The iconic Pleistocene mammalian predators Canis dirus Leidy, 1858 and Smilodon fatalis Leidy, 1868 are frequent components of many late Pleistocene vertebrate faunas throughout midcontinental North America (Kurtén & Anderson, 1980). At many of these localities, however, both species are represented by limited skeletal material. In contrast, literally thousands of individual animals of each species are represented in the assemblage from the Rancho La Brea “tar pits” in Los Angeles, California (Stock, 1992).
In the southern Great Basin and Mojave Desert, Pleistocene vertebrate assemblages are common and include open sites, caves, and middens (Jefferson, McDonald & Livingston, 2004; Scott & Cox, 2008). However, remains of Canis dirus are uncommon, known only from the Bitter Spring playa locality on Fort Irwin, and from an additional record of Canis sp. cf. C. dirus from Lake Manix, both in the west-central Mojave in California (Reynolds & Reynolds, 1994; Scott, 2000). Similarly, fossils of Smilodon are poorly represented from the region; prior to the present study, Smilodon sp. cf. S. fatalis has been reported only from Twentynine Palms (Bacheller III, 1978), whereas Smilodon sp. was reported from China Lake (Fortsch, 1978) and Fort Irwin (Reynolds & Reynolds, 1994; Scott, 2000).
Both Canis dirus and Smilodon fatalis are conspicuously absent from published records describing fossils recovered from the Tule Springs locality and surrounding upper Las Vegas Wash north of Las Vegas, Nevada (Simpson, 1933; Mawby, 1967). In this region, extensive outcrops of groundwater discharge deposits (paleowetlands) are highly fossiliferous (Simpson, 1933; Haynes, 1967; Mawby, 1967; Quade, 1986; Quade & Pratt, 1989; Reynolds, Mead & Reynolds, 1991; Scott & Cox, 2008), and faunal remains have been designated recently as the Tule Springs local fauna (TSLF) (Springer et al., 2011). The TSLF is the largest open-site late Pleistocene vertebrate assemblage known from the southern Great Basin and Mojave Desert. This report documents the first records of C. dirus and S. fatalis in the TSLF and the first definitive records of these taxa in southern Nevada.
Geologic Setting and Age Control
During the late Pleistocene and early Holocene, the Las Vegas Valley in southern Nevada (Fig. 1) supported extensive and diverse wetland ecosystems. Desert wetlands form in arid environments where water tables approach or breach the ground surface and are expressed on the landscape by a variety of hydrologic settings, including seeps, marshes, wet meadows, spring pools, and flowing streams. Over time, eolian and alluvial sediments become trapped by dense vegetation and wet ground conditions, resulting in a unique combination of clastic sediments, chemical precipitates, and organic matter that are collectively referred to as groundwater discharge (GWD) deposits (Pigati et al., 2014). During the late Pleistocene, high-water-table elevations supported vast wetlands that were distributed along the length of the Las Vegas Valley, which in turn supported a diverse flora and fauna (Springer, Manker & Pigati, 2015). The resulting GWD deposits once blanketed much of the Las Vegas Valley floor and areas to the north and were assigned to the Las Vegas Formation (Longwell et al., 1965), although they were initially misinterpreted as a pluvial lake sequence. As a result of urbanization, these once extensive deposits are presently restricted to the upper Las Vegas Wash, the major physiographic drainage of the Las Vegas region and a tributary of the Colorado River (Fig. 1). Here, GWD deposits occur as light-colored, fine-grained sedimentary sequences with distinctive badland topography (Longwell et al., 1965; Haynes, 1967; Quade, 1986; Quade et al., 1995; Quade, Forester & Whelan, 2003; Ramelli et al., 2011; Ramelli et al., 2012; Springer, Manker & Pigati, 2015).
Haynes (1967) informally subdivided the Las Vegas Formation into stratigraphically ascending units designated A through G, of which A–E date to the late Pleistocene and F and G represent the Holocene portion of the sequence. Recent studies (Ramelli et al., 2011; Ramelli et al., 2012; Springer, Manker & Pigati, 2015) have augmented, revised, and expanded this geochronologic and lithostratigraphic framework, while at the same time retaining the alpha notation for the members of the formation. The new frameworks were established using detailed geologic mapping, stratigraphic principles, and radiocarbon (14C) dating of charred vascular plants and, to a lesser extent, small terrestrial gastropod shells, as well as luminescence dating (Ramelli et al., 2011, Ramelli et al., 2012; Springer, Manker & Pigati, 2015).
The specimen assigned herein to Canis dirus was recovered from locality SBCM 2.6.641, in sediments identified as Bed E1b of the Las Vegas Formation (Springer, Manker & Pigati, 2015). This bed represents a discrete discharge event dating to between 14.6 and 14.3 ka, which places this specimen of C. dirus temporally near the end of the Pleistocene.
Fossils referred herein to Smilodon fatalis derive from locality SBCM 2.6.136, in sediments identified as Bed E1a of the Las Vegas Formation, representing an older, discrete discharge event. Bed E1a dates to 16.1–15.0 ka cal BP (Springer, Manker & Pigati, 2015), thereby also establishing the presence of S. fatalis in the southern Nevada region towards the end of the Pleistocene Epoch.
The depositional environments represented by the GWD deposits in the Las Vegas Valley are both spatially complex and time-transgressive, with disparate sedimentological facies related to hydrologic discharge regime and topographic position in the valley. The former desert wetlands, with their attendant vertebrate faunas, are analogous to modern spring ecosystems exhibiting helocrene (wet meadows and marshes), rheocrene (flowing streams), and limnocrene (spring-fed pools) discharge regimes (Springer, & Stevens, 2009; Springer, Manker & Pigati, 2015). Chronologic and lithostratigraphic data suggest that there were multiple outflow streams (rheocrene discharge) along the upper Las Vegas Wash during the late Pleistocene. Specimens of both Canis dirus and Smilodon fatalis were recovered from these groundwater discharge fed outflow streams, and the deposits yielding C. dirus are inset into those yielding S. fatalis.
The discharge event represented by Bed E1a occurred between 16.1 ka and 15.0 ka, corresponding to the Oldest Dryas global cooling event, also termed the “Big Wet” in the southwestern US (Broecker et al., 2009). Abundant vertebrate fossils of multiple taxa, including the fossils of Smilodon described below, occur within this unit. Groundwater discharge ended abruptly at 15.0 ka, as evidenced by intense erosion of the deposits in response to the initiation of the Bølling warm period (D-O 1), but resumed shortly thereafter as represented by Bed E1b. This later discharge interval, again dating to 14.6 and 14.3 ka, is also prolific with respect to vertebrate fossils, including the specimen of Canis dirus reported herein.
Macrofloral evidence obtained from charred organic material in the discharge interval from which the fossil of Canis dirus was obtained indicates mesquite, conifer and possibly juniper were present in the Las Vegas Valley during this period (Springer, Manker & Pigati, 2015). Mehringer’s (1965, 1967) pollen data suggested a lowering of vegetation zones by nearly 1,000 m, corroborating macrofloral evidence of conifers at the valley bottom of the Las Vegas Valley at an elevation of 700 m above sea level. Other plant associations, based on pollen and woodrat midden studies, suggest that an open sagebrush-dominated steppe to lower Mojave Desert scrub prevailed in the valley during the late Pleistocene (Quade, 1986).
Mehringer (1967) advocated that during the late Pleistocene, conditions were much like those observed today on the slopes of the mountain ranges ringing the Las Vegas Valley, a sagebrush desert bordered by piñon-juniper woodland. The long-term desertification of this area (on glacial to interglacial timescales) was in progress during the time, and was punctuated by discharge events, in which the sediments yielding both Canis dirus and Smilodon fatalis were deposited.
This study was conducted from 2008 to 2014 on ∼11,000 acres of federal land managed by the Bureau of Land Management (BLM), Southern Nevada District Office. Work was performed under Grant L08AC13098 entitled “The Upper Las Vegas Wash Conservation Transfer Area, Clark County, NV: Treatment, Protection, and Interpretation of Heritage Paleontological Resources through Public Involvement.”
Specimens assigned herein to Canis dirus and Smilodon fatalis were examined and measured in the collections of the San Bernardino County Museum; comparative fossils were studied and measured at the La Brea Tar Pits and Museum (formerly the George C. Page Museum of La Brea Discoveries). Measurements followed procedures outlined by Von den Driesch (1976) as appropriate and where possible; however, the poor preservation of the fossils necessitated developing additional measurements in order to better constrain the size of some specimens. Data were acquired using Mitutoyo Digimatic calipers connected by a Mitutoyo USB digital interface to a Toshiba Satellite P745 laptop. Comparative metric data for living Canis lupus from Yellowstone National Park and Alaska were provided by Sue Ware. Digital photos were acquired with a Sony DSC F818 Cybershot camera. Graphic plots were generated and basic statistics calculated using SigmaPlot 13. Multiple logistic regression was performed using online software provided by StatPages.org (http://statpages.org/logistic.html).
Referred specimens: SBCM L3160-1257, right patella.
Description: The patella is damaged dorsally, but nevertheless exhibits a typically canid rounded teardrop shape (Fig. 2).
Remarks: In terms of size, SBCM L3160-1257 is far too large to be assigned to Canis latrans, and additionally is larger than like elements of timber wolf, C. lupus (Table 1). Metric comparisons with fossils of C. dirus from Rancho La Brea, as well as with modern specimens of C. lupus from Yellowstone National Park and from Alaska, demonstrate that L3160-1257 falls well within the size range of C. dirus (Fig. 3). Applying multiple logistic regression confirms this interpretation (P = 1.0, df = 2, 99% CI).
|Taxon:||Canis dirus from RLB||Canis lupus (modern)||Canis dirus from TUSK|
Data in millimeters.
SBCM L3160-1257 was recovered from locality SBCM 2.6.641, which also yielded fragmentary but identifiable fossil remains of Lepus, cf. Mammuthus, Camelops, and Odocoileus.
Referred specimens: SBCM L3160-1018, proximal left humerus; SBCM L3160-1019, distal left radius; SBCM L3160-1020, dorsal sacrum.
Description: All of the recovered fossils are poorly preserved. Observed damage appears to have been post-depositional and post-exposure. Breakage is confined to fractures running roughly parallel with, as well as perpendicular to, the long axis of the bones; no spiral fractures, indicative of fresh or “green” bone breakage, are in evidence. The compact bone shows no indications of exfoliation, desiccation, abrasion, weathering, or water wear, indicating that the fossils were not transported any great distance and were not exposed to the elements for very long prior to burial. Rather, damage and loss of missing portions of the fossils is inferred to result from diagenetic processes and prolonged exposure to the elements subsequent to erosion but prior to discovery.
The proximal left humerus, SBCM L3160-1018, is the most complete of the preserved elements, and falls within the size range of both Smilodon fatalis and Panthera atrox (Table 2). The specimen lacks the greater tuberosity but is otherwise largely complete proximal to midshaft (Fig. 4). Viewed dorsally, the diaphysis is broad and massive, while in lateral view it exhibits a gentle dorsoventral curvature. Viewed anteriorly, the teres major tuberosity of SBCM L3160-1018 is relatively straight, paralleling the long axis of the diaphysis, while the deltoid crest forms the outer border of the bone proximally, then angles sharply medially to intersect the teres major tuberosity proximal to midshaft.
|Taxon:||Smilodon fatalis from RLB||Panthera atrox from RLB||Smilodon fatalis from TUSK|
The distal left radius, SBCM L3160-1019, lacks the proximal half and much of the medial face (Fig. 5). The specimen is insufficiently complete to permit obtaining any useful metric data. The distal diaphysis is clearly bowed. The medial border of the styloid process is moderately long and curved or bulbous. The lateral border of the radius curves inward directly from the ulnar articulation. The muscle scar for the insertion of the m. pronator teres is situated well distal to midshaft on the diaphysis.
The partial sacrum, SBCM L3160-1020, lacks most of the ventral portion, including the centra. The remaining dorsal surface does preserve some diagnostic features, however. In particular, the prezygapophyses are relatively small and ovular, and are flanked laterally by a distinct and deep groove that extends from behind each process anteriorly, running between the zygapophyses and the alae.
Remarks: The morphology of the teres major tuberosity of SBCM L3160-1018 confirms that the humerus is machairodont; in other large felines such as Panthera atrox, the teres major tuberosity is angular rather than straight, curving laterally from roughly midline to meet the medially angling deltoid crest. The diaphysis of the humerus SBCM L3160-1018 is more robust and less elongate in dorsal view than the observed condition in humeri of Homotherium, precluding assignment of this specimen to that genus. In like manner, the anteroposterior curvature of the diaphysis, best seen in lateral view, matches the curvature seen in Smilodon fatalis rather than the straighter profile characterizing humeri of Xenosmilus.
The distal diaphysis of radius SBCM L3160-1019 is clearly bowed as in Smilodon, rather than straight as exhibited by Panthera atrox. The medial border of the styloid process is moderately long and curved or bulbous, closely in accord with radii of Smilodon and differing from the longer, straighter processes exhibited by P. atrox as well as the smaller, more rounded processes seen in Homotherium and Xenosmilus. The lateral border of the radius curves inward directly from the ulnar articulation, as seen in Smilodon but differing from the longer, straighter condition characterizing P. atrox. The muscle scar for the insertion of the m. pronator teres is more distally situated on the diaphysis, again as in Smilodon as opposed to P. atrox.
The prezygapophyses exhibited by SBCM L3160-1020 are relatively small and ovular, and are flanked laterally by a distinct and deep groove that extends from behind each process anteriorly, running between the zygapophyses and the alae. These features are characteristic of Smilodon, but differ from the anatomical configuration exhibited by Panthera atrox (Merriam & Stock, 1932).
All of the recovered specimens derive from a single locality, SBCM 2.6.136. The locality was initially discovered and recorded in September of 2003, with the two partial limb elements exposed. Original excavation of the fossils took place in June of 2012; upon recognition that the elements preserved represented Smilodon, a second field visit to expand the quarry yielded the partial sacrum. No other taxa were recovered from this locality.
Prior to the present study, the only large (≥44 kg) predator known definitively from the Las Vegas Formation was the extinct North American lion Panthera atrox (Mawby, 1967). Fossil remains of this extinct species were rare, even though a phalanx of P. atrox was among the first fossils discovered in the valley and preserved by paleontologists in 1919 (Springer et al., 2011). The paucity of fossils of large carnivorans was consistent with the interpretation that the fossils from Tule Springs represented a “normal” distribution, wherein herbivores are far more numerous than predators (e.g., Schaller, 1972). In this context, the absence of remains of other large predators such as dire wolf Canis dirus and the sabre-toothed cat Smilodon fatalis was not considered unusual.
The new records of Canis dirus and Smilodon fatalis from the TSLF add significantly to the sparse record of late Pleistocene carnivorans from Nevada. C. dirus has not previously been confirmed in the state, while the only records of S. fatalisin Nevada are from Smith Creek cave (Kurtén & Anderson, 1980) and the Black Rock Desert (Dansie, Davis & Stafford Jr, 1988; Livingston, 1991), both late Pleistocene sites located north of the Mojave Desert.
A possible record of dire wolf was recently reported in the upper Las Vegas Wash from land belonging to the State of Nevada (Rowland & Bonde, 2015). Based on photographic evidence, the fossil in question, a distal metapodial, appears larger than metapodials of coyote (C. latrans) and domestic dog (C. familiaris). However, metric data discriminating the fossil from other Pleistocene canines such as timber wolf (C. lupus) have not been published, and although the specimen was determined to be “indistinguishable from C. dirus medial metapodials … it is also indistinguishable from gray wolf (C. lupus) medial metapodials” (Rowland & Bonde, 2015: 305–306). Despite this lack of diagnosticity, the fossil was interpreted to be “probably” dire wolf (Rowland & Bonde, 2015: 306), e.g., Canis sp. cf. C. dirus, based on the relative abundance of C. dirus in coastal southern California.
The specimen in question was reported from “Unit D” of the Las Vegas Formation, using the stratigraphy of Haynes (1967) rather than more recent stratigraphic interpretations (e.g., Ramelli et al., 2011; Springer, Manker & Pigati, 2015). Thus, the age of the fossil was estimated to be between 30 and 16 14C ka (∼34–19 cal ka), with no other chronometric age control (Rowland & Bonde, 2015: 306). If confirmed, this fossil would substantially expand the temporal range of C. dirus in the Las Vegas Valley, as well as in the State of Nevada. However, lacking any published metric data, we prefer to recognize this fossil as Canis sp. (large), instead of Canis sp. cf. C. dirus until the necessary corroborative metric data are made available.
In contrast, the depositional history, paleoenvironmental setting, and chronology of the deposits yielding the new records of Smilodon fatalis and Canis dirus are well documented. The lithostratigraphy indicates significant rheocrene discharge occurred at multiple point sources along the upper Las Vegas Wash during the late Pleistocene (Springer, Manker & Pigati, 2015). Given the ongoing desertification of the Las Vegas Valley and the presence of sagebrush desert bordered by piñon-juniper woodland at this time (Mehringer, 1967), these discharge points and their outflow streams would have offered localized sources of fresh water for the regional fauna in an otherwise arid ecosystem. Megafaunal herbivores attracted to this discharge would in turn have offered focused points of interest for carnivorans such as Canis and Smilodon.
Meloro et al. (2013) examined environmental preferences of living felids and employed humeral morphology to infer paleohabitats for extinct felids, including machairodontines, and concluded that the species Smilodon populator was best interpreted to have been adapted to closed habitats. In contrast, the presence of S. fatalis documented herein from the upper Las Vegas Wash demonstrates that some species of Smilodon also thrived in relatively open habitats, as inferred from the available geological evidence. Published palynological data indicate that the Tule Springs region was an open sagebrush desert with surrounding piñon-juniper woodland during the late Pleistocene (Mehringer, 1967). Both the depositional setting and sedimentology of the GWD deposits yielding the remains of S. fatalis indicate spring-derived, low-energy outflow streams, as they are composed predominantly of fine-grained sand and silt (Springer, Manker & Pigati, 2015). The specimens were recovered very near the point source of the discharge (<1 km), demonstrating they did not undergo significant postmortem transport. This is supported by the lack of any evidence of abrasion, rounding, or other water wear of the bones; as noted previously, all observed breakage is post-depositional and post-exposure. This being the case, the fossils are interpreted to have been directly deposited in the open-habitat Tule Springs environment, rather than transported from other, more closed habitats elsewhere. The presence of S. fatalis at Tule Springs therefore negates any inferred similarity in closed-habitat preferences between it and S. populator.
The presence of Smilodon fatalis in open-habitat environments does not preclude considering these animals to have been ambush predators. In fact, multiple studies of the anatomical configuration of Smilodon argue convincingly in favor of these felids having been better adapted to ambush rather than pursuit (e.g., Gonyea, 1976; Anyonge, 1996; Meachen-Samuels & Van Valkenburgh, 2010). The new record of S. fatalis from the TSLF demonstrates that these animals were not restricted to closed habitats, irrespective of their chosen method of predation. Assumptions that Smilodon would have required closed habitats in order to hunt effectively as ambush predators require reconsideration.
Meachen, O’Keefe & Sadleir (2014) proposed that Smilodon fatalis evolved morphologically throughout much of the latter part of the Pleistocene, based upon the rich record of the species preserved at Rancho La Brea. Specifically, mandibles of S. fatalis exhibited larger average size and a more derived morphology, presumably in response to changing climate, in Pleistocene accumulations dating to 14–13 cal ka (Meachen, O’Keefe & Sadleir, 2014). The fossils of S. fatalis from the TSLF did not include mandibular remains, and so direct comparisons with the Rancho La Brea mandibles are not possible. However, measurements from the humerus SBCM L3160-1018 from TUSK are larger than the mean and median measurements obtained from humeri of Smilodon at Rancho La Brea (Table 2), and in one dimension—dorsoventral depth of the humeral head (DVH)—exceed the measured sample from the California locality. The large size of the fossils from TUSK is therefore not inconsistent with the interpretation that S. fatalis increased in size towards the end of the Pleistocene (Meachen, O’Keefe & Sadleir, 2014). The TUSK fossils are between 16.1 ka and 15.0 ka, and so are older than the youngest Rancho La Brea samples.
The present study documents the first confirmed records of Canis dirus and Smilodon fatalis from the Tule Springs site in the eastern Mojave Desert region of Nevada. These finds represent the first documentation of C. dirus in Nevada and the only known occurrence of Smilodon in southern Nevada. The presence of S. fatalis in the assemblage indicates that this species inhabited open habitats. Suggestions that Smilodon would have preferred or required closed habitats in order to function successfully as an ambush predator require further consideration.