- Research article
- Open Access
Ancient feeding ecology inferred from stable isotopic evidence from fossil horses in South America over the past 3 Ma
BMC Ecology volume 11, Article number: 15 (2011)
Stable isotope ratios (13C/12C and 18O/16O) in fossil teeth and bone provide key archives for understanding the ecology of extinct horses during the Plio-Pleistocene in South America; however, what happened in areas of sympatry between Equus (Amerhippus) and Hippidion is less understood.
Here, we use stable carbon and oxygen isotopes preserved in 67 fossil tooth and bone samples for seven species of horses from 25 different localities to document the magnitude of the dietary shifts of horses and ancient floral change during the Plio-Pleistocene. Dietary reconstructions inferred from stable isotopes of both genera of horses present in South America document dietary separation and environmental changes in ancient ecosystems, including C3/C4 transitions. Stable isotope data demonstrate changes in C4 grass consumption, inter-species dietary partitioning and variation in isotopic niche breadth of mixed feeders with latitudinal gradient.
The data for Hippidion indicate a preference varying from C3 plants to mixed C3-C4 plants in their diet. Equus (Amerhippus) shows three different patterns of dietary partitioning Equus (A.) neogeus from the province of Buenos Aires indicate a preference for C3 plants in the diet. Equus (A.) andium from Ecuador and Equus (A.) insulatus from Bolivia show a preference for to a diet of mixed C3-C4 plants, while Equus (A.) santaeelenae from La Carolina (sea level of Ecuador) and Brazil are mostly C4 feeders. These results confirm that ancient feeding ecology cannot always be inferred from dental morphology. While the carbon isotope composition of horses skeletal material decreased as latitude increased, we found evidence of boundary between a mixed C3/C4 diet signal and a pure C4 signal around 32° S and a change from a mixed diet signal to an exclusively C3 signal around 35°S.
We found that the horses living at high altitudes and at low to middle latitude still have a C4 component in their diet, except the specimens from 4000 m, which have a pure C3 diet. The change in altitudinal vegetation gradients during the Pleistocene is one of several possibilities to explain the C4 dietary component in horses living at high altitudes. Other alternative explanations imply that the horses fed partially at lower altitudes.
In South America, horses are represented by two groups: equidiforms and hippidiforms. Hippidion are characterized by a retracted nasal notch which has been interpreted as an adaptation to the presence of a proboscis and limbs with robust metapodials. The upper teeth present an elongate-oval protocone with simple enamel plication and lower teeth have a deep ectoflexid, penetrating the isthmus (Figure 1). On the other hand, in Equus (Amerhippus) a retracted nasal notch is not present and the metapodials are slender. The upper teeth present a triangular protocone and multiple internal posfossette plications. There are features that are common to both of these groups, such as differentiation into horses of both small and large body size, which are possibly a consequence of convergence due to adaptation to similar environments. The three species of hippidiforms are included within the genus Hippidion Owen, 1869 [1, 2] whereas the five species of equidiforms are included in the subgenus Equus (Amerhippus) . Each of these groups has different ecological adaptations that are evident in the cranial morphology, robustness of the limbs and body size [4, 5].
A technique that has proven useful for investigating the ecology of fossil horses is through examination of stable isotope values found in teeth and bone in combination with dental wear [6–16]. Isotopic analyses can reveal information about resource use and resource partitioning among species and is also able to determine diet and habitat use [15, 17]. Here, we will address: (1) whether stable isotope values permit identification of resource use and partitioning among horse species and (2) if resource use and partitioning are determined, do the results support the ecology predicted by morphology or body size? Finally, we compare carbon isotope values and evaluate the hypothesis that dietary niches, inferred from the mean and variation of carbon isotope values, did not change throughout time in the same latitude.
Stable carbon and oxygen isotopes are incorporated into the tooth and bone apatite of horses and are representative, respectively, of the food and water consumed while alive. The carbon isotope ratio is influenced by the type of plant material ingested, which is in turn influenced by the photosynthetic pathway utilized by the plants. During photosynthesis, C3 plants in terrestrial ecosystems (trees, bushes, shrubs, forbs, and high altitude and high latitude grasses) discriminate more markedly against the heavy 13C isotope during fixation of CO2 than C4 plants (tropical grasses and sedges). Thus C3 and C4 plants have distinct δ13C values. C3 plants usually have δ13C values of -30 per mil (‰) to -22‰, with an average of approximately -26‰, whereas C4 plants have δ13C values of -14 to -10‰, with an average of about -12‰ [18–22]. Animals incorporate carbon isotopes from food into their teeth and bone with an additional fractionation of ~12 to 14‰ [23, 24]. Mammals feeding on C3 plants characteristically have δ13C values between -14 and -8‰, while animals that eat C4 tropical grasses have δ13C values between +2 and -2‰. A mixed-feeder would fall somewhere in between these two extremes [25, 26]. Hence, the relative proportions of C3 and C4 vegetation in the diet of an animal can be determined by analyzing the δ13 C value of its teeth and bones.
A number of previous studies have used the carbon and oxygen isotopic abundance of fossils and paleosols from South America to reconstruct the diets of extinct herbivores and the paleoenvironmental parameters of ancient terrestrial communities and ecosystems [27–32]. Carbon isotope data for horses from South America have been presented in several papers [8, 33–35]. In 1999, MacFadden et al.  presented the ancient distributions and latitudinal gradients of C3 and C4 grasses based on isotopic data from New World Pleistocene horses. In addition, some papers have investigated the application of geochemical techniques in conjunction with morphological and dental wear data to reconstruct the feeding ecology and niche characterization of individual species [34, 36, 37].
All equid taxa from South America were sampled for teeth (n:29) and bone (n:38) stable carbon and oxygen isotopes (table 1 and 2). Additional data of thirty samples were taken from MacFadden et al. . Together the data represent five species within the subgenus Equus (Amerhippus): E. (A.) andium, E. (A.) insulatus, E. (A.) neogeus, E. (A.) santaeelenae and E. (A.) lasallei. The genus Hippidion includes three species: H. principale, H. devillei and H. saldiasi. Some of these valid species have a wide geographical distribution whilst others, such as E. (A.) andium and E. (A.) insulatus, are restricted to the Andes region. In contrast, E. (A.) neogeus, E. (A.) santaeelenae and E. (A.) lasallei are found in the non-Andean tropical or subtropical regions of South America such as Argentina, Uruguay, Colombia, Brazil, and the coastal area of Ecuador (Figure 2). H. saldiasi is restricted to a particular habitat in southern Patagonia [38, 39]; while H. principale and H. devillei come from different localities in South America, such as Tarija in Bolivia and the Pampa region in Argentina, that cover a broad range of altitudes from 10 to 4000 m. One restriction to our study is the chronological control of the sample. Most of the samples were collected from old museum collections in Ecuador, Bolivia and Argentina. These old collections were recovered without sufficient stratigraphic control. Anyway we considered this limitation may condition the interpretations about altitudinal and latitudinal gradients for fossil samples, but do not invalidate the suggested patterns.
In order to demonstrate how dietary resources were partitioned we divided the samples into 10 different groups taking into account the genus, as well as the age and the altitude of the corresponding deposit. Data for these groups and descriptive statistics are listed in table 3: (A) all Hippidion; (B) all Equus (Amerhippus); (C) Hippidion from the Late Pleistocene; (D) Hippidion from the Late Pliocene to Early Pleistocene; (E) Equus (Amerhippus) from the Late Pleistocene; (F) Equus (Amerhippus) from the Middle Pleistocene; (G) Equus (Amerhippus) from the plains; (H) Equus (Amerhippus) from the mountain corridor; (I) Hippidion from the plains; and (J) Hippidion from the mountain corridor.
Fossil samples were collected from specimens stored at the following institutions in Argentina: Museo de La Plata, Museo Argentino de Ciencias Naturales "Bernardino Rivadavia" in Buenos Aires and Museo de Ciencias Naturales y Antropológicas "Juan Cornelio Moyano"in Mendoza. Museo de la Escuela Politécnica Nacional of Quito, in Ecuador. The museum specimen number, locality, country, age, skeletal tissue (enamel, bone and dentine) and the altitudinal and latitudinal distribution of each sample are given in Tables 1 and 2. We analyzed 26 samples of Hippidion and 41 carbon and oxygen isotope composition samples of Equus (Amerhippus). Additional 32 samples values (Table 1 and 2) were taken from MacFadden et al. [31, 33, 36] and MacFadden and Shockey .
Pre-treatment of the samples
The samples were finely ground in an agate mortar. The chemical pre-treatment of the samples was carried out as described in Koch et al.  in order to eliminate secondary carbonate. About 40-50 mg of powdered enamel and bone samples were soaked in 2% NaOCl for three days at room temperature to oxidize organic matter. Residues were rinsed and centrifuged five times with de-ionized water, and then treated with buffered 1M acetic acid for one day to remove diagenetic carbonates. Pre-treatment of the enamel was slightly different because samples were soaked in 2% NaOCl for only one day.
Analysis of the samples
Carbon dioxide was obtained by reacting about 40-50 mg of the treated powder with 100% H3PO4 for five hours at 50°C. The carbon dioxide was then isolated cryogenically in a vacuum line. Results are reported as δ = ([Rsample/Rstandard]-1 ) × 1000, where R = 13C/12C or 18O/16O, and the standards are PDB for carbon and V-SMOW for oxygen. We have applied the data corrections for calcite from Koch et al.  to calculate the magnitude of the oxygen isotopic fractionation between apatite CO2 and H3PO4 at 50°C. The analytical variation for repeated analyses was 0,1‰ for δ13C and 0,2‰ for δ18O. For the analysis of phosphate we followed the chemical treatment procedure described by Tudge , which resulted in the precipitation of the phosphate ions in the form of BiPO4. CO2 was obtained by reacting BiPO4 with BrF5 as described by Longinelli . All the samples were run in duplicate and the reported results are the mean of at least two consistent results. The analytical precision for repeated analyses was 0,2‰.
We performed both parametric (t-test) and nonparametric (Wilcoxon Signed-Rank) statistical tests to evaluate δ13C and δ18O differences in Middle and Late Pleistocene populations. SPSS 15.0 software was used for the statistical analysis.
Preservation state of the enamel, dentine and bone in the specimens analyzed
We checked the diagenetic alteration between the different skeletal tissues under the assumption that primary values were similar between different skeletal tissues from one individual. The phosphate oxygen isotope composition is usually considered to be more robust against diagenetic alteration than the carbonate oxygen at least if no bacteria are involved during the alteration processes. We measured both δ18O CO3 and δ18O PO4 values on the same specimens and obtained a regression between both, and compared those with known isotope equilibrium-relationships for biogenic apatite of modern bones and teeth [40, 41]. If samples fall in the range of modern biogenic apatite this would argue for a preservation of primary δ18O CO3 and δ18O PO4 values, and thus likely also δ13C values as they are less easily altered than δ18O CO3 values. This was taken as an indicator that even the bone and dentine samples may be reasonably well-preserved and can be interpreted to infer feeding ecology and habitat use of these ancient horses.
Several authors [42–44] suggest a high correlation between these two phases in some European and North American equids. In South America, the equation obtained for Equus(Amerhippus) from Argentina  was: δ18O CO3 = 16.74 δ18O PO4 + 0.64; R2 = 0.91. More recently, Sánchez et al. [8, 32] also found that a significant relationship existed between the δ18O results in the carbonate and phosphate apatite phases (enamel, dentine, and bone) when they analyzed the oxygen isotopic composition of gomphotheres from several South American localities. The new data shows that δ18O PO4 and δ18O CO3 are highly correlated, with the latter being about 8.6 ‰ more positive than the former.
We analyzed the δ18O PO4 and δ18O CO3 of the 26 samples for Hippidion and 41 samples for Equus (Amerhippus) in this way. The results of δ18O PO4 versus V-SMOW standard are reported in tables 1 and 2. The analytical variation for repeated analysis was 0.2‰. Each pair of δ18O values of teeth and bone belonged to the same individual, generally from the jaw or maxilla, the correlation being: δ18O PO4 = 0.9452 δ18O CO3 - 10.456; R2 = 0.80. We also calculated the correlation between pairs of δ18O PO4 - δ18O CO3 values for the enamel, dentine, and bone, from the same individual. The results are plotted in Figure 3. The correlations between the different PO4-CO3 pairs are:
Enamel δ18O PO4 = 2.3371 δ18O CO3 - 19.095 R2 = 0.97; Dentine δ18O PO4 = 1.2999 δ18O CO3 - 3.4034 R2 = 0.389; and Bone δ18O PO4 = 1.1709 δ18O CO3 - 6.2038 R2 = 0.88. In the first case it appears that the sample might have been modified by diagenesis because the carbonate results among the three skeletal phases (enamel, dentine, and bone) are different. In fact, the range of variation is 2.6‰ in the δ18O PO4 and 5.6‰ in the δ18O CO3 for the samples from the same specimen. Results of δ13C obtained from the bone are similar to those obtained from the dentine and are, in general, equal or more negative than results obtained from the enamel. We observed the same pattern in the δ18O results as we did in the δ13C results. The range of variation between the three skeletal phases (enamel, dentine, and bone) was small and we suppose that they have not been significantly altered by diagenesis. For these reasons, we consider these δ13C values as representative of each group of horses.
The carbon isotopic ratio of Equus (Amerhippus) and Hippidion remains indicate significant ecological differences (Figure 4). The Hippidion samples analyzed here are more homogeneous than the Equus (Amerhippus) samples, with a δ13C range between -12,9 and -8,0 ‰ (Table 1 and 2).
All the species of Hippidion were almost exclusively C3 feeders but some individuals from Bolivia and Argentina fall at the lower end of the mixed C3/C4 range. For instance, H. principale from the Eastern corridor (at sea level) and H. devillei from the Andes corridor yield similar δ13C values suggesting that they ate mainly C3 plants. The same pattern of dietary partitioning was obtained when comparisons were made between the same taxa at different latitudes (between 22°S and 52°S). From the upper Pliocene (H. devillei from Uquía locality) to the lower Pleistocene (H. principale, from the province of Buenos Aires and H. devillei from the Tarija locality) the dietary partitioning remains similar. The same pattern in dietary partitioning is observed throughout the Middle to Late Pleistocene (Figure 5) showing a predominance of C3 plants. Also, we did not find differences between H. saldiasi from the Ultima Esperanza in southern Patagonia and the other Hippidion species present at different localities across South America.
Equus species have predominantly been grazers, and as such, carbon isotopic values provide evidence of the C3 and C4 grasses. The carbon isotope data indicates that Equus (Amerhippus) shows three different patterns of dietary partitioning. Samples of E. (A.) neogeus from the province of Buenos Aires indicate a preference for C3 plants in the diet. The samples from Ecuador and Bolivia [E. (A.) andium and E. (A.) insulatus] show a preference for a diet of mixed C3-C4 plants, while those from La Carolina (sea level of Ecuador), Bolivia, and Brazil are mostly C4 feeders.
As mentioned before, a few outliers (e.g. δ13C values of 9,2; 6,1 and 5,4‰ from La Carolina) cannot be easily explained. These extremely high δ13C values (above 3‰) cannot be explained by consumption of C4 vegetation, which should impart an upper limit of about 3‰. These outliers could be the result from one of several possibilities, such as individuals living in costal peninsula areas of Ecuador during the time in which C4 grasses were abundant and may have produced δ13C values not observed in the modern ecosystem, or the sample presents taphonomic alteration. Specimen number V.3037 has a high variation between dentine, enamel, and bone (9,2; 1,5 and 6,1‰ respectively). MacFadden et al  obtained a δ13C value of 1,8‰ for the enamel of the same specimen but obtained 5,4‰ for the enamel of specimen number v.68 from the same locality. A more definitive explanation for these outliers must await the analysis of additional samples from these regions.
The δ18O CO3 results of the horse remains differ according to altitudinal and latitudinal distribution. There is a clear difference in the δ18O values obtained from the populations from the lower plains and those from high elevations. The lowest δ18O CO3 values are found in high elevation species from Ecuador and Bolivia [E. (A.) insulatus and E. (A.) andium] and range from 21,3 to 28,3‰ with an average of around 25‰. The H. saldiasi samples from southern Patagonia are also included in this group, their low δ18O values being caused by the effects of altitude and latitude. The second group is mostly represented by E. (A.) neogeus, H. principale and H. devillei. These species come from the province of Buenos Aires, Brazil, and Bolivia. The distribution values range from 27,7 to 32,1‰ with an average of around 30‰. The highest values come from the Carolina Peninsula in Ecuador, with δ18O CO3 maximum of 34,9‰.
Areas of sympatry
As might be expected from ecological theory, finer-scale preliminary results from this study suggest feeding and niche differentiation within coexisting horses. Hippidion and Equus (Amerhippus) are sympatric in the same stratigraphic level in two localities: Tarija (22 °S) in Bolivia and the Pampas in Argentina (38 °S). Data from both localities suggest some difference in dietary partitioning. In a previous study, MacFadden and Shockey  presented carbon isotopic results from Tarija herbivores that, based on dental morphology, span the spectrum from presumed browsers (e.g., tapirs) to presumed grazers (e.g., horses) coexisting in the same localities. They suggested than the horses clearly occupied different dietary niches and can be separated using the carbon isotopes and hypsodonty index. Hippidion is the least hypsodont taxon and has the most negative mean δ13C value, whereas the relatively hypsodont Equus has the most positive mean δ13C value. As has been shown in another article , Equus is usually among the most grazing adapted mammalian herbivore in Pleistocene terrestrial ecosystems. This position in the herbivore community is similar at Tarija, whereas Hippidion are more adapted to the browsing end of the spectrum and Equus are primarily C4 grazers based on their carbon isotopic signature.
Our data suggests that the range of δ13C values for H. devillei and H. principale from Tarija falls in the low end of the mixed C3/C4 range (-10,8 to -6,6‰), whereas E. (A.) insulatus falls in the higher end (-8,3 to -2,3‰). There is some overlap with at least the two values of -8,3 and -6,6‰ indicating some differences in isotopic niche, with H. devillei consuming less grass than E. (A.) insulatus at this place and time .
In the data from Arroyo Tapalque (38 °S), one of the localities in the Pampas, the range of δ13C values for H. principale (-11,6 to -9,3‰) and E. (A.) neogeus (-8,5 to -7,9‰) do not overlap, but both are close that they suggest the same pattern of dietary partitioning as in Tarija.
If we look at the morphology, these taxa are very different. Several previous papers based on cranial and limb morphology associate these differences with browsing and grazing diet preference [e.g. ]. In general, the teeth of Equus (Amerhippus) are more hypsodont than Hippidion, and the enamel patterns are more complicated in Equus (Amerhippus).
Another difference between sympatric species is body sizes. For instance, H. principale and E. (A.) neogeus are sympatric in the Pampas in Argentina. Both have a large body size, adapted to open habitat, but they differ in body mass (460 kg and 378 kg, respectively) . The skulls of E. (A.) neogeus are big and show an enlarged preorbital and nasal region. The limb bones are large and robust, but more slender than in the other South American Equus species [3, 4]. On the other hand, H. principale has a retracted nasal notch might signify some sort of proboscis. The skeleton is large and bulky, and the extremities are robust, mainly the metapodials and phalanges. It is the largest and strongest of the South American hippidiforms. These characteristics are classically associated with dietary and habitat preferences. The morphology indicated that H. principale may have been a browser but was able to live in open grasslands and that E. (A.) neogeus is the most hypsodont horse, and has the relatively straight muzzle characteristic of grazing horses .
The effect of latitude
Some of the most fundamental patterns in global biogeography are those that are structured by the latitudinal gradients that extend from pole to equator (Figure 6). The proportion of C3 to C4 grasses in most modern ecosystems rises with increasing latitude. C3 grasses are predominant (>90%) in high-latitude steppes and prairies, whereas C4 grasses are predominant (>70-90%) in most low-elevation, and equatorial grasslands. The transition between C3 and C4 dominance in grasslands occurs at about 40-45° latitude in the Northern Hemisphere [48–50]. Exceptions to this general rule include grasses at high-elevations or in climates with cool-growing seasons (e.g. the Mediterranean basin), where the grasses are predominantly C3 regardless of latitude [50–52], and the occasional C4 grass species that are found in Arctic regions .
MacFadden et al.  used the Pleistocene distribution of Equus (Amerhippus) in the Americas to present a general δ13C gradient that seems to be symmetrical on either side of the Equator. They found that the isotopic transition between a full C4 signal and full C3 signal is observed at about 45°N in the northern hemisphere. Although there are considerably fewer data points in the southern hemisphere they  have found a signal of exclusively C3 feeders at around 35°S (province of Buenos Aires). A similar pattern in the Southern Hemisphere was found by Sánchez et al.  in the distribution of gomphotheres in South America. Samples of gomphotheres from the province of Buenos Aires, at around 39°S latitude show a mean δ13C value of -10,8‰, while samples from Chile (from several localities around 35° to 41°S) show a mean δ13C value of -12,3‰. This fact would confirm the existence of a latitudinal gradient for the Southern Hemisphere, and places the transition between a full C3 signal and mixed C3/C4 signal around 35° to 41°S.
The new data for the genus Equus (Amerhippus) analyzed in this paper are in agreement with the δ13C latitudinal pattern postulated by MacFadden et al. , while data for Hippidion also seem to follow a clear pattern. Samples of Hippidion show a boundary between an exclusively C3 to a mixed C3/C4 diet at Tarija (22°S), but in this case there is an effect of altitude combined with latitude. At the highest latitude specimens from Patagonia (52°S), the mean value is -12.2‰. The middle latitude samples, from the province of Buenos Aires (34°S), show δ13C values that range between -12,9 and -8,1‰, while the lowest latitude specimens, from Tarija (22°S), show δ13C values that range between -6,6 to -0,8‰.
There are also significant differences between the δ18O CO3 values for the two genera, even when the range of δ18O values for high altitude and equatorial samples are taken into account (Table 4). This demonstrates the effects of an altitudinal gradient. The Hippidion specimens from the Andes corridor (Bolivia and northern Argentina) and the Equus (Amerhippus) specimens from Ecuador and Bolivia show the lowest values (between 21,7 and 28,3‰). On the other hand, samples from around 500 m of altitude (Bolivia, Ecuador, Brazil, Peru, and Argentina) present values that correspond with more temperate conditions (27,7 to 32,1‰). The effects of low altitude and latitude on δ18O CO3 may also explain the higher value obtained for the samples from La Carolina, Ecuador (sea level, latitude 2°S), where samples showed δ18O values ranging from 32 to 34,9‰.
We calculated a regression of δ18O PO4 values with altitude to quantify the effects of altitude. Bryant et al.  suggest a high correlation between δ18O PO4 and δ18O CO3 in Miocene North American equids. We found a good correlation between δ18O PO4 values and altitude. The equation obtained was: δ18O PO4 = -0.0016 altitude + 20.47 (R2 = 0.63). We obtained an altitudinal gradient of -0.16 δ unit/100 meters.
An important point concerns altitudinal gradients. It seems that the horses living at high altitudes, 1866 up to 2780 m above sea level, and at low to middle latitude (2° to 22°S) still have a C4 component in their diet. This is not surprising at all given the distribution of modern C4 plants in the central Andes. At present, three C4 Amaranthaceae species occur at high elevations (>4000 m) where C4 plants are rarely observed and the altitude record reported for any confirmed C4 species worldwide is 4800 m for the grass Muhlenbergia peruviana. However, this is not true for our specimens from 4000 m, which have a pure C3 diet. In this central Andean region, a clear altitudinal vegetation gradient is present. Subparamo (2000-3000 m) presents mosaics where shrubs and small trees which alternate with grasslands; and Paramo proper (3000 - 4100 m), is dominated by grasslands and shows patches of woody species which occur only in sheltered locations and along water streams. This altitudinal vegetation gradient changed during the Pleistocene. The treeless vegetation above the upper forest line was most widespread during glacial times, whereas it was limited to small areas on mountain tops during interglacial times . The fossil pollen records show that such oscillations in patterns of plant distribution were repeated many times during the Pleistocene Ice Ages . During the Last Glacial Maximum, when atmospheric p CO2 was reduced by some 50%, C4 plants dominated the Paramo vegetation, while only the highest mountain tops were covered by C3 grasses because of the low temperatures. Such small patches of C4-rich vegetation are probably relicts from the last ice age during which paramo vegetation was mainly composed of small tussocks and tufts of C4 grasses .
The change in altitudinal vegetation gradients during the Pleistocene is one of several possibilities to explain the C4 dietary component in horses living at high altitudes. Another alternative explanation might be that the horses partially fed at lower altitudes.
Based on modern analogues, Pleistocene horses are inferred to be grazers but none of the grazing horses were interpreted as consumers of only C4 grasses. Our data shows that Equus (Amerhippus) had three different patterns of dietary partitioning. E. (A.) neogeus from the province Buenos Aires indicates a preference for C3 plants. E. (A.) andium from Ecuador and E. (A.) insulatus from Bolivia show a preference in a mixed diet of C3-C4 plants, while E. (A.) santaeelenae from La Carolina (sea level of Ecuador) and Brazil are mostly C4 feeders. These results confirm that ancient feeding ecology cannot always be inferred from dental morphology.
The record from South America suggests that Hippidion is in general a higher latitude taxon than Equus (Amerhippus). The highest latitude occurrence of Hippidion appears to be in southern Bolivia, in contrary to Equus (Amerhippus) where the occurrences are further north, and alone goes a long way in explaining the isotopic differences.
The data for Hippidion indicates a preference for C3 plants and mixed C3-C4 plants, but most of this data came from high altitude or latitude specimens. One possible, but unconfirmed explanation is that Hippidion were living in a "C4 World" and were browsers as indicated by their morphology, but more southern individuals were living at latitudes high enough to support C3 and C4 grasses.
The current study demonstrates the utility of using wide-ranging fossil mammals to explore latitudinal gradients and patterns of C3/C4 grass distribution and continental palaeotemperature during the Pleistocene. The carbon isotope composition of horses decreased as latitude increased. In Equus (Amerhippus) we found a change in signal between a mixed C3/C4 diet and a pure C4 diet around 32°S and a boundary between mixed diet and exclusively C3 signals at 35°S.
We also found that the horses living at high altitudes and at low to middle latitudes still have a C4 component in their diet, except for those specimens living at 4000 m, which have a pure C3 diet. The change in altitudinal vegetation gradients during the Pleistocene is one of several possibilities to explain the C4 dietary component in horses that lived at high altitudes. Another alternative explanation implies that the horses fed partially at lower altitudes.
Museo de La Plata
Museo Argentino de Ciencias Naturales "Bernardino Rivadavia", Buenos Aires
- and (NCNAM):
Museo de Ciencias Naturales y Antropológicas "Juan Cornelio Moyano", Mendoza, in Argentina
- and (MEPN):
Museo de la Escuela Politécnica Nacional of Quito, in Ecuador.
Alberdi MT: La familia Equidae, Gray, 1821 (Perissodactyla, Mammalia) en el Pleistoceno de Sudamérica. IV Congreso Latinoamericano de Paleontología. 1987, Santa Cruz de la Sierra, Bolivia, 1: 484-499.
Alberdi MT, Prado JL: Review of the genus Hippidion Owen, 1869 (Mammalia; Perissodactyla) from the Pleistocene of South America. Zoological Journal of the Linnean Society. 1993, 108: 1-22. 10.1111/j.1096-3642.1993.tb02559.x.
Prado JL, Alberdi MT: A quantitative review of the horse Equus from South America. Paleontology. 1994, 37: 459-481.
Alberdi MT, Prado JL: El registro de Hippidion Owen, 1869 y Equus (Amerhippus) Hoffstetter, 1950 (Mammalia, Perissodactyla) en América del Sur. Ameghiniana. 1992, 29: 265-284.
MacFaddden BJ: Fossil Horses. Systematics, Paleobiology, and Evolution of the Family Equidae. 1992, Cambridge University Press
MacFadden BJ, Cerling TE: Mammalian herbivore communities, ancient feeding ecology, and carbon isotopes: a 10 million year sequence from the Neogene of Florida. Journal of Vertebrate Paleontology. 1996, 16: 103-115. 10.1080/02724634.1996.10011288.
Cerling TE, Harris JM, MacFadden BJ, Leakey MG, Quade J, Eisenmann V, Ehleringer JR: Global vegetation change through the Miocene/Pliocene boundary. Nature. 1997, 389: 153-158. 10.1038/38229.
Sánchez B, Prado JL, Alberdi MT: Ancient feeding ecology and extinction of Pleistocene Horses from Pampean Region (Argentina). Ameghiniana. 2006, 43: 427-436.
Bryant JD, Luz B, Froelich PN: Oxygen isotopic composition of fossil horse tooth phosphate as a recorder of continental paleoclimate. Palaeogeography Palaeoclimatology Palaeoecology. 1994, 107: 303-316. 10.1016/0031-0182(94)90102-3.
Wang Y, Cerling TE, MacFadden BJ: Fossil horses and carbon isotopes: new evidence for Cenozoic dietary, habitat, and ecosystem changes in North America. Palaeogeography Palaeoclimatology Palaeoecology. 1994, 107: 269-279. 10.1016/0031-0182(94)90099-X.
Cerling TE, Harris JM, MacFadden BJ: Carbon isotopes, diets of North American equids, and the evolution of North American C4 grasslands. Stable Isotopes. Edited by: Griffiths H. 1998, BIOS Scientific Publishers Ldt, Oxford, 363-379.
MacFadden B, Solounias N, Cerling TE: Ancient diets, ecology, and extinction of 5-million-year-old horses from Florida. Science. 1999, 283: 824-827. 10.1126/science.283.5403.824.
Passey BH, Cerling TE, Perkins ME, Voorhies MR, Harris JM, Tucker ST: Environmental change in the great plains: An isotopic record from fossil horses. The Journal of Geology. 2002, 110: 123-140. 10.1086/338280.
Domingo L, Grimes ST, Domingo MS, Alberdi MT: Paleoenvironmental conditions in the Spanish Miocene-Pliocene boundary: isotopic analyses of Hipparion dental enamel. Naturwissenschaften. 2009
Tütken T, Vennemann TW: Stable isotope ecology of Miocene mammals of Sandelzhausen, Germany. Paläontologische Zeitschrift. 2009, 83: 207-226.
Van Dam JA, Reichart GJ: Oxygen and carbon isotope signatures in late Neogene horse teeth from Spain and application as temperature and seasonality proxies. Palaeogeography, Palaeoclimatology, Palaeoecology. 2009, 274: 64-81. 10.1016/j.palaeo.2008.12.022.
Feranec RS, Hadly EA, Paytan A: Stable isotopes reveal seasonal competition for resources between late Pleistocene bison (Bison) and horse (Equus) from Rancho La Brea, southern California. Palaeogeography, Palaeoclimatology, Palaeoecology. 2009, 271: 153-160. 10.1016/j.palaeo.2008.10.005.
Smith BN, Epstein S: Two categories of 13C/12C ratios for higher plants. Plant Physiology. 1971, 47: 380-384. 10.1104/pp.47.3.380.
Vogel JC, Fuls A, Ellis RP: The geographical distribution of kranz grasses in South Africa. South African Journal of Science. 1978, 74: 209-215.
Ehleringer JR, Field CB, Lin ZF, Kuo CY: Leaf carbon isotope and mineral composition in subtropical plants along an irradiance cline. Oecologia. 1986, 70: 520-526. 10.1007/BF00379898.
Ehleringer JR, Sage RF, Flanagan LB, Pearcy RW: Climatic change and evolution of C4 photosynthesis. Trends in Ecology and Evolution. 1991, 6: 95-99. 10.1016/0169-5347(91)90183-X.
Cerling TE, Wang Y, Quade J: Expansion of C4 ecosystems as an indicator of global ecological change in the Late Miocene. Nature. 1993, 361: 344-45. 10.1038/361344a0.
Cerling TE, Harris JM: Carbon isotope fractionation between diet and bioapatite in ungulate mammals and implications for ecological and paleoecological studies. Oecologia. 1999, 120: 347-363. 10.1007/s004420050868.
Passey BH, Cerling TE, Schuster GT, Robinson TF, Roeder BL, Ehleringer JR: Inverse methods for estimating primary input signals from time-averaged isotope profiles. Geochim Cosmochim Acta. 2005, 69: 4101-4116. 10.1016/j.gca.2004.12.002.
Lee-Thorp JA, Van der Merwe NJ: Carbon isotope analysis of fossil bones apatite. South African Journal of Science. 1987, 83: 712-715.
Quade J, Cerling TE, Barry JC, Morgan ME, Pilbeam DR, Chivas AR, Lee-Thorp JA, van der Merwe : A 16-Ma record of paleodiet using carbon and oxygen isotopes in fossil teeth from Pakistan. Chemical Geology (Isotope Geoscience Section). 1992, 94: 183-192. 10.1016/0168-9622(92)90011-X.
Latorre C, Quade J, McIntosh WC: The expansion of C4 grasses and global change in the late Miocene: Stable isotope evidence from the Americas. Earth and Planetary Science Letters. 1997, 146: 83-96. 10.1016/S0012-821X(96)00231-2.
MacFadden BJ: Middle Pleistocene climate change recorded in fossil mammal teeth from Tarija, Bolivia, and upper limit of the Ensenadan Land-Mammal Age. Quaternary Research. 2000, 54: 121-131. 10.1006/qres.2000.2146.
MacFadden BJ: Diet and habitat of toxodont megaherbivores (Mammalia, Notoungulata) from the late Quaternary of South and Central America. Quaternary Research. 2005, 64: 113-124. 10.1016/j.yqres.2005.05.003.
MacFadden BJ, Higgins P: Ancient ecology of 15-million-year-old browsing mammals within C3 plant communities from Panamá. Oecologia. 2004, 140: 169-182. 10.1007/s00442-004-1571-x.
MacFadden BJ, Cerling TE, Prado JL: Cenozoic terrestrial ecosystem evolution in Argentina: evidence from carbon isotopes of fossil mammal teeth. Palaios. 1996, 11: 319-327. 10.2307/3515242.
Sánchez B, Prado JL, Alberdi MT: Feeding ecology, dispersal, and extinction of South American Pleistocene gomphotheres (Gomphotheriidae, Proboscidea). Paleobiology. 2004, 30: 146-161. 10.1666/0094-8373(2004)030<0146:FEDAEO>2.0.CO;2.
MacFadden BJ, Wang Y, Cerling TE, Anaya F: South American fossil mammals and carbon isotopes: A 25 million - year sequence from the Bolivian Andes. Palaeogeography, Palaeoclimatology, Palaeoecology. 1994, 107: 257-268. 10.1016/0031-0182(94)90098-1.
MacFadden BJ, Shockey BJ: Ancient feeding ecology and niche differentiation of Pleistocene mammalian herbivores from Tarija, Bolivia: morphological and isotopic evidence. Paleobiology. 1997, 23: 77-100.
MacFadden BJ: Cenozoic mammalian herbivores from the Americas: reconstructing ancient diets and terrestrial communities. Annual Reviews Ecology and Systematic. 2000, 31: 33-59. 10.1146/annurev.ecolsys.31.1.33.
MacFadden BJ, Cerling TE, Harris JM, Prado JL: Ancient latitudinal gradients of C3/C4 grasses interpreted from stable isotopes of New World Pleistocene horse (Equus) teeth. Global Ecology and Biogeography. 1999, 8: 137-149.
MacFadden BJ: Tale of two rhinos: isotopic ecology, paleodiet, and niche differentiation of Aphelops and Teleoceras from the Florida Neogene. Paleobiology. 1998, 24: 274-286.
Alberdi MT, Menegaz AN, Prado JL: Formas terminales de Hippidion (Mammalia, Perissodactyla) de los yacimientos del Pleistoceno tardío - Holoceno de la Patagonia (Argentina y Chile). Estudios Geológicos. 1997, 43: 107-115.
Alberdi MT, Prado JL, Miotti L: Hippidion saldiasi Roth, 1899 (Mammalia, Perissodactyla) at the Piedra Museo Site (Patagonia): their implication for the regional economy and environmental reconstruction. Journal of Archaeological Science. 2001, 28: 411-419. 10.1006/jasc.2000.0647.
Iacumin P, Bocherens H, Mariotti A, Longinelli A: Oxygen isotope analyses of coexisting carbonate and phosphate in biogenic apatite: a way to monitor diagenetic alteration of bone phosphate?. Earth and Planetary Science Letters. 1996, 142: 1-6. 10.1016/0012-821X(96)00093-3.
Martin C, Bentaleb I, Kaandorp R, Iacumin P, Chatri K: Intra-tooth study of modern rhinoceros enamel δ18O: Is the difference between phosphate and carbonate δ18O a sound diagenetic test?. Palaeogeography, Palaeoclimatology, Palaeoecology. 2008, 266: 183-189. 10.1016/j.palaeo.2008.03.039.
Sánchez-Chillón B, Alberdi MT, Leone G, Bonadonna FP, Stenni B, Longinelli A: Oxygen isotopic composition of fossil equid tooth and bone phosphate: an archive of difficult interpretation. Palaeogeography, Palaeoclimatology, Palaeoecology. 1994, 107: 317-328. 10.1016/0031-0182(94)90103-1.
Delgado A, Iacumin P, Stenni B, Sánchez B, Longinelli A: Oxygen isotope variations of phosphate in mammalian bone and tooth enamel. Geochimica et Cosmochimica Acta. 1995, 59: 4299-4305. 10.1016/0016-7037(95)00286-9.
Bryant JD, Froelich PN, Showers WJ, Genna BJ: Biologic and climatic signals in the oxygen isotopic composition of Eocene-Oligocene equid enamel phosphate. Palaeogeography, Palaeoclimatology, Palaeoecology. 1996, 126: 75-89. 10.1016/S0031-0182(96)00071-5.
Sánchez-Chillón B, Alberdi MT: Taphonomic modification of oxygen isotopic composition in some South American Quaternary mammal remains. II Reunión de Tafonomía y Fosilización. Edited by: Meléndez G, Blasco MF, Pérez I. 1996, 353-356.
Alberdi MT, Prado JL: Caballos fósiles de América del Sur. Una historia de tres millones de años. 2004, INCUAPA Serie Monográfica
Alberdi MT, Ortiz Jaureguizar O, Prado JL: Patterns of body size changes in fossil and living Equini (Perissodacyla). Biological Journal of the Linnean Society. 1995, 54: 349-379.
Ehleringer JR, Cerling TE, Helliker BK: C4 photosynthesis, atmospheric CO2, and climate. Oecologia. 1997, 112: 285-299. 10.1007/s004420050311.
Epstein HE, Lauenroth WK, Burke IC, Coffin DP: Productivity patterns of C3 and C4 functional types in the U.S. Great Plains. Ecology. 1997, 78: 722-731.
Tieszen LL, Hein D, Qvortrup SA, Troughton HJ, Imbamba SK: Use of δ13C values to determine vegetation selectivity in East African herbivores. Oecologia. 1979, 37: 351-359.
Cavagnaro JB: Distribution of C3 and C4 grasses at different altitudes in a temperate arid region of Argentina. Oecologia. 1988, 76: 273-277. 10.1007/BF00379962.
Cabido M, Ateca N, Astegiano ME, Anton ME: Distribution of C3 and C4 grasses along an altitudinal gradient in northern Argentina. Journal of Biogeography. 1997, 24: 197-204. 10.1046/j.1365-2699.1997.00085.x.
Schwarz AG, Redman RE: C4 grasses from the boreal forest region of Northwestern Canada. Canadian Journal of Botany. 1988, 66: 2424-2430. 10.1139/b88-329.
Ruthsatz B, Hofmann U: Die Verbreitung von C4-Pflanzen in den semiariden Anden NW-Argentiniens mit einem Beitrag zur Blattanatomie ausgewahlter Beispiele. Phytocoenologia. 1984, 12: 219-249.
Van der Hammen T: The Pleistocene changes of vegetation and climate in tropical South America. Journal of Biogeography. 1974, 1: 3-26. 10.2307/3038066.
Boom AM, Marchant R, Hooghiemstra H, Sinninghe Damsté JS: CO2- and temperature-controlled altitudinal shifts of C4- and C3-dominated grasslands allow reconstruction of palaeoatmosphere p CO2. Palaeogeography, Palaeoclimatology, Palaeoecology. 2002, 177: 151-168. 10.1016/S0031-0182(01)00357-1.
Hooghiemstra H, Van der Hammen T: Quaternary Ice-Age dynamics in the Colombian Andes: developing an understanding of our legacy. Phil. Trans. R. Soc. Lond. 2004, 359: 173-181. 10.1098/rstb.2003.1420.
Koch PL, Tuross N, Fogel ML: The effects of sample treatment and diagenesis on the isotopic integrity of carbon in biogenic hydroxylapatite. Journal of Archaeological Science. 1997, 24: 417-429. 10.1006/jasc.1996.0126.
Koch PL, Fisher DC, Dettman D: Oxygen isotope variation in the tusks of extinct proboscideans: a measure of season of death and seasonality. Geology. 1989, 17: 515-519. 10.1130/0091-7613(1989)017<0515:OIVITT>2.3.CO;2.
Tudge AP: A method of analysis of oxygen isotopes in orthophosphate: its use in the measurement of paleotemperatures. Geochimica et Cosmochimica Acta. 1960, 18: 81-93. 10.1016/0016-7037(60)90019-3.
Longinelli A: Oxygen isotopic composition of orthophosphate from shells of living marine organisms. Nature. 1965, 207: 716-718. 10.1038/207716a0.
We wish to thank the curators of the Museo de La Plata and the Museo Argentino de Ciencias Naturales "Bernardino Rivadavia", Argentina; the Museo de la Escuela Politécnica Nacional de Quito, Ecuador, and specially S. López, who was responsible for the samples; the isotope geochemistry laboratory at the Università di Trieste, Centrum voor Isotopenonderzoek, Groningen and Servicio de Isótopos estables of the Salamanca University. The manuscript was greatly improved by thoughtful review from three anonymous referees. Dan Rafuse revised the English text. Funding was provided by a Projects CGL2007-60790/BTE and CGL2010-19116/BOS from the Dirección General de Investigación Científica y Técnica of Spain and Projects AECID A/023681/09 and A/030111/10; grants from the Universidad Nacional del Centro de la provincial de Buenos Aires (http://www.unicen.edu.ar) and the Project ANPCYT (http://www.agencia.gov.ar) PICT 07-01563, Argentina. The funders had no role in study design, data collection and analysis, decision to publish, or preparation of the manuscript.
Conceived and designed the experiments: JLP MTA. Performed the experiments: BS. Analyzed the data: BS. Wrote the paper: JLP BS. Intellectual support and editorial input: JLP MTA. All authors read and approved the final manuscript.
Authors’ original submitted files for images
About this article
Cite this article
Prado, J.L., Sánchez, B. & Alberdi, M.T. Ancient feeding ecology inferred from stable isotopic evidence from fossil horses in South America over the past 3 Ma. BMC Ecol 11, 15 (2011). https://doi.org/10.1186/1472-6785-11-15
- Stable Isotopes
- C4 plants
- South America