from the southwest. Abbreviations: LU = lower unit. TBSU = thick brown sand unit. UU = upper unit (Pei et al., 2019).

Stable isotope (C, O) analysis of tooth enamel provides direct evidence of the ecology and habitat of fossil mammals (Quade et al., 1992; Cerling et al., 1997; Cerling and Harris, 1999; Van der Merwe, 2013; Rivals et al., 2018; Uno et al., 2018), but is yet to be applied systematically to the Nihewan Pleistocene sequence. Here we contribute to this effort by presenting the first analysis of isotope values to mammalian teeth from the Madigou site (MDG). Our study includes bulk sampling from the whole teeth enamel and sequential sampling of several specimens, which were used to reconstruct paleolandscapes and seasonal variability in Early Pleistocene Nihewan, and to contextualize both with dynamics observed in the use of stone tools by early humans at the site.

Principles of Stable Isotope (C, O) Analysis of Fossil Enamel

According to different pathways of photosynthesis, terrestrial plants are generally divided into three categories, C₃ (Calvin), C₄ (hatch slack) and CAM (Crassulacean acid metabolic acid), which cause the differences of carbon isotopic fractionation during the processes of carbon fixation. δ¹³C values of C₃ plants, including trees, shrubs and cold-tolerant herbs (Deng et al., 2001), range from −34‰ to −22‰, while those of C₄ plants, typical of drier and warmer environments (Raven et al., 1999), range from −17‰ to −9‰ (O'Leary, 1988; Farquhar et al., 1989; Cerling et al., 1997). Other factors such as rainfall, altitude, light intensity, atmospheric carbon dioxide concentration and the canopy effect also affect the δ¹³C values of plants (Farquhar et al., 1989). δ¹³C values of C₃ plants become more negative with the increase of the rainfall, altitude and latitude (Kohn, 2010). Isotopic fractionation takes place from diets to teeth enamel when plants are eaten by herbivores, and when herbivores are consumed by carnivores. Compared to those in plants, δ¹³C values of teeth enamel from large herbivores and carnivores increase by ∼14‰ and ∼9‰ respectively (Cerling and Harris, 1999; Tejada-Lara et al., 2018). Following earlier work (Cerling et al., 1997; Wang et al., 2008; Biasatti et al., 2010; Uno et al., 2018), the δ¹³C values in tooth enamel lower than -8‰ are attributed in this study to animals that only eat C₃ food, from -8‰ to −2‰ to those with a C₃-C₄ mixed diet, and higher than −2‰ to those consuming mainly C₄ foods.

The oxygen isotope composition in mammalian teeth is mainly determined by that of body water, which derives directly from drinking water (Pederzani and Britton, 2019). Due to evaporation, δ¹⁸O values in plant leaves are higher than those in meteoric water. This results in leaf-eating herbivores having higher δ¹⁸O values than those drinking meteoric water (Pederzani and Britton, 2019), thus enabling to distinguish browsers from grazers. Additionally, δ¹⁸O values vary with the altitude, temperature and latitude, which helps to track animal movement across different ecozones (Pederzani and Britton, 2019).

Two sampling strategies are usually applied to the isotopic analysis of fossil teeth enamel. Bulk sampling of the whole enamel is used to reconstruct the average diet and ecological setting during the period of tooth formation (Feranec and MacFadden, 2000). Sequential sampling of the enamel along the direction of enamel growth may reveal the spatiotemporal dietary and environmental changes throughout the development of the tooth (Balasse, 2002).

Material and Methods

Geological Setting of the Madigou Site

The Nihewan Basin (which includes the Yangyuan Basin and Yuxian Basin in Hebei Province, and the Datong Basin in Shanxi Province), is an intermontane basin between the Inner Mongolian Plateau and North China (Deng et al., 2019; Pei et al., 2019) (Figure 1A). It is well known for its extensive late Cenozoic fluvio-lacustrine sequence (the Nihewan Beds), reliably-constrained geochronology, and abundant archaeological sites (Schick et al., 1991; Zhu et al., 2001, 2004; Deng et al., 2006, 2007; Ao et al., 2010, 2013; Zuo et al., 2011). (Figures 1A–C). The Nihewan Beds contain fluvio-lacustrine deposits from the Late Pliocene to the late Middle/Upper Pleistocene (Zhao et al., 2010; Nian et al., 2013; Deng et al., 2019). These deposits include the Pliocene-Pleistocene boundary (Liu et al., 2012) and the Nihewan faunas (sensu lato) (Teilhard de Chardin and Piveteau, 1930; Zhou et al., 1991; Qiu and Qiu, 1995), and are constrained at the bottom by the Pliocene red clay and overlain by the Late Pleistocene Malan loess (Deng et al., 2019) at the top of the sequence. Current geochronological and archaeological research show that early hominins may have continuously occupied the Nihewan Basin from 1.66 Ma (Zhu et al., 2004) to the Late Pleistocene (Schick et al., 1991; Zhu et al., 2001, 2004; Pei et al., 2019).

Madigou (40°13′07–16″N, 114°39′58″–40′18″E) is located in the northwest margin of the Cenjiawan platform (eastern part of the Nihewan Basin). Paleomagnetism indicates that the MDG stratigraphy comprises the early Brunhes normal chron and the late Matuyama reverse chron, including the Jaramillo normal subchron (Figure 2). The MDG archaeological layers are positioned within the pre-Jaramillo Matuyama chron, with an estimated age of ca. 1.2 Ma, i.e., chronologically within the onset of the MPT. Stratigraphic correlations of seven trenches excavated at MDG indicate that the MDG chronostratigraphic sequence begins with MDG-E2, followed by MDG-E3, MDG-E5 and MDG-E7, and contains the most recent units at MDG-E6 (Figure 1D) (Pei et al., 2019). A total of 1,517 lithic artifacts and over 900 fossil remains, including Equus, Coelodonta antiquitatis, Cervidae, Bovidae, and others, were unearthed from the lower part of the sequence in each trench, especially in MDG-E2 and MDG-E3 (Pei et al., 2019). Predominance of ungulates in the fossil assemblage suggested open grasslands and a sparse steppe (Pei et al., 2019).

FIGURE 2

FIGURE 2. Lithostratigraphy and magnetic stratigraphy of MDG-E2, MDG-E3 and MDG-E6, and positions of the samples studied (excluding one sample from MDG-E7) (Hilgen et al., 2012; Pei et al., 2019).

Chert dominates among lithic raw materials, followed by siliceous dolomite (Pei et al., 2019). MDG knappers showed a preference for specific rock types, such as siliceous dolomite cobble for bipolar knapping, brecciated chert blocks for freehand hard hammer flaking, and high-quality chert for retouching tools (Pei et al., 2019).

The MDG fossils were spatially associated with stone artifacts, and preliminary zooarchaeological results suggest human action over part of the fossil assemblage (Pei et al., 2019). Thus, the ecological and environmental data retrieved from the isotopic analysis of fossil enamel presented herein also informs on the landscapes occupied by early humans at Nihewan.

Sample Selection

Seventy-seven fossil teeth from archaeological layers at MDG were selected for isotopic analysis: 67 from trench MDG-E2, 8 from trench MDG-E3, and one from each MDG-E6, and MDG-E7 (Figure 2). Bulk sampling was made from 71 teeth of Cervidae (Muntiacus sp.), Moschidae, Bovidae, Rhinocerotidae (Coelodonta antiquitatis), Equidae (Equus wangi sp. Nov. and Equus qingyangensis sp. Nov.), Canidae (Canis chihliensis?) and others (Table 1; Supplementary Table S1).

TABLE 1

TABLE 1. Sampled teeth per taxa and trench at MDG.

Six additional teeth were serially sampled: 2 of Coelodonta antiquitatis, 3 of Equus wangi sp. Nov., and 1 of Equus qingyangensis sp. Nov. (see details in Supplementary Tables S2–7). No first molars were included, to prevent the breastfeeding effect on isotopic data.

Sample Preparation and Isotopic Measurements

Bioapatite pretreatment was undertaken at the Institute of Vertebrate Paleontology and Paleoanthropology, Chinese Academy of Sciences (IVPP), and followed the protocols described in Lee-Thorp et al. (1989), Bocherens et al. (1994), Koch et al. (1997), and Wright and Schwarcz (1999). Before sampling, any contaminations on the enamel surface were removed with a dental drill. For the 71 teeth selected for bulk sampling, 15–30 mg enamel powder were extracted evenly from different parts of the enamel and grinded to below 200 meshes with agate mortar. Sequential samples of six additional teeth were collected from crown to neck along the enamel growth axis. The average sampling interval was 5 mm, and 15–20 mg of each sample was collected.

To remove the organic matter, about 1.5 ml of 2.5% sodium hypochlorite was added into the 2.0 ml tubes for each sample. After full reaction, samples were centrifuged and washed to neutrality with distilled water. Subsequently, 1.5 ml of 1 M acetic acid was added for 20 h to each sample to remove the secondary carbonate. Samples were subsequently cleaned with distilled water, freeze-dried and ground into powder again.

Isotopic measurements were undertaken in an Isotope Ratio Mass spectrometer (MAT-253) combined with a Gas bench system in the Laboratory for Stable Isotope Geochemistry, Institute of Geology and Geophysics, Chinese Academy of Sciences. The isotopic results were expressed as δ¹³C and δ¹⁸O, relative to the VPDB. The isotopic standards used for isotopic calibration were NBS 18, NBS 19 and GBW04405 (δ¹³C_VPDB = 0.57 ± 0.03‰, δ¹⁸O _VPDB = −8.49 ± 0.14‰; Certified reference material approved by the State Bureau of Technical Supervision, the People’s Republic of China). The precisions of δ¹³C and δ¹⁸O values are better than 0.15‰ and 0.20‰ respectively. Isotopic data are listed in Supplementary Tables S1–7.

Results

Isotopic Analysis of Bulk Samples

Figure 3 shows large isotopic variations among specimens that suggest different niches. The δ¹³C values range from −13.0‰ to −2.1‰ and average −7.3 ± 2.7‰ (n = 77), while the δ¹⁸O values range from −12.5‰ to −1.1‰ and average −8.8 ± 1.9‰ (n = 77).

FIGURE 3

FIGURE 3. δ¹³C and δ¹⁸C values of the MDG teeth assemblage.

Artiodactyls

The δ¹³C value of Moschidae (n = 1) is −13.0‰, indicating a closed C₃ environment. This sample shows the highest δ¹⁸O value (−1.1‰).

Cervidae (n = 6) includes Muntiacus sp. and other unidentifiable Cervidae taxa. Their δ¹³C values range from−12.9‰ to −10.0‰, with a mean of −12.0 ± 1.1‰. δ¹⁸O values range between −11.4‰ and −4.5‰, averaging −6.9 ± 2.7‰ (n = 6). However, given the abnormally low δ¹⁸O values of MDG13 (−8.3‰), MDG55 (−7.4‰) and MDG57 (−11.4‰), which might be due to the fact that the individuals come from other regions, the isotope data from those teeth are excluded from the following statistical analysis and discussion. The mean values of δ¹³C and δ¹⁸O in remaining Cervidae (n = 3) are −12.6 ± 0.5‰ and −4.7 ± 0.1‰ respectively, which indicates that MDG Cervidae fed in a pure C₃ environment.

Bovidae (n = 5) show δ¹³C values from −6.6‰ to −2.1‰, averaging −4.2 ± 1.9‰ and δ¹⁸O values from −11.5‰ to −7.4‰ (average of −9.4 ± 1.9‰). This suggests that they consumed mixed C₃-C₄ plants. It is notable that one specimen (MDG61) has the highest δ¹³C value (−2.1‰) among the entire assemblage, indicating a nearly neat C₄ environment.

Perissodactyls

The δ¹³C values of Coelodonta antiquitatis (n = 29) differ from those of carnivores and artiodactyls, ranging from −11.7‰ to -5.5‰ (mean = −7.9 ± 1.4‰). This indicates that the habitat of Coelodonta antiquitatis ranged between closed forest and open grassland landscapes. MDG Coelodonta teeth yield the lowest average δ¹⁸O value [−10.0 ± 1.2‰, (n = 29)] in the entire assemblage, which could be related to consumption of meteoric water.

The δ¹³C values of Equus (n = 23) range from −8.7‰ to −3.4‰ (average of −6.0 ± 1.8‰) and their δ¹⁸O values range from −9.7‰ to -5.3‰ (mean = −8.3 ± 1.0‰). This indicates their preference for more open environments compared to Coelodonta antiquitatis.

Carnivores

The δ¹³C value of a sole specimen of Canidae is −12.2‰. Its δ¹⁸O value is −5.3‰, higher than those from Coelodonta, Equus, and Bovidae.

Isotopic Analysis of Sequential Samples

The δ¹³C profiles from sequential samples of Coelodonta antiquitatis, Equus wangi sp. Nov., and Equus qingyangensis sp. Nov., suggest considerable variations of the diet throughout the life history of these specimens. Pure C₃ or nearly pure C₄ vegetation predominated occasionally, but C₃-C₄ mixed vegetation dominated. Variations observed in δ¹³C profiles could indicate an oscillation between dry and wet seasons, while variability in δ¹⁸O profiles may indicate periodic or seasonal fluctuations in precipitation (Figure 4; Table 2).

FIGURE 4

FIGURE 4. Sequential isotopic profiles from MDG teeth (A). MDG10: Coelodonta antiquitatis, Frag; (B). MDG11: Coelodonta antiquitatis, M3; (C). MDG16: Equus wangi sp. Nov., m3; (D). MDG19: Equus wangi sp. Nov., P4; (E). MDG22: Equus wangi sp. Nov., P4; (F). MDG23: Equus qingyangensis sp. Nov., p4).

TABLE 2

TABLE 2. Serial sampling data of MDG teeth.

Discussion

Niche Reconstruction in the Nihewan Basin at the Beginning of the MPT

Considering the fractionation of carbon isotope from diet to enamel bioapatite (with an enrichment of 14‰ in large herbivorous and of 9‰ in carnivores) (Tieszen et al., 1983; Cerling and Harris, 1999; Tejada-Lara et al., 2018), the niches of the MDG fauna can be reconstructed on the basis of isotopic data from bulk samples (Figure 5). We conclude that the fauna accumulated at the MDG site occupied a relatively broad niche, from open grassland to closed forest.

FIGURE 5

FIGURE 5. Niche reconstruction of the MDG fossil assemblage, based on δ¹³C _diets and δ¹⁸O_enamel values.

In terms of δ¹³C_diets values, Moschidae and Cervidae have the highest negative δ¹³C_diets values, indicative of a closed forest. On the other end, Equus and Bovidae have the most positive δ¹³C_diets values, typical of open environments. The large standard deviations in Bovidae (δ¹³C_diets: 1.9‰) and Equus (δ¹³C_diets: 1.8‰) suggest that they had a more flexible dietary breadth. Conversely, the smaller standard deviations in Coelodonta antiquitatis (δ¹³C_diets: 1.4‰) may indicate a more specialized diet.

Regarding δ¹⁸O_enamel values, Figure 4 shows that Moschidae (−1.1‰) and Cervidae (−4.7 ± 0.1‰) have more positive average δ¹⁸O_enamel values than Equus (−8.3 ± 1.0‰), Bovidae (−9.4 ± 1.9‰) and Coelodonta antiquitatis (−10.0 ± 1.2‰). This indicates a preference in Moschidae and Cervidae for more ¹⁸O-enriched foods (such as leaves). Overall, the standard deviation in Coelodonta antiquitatis (δ¹³C_diets: 1.4‰, δ¹⁸O_enamel: 1.2‰) suggests more limited foraging flexibility, habitat and narrower ecological adaptability than Equus (δ¹³C_diets: 1.8‰, δ¹⁸O_enamel: 1.0‰) and Bovidae (δ¹³C_diets: 1.9‰, δ¹⁸O_enamel: 1.9‰).

As shown in Figure 6, the isotopic profiles from Coelodonta antiquitatis and Equus indicate seasonal changes. MDG23 (Equus qingyangensis sp. Nov.) (δ¹³C_diets: 1.7‰) and MDG16 (Equus wangi sp. Nov.) (δ¹³C_diets: 1.4‰) have the largest variation in the δ¹³C_diets standard deviation, which suggests their adaptability to varied landscapes in nearly pure C₄, mixed C₃-C₄ and nearly pure C₃ vegetation. In contrast, the low standard deviation in MDG11 (Coelodonta antiquitatis) (δ¹³C_diets: 0.3‰) indicates a relatively fixed niche and narrow ecological adaptability for this individual. On the other hand, standard deviations of MDG16 (δ¹⁸O_enamel: 1.5‰), MDG19 (Equus wangi sp. Nov.) (δ¹⁸O_enamel: 1.1‰), MDG10 (Coelodonta antiquitatis) (δ¹⁸O_enamel: 0.9‰) and MDG22 (Equus wangi sp. Nov.) (δ¹⁸O_enamel: 0.9‰) are large, which reflects a seasonal variation of regional temperature and precipitation.

FIGURE 6

FIGURE 6. Reconstructed δ¹³C_diets and δ¹⁸O_enamel values from sequential samples of MDG teeth. MDG10 and MDG11: Coelodonta antiquitatis. MDG16, 19 and 22: Equus wangi sp. Nov. MDG23: Equus qingyangensis sp. Nov.

Changing Landscapes and Human Behavioral Adaptations in the Nihewan Basin at the Onset of the MPT

It has been proposed that human occupation of the Nihewan Basin during the Early Pleistocene was discontinuous and that the area would only be populated during interstadial periods and in the warm seasons (Dennell, 2003, 2013). While systematic testing is still needed through multiple proxies and across the archaeological sequence (de la Torre et al., 2020), our contribution on the isotopic analysis of the MDG faunal assemblages does not seem to support such hypothesis. Variability of patterns in δ¹⁸O and δ¹³C values (Figure 4) strongly suggests input of mammal carcasses to the site during various seasons. In addition, considering other archaeological evidence in the Nihewan Basin, it has been suggested that Early Pleistocene humans in North China could have adopted flexible technological strategies as a response to environmental fluctuations (Pei et al., 2019).

In the case of MDG, early humans preferentially used preferentially siliceous dolomite cobbles in the bipolar technique, breccia chert blocks for freehand hard-hammer percussion, and selected high-quality chert for retouching tools (Pei et al., 2017, 2019). This suggests a structured procurement of raw materials based on the technological requirements of each knapping activity.

Conclusion

Mammal fossils unearthed in archaeological sites play an important role in assessing the impact of environmental instability in human behavioral adaptations. This paper analyzed stable isotope ratios of fossil tooth enamel at the recently discovered Early Pleistocene site of MDG, in the Nihewan Basin. Isotopic data from bulk teeth enamel shows that the MDG fauna occupied a wide niche, including pure C₃, C₃-C₄ mixed, and nearly pure C₄ environments. The δ¹³C and δ¹⁸O profiles of tooth sections indicate substantial regional dry/cold and warm/wet fluctuations and seasonal variations.

Most likely, changing environments had an impact on human behavioral adaptations archaeologically detectable through stone tool technological variability. Previous studies (Pei et al., 2019) have discussed the technological plasticity of MDG hominins in raw material procurement strategies, knapping techniques, tool preferences and lithic reduction sequences, all of which might potentially be linked to environmental fluctuations such as those reported in this study. Further studies should explore other paleoenvironmental proxies and their application to other archaeological assemblages at the Nihewan Basin, in order to test how early humans coped with the instability characteristic of the MPT, and to portrait more accurately dynamics of hominin occupation in north China during this period.

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

ZX: Investigation, analysis, writing, and original draft preparation. SP: Investigation, designed the research and writing. YH: Academic support and writing. IdlT: Writing. DM: Investigation and analysis. All authors have contributed to the article and approved the submitted version.

Funding

This research was supported by the Strategic Priority Research Program of Chinese Academy of Sciences (Gran No. XDB26000000), the National Natural Science Foundation of China (41872029, 41372032), and an ERC-Advanced Grant (Horizon 2020; BICAEHFID grant agreement No. 832980).

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.

The reviewer CD declared a past co-authorship with the authors SP, IT, DM to the handling Editor.

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.

Acknowledgments

We would like thank professors Wei Dong, Haowen Tong and Dr. Boyang Sun from the Institute of Vertebrate Paleontology and Paleoanthropology (IVPP), Chinese Academy of Sciences, and Dr. Xiaomin Wang from Institute of Archaeology, Chinese Academy of Social Sciences, for their help in the taxonomic identification. We are also thankful to Dr. Jiao Ma from IVPP for her help in stable isotope analysis. Further thanks are due to Dr. Hao Li from IVPP for discussions and instructive comments.

Supplementary Material

The Supplementary Material for this article can be found online at: https://www.frontiersin.org/articles/10.3389/feart.2021.789781/full#supplementary-material

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