Modern beavers (Castor) are prolific ecosystem engineers and dramatically alter the landscape through tree harvesting and dam building. Little is known, however, about the evolutionary drivers of their woodcutting behaviour. Here we investigate if early woodcutting behaviour in Castoridae was driven by nutritional needs. We measured stable carbon and nitrogen isotopes (δ13C and δ15N) of coeval subfossil plants and beaver collagen (Dipoides sp.) from the Early Pliocene, High Arctic Beaver Pond fossil locality (Ellesmere Island), in order to reconstruct Dipoides sp. diet. Isotopic evidence indicates a diet of woody plants and freshwater macrophytes, supporting the hypothesis that this extinct semiaquatic beaver engaged in woodcutting behaviour for feeding purposes. In a phylogenetic context, the isotopic evidence implies that woodcutting and consumption of woody plants can be traced back to a small-bodied, semiaquatic Miocene castorid, suggesting that beavers have been consuming woody plants for over 20 million years. We propose that the behavioural complex (swimming, woodcutting, and consuming woody plants) preceded and facilitated the evolution of dam building. Dam building and food caching behaviours appear to be specializations for cold winter survival and may have evolved in response to late Neogene northern cooling.
Beavers today are renowned for their woodcutting behaviour and construction abilities. The extant genus Castor harvests trees and shrubs for sustenance (particularly during the winter1), but also for the purpose of lodge and dam building. These behaviours have a profound effect on regional hydrology, nutrient flow across the landscape, and local biodiversity, thus making them exemplary “ecosystem engineers”2,3,4. Modern beavers also are known to feed on trees. This food source is particularly important for northern populations that survive freezing winters, subsisting on their underwater caches of leafy branches5,6.
Castoridae is a diverse family of herbivorous Holarctic rodents, originating during the late Eocene7,8,9. The only definitive evidence of woodcutting in extinct beavers is from the Pliocene-aged High Arctic Beaver Pond fossil site, which preserves evidence of beaver-cut wood and a possible dam-core associated with the extinct beaver genus, Dipoides (species not yet described)9,10,11. Examination of Dipoides sp. incisors and cut marks on wood from the Beaver Pond site suggest that Dipoides sp. woodcutting performance was poorer than that of modern Castor11. The appearance of woodcutting in Dipoides sp., a distant relative of Castor, implies that this behaviour originated 20 to 24 Ma ago, in a group of semiaquatic beavers that includes both extant species (Castor canadensis and Castor fiber), the small Holarctic genus Dipoides, and the North American Ice Age giant beaver Castoroides7,9,12. And yet recent research shows that the diet of Ice Age Castoroides, a close relative of Dipoides, was dominated by submerged plants, not trees and shrubs13. This finding, alongside a lack of definitive evidence of lodges or dams at the Beaver Pond site highlights the question: Does the cut wood at the Beaver Pond site represent a means of gathering food?
Here, we present stable carbon and nitrogen isotope data for Pliocene-age (i) plant macrofossils and (ii) bone collagen from High Arctic Dipoides sp. subfossil remains. The specimens originate from a peat deposit at the Beaver Pond fossil site, located on Ellesmere Island (locally known as Umingmak Nuna, meaning “land of muskoxen”), situated within the Canadian Arctic Archipelago (78° 33′ N, 82° 25′ W) (Fig. 1). We reconstruct High Arctic Dipoides sp. palaeodiet within the context of coeval terrestrial and freshwater plant macrofossil remains excavated from the same ~ 4 Ma old peat layer. The Beaver Pond site provides a very rare opportunity for such a palaeodiet reconstruction using coeval herbivore and plant remains.
The Beaver Pond fossil site
The Beaver Pond site is a succession of fossiliferous peat deposits interspersed within 40 m of sandy, cross-bedded, fluvial deposits and capped with glacial till14. The thickest peat deposit within this sequence, which yielded material for this study, sits 380 m above present day sea-level overlooking Strathcona Fiord. Most recent terrestrial cosmogenic nuclide burial dating of sands above this peat layer have yielded a date of 3.9 + 1.5/− 0.5 Ma15, placing the minimum age of peat formation during the late Early Pliocene (late Zanclean). This peat unit is characterized by an abundance of beaver-cut sticks10,11 and has yielded a wide array of beautifully preserved plant macrofossils, invertebrates, and vertebrate fossil remains (Fig. 2). Rybczynski and Harington16, Matthews and Fyles17, Hutchison and Harington18, Tedford and Harington10, Dawson and Harington19, Murray et al.20, Mitchell et al.21, Gosse et al.22, and Wang et al.23 provide detailed descriptions of Pliocene terrestrial flora and faunal assemblages associated with the Beaver Pond site.
Ellesmere Island today is a polar desert, with sparse flora and very little precipitation24. The landscape was very different during the Early Pliocene warm period, when the climate supported wetland habitat surrounded by open larch forest10,21,22,25. During the Pliocene, Ellesmere Island was on the eastern edge of a large coastal plain, where intense Neogene thawing and weathering liberated sediment to create a thick, continuous clastic wedge across the Canadian Arctic Archipelago (referred to as the Beaufort Formation in the western Canadian Arctic islands). It is hypothesized that northwest passages did not exist during the Pliocene, as they had yet to be incised by fluvial and glacial erosion22,26. This unbroken coastal plain altered ocean circulation patterns in the High Arctic, and along with the Bering Isthmus that connected North American and Eurasia until 5.5 Ma ago27 would have enabled the migration of terrestrial species across the Neogene High Arctic10.
Late Early Pliocene mean global temperature was 2–3 °C above modern28 and high latitude regions experienced amplified warming. Pliocene Arctic mean annual temperature was near freezing, which is ~ 15–22 °C warmer than present day, and tree line was ~ 2000 km further north15,24,29,30,31,32,33. Summer temperatures at the Beaver Pond site reached 20 °C, while winter temperatures were more moderate than present day, with a low of ~ – 12 °C24. Despite the relatively mild conditions, the Beaver Pond site still experienced total darkness and subzero temperatures during the winter months.
There is no modern analog for the ecological community found at the Beaver Pond site, although the flora of present-day Labrador (Canada) is considered to be similar22,34,35,36. The Beaver Pond macrofossil assemblage indicates a larch forest, although birch, alder, spruce, pine, cedar, and cold-adapted woody shrubs were also present (see Matthews and Fyles17 for a complete list of identified flora). The Beaver Pond site supported higher faunal biodiversity than any modern near-tree line communities.
The remains of a complex faunal community were discovered at the Beaver Pond site, including beaver (Dipoides sp., see below), three-toed horse, bear, badger, “deerlet”, water fowl, fish and a rabbit relative10,22. Pliocene-age sites with similar fauna and flora community composition are very rare—Idaho in mid-continent North America, and the high altitude Yushe Basin, in northeastern China are the only known sites with similar (but not equivalent) faunal assemblages37,38.
The most common vertebrate remains at the Beaver Pond site belong to Dipoides, an extinct genus of beaver known from the Neogene of Eurasia and North America, represented by 12 different species7,39,40,41. Although not directly related to the extant Castor, both genera share semiaquatic and woodcutting behaviours9,11,42.
The Beaver Pond site is the only known locality with sufficiently well-preserved plant macrofossils to record evidence of Dipoides sp. woodcutting behaviour. The peat deposits are hypothesized to be the remnants of an ancient beaver pond due to the presence of many beaver-cut sticks, and even a cluster of cut sticks, cobbles, and silt that resemble the core of a beaver dam10.
Here we use stable isotope data to understand Dipoides sp. diet and elucidate the purpose of their woodcutting behaviour. Our study aims to describe the relative contributions of woody vegetation and aquatic plants to the diet of Dipoides sp. using stable carbon and nitrogen isotope analysis of contemporary sub-fossil skeletal and plant macrofossil material from the Beaver Pond site. This new information is used to better interpret (i) the ecological impact of Dipoides sp. on the Pliocene landscape, (ii) Dipoides sp. potential for winter survival strategies such as underwater food caching, and (iii) the evolutionary context of tree-exploitation within the Castoridae family.
Stable isotopes and palaeodiet
The stable carbon (δ13C) and nitrogen (δ15N) isotope compositions of an animal’s bodily tissues correlate closely with that of its diet, when adjusted for 13C- and 15N-enrichment that occurs during collagen formation and with each successive trophic level43,44. Well-preserved bone collagen is therefore a useful integrator of an animal’s diet. In addition, sufficient context is required to accurately describe the nutrient flow between subsequent trophic levels of an ecosystem. In particular, the diet of an organism must be interpreted within the context of an appropriate dietary baseline. This baseline is composed of isotopically defined food or “menu-items” available to the organism.
The isotopic composition of primary producers at the base of the food chain control the δ13C and δ15N of the dietary baseline for herbivores. The δ13C and δ15N of primary producers depend on physiology (i.e. which photosynthetic pathway the plant employs) and the isotopic composition of bioavailable sources of C and N (i.e. atmospheric CO2). Casey and Post45 provide a thorough review of how primary producer δ13C and δ15N vary with physiology and local terrestrial and aquatic environmental conditions. A particular challenge in many forested-wetland environments, however, is that the carbon and nitrogen isotope range of terrestrial and freshwater plants overlap. There are, however, sufficient differences between the δ13C and δ15N of terrestrial vegetation utilizing the C3-photosynthetic pathway and vascular freshwater plants (macrophytes) for them to serve as useful endmembers of herbivore diet in such environments (see Methodology).
Another challenge is that the isotopic composition of regional and global C and N baselines (and subsequently, that of primary producers that use them) can change over time46,47. Hence, reconstructing the diet of herbivores that lived thousands or millions of years ago can be problematic when using isotopic data, as is very rare to find sufficiently preserved coeval plant material and faunal remains from the same geologic locality. Typically, isotopic data for modern plants are all that are available in palaeodiet studies. Fortunately, much of this concern is alleviated at the Beaver Pond site, given the excellent organic preservation of coeval plant and animal tissues.
Bone collagen stable carbon and nitrogen isotopes
Dipoides sp. (n = 5) bone collagen stable isotope results (δ13Ccol and δ15Ncol) are presented in Table 1. Dipoides sp. δ13Ccol ranges from − 20.8 to − 19.1‰, with a mean of − 20.3‰, and δ15Ncol ranges from + 3.2 to + 5.8‰, with a mean of + 4.7‰ (Fig. 3).
Atomic C:N ratio and carbon and nitrogen contents (wt%) were used to assess collagen preservation for Dipoides skeletal material (Table 1). All specimen parameters are within the accepted range for well-preserved archaeological or palaeontological skeletal material from temperate or polar regions reported by van Klinken48 (acceptable parameters: C wt% = 34.8 ± 8.8%; N wt% = ~ 11–16%; atomic C:N = 3.1–3.5).
Plant macrofossil species diversity
By volume, the Beaver Pond peat sample examined in this study consisted of 85% bryophytes, 10% wood and twigs, and 5% macrofossils. Eleven genera were identified, representing a diverse assemblage of terrestrial and freshwater plants (Table 2). Seven taxa were analyzed for stable carbon and nitrogen isotope compositions (Scorpidium scorpioides, Larix, Betula, Stuckenia filiformis, Scheuchzeria sp., Cornus sericea, Menyanthes trifoliata) (Table 2). The dominant moss type was Scorpidium scorpioides (hooked scorpion moss). Larix (larch—a deciduous conifer) was the only conifer species identified from this peat sample (although many other tree species have been previously identified from the Beaver Pond site—see Introduction). Plant macrofossils from multiple genera (Myrica, Shepherdia, Potamogeton, and Hippuris) and from three species of Carex (Carex aquatilis, Carex diandra, and Carex maritime) were also recognized, but in insufficient quantities for stable isotope analysis.
Plant macrofossil stable carbon and nitrogen isotopes
Plant macrofossil stable isotope results are presented in Table 2 and Fig. 4. Macrofossil δ13C, δ15N, C (wt%), N (wt%), C/N (wt%), and atomic C:N ratios are all within the range expected for terrestrial and freshwater plants (Table 2, Figs. 4 and 5). Beaver Pond plant macrofossil δ13C and δ15N range from − 36.6 to − 22.7‰, and + 0.1 to + 4.8‰, respectively.
The chemical and elemental compositions of plants vary widely by species, life history stage (i.e. senescence), and environment conditions. For these reasons, atomic C:N ratio and carbon and nitrogen content are not considered to be infallible indicators of organic preservation in subfossil plants49. That said, the plant macrofossil C (wt%) values obtained in the present study are within or close to the mean carbon content for modern plants (between ~ 40 and 47%) (Metcalfe and Mead49, and references therein). Plant macrofossil N (wt%) values are lower than the mean nitrogen contents of modern plants (between ~ 1 and 3%) but are not outside the reported range for modern plants.
Stable isotope analysis in R (SIAR) mixing model
Next, we evaluate Dipoides sp. δ13Ccol and δ15Ncol within the context of the isotopic dietary baseline composed of coeval terrestrial and freshwater vegetation from the High Arctic Beaver Pond fossil site. The faunal and plant macrofossil isotope data were incorporated into a Bayesian mixing model to determine the relative input of terrestrial versus freshwater plants to Dipoides sp. diet (Fig. 6). This also allowed us to better assess the connection between Dipoides sp. woodcutting behaviour and its consumption of woody plants.
The SIAR model is a statistical tool that uses biotracers (stable isotopes) to estimate the relative input of different sources to a product or mixture. In (palaeo)ecology, mixing models use the stable isotope compositions of different food sources to infer their relative contributions to the composition of overall diet, and assess the probability that the inferred proportions are correct. There are systematic differences in the isotopic composition between a consumer’s collagen and its diet, both for carbon and for nitrogen. Hence, a correction factor must be applied to render data for consumers and possible diet items directly comparable.
Plant macrofossils were divided into three sources, or functional types: terrestrial woody plants, vascular freshwater macrophytes, and bryophytes (mosses). These groupings were created to assess how terrestrial and freshwater resources contributed separately to Dipoides sp. diet. The functional types were statistically defined and their relative contribution to diet was assessed using scripts from SIAR V4 in R Studio 3.1.2 (Stable Isotope Analysis in R: An Ecologist’s Guide). Based on existing literature, respective bone collagen-to-diet offsets of + 4.2‰ and + 3.0‰ were subtracted from Dipoides sp. δ13Ccol and δ15Ncol when incorporated into the mixing model50,51,52,53.
Dipoides sp. palaeoecology
The Bayesian mixing model indicates that Dipoides sp. consumed both woody plants and freshwater macrophytes in approximately equal proportions (Figs. 6 and 7), although it relied slightly more on freshwater macrophytes. This suggests that Dipoides sp. spent a greater proportion of time feeding in the water than on land.
The distribution of Dipoides sp. δ13Ccol and δ15Ncol is not entirely enclosed within the three primary producer functional groups analyzed (Fig. 6). This is likely the result of the relatively small plant macrofossil sample size. Submerged aquatic macrophytes, for example, are under-represented in the plant macrofossils available for stable isotope analysis. Macrophytes have highly variable δ13C and may have contributed more to Dipoides sp. diet than the mixing model suggests. Submerged macrophytes can be highly enriched in 13C because of physiological differences (primarily the use of 13C-enriched dissolved bicarbonate) or environmental conditions in the water column (i.e. boundary-layer effect)54,55,56. In addition, tree bark is more enriched in 13C than tree foliage57 and may have been a key resource for Dipoides sp.
The results of the dietary mixing model support the interpretation that woody plants were an important contributor to Dipoides sp. diet. It is likely that Dipoides sp. also used shrubs and trees as a source of construction material10,11, but more evidence is needed to confirm this. Similar to extant Castor, Dipoides sp. may have also demonstrated regional differences in diet, where northern and southern populations utilized different resources according to their availability.
Nitrogen content and C/N as indicators of forage quality
Plant macrofossil nitrogen content (N wt%) and C/N are indicators of forage quality and may be used to interpret the relative nutrition of dietary inputs. Plants with high N (wt%) contain more protein and energy—likewise, low N (wt%) correlates with low plant digestibility, high fiber and high lignin compound content58. Beaver Pond plant macrofossil N (wt%) and C/N are highly variable (Table 2, Fig. 5). Although there is considerable variability in C/N ratios depending upon which plant part was analyzed (i.e. seeds versus woody tissue), woody vegetation tends to have higher C/N ratios than macrophytes, and thus tends to be of lower food quality. However, the increased structural tissues in woody plants may have rendered them more effective winter cache foods.
In extremely seasonal environments such as the High Arctic, herbivores must use plant resources in a highly efficient manner. Herbivores must consume the highest quality forage possible during the brief growing season to maximize nutrient and energy gain. High quality forage typically includes young leaves with high nitrogen content, minimal structural (fibrous) tissues, and low defense compound content59,60.
Within the Beaver Pond macrofossil assemblage, pod grass (an emergent macrophyte) and birch have the highest nitrogen content and lowest C/N (Fig. 5). A larger sample set is necessary to confirm this observation; however, current data supports the conclusion that emergent macrophytes and deciduous broadleaf trees were among the more nutritious types of forage available to Dipoides sp. at the Beaver Pond site. It should be noted that forage quality is not the only factor that governs herbivore feeding behaviour. Animals may preferentially target plants with higher biomass to minimize energy expenditure traveling between forage sites or select plants that grow in locations that minimize the risk of predation.
The C/N of high Arctic shrubs decreases over the course of the growing season58. As there is no time-constraint on macrofossil deposition at the Beaver Pond site, variation in C/N may also be due to differences in plant phenological stage at time of incorporation into the peat layer. The incorporation of senescent plants into the peat deposit at the end of each growing season may in part account for the lower than expected macrofossil N (wt%) values reported from this site.
Beaver Pond site flora δ13C and δ15N
The Beaver Pond macrofossil assemblage contains a diverse range of terrestrial and freshwater plant species. The identified plant species in this study concur with previous interpretations that this was an open-forest landscape interspersed with shallow wetlands. Larch trees and cool-climate woody shrubs dominated the forest community. The wetlands supported both vascular macrophytes and dense assemblages of bryophytes.
The macrofossil δ13C are all within the range expected for primary producers utilizing the C3 photosynthetic pathway and accessing either ambient or dissolved atmospheric CO2 as their dominant carbon source. The δ15N of the macrofossils are also within the expected range for a riparian ecosystem in a cool climate biome.
While Dipoides sp. most likely consumed leafy tree branches and woody tissues (cambium), it is worth noting that plant seeds and cone bracts were analyzed in this study due to ease of macrofossil taxonomic identification. Leaf δ13C is typically lower than that of other plant parts61, although there is no clear pattern in intra-plant variation of δ15N.
Samples of the dominant Beaver Pond site bryophyte, Scorpidium (hooked scorpion moss), have very low δ13C for a primary producer (− 36.6 to − 34.6‰). This pattern is consistent with modern mosses collected from freshwater habitats in Subarctic and Arctic regions13,62,63,64.
Environmental conditions dictate moss δ13C rather than species-specific physiological differences. Peat mosses can grow partially or fully submerged in water. Given that mid-Pliocene atmospheric CO2 concentration levels were similar to modern (~ 400 ppm)15,65,66, moss exposed to the atmosphere would preferentially have used the abundant 12CO2, resulting in low δ13C. Alternatively, low δ13C in peat mosses can also indicate an underwater growing environment rich in 13C-depleted respired CO2 from surrounding plants62.
Moss macrofossil δ15N is relatively high for a photosynthetic organism (mean = + 4.8‰). This is indicative of either the presence of 15N-enriched sources of bioavailable N (i.e. dissolved nitrates, organic proteins such as urea or amino acids), or increased nutrient availability45,61. Unlike vascular plants, mosses do not uptake compounds through their roots. Rather, they obtain nutrients from wet or dry deposition through their leaves67,68. Today, beaver ponds are considered to be N sinks, with elevated rates of bacterially mediated denitrification69. These bacterial processes result in 15N-enriched products that are readily dissolved and used by plants (including moss) living in an aqueous environment. Decomposition processes also increase plant δ15N over time47 and remineralized organic debris decomposing in wetlands may be particularly 15N-enriched.
Beaver Pond bulk peat samples and moss macrofossils show a similar isotopic pattern (low δ13C and high δ15N), which suggests that hooked scorpion moss contributed substantially to peat biomass accumulation at the Beaver Pond site.
Beaver Pond macrophyte δ13C fall well within the albeit very wide known range for modern freshwater plants (− 50 to − 11‰, see Osmond et al.70, Keeley and Sandquist54, Mendonça et al.55, and Chappuis et al.56). It is reasonable to assume, however, that the very small sample size in this study hides the potential extent of the carbon isotope variability of macrophytes at the site.
Pod grass and bogbean are classified as emergent macrophytes (they grow rooted in water-logged substrates, but their leaves are exposed to the atmosphere), while pondweed grows entirely submerged. Submerged macrophytes become more enriched in 13C as the dissolved CO2 pool (the dominant carbon source) becomes increasingly limited54.
The Beaver Pond site pondweed δ13C is relatively low (− 26.5‰) for a submerged macrophyte. This indicates that it grew in an aquatic environment with adequate dissolved CO2. This is in keeping with the interpretation that the Beaver Pond was a fen (near neutral pH, cool water temperature) during the Pliocene. A low δ13C may also indicate high influx of terrestrial organic biomass or mosses (with low δ13C) into the water that subsequently remineralized and contributed to the dissolved inorganic carbon pool.
Environmental conditions strongly influence aquatic plant δ15N. Beaver Pond macrophyte δ15N (range = + 0.2 to + 2.7‰) indicate interspecific access and use of a variety of different sources of bioavailable N within the water column and substrate. The most likely N sources are microbial-fixed atmospheric N2 (which ranges from –2 to + 2‰), the products of nitrification/denitrification processes (15N-enriched NH4+ or NOx), and remineralized 15N-enriched organic material (either terrestrial or aquatic)71,72,73.
Larch (the extinct species Larix groenlandii) is the most common vascular plant species in this macrofossil assemblage.
There is an offset of ~ 2‰ between the δ13C of (i) larch shoots/buds (which bear the needles) and cone bracts, and (ii) larch seeds. Larch shoots and cones (δ13C range = ‒25.4 to − 25.1‰; mean = − 25.3‰) are more depleted of 13C than larch seeds (δ13C range = − 23.3 to − 22.7‰, mean = − 23.1‰). This could be indicative of seasonal physiological or environmental conditions experienced by larch trees at the Beaver Pond site. The cones and shoots of extant larch trees begin growing in the early spring and have lower δ13C, whereas their seeds (higher δ13C) do not develop and mature until mid to late summer74.
A number of physiological and environmental conditions could be responsible for this offset between needle/-bearing structures and seeds. Atmospheric vapor pressure deficit (aridity) induces stomatal closure in vascular plants75. This restricts not only the rate of water leaving the needle/tree, but also that of atmospheric CO2 entering it. Stomatal closure reduces CO2 entry and results in less discrimination against 13CO2. High levels of solar irradiance in the summer increase the rate of CO2 assimilation. Plants growing at very high latitudes experience 24-h of daylight during the summer. This creates a greater demand for CO2 to maintain photosynthesis and less discrimination against 13CO2. Both aridity and increased light levels could contribute to why Beaver Pond larch tissues grown late in the summer are more 13C-enriched than those grown in the early spring/the previous fall.
Alternatively, trees can use water and carbon (in the form of sugars) stored during the previous year to promote new growth during the early spring when leaves are absent and light levels are low. Tissues that develop early in the growing season (i.e. needle-bearing buds and shoots) can therefore reflect the δ13C of photosynthetic conditions from the previous growing season76,77. In addition, differences in the macromolecular (lipid, protein, sugar) composition of larch buds/needles versus seeds could account for their offset in δ13C (i.e. lipids are typically more 13C-depleted than proteins).
Larch δ15N (mean = + 2.7‰) indicate that these conifer trees had access to N sources other than “light” fixed atmospheric N2. Given the proximity of wetlands, the root systems of larch trees may have had access to 15N-enriched dissolved nitrates in the surrounding water-logged soils. Increasing foliar N concentration due to atmospheric N deposition also drives up plant δ15N78,79.
Aridity may also have influenced terrestrial plants growing at the Beaver Pond site. Higher rainfall is inversely correlated with δ15N, where rainier ecosystems tend to produce more 15N-depleted plants80.
Similar to δ13C, there is an offset in δ15N (and N wt%) between larch needle-bearing structures (mean = + 3.8‰; 0.9%) and larch seeds (mean = + 2.1‰; 0.3%). This could indicate differences in the macromolecular composition of these different tissue types (where high N content typically indicates higher tissue protein content).
Comparison of Dipoides within Castoridae
The composition of Dipoides sp. diet differs from that of other members of Castoridae that lived in North America during the late Cenozoic. Pliocene High Arctic Dipoides sp. (n = 5), modern subarctic Castor canadensis (n = 4) (Table 1), and late Pleistocene Castoroides ohioensis (n = 11) (Table 1) δ13Ccol and δ15Ncol are compared in Fig. 3. A correction for the Suess effect was first necessary render the δ13C of all three genera comparable. The carbon isotope composition of atmospheric CO2 has changed over time with global climatic conditions. More recently, anthropogenic burning of fossil fuels that has rapidly released CO2 enriched in 12C into the atmosphere46,81. Hence, a correction is needed when comparing δ13C of organic samples from different time periods to account for this isotopic variation in the primary carbon source of photosynthetic organisms at the base of the food web.
Suess effect corrections of + 2.02‰ and − 0.1‰ were applied to the δ13Ccol of modern C. canadensis (collected in 2013 and 2014) and Castoroides (late Pleistocene in age), respectively. These corrections were based on the average δ13C of atmospheric CO2 (δ13CCO2) calculated from Pliocene dual-benthic and planktonic foraminifera proxy records, spanning from ~ 4.1 to 3.8 Ma (average δ13CCO2 = − 6.55‰)76. These foraminifera proxy records are approximately contemporary with the Beaver Pond site. Average δ13CCO2 for 2014 (− 8.57‰) was compiled from the Scripps CO2 monitoring program. Average δ13CCO2 for the late Pleistocene (− 6.45‰) was compiled using ice core data from Schmitt et al.82.
Plants growing during these three different time periods (Pliocene, late Pleistocene, and modern/2014) would reflect the δ13C of contemporary atmospheric CO2. Therefore, changes in δ13CCO2 help explain differences in δ13C between Dipoides sp. and modern C. canadensis. Additional factors, however, are important in explaining the wide range of δ13C and large enrichment in 13C measured for Castoroides.
Dipoides sp. diet composition differs from that of Castoroides (the Pleistocene giant beaver) (Figs. 3 and 7). Castoroides’ high δ13Ccol and δ15Ncol (mean δ13Ccol = − 17.6‰ and mean δ15Ncol = + 5.8‰) indicate a diet composed predominantly of aquatic (particularly submerged) macrophytes and minimal woody plant material (Table 1)13.
In comparison with Castoroides, both Dipoides sp. and C. canadensis have a relatively small range of δ13Ccol and δ15Ncol (Table 1) (Fig. 3). Dipoides sp. mean δ13Ccol and δ15Ncol are higher than those of modern C. canadensis (Fig. 3). This is attributable to either variation in diet between the two species, or changes in global C and N baselines over geologic time.
Previous mixing model studies predict that extant C. canadensis diet is composed of approximately equal proportions of woody terrestrial plants and aquatic macrophytes13. However, this can vary by latitude and season. For example, extant C. canadensis in the Canadian subarctic vary their winter diet significantly depending on habitat83. It is worth noting that extant C. canadensis does not occur north of 70° latitude and High Arctic Dipoides sp. living at 78° latitude may have employed different dietary strategies.
Dipoides sp. may have relied more heavily than C. canadensis on underwater stores of tree branches to survive the long, dark polar winter. Tree bark is more 13C-enriched than leafy vegetation57 and increased consumption could account for the higher δ13Ccol seen in Dipoides sp. Variation in the quantity and type of macrophytes consumed by each beaver species could also account for this difference (i.e. emergent and floating macrophytes are, on average more 15N-enriched than submerged macrophytes).
Changes in the isotopic composition of the C and N baseline between the Pliocene and the present could also account for the isotopic offset between beaver species. Further investigation of possible changes in the δ15N baseline of flora in terrestrial high latitude environments during the Pliocene would be a valuable avenue of future research.
Dipoides sp. behaviour and evolutionary implications
Evidence from the Beaver Pond site has implications for our understanding of Dipoides sp. ecology. These data also contribute to our understanding of the evolution of behavioural transitions within Castoridae. In particular, how Castor’s distinctive complex of behavioural traits (tree harvesting, underwater food caching, and construction behaviour) may have evolved. A new hypothesis of behavioural evolution in castorids based on evidence from the fossil record (i.e. fossil burrows, cut wood, and stable isotope measurements) and skeletal-dental morphology is mapped onto a simplified phylogenetic tree in Fig. 842,84,85,86,87.
Castoridae is a group of herbivorous rodents comprising roughly two dozen genera. Most fossil castorids fall within two major groups: a clade of fossorial specialists (Palaeocastorinae) and a semiaquatic clade42,84,86,88,89,90. The latter includes Castor and Dipoides. Members of the fossorial clade (~ 7 genera) possess striking specializations such large digging claws, extremely reduced tails, and broad, procumbent incisors for digging. In some cases, specimens have been found within fossil burrows (i.e. Palaeocastor, or “The devil’s corkscrew” burrows discovered in the plains of North America88). The semiaquatic group comprises two subfamilies, Castorinae (~ 6 genera, including Steneofiber and the extant Castor), and Castoroidinae (~ 7 genera, including Dipoides and the giant beaver, Castoroides). The oldest definitive Castorinae in the fossil record is Steneofiber eseri from the early Miocene (France, MN2, ~ 23 Ma). S. eseri shows evidence of living in family groups and swimming specializations91. This, in combination with aDNA evidence12, suggests Castorinae and Castoroidinae are derived from a semiaquatic ancestor in the early Miocene.
Digging behaviour was not just characteristic of the fossorial group and appears within the semiaquatic clade as well. Castor, though not morphologically highly specialized for the task, digs bank burrows and creates extensive canal systems92. In addition, the extinct semiaquatic beaver Steneofiber eseri was found within a burrow91. Considering the phylogenetic distribution of burrowing behaviour within the Castorid tree (Fig. 8), it is likely that the common ancestor of the fossorial and semiaquatic clades also burrowed. Thus, the appearance of burrowing behaviour within Castor and Steneofiber are seen as a retention of a primitive trait9.
If burrowing behaviour in semiaquatic castorids is the primitive condition, it is likely Dipoides burrowed as well, as seen in other semiaquatic rodents today such as Castor, but also Crossomys (earless water rat), Myocastor (nutria), and Ondatra (muskrat)92. It is also possible that Dipoides constructed lodges. Extant Castor and Ondatra are known to construct burrows and lodges, depending on the characteristics of the habitat. Bank burrows are associated with stream environments, whereas lodges are better suited to calmer waters92. Unlike Castor, extant Ondatra construct their push-up lodges using cattails and other fibrous vegetation rather than wood. The abundance of cut wood at the Beaver Pond site11 suggests that Dipoides sp. had the option to incorporate wood into their nesting structures, and possibly built lodges.
Given the occurrence of woodcutting and woody plant consumption within both subfamilies of semiaquatic castorids (represented by Castor and Dipoides in Fig. 8), it seems likely these behaviours appeared in the common ancestor of the semiaquatic group. Woody plant consumption may have preadapted castorids to exploit colder environments that arose during and after the late Miocene. Castor canadensis does not hibernate, but builds and sink rafts of branches and foliage to use as a source of fresh food during the winter months1,93. Dipoides sp. may have also engaged in this behaviour and used underwater caches of branches as a primary food source to survive the consecutive months of darkness during the high latitude winter when plants become dormant. The use of woody plants in this way may have been key to allowing beavers to disperse between North American and Eurasia, which required crossing the Bering Isthmus94, a high latitude landmass. Curiously, given that a diet rich in woody plants appears to be the primitive condition of semiaquatic castorids, the absence of woody plant consumption seen in the Pleistocene giant beaver Castoroides13 must be interpreted here as an evolutionary loss and potentially a leading factor in their extinction (Fig. 8).
Among living mammals, Castor’s dam construction is a unique and highly derived behaviour – an evolutionary puzzle, associated with a set of innate behavioural specializations95. For example, dam construction is well known to be triggered by the sound of running water alone95. The presence of such “hard-wired” behaviours may be associated with the ancient origins of this behaviour. Molecular and fossil occurrence records indicate that the split between Eurasian and North American Castor arose around 7.5 Ma ago96,97, implying that dam building behaviour itself is at least as old.
Definitive fossil evidence for dam building by an extinct beaver is currently lacking. Consequently, dam building behaviour is shown as possibly arising only on the lineage leading to Castor. Hypothetically, dam building may have arisen from beavers collecting branches near their burrow/lodge for feeding purposes and the accumulations of sticks could have dammed streams by happenstance. The effects may have been multifold. A deeper pond is an effective defense mechanism and provides a safe refuge from predators. Raised water levels also create more favourable conditions for underwater food caching of branches in sub-freezing winter conditions because the deeper water would prevent an underwater food cache from being locked in ice. As such, natural selection would have favoured animals that maintained the dam, presumably as an extension of their pre-existing nesting behaviour such as lodge building. In this scenario, the climate cooling that started around 15 Ma ago and continued into the Pleistocene would have provided an interval where behaviours promoting over-wintering survival, such as underwater food caching branches and dam building, would have been increasingly reinforced by natural selection.
It seems unlikely that the common ancestor of all semiaquatic beavers was a dam-builder. Extant Castor is a large powerful rodent weighing 12–25 kg, with some individuals as large as 40 kg92. Its body size is one factor that allows the animal to harvest branches and whole trees to build lodges and maintain dams over multiple years. The Beaver Pond site Dipoides sp. was also a large rodent and was roughly two-thirds the size of an average extant Castor. In contrast, the less-derived semiaquatic beavers, such as the Miocene Eucastor tortus (Castoroidinae) and Steneofiber eseri (Castorinae) were small (~ 1 kg, or less), suggesting that the common ancestor of the semiaquatic lineage was also small bodied. Although the common ancestor of the semiaquatic beaver lineage is inferred to have consumed woody plants (this study), and may have used branches in creating food piles and wood for lodge construction, it would have been too small to have had the capacity to build and maintain dams. As such, if Dipoides sp. did exhibit dam building behaviour, it would be the result of parallel evolution within the Castoroidinae and Castorinae lineages.
Here, we reconstruct Pliocene High Arctic Dipoides sp. palaeodiet from bone collagen δ13C and δ15N within the context of an isotopic dietary baseline composed of coeval ~ 4 Ma old terrestrial and freshwater plant macrofossil remains. The Beaver Pond site provides a very rare opportunity for such a palaeodiet reconstruction using coeval herbivore and plant remains. A Bayesian mixing model indicates that Dipoides sp. diet was composed of approximately equal proportions of woody plant material and freshwater macrophytes, with slightly more emphasis on macrophyte consumption. Dipoides sp. dietary preferences lie somewhere in between those of other North American late Cenozoic semiaquatic beavers (extant Castor and extinct Pleistocene giant beaver, Castoroides).
The consumption of woody plant material suggests that a proportion of the assemblage of the wood cut by Dipoides sp. at the Beaver Pond fossil site was the result of harvesting for consumption, possibly as part of an underwater winter food cache. The results also suggest that the early Miocene ancestor of the semiaquatic beaver lineage engaged in woodcutting and consumed woody plants as part of its diet. Swimming, woodcutting, and a diet of woody plants could have set the stage for the evolution of dam building behaviours—advantageous traits that may have been selected for by the cooling climate of the late Neogene, and which have resulted in Castor’s modern role as a keystone species and ecosystem engineer.
The Dipoides sp. skeletal material and the plant macrofossils used in this study originated from the Beaver Pond fossil site, Unit III, as defined by Mitchell et al.21. Unit III is a peat layer that yielded the majority of the beaver-cut sticks and vertebrate faunal remains discovered at the site. It is interpreted to have been a rich fen connected to open water, within a larch-dominated forest ecosystem21.
Plant macrofossil preparation
Plant macrofossils were isolated from bulk samples of Unit III peat and identified to taxon. Macrofossils were extracted from the peat using a combination of water-flotation and wet-sieving. Organic material greater than 0.425 mm was retained for further cleaning. Adhered sediment and moss were removed from the macrofossils using surgical forceps and repeated ultrasonic water baths. Cleaned macrofossils were dried at 26 °C for 24 h and identified to taxon using a binocular microscope.
Stable isotope analysis
Dipoides sp. bone collagen was extracted and its δ13C and δ15N measured at the Alaska Stable Isotope Facility (UAF). Collagen extraction was performed using a modified Longin98 method of gelatinization. Organic contaminants were removed using XAD-2 resin99,100 and collagen purification was performed according to methods developed by Matheus101. Non-soluble collagenous portions were rinsed to neutral pH, but not subjected to base treatment. Collagen was gelatinized in weak HCl (pH 3) under N2 gas at 105° C until dissolved (2 to 6 h). The solution was centrifuged and filtered with a 0.45 µm syringe-type PTFE filter and the supernatant containing dissolved collagen was lyophilized and weighed to determine the percent collagen yield. Lyophilized collagen was then hydrolyzed in 6 N HCL under N2 gas for 4 h at 120 °C. The hydrolyzates were passed by gravity flow through 2 cc of compacted Serva XAD-2 HPLC resin in syringe columns to extract humates and other long-chain organic contaminants that can adhere to fossil collagen. The hydrolyzates were passed through a 0.45 µm PTFE filter placed at the distal end of each syringe column and were dried by rotary evaporation. Stable carbon and nitrogen isotope analysis of the hydrolyzed collagen was performed using a GC-Isolink gas chromatography combustion system coupled to a Thermo Scientific Delta V Plus isotope ratio mass spectrometer operated in continuous flow mode, using helium as the carrier gas.
Plant macrofossils were powdered using a ball-bearing mill and weighed into tin capsules (0.38 ± 0.02 mg). Stable carbon and nitrogen isotope analysis of macrofossil remains was conducted at the LSIS-AFAR facility at the University of Western Ontario (London, Canada). Samples were analyzed in continuous flow mode using a Costech elemental analyzer (ECS 4010), coupled to a Thermo Scientific ConFlo IV and Delta V Plus isotope ratio mass spectrometer in continuous flow mode, using helium as the carrier gas. One method duplicate (complete duplication of sample preparation and isotopic analysis) and one analytical duplicate (separate isotopic analysis of sample powder) were included for every ten samples. The carbon and nitrogen isotope measurements of the plant macrofossils were completed in separate analytical sessions. The first session was used to determine δ13C and nitrogen content (weight percent, N wt%); values of δ15N were determined in the second session, using individually tailored weights based on each sample’s N wt%.
All isotopic results are reported in δ-notation in per mil (‰) relative to international standards. Collagen δ13C and δ15N were calibrated to VPDB and AIR, respectively. Analytical accuracy and precision were 0.0‰ for δ13C measurements, and 0.2‰ for δ15N measurements.
Plant macrofossil δ13C and δ15N were calibrated to VPDB and AIR, respectively using USGS40 (accepted δ13C = − 26.39‰, SD = ± 0.0‰; accepted δ15N = − 4.52‰, SD = ± 0.2‰) and USGS41a (accepted δ13C = + 36.55‰, SD = ± 0.1‰; accepted δ15N = + 47.55‰, SD = ± 0.2‰). Additional reference materials IAEA-CH-6 (accepted δ13C = − 10.45‰, SD = ± 0.0‰) and NIST-1547 (Peach Leaves) (internally calibrated δ15N = + 1.98‰, SD = ± 0.1‰) were used to evaluate instrument precision and accuracy for δ13C and δ15N, respectively. A keratin powder (Spectrum Chemicals Mfg. Corp., derived from pig skin and hair) was also included to monitor instrument drift. Combined instrument and analytical errors were ± 0.1‰ for δ13C, and ± 0.2‰ for δ15N.
The Dipoides sp. and plant macrofossil isotopic results were incorporated into a statistically-based Bayesian mixing model (SIAR V4). This approach provides a statistically robust means of evaluating the relative dietary contributions of woody plants and aquatic primary producers to Dipoides sp. Diet102.
The authors declare no limitations on data or standard operating protocol availability.
Slough, B. G. Beaver food cache structure and utilization. J. Wildl. Manag. 42, 644–646 (1978).
Wright, J. P., Jones, C. G. & Flecker, A. S. An ecosystem engineer, the beaver, increases species richness at the landscape scale. Oecologia 132, 96–101 (2002).
Müller-Schwarze, D. & Sun, L. The Beaver: Natural History of a Wetlands Engineer (Cornell University Press, Ithaca, 2003).
Rosell, F., Bozser, O., Collen, P. & Parker, H. Ecological impact of beavers Castor fiber and Castor canadensis and their ability to modify ecosystems. Mammal Rev. 35, 248–276 (2005).
Aleksiuk, M. The seasonal food regime of arctic beavers. Ecology 51, 254–270 (1970).
Lancia, R. A., Dodge, W. E. & Larson, J. S. Winter activity patterns of two radio-marked beaver colonies. J. Mammal. 63, 598–606 (1982).
Korth, W. W. Comments on the systematics and classification of the beavers (Rodentia, Castoridae). J. Mammal. Evol. 8, 279–296 (2002).
Korth, W. W. & Rybczynski, N. A new, unusual castorid (Rodentia) from the earliest Miocene of Nebraska. J. Vertebr. Paleontol. 23, 667–675 (2003).
Rybczynski, N. Castorid phylogenetics: implications for the evolution of swimming and tree–exploitation in beavers. J. Mammal. Evol. 14, 1–35 (2007).
Tedford, R. H. & Harington, C. R. An Arctic mammal fauna from the early Pliocene of North America. Nature 425, 388–390 (2003).
Rybczynski, N. Woodcutting behavior in beavers (Castoridae, Rodentia): estimating ecological performance in a modern and a fossil taxon. Paleobiology 34, 389–402 (2008).
Xenikoudakis, G. et al. Ancient DNA reveals twenty million years of aquatic life in beavers. Curr. Biol. 30, R110–R111 (2020).
Plint, T., Longstaffe, F. J. & Zazula, G. Giant beaver palaeoecology inferred from stable isotopes. Sci. Rep. 9, 1–12 (2019).
Rybczynski, N. et al. Mid-Pliocene warm–period deposits in the High Arctic yield insight into camel evolution. Nat. Commun. 4, 1–9 (2013).
Fletcher, T. L. et al. Evidence for fire in the Pliocene Arctic in response to amplified temperature. Clim. Past 15, 1063–1081 (2019).
Rybczynski, N. & Harington, C. R. Tarsal evidence for ecomorph reconstruction in fossil lagomorphs. J. Vertebr. Paleontol. 17, 72A (1997).
Matthews, J. V. Jr. & Fyles, J. G. Late Tertiary plant and arthropod fossils from the High Terrace Sediments on the Fosheim Peninsula of Ellesmere Island (Northwest Territories, District of Franklin). Geol. Surv. Can. Bull. 529, 295–317 (2000).
Hutchison, J. H. & Harington, C. R. A peculiar new fossil shrew (Lipotyphla, Soricidae) from the High Arctic of Canada. Can. J. Earth Sci. 39, 439–443 (2002).
Dawson, M. R. & Harington, C. R. Boreameryx, an unusual new artiodactyl (Mammalia) from the Pliocene of Arctic Canada and endemism in Arctic fossil mammals. Can. J. Earth Sci. 44, 585–592 (2007).
Murray, A. M., Cumbaa, S. L., Harington, C. R., Smith, G. R. & Rybczynski, N. Early Pliocene fish remains from Arctic Canada support a pre-Pleistocene dispersal of percids (Teleostei: Perciformes). Can. J. Earth Sci. 46, 557–570 (2009).
Mitchell, W. T. et al. Stratigraphic and paleoenvironmental reconstruction of a mid-Pliocene fossil site in the High Arctic (Ellesmere Island, Nunavut): evidence of an ancient peatland with evidence of beaver activity. Arctic 69, 185–204 (2016).
Gosse, J. C. et al. PoLAR-FIT: Pliocene landscapes and arctic remains-frozen in time. Geosci. Can. 44, 47–54 (2017).
Wang, X., Rybczynski, N., Harington, C. R., White, S. C. & Tedford, R. H. A basal ursine bear (Protarctos abstrusus) from the Pliocene High Arctic reveals Eurasian affinities and a diet rich in fermentable sugars. Sci. Rep. 7, 1–14 (2017).
Fletcher, T., Feng, R., Telka, A. M., Matthews, J. V. Jr. & Ballantyne, A. Floral dissimilarity and the influence of climate in the Pliocene High Arctic: Biotic and abiotic influences on five sites on the Canadian Arctic Archipelago. Front. Ecol. Environ. 5, 1–19 (2017).
Davies, N. S., Gosse, J. C. & Rybczynski, N. Cross-bedded woody debris from a Pliocene forested river system in the High Arctic: Beaufort Formation, Meighen Island, Canada. J. Sedim. Res. 84, 19–25 (2014).
Tozer, E. T. Geological reconnaissance: Prince Patrick, Eglinton, and Western Melville Islands, Arctic Archipelago, Northwest Territories. Geol. Surv. Can. 55, 1–32 (1956).
Gladenkov, A. Y. & Gladenkov, Y. B. Onset of connections between the Pacific and Arctic Oceans through the Bering Strait in the Neogene. Stratigr. Geol. Correl. 12, 175–187 (2004).
Lisiecki, L. E. & Raymo, M. E. A Pliocene-Pleistocene stack of 57 globally distributed benthic δ18O records. Paleoceanogr. Paleoclimatol. 20, 1–17 (2005).
Elias, S. A. & Matthews, J. V. Jr. Arctic North American seasonal temperatures from the latest Miocene to the Early Pleistocene, based on mutual climatic range analysis of fossil beetle assemblages. Can. J. Earth Sci. 39, 911–920 (2002).
Ballantyne, A. P., Rybczynski, N., Baker, P. A., Harington, C. R. & White, D. Pliocene Arctic temperature constraints from the growth rings and isotopic composition of fossil larch. Palaeogeogr. Palaeoclimatol. Palaeoecol. 242, 188–200 (2006).
Ballantyne, A. P. et al. Significantly warmer Arctic surface temperatures during the Pliocene indicated by multiple independent proxies. Geology 38, 603–606 (2010).
Csank, A. Z., Patterson, W. P., Eglington, B. M., Rybczynski, N. & Basinger, J. F. Climate variability in the Early Pliocene Arctic: Annually resolved evidence from stable isotope values of sub-fossil wood, Ellesmere Island, Canada. Palaeogeogr. Palaeoclimatol. Palaeoecol. 308, 339–349 (2011).
Csank, A. Z. et al. Estimates of Arctic land surface temperatures during the early Pliocene from two novel proxies. Earth Planet. Sci. Lett. 304, 291–299 (2011).
Hills, L. V. Late Tertiary floras Arctic Canada: an interpretation. Proc. Circ. Conf. North. Ecol. Natl. Res. Counc. Can. 1, 165–171 (1975).
Matthews, J. V. Jr. Plant macrofossils from the Neogene Beaufort Formation on Banks and Meighen islands, District of Franklin. Curr. Res. Part A Geol. Surv. Can. 871, 73–87 (1987).
Fyles, J. G., Marincovich, J. L., Matthews, J. V. Jr. & Barendregt, R. Unique mollusc find in the Beaufort formation (Pliocene) on Meighen Island, Arctic Canada. Curr. Res. Part B Geol. Surv. Can. 91, 105–112 (1991).
Ruez, D. R. Revision of the Blancan (Pliocene) mammals from Hagerman Fossil Beds National Monument, Idaho. JIAS 45, 1–144 (2009).
Tedford, R. H., Flynn, L. J., Zhanxiang, Q., Opdyke, N. D. & Downs, W. R. Yushe Basin, China: paleomagnetically calibrated mammalian biostratigraphic standard from the late Neogene of eastern Asia. J. Vertebr. Paleontol. 11, 519–526 (1991).
Xu, X. Evolution of Chinese Castoridae. Natl. Sci. Mus. Monogr. 8, 77–97 (1994).
Hugueney, M. Family Castoridae. In: The Miocene Land Mammals of Europe (Verlag F. Pfeil, 1999), 281–300.
Qiu, Z. D. & Li, Q. Neogene rodents from central Nei Mongol, China. Palaeontol. Sin. 198, 1–676 (2016).
Samuels, J. X. & Van Valkenburgh, B. Skeletal indicators of locomotor adaptations in living and extinct rodents. J. Morphol. 269, 1387–1411 (2008).
Schoeninger, M. J. Diet reconstruction and ecology using stable isotope ratios. In: A Companion to Biological Anthropology (Blackwell Publishing Ltd., 2010), 445–464.
Koch, P. L., Fox-Dobbs, K. E. N. A. & Newsome, S. D. The Isotopic Ecology of Fossil Vertebrates and Conservation Paleobiology 101–118 (The University of Chicago Press, Chicago, 2017).
Casey, M. M. & Post, D. M. The problem of isotopic baseline: reconstructing the diet and trophic position of fossil animals. Earth Sci. Rev. 106, 131–148 (2011).
Long, E. S., Sweitzer, R. A., Diefenbach, D. R. & Ben-David, M. Controlling for anthropogenically induced atmospheric variation in stable carbon isotope studies. Oecologia 146, 148–156 (2005).
Tahmasebi, F., Longstaffe, F. J. & Zazula, G. Nitrogen isotopes suggest a change in nitrogen dynamics between the Late Pleistocene and modern time in Yukon, Canada. PLoS ONE 13, 1–31 (2018).
Van Klinken, G. J. Bone collagen quality indicators for palaeodietary and radiocarbon measurements. J. Archaeol. Sci. 26, 687–695 (1999).
Metcalfe, J. Z. & Mead, J. J. Do uncharred plants preserve original carbon and nitrogen isotope compositions?. J. Archaeol. Method Theory 26, 844–872 (2019).
DeNiro, M. J. & Epstein, S. Influence of diet on the distribution of carbon isotopes in animals. Geochim. Cosmochim. Acta 42, 495–506 (1978).
DeNiro, M. J. & Epstein, S. Influence of diet on the distribution of nitrogen isotopes in animals. Geochim. Cosmochim. Acta 45, 341–351 (1981).
Kelly, J. Stable isotopes of carbon and nitrogen in the study of avian and mammalian trophic ecology. Can. J. Zool. 45, 1–27 (2000).
Froehle, A. W., Kellner, C. M. & Schoeninger, M. J. FOCUS: effect of diet and protein source on carbon stable isotope ratios in collagen: follow up to Warinner and Tuross (2009). J. Archaeol. Sci. 37, 2662–2670 (2010).
Keeley, J. E. & Sandquist, D. R. Carbon: freshwater plants. Plant Cell Environ. 15, 1021–1035 (1992).
Mendonça, R. et al. Bimodality in stable isotope composition facilitates the tracing of carbon transfer from macrophytes to higher trophic levels. Hydrobiologia 710, 205–218 (2013).
Chappuis, E., Seriñá, V., Martí, E., Ballesteros, E. & Gacia, E. Decrypting stable-isotope (δ13C and δ15N) variability in aquatic plants. Freshw. Biol. 62, 1807–1818 (2017).
Larson, T. E. & Longstaffe, F. J. Deciphering seasonal variations in the diet and drinking water of modern White-Tailed deer by in situ analysis of osteons in cortical bone. J. Geophys. Res. Biogeol. 112, 1–12 (2007).
Van der Wal, R. Trading forage quality for quantity? Plant phenology and patch choice by Svalbard reindeer. Oecologia 123, 108–115 (2000).
Crawley, M. J. Herbivory: The Dynamics of Animal–Plant Interactions (Blackwell, Hoboken, 1983).
Hartley, S. E. and Jones, C. G. Plant chemistry and herbivory, or why the world is green. In: Plant Ecology (Blackwell Science Ltd, 1996), 284–324.
Tahmasebi, F., Longstaffe, F. J., Zazula, G. & Bennett, B. Nitrogen and carbon isotopic dynamics of subarctic soils and plants in southern Yukon Territory and its implications for paleoecological and paleodietary studies. PLoS ONE 12, 1–26 (2017).
Proctor, M. C. F., Raven, J. A. & Rice, S. K. Stable carbon isotope discrimination measurements in Sphagnum and other bryophytes: physiological and ecological implications. J. Bryol. 17, 193–202 (1992).
Hornibrook, E. R., Longstaffe, F. J., Fyfe, W. S. & Bloom, Y. Carbon-isotope ratios and carbon, nitrogen and sulfur abundances in flora and soil organic matter from a temperate-zone bog and marsh. Geochem. J. 34, 237–245 (2000).
Granath, G. et al. Environmental and taxonomic controls of carbon and oxygen stable isotope composition in Sphagnum across broad climatic and geographic ranges. Biogeosciences 15, 5189–5202 (2018).
Lüthi, D. et al. High–resolution carbon dioxide concentration record 650,000–800,000 years before present. Nature 453, 379–382 (2008).
Pagani, M., Liu, Z., LaRiviere, J. & Ravelo, A. C. High Earth–system climate sensitivity determined from Pliocene carbon dioxide concentrations. Nat. Geosci. 3, 27–30 (2010).
Schröder, W. et al. First Europe-wide correlation analysis identifying factors best explaining the total nitrogen concentration in mosses. Atmos. Environ. 44, 3485–3491 (2010).
Harmens, H. et al. Nitrogen concentrations in mosses indicate the spatial distribution of atmospheric nitrogen deposition in Europe. Environ. Pollut. 159, 2852–2860 (2011).
Lazar, J. G. et al. Beaver ponds: resurgent nitrogen sinks for rural watersheds in the northeastern United States. J. Environ. Qual. 44, 1684–1693 (2015).
Osmond, C. B., Valaane, N., Haslam, S. M., Uotila, P. & Roksandic, Z. Comparisons of δ13C values in leaves of aquatic macrophytes from different habitats in Britain and Finland; some implications for photosynthetic processes in aquatic plants. Oecologia 50, 117–124 (1981).
Hoering, T. C. & Ford, H. T. The isotope effect in the fixation of nitrogen by Azotobacter. J. Am. Chem. Soc. 82, 376–378 (1960).
Mariotti, A. et al. Experimental determination of nitrogen kinetic isotope fractionation: some principles: illustration for the denitrification and nitrification processes. Plant Soil 62, 413–430 (1981).
Shearer, G. & Kohl, D. H. N2–fixation in field settings: estimations based on natural 15N abundance. Funct. Plant Biol. 13, 699–756 (1986).
Farrar, J. L. Trees in Canada (Fitzhenry and Whiteside Limited, Markham, 1995).
Farquhar, G. D., Hubick, K. T., Condon, A. G. & Richards, R. A. Carbon isotope fractionation and plant water-use efficiency. In: Stable Isotopes in Ecological Research. Ecological Studies (Analysis and Synthesis) (Springer, 1989), 21–40.
Tipple, B. J., Meyers, S. R. & Pagani, M. Carbon isotope ratio of Cenozoic CO2: a comparative evaluation of available geochemical proxies. Paleoceanogr. Paleoclimatol. 25, 1–11 (2010).
Dietze, M. C. et al. Nonstructural carbon in woody plants. Annu. Rev. Plant Biol. 65, 667–687 (2014).
Swap, R. J., Aranibar, J. N., Dowty, P. R., Gihooly, W. P. III. & Macko, S. A. Natural abundance of 13C and 15N in C3 and C4 vegetation of southern Africa: patterns and implications. Glob. Change Biol. 10, 350–358 (2004).
Craine, J. M. et al. Global patterns of foliar nitrogen isotopes and their relationships with climate, mycorrhizal fungi, foliar nutrient concentrations, and nitrogen availability. New Phytol. 183, 980–992 (2009).
Handley, L. L. et al. The 15N natural abundance (δ15N) of ecosystem samples reflects measures of water availability. Funct. Plant Biol. 26, 185–199 (1999).
Keeling, R. F., Walker, S. J., Piper, S. C. & Bollenbacher, A. F. Scripps CO2 Program. Scripps Institution of Oceanography: University of California, https://scrippsco2.ucsd.edu (2014).
Schmitt, J. et al. Carbon isotope constraints on the deglacial CO2 rise from ice cores. Science 336, 711–714 (2012).
Milligan, H. E. & Humphries, M. M. The importance of aquatic vegetation in beaver diets and the seasonal and habitat specificity of aquatic-terrestrial ecosystem linkages in a subarctic environment. Oikos 119, 1877–1886 (2010).
Samuels, J. X. & Van Valkenburgh, B. Craniodental adaptations for digging in extinct burrowing beavers. J. Vertebr. Paleontol. 29, 254–268 (2009).
Samuels, J. X. Cranial morphology and dietary habits of rodents. Zool. J. Linnean Soc. 156, 864–888 (2009).
Calede, J. J. M. Skeletal morphology of Palaeocastor peninsulatus (Rodentia, Castoridae) from the Fort Logan Formation of Montana (early Arikareean): ontogenetic and paleoecological interpretations. J. Mammal. Evol. 21, 223–241 (2014).
Calede, J. J. M., Samuels, J. X. & Chen, M. Locomotory adaptations in entoptychine gophers (Rodentia: Geomyidae) and the mosaic evolution of fossoriality. J. Morphol. 280, 879–907 (2019).
Peterson, O. A. Description of new rodents and discussion of the origin of Daemonelix. Mem. Carn. Mus. 32, 139–203 (1905).
Stirton, R. A. A new beaver from the Pliocene of Arizona with notes on the species of Dipoides. J. Mammal. 17, 279–281 (1936).
Korth, W. W. Castoridae. In: The Tertiary Record of Rodents in North America (Springer, 1994), 135–148.
Hugueney, M. & Escuillié, F. K-strategy and adaptative specialization in Steneofiber from Montaigu-le-Blin (dept. Allier, France; Lower Miocene, MN 2a, ±23 Ma): first evidence of fossil life-history strategies in castorid rodents. Palaeogeogr. Palaeoclimatol. Palaeoecol. 113, 217–225 (1995).
Nowak, R. M. & Walker, E. P. Walker’s Mammals of the World (John Hopkins University Press, Baltimore, 1999).
Busher, P. E. Food caching behavior of beavers (Castor canadensis): selection and use of woody species. Am. Midl. Nat. 135, 343–348 (1996).
Flynn, L. J. & Jacobs, L. L. Castoroidea. In: Evolution of Tertiary Mammals of North America: Small Mammals, Xenarthrans, and Marine Mammals (Vol 2), 391–405 (Cambridge University Press, 2008).
Wilsson, L. Observations and Experiments on the Ethology of the European Beaver (Castor fiber L.): A Study in the Development of Phylogenetically Adapted Behavior in a Highly Specialized Mammal (Doctoral Disseration, 1971).
Horn, S. Mitochondrial genomes reveal slow rates of molecular evolution and the timing of speciation in beavers (Castor), one of the largest rodent species. PLoS ONE 6, 1–9 (2011).
Samuels, J. X. & Zancanella, J. An early Hemphillian occurrence of Castor (Castoridae) from the Rattlesnake Formation of Oregon. J. Paleontol. 85, 930–935 (2011).
Longin, R. New method of collagen extraction for radiocarbon dating. Nature 230, 241–242 (1971).
Stafford, T. W. Jr., Brendel, K. & Duhamel, R. C. Radiocarbon, 13C and 15N analysis of fossil bone: removal of humates with XAD-2 resin. Geochim. Cosmochim. Acta 52, 2257–2267 (1988).
Stafford, T. W. Jr., Hare, P. E., Currie, L., Jull, A. T. & Donahue, D. J. Accelerator radiocarbon dating at the molecular level. J. Archaeol. Sci. 18, 35–72 (1991).
Matheus, P. E. Diet and co-ecology of Pleistocene short-faced bears and brown bears in eastern Beringia. Quat. Res. 44, 447–453 (1995).
Inger, R., Jackson, A., Parnell, A. & Bearhop, S. SIAR V4 (Stable Isotope Analysis in R) An Ecologist’s Guide (2010).
Schlosser, M. Extinct beaver (Castor neglectus) from Tertiary of South Germany. Neues Jahrb Geol. Part A 9, 136 (1902).
Flynn, L. J. The antiquity of Rhizomys and independent acquisition of fossorial traits in subterranean Muroids. Bull. Am. Mus. Nat. Hist. 331, 128–156 (2009).
Samuels, J. X. & Hopkins, S. S. B. The impacts of Cenozoic climate and habitat changes on small mammal diversity of North America. Glob. Planet. Change 149, 36–52 (2017).
Hulbert, R., Kerner, A. & Morgan, G. Taxonomy of the Pleistocene giant beaver Castoroides (Rodentia: Castoridae) from the southeastern United States. Bull. Florida Mus. Nat. Hist. 53, 26–43 (2014).
The Pliocene peat sample was collected in 2006, supported by the Canadian Museum of Nature (N.R.), National Geographic Exploration Grant, Scientific Research Grant # 7902-05 (N.R.) and with logistical support by the Polar Continental Shelf Program (N.R.). Collection permit from Nunavut’s Department of Culture, Language, Elders and Youth (Permit No. 2006-002P), and with permission from the Qikiqtani Inuit Association and the Hamlet of Grise Fiord (Aujuittuq). Financial support for this research was provided by a Natural Sciences and Engineering Research Council Discovery grant (F.J.L.), Canada Research Chairs program (F.J.L.), Canada Foundation for Innovation (F.J.L.) and the Ontario Research Fund (F.J.L.). This is Western’s Laboratory for Stable Isotope Science Contribution #378. Dipoides sp. bone collagen stable isotope measurements provided by Paul Matheus (University of Alaska Fairbanks). We thank Martin Lipman for providing photographs of the Beaver Pond site, Donna Naughton for provision of map templates, and Michael Burzynski for additional advice concerning plant physiology.
The authors declare no competing interests.
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Plint, T., Longstaffe, F.J., Ballantyne, A. et al. Evolution of woodcutting behaviour in Early Pliocene beaver driven by consumption of woody plants. Sci Rep 10, 13111 (2020). https://doi.org/10.1038/s41598-020-70164-1