Translator Disclaimer
1 December 2008 Mud-Trapped Herd Captures Evidence of Distinctive Dinosaur Sociality
Author Affiliations +
Abstract

A unique dinosaur assemblage from the Cretaceous beds of western Inner Mongolia preserves geologic and paleontologic data that clearly delineate both the timing and mechanism of death. Over twenty individuals of the ornithomimid Sinornithomimus dongi perished while trapped in the mud of a drying lake or pond, the proximity and alignment of the mired skeletons indicating a catastrophic mass mortality of a social group. Histologic examination reveals the group to consist entirely of immature individuals between one and seven years of age, with no hatchlings or mature individuals. The Sinornithomimus locality supports the interpretation of other, more taphonomically ambiguous assemblages of immature dinosaurs as reflective of juvenile sociality. Adults of various nonavian dinosaurs are known to have engaged in prolonged nesting and post hatching parental care, a life history strategy that implies juveniles spent considerable time away from reproductively active adults. Herding of juveniles, here documented in a Cretaceous ornithomimid, may have been a common life history strategy among nonavian dinosaurs reflecting their oviparity, extensive parental care, and multi-year maturation.

Introduction

Fossil assemblages from trilobites to tyrannosaurs provide important insight into the sociality and population dynamics of extinct species (Voorhies 1969; Hulbert 1982; Klein 1982; Speyer and Brett 1985; Speyer 1991; Currie 2000; Tinn and Meidla 2003). However, discerning the biological significance of these assemblages requires an unambiguous understanding of the underlying processes governing their formation (Voorhies 1969; Klein 1982; Speyer and Brett 1985; Patterson et al. 2007).

Sites dominated by a single dinosaur species have commonly been used to support hypotheses of herding, sociality and population structure and growth (Gilmore 1917; Currie and Dodson 1984; Ostrom 1986; Norman 1987; Forster 1990; Rogers 1990; Jerzykiewicz et al. 1993; Varricchio and Horner 1993; Schwartz and Gillette 1994; Bilbey 1999; Ryan et al. 2001; Fiorillo and Eberth 2004; Eberth and Getty 2005; Scherzer and Varricchio 2005; Lehman 2006; Zanno and Erickson 2006; Garrison et al. 2007; Gates 2006; Myers and Storrs 2007; C. Suarez et al. 2007; M. Suarez et al. 2007; Zhao et al. 2007). However, these assemblages typically show significant evidence of post-mortem processes such as disarticulation, carcass and bone transport, and bone loss through winnowing, sorting, scavenging, and weathering (e.g., Rogers 1990; Varricchio and Horner 1993; Eberth and Getty 2005; Myers and Storrs 2007). The overprinting of these assemblages by largely abiotic and protracted processes makes determination of both the cause and timing of death impossible or speculative at best and complicates behavioral and ecological interpretations. Some localities may simply reflect attritional and selective processes such as serial predation and agonistic interactions at favored waterholes (Haynes 1988; Roach and Brinkman 2007). The least biased assemblages result from catastrophic and non-selective mortality, in which animals make a rapid transition from the biosphere to the rock record (Voorhies 1985).

Fig. 1.

Suhongtu site, partial quarry map, locality map, and orientation data. A. Map of the central and northern portions of site showing the position of 12 of 13 skeletons. Skeletons 3 and 4 enlarged in Fig. 3. B. Fossil locality (41°17′ 10″N, 103°52′38″E) located 90 km northwest of Bayan Mod, Inner Mongolia, China. C. Rose-diagram showing trends for skeletons (black, numbers denote skeleton count) and ripples (white). D. Mirror rose-diagram of elongated, isolated elements (n = 13). Trends of skeletons have a strong, non-random (p < 0.002) alignment to southeast. Flow direction of ripples is roughly perpendicular to that of elongate elements.

f01_567.eps

A dense, monospecific assemblage of the recently named ornithomimid dinosaur Sinornithomimus dongi Kobayashi and Lü, 2003 comes from the Upper Cretaceous Ulansuhai Formation of Inner Mongolia (Fig. 1B). Previous excavations had collected an assemblage of 14 primarily juvenile individuals showing uniform preservation with no weathering and little evidence of post-mortem transport. Although the exceptional preservation of these specimens has been noted (Kobayashi et al. 1999; Kobayashi and Lü 2003), the circumstances surrounding their accumulation have remained elusive. We present evidence that these ornithomimids perished after becoming entrapped along the margins of a drying lake. Their uniform, circumscribed death and aligned arrangement indicates a catastrophic miring of a herd of Sinornithomimus, the juvenile age-profile of which we document with long bone measurements and bone histology.

Institutional abbreviation.

  • LH, Long Hao Institute for Paleontology, Hohhot, Nei Mongol Autonomous Region, China.

Other abbreviation.

  • LAG, line of arrested growth.

Geological setting

The Upper Cretaceous Ulansuhai Formation crops out in the southern Gobi Desert within the western portion of the Nei Mongol (Inner Mongolia) Autonomous Region, People's Republic of China. The formation unconformably overlies Lower Cretaceous elastics and volcanics (Bureau of Geology 1991). Radiometric dating of these volcanic rocks suggests a maximum age of 92 Ma for the Ulansuhai Formation (Bureau of Geology 1991). Although dominated by red mudstone and siltstone, the formation also contains evaporites, calcretes, and coarser fluvial clastics. The Ulansuhai Formation is one of many rock units representing continental deposition within the Cretaceous Gobi Basin. Through this period the region experienced an increase in overall aridity and a shift from lacustrine and fluvial Lower Cretaceous facies to predominantly aeolian dune and associated interdune facies in the Upper Cretaceous (Jerzykiewicz 2000). The Sinornithomimus locality occurs approximately 30 km northwest of the town of Suhongtu, Nei Mongol (Fig. 1B).

Site description

Sedimentology.—The skeletons are preserved within a 1.3 m-thick unit consisting predominantly of red and blue-gray claystone interbedded with siltstone to very fine sandstone (Fig. 2). Although some of the coarser units are tan to reddish tan in color, coloration is otherwise not controlled by grain-size. Blue-gray mottling occurs within red horizons and visa versa. Mottling is often concentrated along contacts between red and blue-gray beds (Fig. 2B). Bed thicknesses, visible even within extensive zones of deformed bedding, range from thinly laminated to very thinly bedded (< 3 to 30 mm thick). Ripple-scale cross-bedding occurs in the very thin sandstone beds (Fig. 2C). Planar exposures reveal at least two horizons with sand-filled mudcracks. Deformed bedding consists either of convoluted or disrupted laminae. In the latter, bedding laminae in a zone several centimeters thick are crosscut by vertical gaps 1–2 cm wide and infilled with red mudstone. Laminae curve downwards as they approach the gap (Fig. 2C).

The upper 12 cm of this unit displays vertical root-traces, clay-lined peds, i.e., aggregates of soil (Retallack 1990), and burrows with reduction halos and grades into the overlying mudstone. This and subsequent overlying massive and blocky mudstone units exhibit a variety of additional pedogenic features, including mottling, slickensides, uncommon calcite concretions, and gilgai microrelief (Retallack 1990). Only 40 cm of the unit underlying the 1.3 m skeleton-bearing unit were exposed. This tan red mudstone exhibited blue-gray mottling concentrated towards its top and burrows with reduction halos.

The bulk of the ornithomimid skeletons lay at the top of a 10 cm-thick zone of deformed bedding and 20 cm above the base of the 1.3 m thick unit (Fig. 2B, C). Abundant blue-gray mottling distinguishes the upper 2–3 cm of mudrock just beneath the bone. Planar exposures of the bone horizon in the northwest portions of the quarry reveal sand-filled mudcracks. Concentrations of ostracods, cf. Cypridea or Pseudocypridea, up to 5 mm thick, occur in irregular patches sometimes adjacent to or on top of the uppermost bones. More commonly, a 2-cm thick, very fine sandstone with ripple-scale cross-stratification indicating a current direction of 230° overlies the bones (Fig. 2B, C).

Fig. 2.

Sedimentary profile of the Suhongtu quarry. A. Laminated to very thinly bedded, red and blue-gray unit with a total thickness of 1.3 m. More massive mudstones (not shown) under- and overlie this unit. Main bone-producing horizon located near base (marked by > <) at top of mottled interval. Scale bar 10 cm. B. Close-up sedimentary profile of the Suhongtu quarry. The principal bone horizon lies at the midway point of the hammer handle. This unit consists of abundant convoluted bedding and is marked by blue-gray mottling near its top. A thin, light-colored sandstone immediately overlies this unit. Hammer length equals 27.6 cm. C. Close-up of main bone-bearing unit with partially collapsed, infilled footprint structures in laminated claystone. Ripple-scale cross-stratification (R) in thin (1 to 2 cm) very fine sandstone that lies immediately above the main bone horizon. A great abundance of mottling occurs near the top of this bone-bearing unit. Asterisks mark the lower ends of V-shaped disruption structures, where footfalls and digits have bisected underlying laminated units. The down curved lamina and uniform fills of these structures suggest the original substrate was soft and only partially consolidated. Scale bar 10 cm.

f02_567.eps

Table 1.

Taphonomic condition of the recently excavated Sinornithomimus skeletons from the Upper Cretaceous Suhongtu locality, Nei Mongol. Numbers correspond to Fig. 1A. Femur lengths in cm. Skeletons are fully articulated except for disarticulated associated material or missing elements. Several specimens were in part truncated by recent weathering resulting in bone loss (marked †). Loss of ilia or other pelvic elements, however, cannot be attributed to recent weathering. Posture refers to the orientation of the pelvis and hind limbs with upright referring to specimens whose hindlimbs and pelvic girdles maintain a life-like orientation and extend deep into underlying strata. Specimens 3, 4, and 9 were sampled for histology.

t01_567.gif

Two additional horizons within the 1.3 m unit produce minor amounts of isolated bones. As with the main bone horizon (Fig. 2B), both sit at the top of a zone of convoluted bedding and are associated with some or all of the following: drab, blue-gray burrows, mudcracks, V-shaped disruption structures, and ostracods.

Bone assemblage.—Recent excavations yielded 13 partially articulated skeletons. Although these vary in their completeness from a minimum of the pelvic girdle with portions of the hind and fore limbs to nearly complete skeletons, they all show a consistent pattern of preservation (Figs. 1A, 3, Table 1). Twelve of the 13 individuals retain an articulated pelvis and hind limbs with most in a life-like crouched posture. All flexed hind limbs, elongate shafts of the ventral pelvis, and some forelimbs plunge down into the sediments as deep as 40 cm crosscutting underlying strata (Fig. 3E, F). Articulated tail sections occur in some specimens and often extend down 25 to 30 cm and occasionally curl back up through the underlying beds. The extraordinary burial depth for such small-sized skeletons and flexed posture of many intact pedes suggest entrapment within deformable mud. Penetration depths likely represent minimum values given normal sediment compaction resulting from burial. One skeleton shows an unusual twisted cervical series (Fig. 3B) rather than the posteriorly arched death pose common to many theropod specimens (Faux and Padian 2007). Throughout, a drab, blue-gray halo, roughly 5 mm thick, surrounds nearly all articulated skeletal elements (Fig. 3E, F) and suggests that decomposition of the trapped carcasses rapidly shifted from aerobic to anaerobic pathways creating reducing conditions in immediately adjacent sediments (Allison 1988).

In contrast to the plunging limbs and tails, skeletal portions on the main bone horizon are more variably preserved. This difference likely reflects their exposure to postmortem disarticulation, scavenging and transport. Final resting posture strongly influenced preservation. For example, skeletons resting on their ventral side retain articulated gastral baskets (Fig. 3A) but sometimes lack dorsal vertebrae and ribs. Skeletons lying on their right side, similarly, preferentially preserve the right rib series as compared to the left. Only a few individuals retain full dorsal and cervical vertebral series. More commonly, a scattering of associated bones lies on the main bone horizon anterior to the pelvis. Despite the universal presence of pubes and ischia in natural articulation, few preserve either ilium, a large bone that would have been exposed near the surface (Fig. 3C). Nine of 13 skeletons lack both ilia and several are missing the sacrum as well. Further, evidence of selective bone removal after entrapment includes a series of centra and another of chevrons that remain in life position despite the absence of neural arches and vertebrae, respectively. Nevertheless, several individuals display exceptional preservation. Presence of intact gastrolith masses (Kobayashi et al. 1999), carbonized stomach contents (Fig. 3D), and sclerotic rings within orbits suggests limited subaerial exposure.

Fig. 3.

Skeletons 3 and 4 (Fig. 1), respectively LH PV5 and LH PV6 (to left), of Sinornithomimus dongi Kobayashi and Lü, 2003 at Suhongtu, showing preservational features indicative of catastrophic miring of an immature herd; in plan view (A–D) and in cross-sectional view (E, F). A. Skeletons overlap and have parallel body axis orientation. B. The short snout, unfused neurocentral sutures and estimated age (1–2 years) indicate immaturity. Note the unusual curvature in the neck. C. The intact pelvis is missing only the superficially positioned left ilium. D. A gastrolith mass and carbonized stomach contents (anterior and posterior to the gastroliths) lie within the ribcage and gastral basket. Left shank and pes (E) and forelimb (F) with flexed ungual phalanges lodged deep in the claystone in near-vertical orientations. Remaining portions of the skeletons lie above in a horizontal plane that represents the ground surface at the time of miring (marked by > <). A bluish-gray halo surrounds all bones. Scale bars 10 cm.

f03_567.eps

Trends of individual skeletons were measured toward the head and perpendicular to a line connecting right and left sides of the pelvis. The skeletons show a strong preferred orientation toward the southeast, with ten of the 13 specimens facing between 87° and 188° (Fig. 1C, Table 1). That this represents chance alignment is extremely improbable (p < 0.002).

Additional skeletal material not clearly associated with specific individuals occurs across the main bone horizon. This includes a few articulated sections of caudal and cervical vertebrae, four forelimbs, and isolated elements. The 52 isolated elements consist primarily of vertebrae, centra, ribs and gastralia. Bones of the forelimb, shoulder girdle and skull are rare (n = 3) and with the exception of a single ilium, no pelvic or hind limb elements occur. Eleven elements remained unidentifiable in the field. Of the identifiable material, all but one element are assignable to Sinornithomimus. This material largely corresponds to elements missing from the articulated skeletons. All lack the drab, blue-gray halo that surrounds the skeletons. Elongate, isolated elements show a preferred orientation, aligning along a west-north-west to east-southeast axis (Fig. 1D, Table 2). Nearly all bones, whether isolated or from articulated skeletons, are well preserved, complete, and un-weathered.

Table 2.

Trends and plunges of isolated, elongate elements. Strike and dip of bedding plane measured 80°, 10° N.

t02_567.gif

Among both articulated and disarticulated material, only four bones clearly show breaks, although final preparation of all specimens may potentially reveal more broken elements. A femur of the most disturbed skeleton is truncated high on the shaft, leaving the proximal end in articulation with the ischium and pubis, while the remainder lies some 40 cm away. A partial femur on another specimen similarly remains in articulation. Two breaks occur within a tibia of an articulated hind limb with the mid shaft slightly displaced. Broken pieces of the sole remaining disarticulated ilium remain in contact; the crushed, abnormal, and concave-up arrangement of these fragments suggests damage by trampling. Although tooth marks and borings were not observed on any bones, elongate irregular masses less than 2 cm wide and consisting of finely macerated bone fragments occur on and below the bone horizon. These may represent coprolites or possibly bone-chipped filled burrows (Paik 2000).

Histology

All of the recently excavated Suhongtu ornithomimids are immature individuals (Figs. 4, 5). The largest retains completely open neurocentral sutures in all preserved vertebrae (dorsal to mid caudal) while the smallest exhibits a proportionately short snout. Using the femur as a rough proxy for body size, most of the skeletons have femora between 18 and 24 cm in length, or less than half the femoral length (48 cm) estimated for the largest known individual (Kobayashi and Lü 2003) (Fig. 5). To assess the ontogenetic age of the ornithomimids, histologic samples of tibia, fibula and rib were obtained for three individuals with femoral lengths of 19.4, 21.6, and 36.4 cm, respectively. Cross-sections were prepared for each element using standard paleohistologic techniques (Wilson 1993; Lamm 1999, 2001), and examined with light microscopy. Age at death was assessed from annual lines of arrested growth (LAGs) (Erickson 2005). Histology of the three elements is largely consistent for each individual. For example, the fibula of the largest individual shows a comparable set of LAGs within the fibrolamellar tissue to that of the tibia. Additionally, the cortex of all elements consists of fibrolamellar bone with primarily longitudinally arranged osteons.

The pair of smaller individuals (Fig. 3A) shows only a single line of arrested growth. The tibia of the slightly larger one (Fig. 3A, right skeleton) bears a circumferential band of laminar bone with a parallel crystal arrangement that likely corresponds with the single LAG in the rib and fibula (Fig. 4A). Presence of a single LAG indicates that these two individuals were between one and two years of age at the time of death. The longer skull length (134 versus 114 mm) of the slightly larger individual suggests that it may belong to an earlier brood from the same breeding season.

The tibia and fibula of the largest individual sampled display four LAGs, but their larger medullary cavity (compared to smaller individuals) suggests that a few initial LAGs may have been lost to endosteal remodeling (Fig. 4B). Spacing of preserved LAGs is consistent between the tibia and fibula and both possess incompletely developed outer osteons with wide osteonal canals (Fig. 4C). The rib bears seven unequally spaced LAGs. A wide region with multiple rows of osteons separates an inner and outer set of more closely spaced LAGs.

Discussion

Depositional environment.—The short stratigraphic section visible at the Sohongtu locality consists of a fine-grained, laminated to very thinly bedded unit sandwiched between more massive, fine-grained units with a variety of soil-related features. These underlying and overlying units lack any architectural elements suggestive of fluvial channels and are more representative of overbank deposition (Miall 1996). The lamination and very thin beds of the intervening unit represent slow deposition under quiet, low-energy conditions and an absence of significant invertebrate or vertebrate bioturbation. Abundance of ostracods like Cypridea within this interval favors a freshwater environment such as a pond or lake for the main burial unit. Insufficient outcrop exists at the locality to determine the aerial extent of this ponding environment. However, the short stratigraphic extent and bounding overbank units suggest a temporarily limited feature. The gradual transition of the laminated unit to more massive mudstones with a variety of soil-related features (e.g., slickensides, peds, carbonate nodules) reflects the eventual infilling of the pond or lake. An arid to semi-arid climate is suggested by caliche horizons, evaporites and gilgai structures found either in the Sohongtu locality section or in nearby outcrops of the Ulansuhai Formation (Bureau of Geology 1991).

A striking aspect of the laminated unit is the alternating red and blue-gray coloration (Fig. 2A, B). The color and concentration of blue-gray mottling along specific horizons is consistent with gleization. In this process, the activity of microorganisms depletes stagnant water of oxygen leading to the eventual reduction of minerals by anaerobic microbes (Retallack 1990). A similar process also likely accounts for the blue-gray coloration surrounding articulated skeletons (see below) and the alternating red and blue-gray horizons throughout the unit. The latter suggests the frequent and repeated stagnation of the water body.

We regard the V-shaped deformation structures of the bone-bearing and two additional horizons as partially collapsed, infilled, toe prints that were made in wet laminated clay. The deformed strata match those identified as footprints at other localities (Agenbroad 1984: fig. 4.4; Melchor et al. 2006: fig. 9H, I) and experimentally produced in wet sediments (Milàn and Bromley 2008). The narrow-toed, sharp-clawed pedes of the ornithomimids are the appropriate size and shape to have generated these structures.

Fig. 4.

Histologic cross-sections and age profile of skeletons. A. Cross-section of tibial mid shaft from small individual (LH PV5, femur length = 21.6 cm) showing a single band of laminar bone (marked by <) but no LAGs (lines of arrested growth). B. Histologic cross-section of tibial mid shaft of the large individual (LH PV7, femur length = 36.4 cm) showing four LAGs (marked by <). C. Histologic cross-section showing the exterior of the tibial mid-shaft cortex for the large individual (LH PV7). Note row of developing osteons at the exterior (top of photograph). One LAG visible near bottom of photograph. Scale bar is 2 mm for A, B and 0.25 mm for C.

f04_567.eps

Taphonomic history.—The Suhongtu site records the catastrophic miring of an ornimomimid herd within a shrinking lake or pond under drying conditions. The mud-anchored carcasses were then scavenged, with some postmortem, low-energy transport of disarticulated elements prior to or during final burial. Although both miring and drought conditions likely contributed to the deaths of the Sinornithomimus at this locality, we consider miring as discussed below as the more proximal cause given the more restricted temporal and geographic conditions under which it acts.

Miring.—In modern environments, entrapment in mud is a rare cause of death that requires particular substrate viscosity usually involving the partial drying of water-saturated sediment (Weigelt 1989). Waterlogged initial conditions are evidenced at Suhongtu by the deep penetration of limbs and tails into underlying horizons and the V-shaped footprint disruption structures of these laminae (Fig. 2C). The mud infilling of these footprints indicates the immediate slumping and collapse of the track as the foot was withdrawn, conditions common to waterlogged sediments (Agenbroad 1984; Melchor et al. 2006; Milàn and Bromley 2008). The crosscutting relationship of both the skeletons and footprints with the underlying strata indicates that miring post-dates deposition of these horizons. The coincident die-off of ostracods near and adjacent to the skeletons and sand-filled mudcracks suggest deterioration of the ponding environment and desiccation. Finally, the presence of entrapped ornithomimids (and their associated traces) in a sequence of otherwise finely laminated strata suggests that miring occurred at a time of low water level. Suitable conditions for entrapment are often short-lived, weather dependent, and may last for only days (Weigelt 1989).

Recent and fossil cases of death by miring include a variety of terrestrial vertebrates ranging in size from the foals of feral horses (Berger et al. 2001) to multi-ton dinosaurs (Sander 1992) and include both quadrupeds and bipeds (Stirling 1894; Weigelt 1989; Berger et al. 2001). When trapped in mud, living vertebrates ultimately die from dehydration, starvation and/or predation (Stirling 1894; Weigelt 1989; Berger et al. 2001). Death postures and preservational patterns match those of the Suhongtu ornithomimids and include plunging limbs and preferential preservation of entrapped body parts (Stirling 1894; Weigelt 1989; Sander 1992; Berger et al. 2001) (Fig. 3). Limbs typically extend into the underlying substrate whereas the trunk and head remain at ground level. This condition occurs in 12 of the 13 recently excavated Sinornithomimus. Following death, buried limbs remain articulated and intact, while exposed portions experience greater levels and ranges of disarticulation, weathering, and scavenging (Stirling 1894; Weigelt 1989; Sander 1992). The significance of the plunging Sinornithomimus tail sections remains ambiguous, but may reflect the struggles of these bipedal animals to free themselves once entrapped.

Variable preservation of the upper portions of the Sinornithomimus skeletons suggests a brief period of exposure, decay, and possibly scavenging prior to final burial. Aerobic decay of carcasses requires a large oxygen supply; consequently, most carcasses decompose anaerobically and create reducing conditions and anoxic microenvironments in adjacent sediments (Allison 1988). The drab haloes occurring within the otherwise red and oxic sediments and surrounding the articulated portions of the ornithomimids skeletons (Fig. 3) likely reflect the oxic, then anoxic decay of soft tissue. The absence of such haloes around isolated elements indicates that either scattering occurred after rotting of the flesh or these skeletal portions were of insufficient size to deplete local microenvironments of oxygen. Scavenging may account for the curious absence of ilia and sacra from otherwise articulated pelves. Perhaps carnivores favored the large muscle mass of the hips (Lyman 1994). However, no shed theropod teeth occurred amongst the Sinornithomimus skeletons.

Mass mortality.—Several taphonomic attributes of the Suhongtu locality indicate a mass mortality of a social group rather than attritional death of individuals. First, the ornithomimids occur on a single bedding plane. Although some have disarticulated and likely been subjected to scavenging, the absence of weathering on any element indicates minimal subaerial exposure, probably less than one year (Behrensmeyer 1978). Exceptional preservation, including intact gastrolith masses within the ribcage (Kobayashi et al. 1999), carbonized stomach contents (Fig. 3D), and intact sclerotic rings in several individuals, favors relatively rapid burial. Further, miring depends upon specific conditions of water level and substrate viscosity. Any deviations, whether to drier or wetter conditions, would prohibit entrapment. Uniform carcass appearance at modern miring localities reflects both herding behavior and synchronous mortality (Weigelt 1989; Berger et al. 2001). In contrast to the alignment of elongate, isolated bones, the skeletons show a strong orientation to the southeast with ten of the 13 specimens oriented within a 101° arc (Fig. 1C). Similar parallel alignment has been observed in a small flock of flightless birds mired in a Pleistocene lacustrine deposit (Stirling 1894). The consistent preservation, close proximity, and preferred orientation of the Sinornithomimus skeletons suggest that these individuals arrived and perished together at this site.

Drought conditions.—Evidence for drying conditions within the lake or pond includes the marginal mudcracks, the associated ostracod assemblages, and the presence of the ornithomimids and their traces. The latter is significant, because the bone-bearing unit consists sequentially of laminated horizons, the mass death horizon, a thin sandstone and a return to laminated strata. The unbioturbated laminae suggest deeper water (Fig. 2A). The presence of the ornithomimids and their traces indicates a time of low water in what was otherwise a deeper water sequence. Although several dinosaur bonebeds have been interpreted as potentially originating due to past drought conditions (Norman 1987; Rogers 1990; Schwartz and Gillette 1994; Gates 2005; Eberth et al. 2006; Myers and Storrs 2007) physical indicators of drought have been limited. Evidence primarily consists of (i) an overall arid to semi-arid paleoenvironment and (ii) the concentration of bones and/or individuals in a flood plain lake or depression. However, these localities may simply represent favorable areas of preservation where weathering rates of bone are slowed and sedimentation rates are higher. Furthermore, most of these assemblages also record significant post-mortem transport of carcasses or bones (Norman 1987; Schwartz and Gillette 1994; Eberth et al. 2006; Myers and Storrs 2007). The Suhongtu locality is unusual in its association with several indicators of drought (ostracod die-off, mudcracks, and footprints in otherwise deeper water deposits) independent of the bone assemblage and a direct linking of mortality (miring) to the drought conditions. The frequent alternation between red and blue-gray horizons within the laminated to thinly bedded unit indicates irregular alternating periods of aeration and stagnation, possibly reflecting wetter and drier conditions. Consequently, the occurrence of three horizons with some combination of footprints, ostracods, and mudcracks within this section suggests a more extreme and uncommon drying within this alternating pattern. The Suhongtu site emphasizes the important role of drought in the fossil record both as an agent of mortality and as a mechanism driving vertebrates into depositional settings where preservation can occur (Shipman 1975; Rogers 1990).

Population structure and sociality.—Histologic examination of the Suhongtu ornithomimids confirms that the absence of neurocentral fusion and small size in these specimens reflects immaturity (Fig. 4). Presence of a single LAG in the small individuals sampled indicates that these two were between one and two years of age at the time of death. The longer skull length of the slightly larger individual suggests that it may belong to an earlier brood from the same breeding season. The rib of the largest individual sampled has seven LAGs, suggesting a minimum age of seven years. This number is consistent with the number of LAGs and the size of the medullary cavity observed in the limb elements. The developing osteons at the periphery of the limb elements indicates that this individual was still undergoing rapid growth at the time of death (Fig. 4C) (Ricqlès 1980). Consequently, the Sinornithomimus herd consisted entirely of juveniles and subadults from one to seven years old (Fig. 5).

Fig. 5.

Size distribution of individuals from the Suhongtu quarry representing a juvenile to subadult herd. Missing hatchling and adult sizes shown in gray. Colors in plot differentiate skeletons from this study (rust) from those excavated previously (orange) (Kobayashi and Lü 2001).

f05_567.eps

Skeletal assemblages composed predominantly of juveniles have been reported for other nonavian dinosaurs including the therizinosaur Falcarius (Zanno and Erickson 2006), a diplodocid sauropod (Myers and Storrs 2007), the ankylosaurid Pinacosaurus (Jerzykiewicz et al. 1993), ceratopsians (Gilmore 1917; Lehman 2006; Zhao et al. 2007), and several ornithopods (Forster 1990; Varricchio and Horner 1993; Scherzer 2008; Scherzer and Varricchio 2005; Garrison et al. 2007). However, taphonomic ambiguity concerning the causative agents of these assemblages weakens the interpretation of these sites as reflecting social groups. The Sinornit homimus locality suggests that these other assemblages indeed record a true behavioral signal. In general, catastrophic death assemblages of extant vertebrates are highly representative of living social groups (Berger et al. 2001).

In extant archosaurs sociality among juveniles is uncommon. In crocodilians the most common juvenile associations are “pods” that form for several weeks after hatching and are generally accompanied by an adult (Lang 1989). Among some birds more persistent juvenile aggregations occur when sexual maturity is delayed for several years (Boarman and Heinrich 1999; Davies 2002) as in nonavian dinosaurs (Erickson et al. 2008). Ostrich broods often coalesce into large and fairly stable flocks with or without attending males, and large numbers of yearlings with some non-breeding adults form flocks in the greater rhea (Rhea americana) (Davies 2002). In the common raven (Corvus corax) juveniles and non-breeders maintain foraging crowds and communal roosts (Boarman and Heinrich 1999).

Three life-history attributes would have favored sociality of immature and non-breeding individuals in nonavian dinosaurs: (i) oviparity with relatively small hatchlings, (ii) extensive parental care of eggs and young (Horner 2000), and (iii) a multi-year growth phase prior to sexual maturation (Erickson 2005). Both crocodilians and birds invest significant time to mating, nest building, and parental care. For example, the Orinoco crocodile (Crocodylus intermedius) requires nearly six months (Thorbjarnarson and Hernandez 1993) and the ostrich some two to eleven months (Davies 2002). Growing evidence now supports parental care of eggs and young in many dinosaurs (Norell et al. 1995; Horner 2000; Meng et al. 2001; Varricchio et al. 2007) perhaps with the exception of some sauropods (Sander et al. 2008). Time to maturation for non-avian dinosaurs, despite relatively rapid growth rates, remains greater than one year and often more than a decade for larger species (Erickson 2005). Thus, as in modern birds like ostrich and raven, while adults were preoccupied with breeding, nesting, and the care of eggs and hatchlings, non-breeding juveniles and adults may have congregated elsewhere in social groups of mixed age, as preserved by the miring at Suhongtu. Such groups would potentially differ from those of modern birds, e.g., raven. Because fledged birds are nearly the same size as adults, avian aggregations include a much narrower range of body sizes than could potentially be represented by non-avian dinosaur groups. Given the taxonomic diversity of juvenile-dominated assemblages, herding of immature individuals may have been common behavioral pattern among nonavian dinosaurs.

In addition to the ornithomimid locality described here, exclusively or predominantly juvenile assemblages occur among sauropods, theropods, ankylosaurs, ceratopsians, and ornithopods (Gilmore 1917; Forster 1990; Jerzykiewicz et al. 1993; Varricchio and Horner 1993; Scherzer and Varricchio 2005; Zanno and Erickson 2006; Lehman 2006; Garrison et al. 2007; Myers and Storrs 2007). Whether the sociality of immature individuals found in non-avian dinosaurs and modern birds is a shared derived feature remains unclear. However, the rarity of such sociality among extant avians might favor the independent evolution of this behavior. Despite filling similar terrestrial niches in comparison to modern mammals, nonavian dinosaurs exhibited drastically different life history strategies in terms of their reproduction and sociality.

Recently, studies have interpreted Sinornithomimus and ornithomimids as unusual among theropods in being herbivorous (White et al. 1998; Kobayashi et al. 1999; Ji et al. 2003; Norell et al. 2004). Whether this shift in diet can be associated with the acquisition of more complex social behavior remains to be determined.

Finally, the age profile of the Sinornithomimus assemblage indicates a population with normally high juvenile mortality. This pattern conforms to that suggested for other herbivorous dinosaurs (Varricchio and Horner 1993; Sander et al. 2008) but differs markedly from that of tyrannosaurs (Erickson et al. 2006). The unusual mortality pattern proposed for tyrannosaurs (Erickson et al. 2006) may reflect their distinct ecology as large-bodied predators or may be a non-biologic artefact as the population structure was based upon attritional remains of unclear taphonomic origin (Roach and Brinkman 2007).

Conclusions

  • Sedimentary and taphonomic evidence at the Suhongtu locality indicate the mass miring of a juvenile herd of Sinornithomimus. Mudcracks, ostracod assemblages, and the occurrence of footprints in otherwise deeper water deposits reflect the deterioration and drying of the lake environment. The deeply plunging limbs and tails that crosscut underlying laminated strata denote death by entrapment within muddy sediments. The variable preservation of the skeletal portions on the main bone horizon reflects their greater exposure to postmortem decay, scavenging, and transport. The uniform preservation, close proximity on a single bedding plane, and parallel alignment of skeletons supports a catastrophic mass mortality of a group rather than attritional death of individuals.

  • The Suhongtu site is exceptional among dinosaur bonebeds in preserving several indicators of drought (ostracod assemblages, mudcracks, and footprints in deeper water strata) independent of the bone assemblage.

  • The age profile of the Sinornithomimus herd represents strictly immature individuals and supports other juvenile-dominated dinosaur bonebeds as biologically real.

  • Nonavian dinosaurs differed from modern terrestrial vertebrates in their proclivity to form juvenile herds. This reflects their mobile lifestyle, oviparity, parental care of eggs and hatchlings, and slow (i.e., mutli-year) maturation.

  • The population structure of the Sinornithomimus herd conforms to those of other herbivorous dinosaurs and suggests high juvenile mortality.

Acknowledgements

We thank Yoshitsugu Kobayashi (Hokkaido University Museum, Sapporo, Japan) for providing additional data on the site, Carol Abraczinskas (University of Chicago, Chicago, USA), and Lee Hall (Montana State University, Bozeman, USA) for figures; Robert Masek and Tyler Kiellor (University of Chicago, Chicago, USA) for preparation, molding and casting of fossils; the 2001 Chinese-American Dinosaur Expedition team for excavation of the site; Ellen Lamm and Jack Horner at the Gabriel Laboratory for Cellular and Molecular Paleontology (Museum of the Rockies, Bozeman, USA) for histological work; Deborah Wharton; and the reviewers, David Eberth and Martin Sander for their helpful comments. This research was supported by the David and Lucile Packard Foundation and the National Geographic Society (to P. Sereno).

References

  1. L.D. Agenbroad 1984. Hot Springs, South Dakota. Entrapment and taphonomy of Columbian mammoth. In : P.S. Martin and R.G. Klein (eds.), Quaternary Extinctions: A Prehistoric Revolution , 113–127. University of Arizona, Tucson. Google Scholar

  2. P.A. Allison 1988. The role of anoxia in the decay and mineralization of proteinaceous macro-fossils. Paleobiology 14: 139–154. Google Scholar

  3. A.K. Behrensmeyer 1978. Taphonomic and ecologic information from bone weathering. Paleobiology 4: 150–162. Google Scholar

  4. J. Berger , S. Dulamtseren , S. Cain , D. Enkkhbileg , P. Lichtman , Z. Namshir , G. Wingard , and R. Reading 2001. Back-casting sociality in extinct species: new perspectives using mass death assemblages and sex ratios. Proceedings of the Royal Society London B 268: 131–139. Google Scholar

  5. S.A. Bilbey 1999. Taphonomy of the Cleveland-Lloyd dinosaur quarry in the Morrison Formation, central Utah—a lethal spring-fed pond. Miscellaneous Publications, Utah Geological Survey 99-1: 121–133. Google Scholar

  6. W.I. Boarman and B. Heinrich 1999. Common raven (Corvus corax). In : A. Poole (ed.), The Birds of North America Online, no. 476. Ithaca: Cornell Lab of Ornithology; Retrieved from the Birds of North America Online:  http://bna.birds.Cornell.edu/bna/species/476Google Scholar

  7. Bureau of Geology and Mineral Resources of Nei Mongol 1991. Regional Geology of Nei Mongol (Inner Mongolia) Autonomous Region. People's Republic of China, Ministry of Geology and Mineral Resources, Geological Memoirs 1: 1–725. Google Scholar

  8. P.J. Currie 2000. Possible evidence of gregarious behavior in tyrannosaurids. Gaia 15: 271–278. Google Scholar

  9. P.J. Currie and P. Dodson 1984. Mass death of a herd of ceratopsian dinosaurs. In : W.-E. Reif and F. Westphal (eds.), Third Symposium of Mesozoic Terrestrial Ecosystems , 52–60. Attempto Verlag, Tübingen. Google Scholar

  10. S.J.J.F. Davies 2002. Ratites and Tinamous. 310 pp. Oxford University Press, Oxford. Google Scholar

  11. D.A. Eberth and M.A. Getty 2005. Ceratopsian bonebeds: Occurrence, origins, and significance. In : P.J. Currie and E.B. Kopplhus (eds.), Dinosaur Provincial Park: A Spectacular Ancient Ecosystem Revealed , 501–536. Indiana University Press, Bloomington. Google Scholar

  12. D.A. Eberth , B.B. Britt , R. Scheetz , K.L. Stadtman , and D.B. Brinkman 2006. Dalton Wells: geology and significance of debris-flow-hosted dinosaur bonebeds in the Cedar Mountain Formation (Lower Cretaceous) of eastern Utah, USA. Palaeogeography, Palaeoclimatology, Palaeoecology 236: 217–245. Google Scholar

  13. G.M. Erickson 2005. Assessing dinosaur growth patterns: A microscopic revolution. Trends in Ecology & Evolution 20: 677–684. Google Scholar

  14. G. Erickson , P.J. Currie , B.D. Inouye , and A.A. Winn 2006. Tyrannosaur life tables: an example of nonavian dinosaur population biology. Science 313: 213–217. Google Scholar

  15. G.M. Erickson , K.C. Rogers , D.J. Varricchio , M.A. Norell , and X. Xu 2008. Growth patterns in brooding dinosaurs reveals the timing if sexual maturity in non-avian dinosaurs and genesis of the avian condition. Biology Letters 3: 558–561. Google Scholar

  16. C.M. Faux and K. Padian 2007. The opisthotonic posture of vertebrate skeletons: postmortem contraction or death throes? Paleobiology 33: 201–226. Google Scholar

  17. A.R. Fiorillo and D.A. Eberth 2004. Dinosaur taphonomy. In : D.B. Weishampel , P. Dodson , and H. Osmólska (eds.), The Dinosauria , 2nd Edition , 607–613. University of California Press, Berkeley. Google Scholar

  18. C.A. Forster 1990. Evidence for juvenile groups in the ornithopod dinosaur Tenontosaurus tilletti Ostrom. Journal of Paleontology 64: 164–165. Google Scholar

  19. J.R. Garrison Jr. , D. Brinkman , D.J. Nichols , P. Layer , D. Burge , and D. Thayn 2007. A multidisciplinary study of the Lower Cretaceous Cedar Mountain Formation, Mussentuchit Wash, Utah: a determination of the paleoenvironment and paleoecology of the Eolambia caroljonesa dinosaur quarry. Cretaceous Research 28: 461–494. Google Scholar

  20. T.A. Gates 2005. The Late Jurassic Cleveland-Lloyd dinosaur quarry as a drought-induced assemblage. Palaios 20: 363–375. Google Scholar

  21. C.W. Gilmore 1917. Brachyceratops, a ceratopsian dinosaur from the Two Medicine Formation of Montana with notes on associated reptiles. United States Geological Survey Professional Paper 103: 1–45. Google Scholar

  22. G. Haynes 1988. Mass deaths and serial predation: Comparative taphonomic studies of modern large-mammal deathsites. Journal of Archaeological Science 15: 219–235. Google Scholar

  23. J.R. Horner 2000. Dinosaur reproduction and parenting. Annual Review of Earth and Planetary Sciences 28: 19–45. Google Scholar

  24. R.C. Jr. Hulbert 1982. Population dynamics of the three-toed horse Neohipparion from the late Miocene of Florida. Paleobiology 8: 159–167. Google Scholar

  25. T. Jerzykiewicz 2000. Lithostratigraphy and sedimentary settings of the Cretaceous dinosaur beds of Mongolia. In : M.J. Benton , M.A. Shishkin , D.M. Unwin , and E.N. Kurochkin (eds.), The Age of Dinosaurs in Russia and Mongolia , 279–296. Cambridge University Press, Cambridge. Google Scholar

  26. T. Jerzykiewicz , P.J. Currie , D.A. Eberth , P.A. Johnston , E.H. Koster , and J.-J. Zheng 1993. Djadokhta Formation correlative strata in Chinese Inner Mongolia: an overview of the stratigraphy, sedimentary geology, and paleontology and comparisons with the type locality in the pre-Altai Gobi. Canadian Journal of Earth Sciences 30: 2180–2195. Google Scholar

  27. Q. Ji , M.A. Norell , P.J. Makovicky , K. Gao , S. Ji , and C. Yuan 2003. An early ostrich dinosaur and implication for ornithomimosaur phylogeny. American Museum Novitates 3420: 1–19. Google Scholar

  28. R.G. Klein 1982. Patterns of ungulate mortality and ungulate mortality profiles from Langebaanweg (early Pliocene) and Elandsfontein (middle Pleistocene), south-western Cape Province, South Africa. Annals of the South African Museum 90 (2): 49–94. Google Scholar

  29. Y. Kobayashi and J.-C. Lü 2003. A new ornithomimid dinosaur with gregarious habits from the Late Cretaceous of China. Acta Palaeontologica Polonica 48: 235–259. Google Scholar

  30. Y. Kobayashi , J.-C. Lü , Z.-M. Dong , R. Barsbold , Y. Azuma , and Y. Tomida 1999. Herbivorous diet in an ornithomimid dinosaur. Nature 402: A80–A81. Google Scholar

  31. E.T. Lamm 1999. Histological techniques for small paleontological specimens. Journal of Vertebrate Paleontology 19: 58A. Google Scholar

  32. E.T. Lamm 2001. Put it back the way you found it: restoration of histological fossil specimens. Journal of Vertebrate Paleontology 21: 71A. Google Scholar

  33. J.W. Lang 1989. Social behavior. In : C.A. Ross and S. Garnett (eds.), Crocodiles and Alligators , 102–117. Facts on File, New York. Google Scholar

  34. T.M. Lehman 2006. Growth and population age structure in the horned dinosaur Chasmosaurus. In : K. Carpenter (ed.), Horns and Beaks: Ceratopsian and Ornithopod Dinosaurs , 259–317. Indiana University Press, Bloomington. Google Scholar

  35. L.R. Lyman 1994. Vertebrate Taphonomy. 524 pp. Cambridge University Press, Cambridge. Google Scholar

  36. R.N. Melchor , E. Bedatou , S. de Valais , and J.F. Genise 2006. Lithofacies distribution of invertebrate and vertebrate trace-fossil assemblages in an early Mesozoic ephemeral fluvio-lacustrine system from Argentina: Implications for the Scoyenia ichnofacies. Palaeogeography, Palaeoclimatology, Palaeoecology 239: 253–285. Google Scholar

  37. Q. Meng , J. Liu , D.J. Varricchio , T. Huang , and C. Gao 2004. Parental care in an ornithischian dinosaur. Nature 431: 145–146. Google Scholar

  38. A.D. Miall 1996. The Geology of Fluvial Deposits: Sedimentary Facies, Basin Analysis, and Petroleum Geology. 582 pp. Springer-Verlag, Berlin. Google Scholar

  39. J. Milàn and R.G. Bromley 2008. The impact of sediment consistency on track and undertrack morphology: Experiments with emu tracks in layered cement. Ichnos 15: 19–27. Google Scholar

  40. T.S. Myers and G.W. Storrs 2007. Taphonomy of the Mother's Day Quarry, Upper Jurassic Morrison Formation, south-central Montana, USA. Palaios 22: 651–666. Google Scholar

  41. M.A. Norell , J.M. Clark , L.M. Chiappe , and D. Dashzeveg 1995. A nesting dinosaur. Nature 378: 774–776. Google Scholar

  42. M.A. Norell , P.J. Makovicky and P.J. Currie 2004. The beaks of ostrich dinosaurs. Nature All : 873–874. Google Scholar

  43. D.B. Norman 1987. A mass-accumulation of vertebrates from the Lower Cretaceous of Nehden (Sauerland), West Germany. Proceedings of the Royal Society of London B 230: 215–255. Google Scholar

  44. J.H. Ostrom 1986. Social and unsocial behavior in dinosaurs. In : M.H. Nitecki and J.A. Kitchell (eds.), Evolution of Animal Behavior , 41–61. Oxford University Press, Cambridge. Google Scholar

  45. I.S. Paik 2000. Bone chip-filled burrows associated with bored dinosaur bone in floodplain paleosols of the Cretaceous Hasandong Formation, Korea. Palaeogeography, Palaeoclimatology, Palaeoecology 157: 213–225. Google Scholar

  46. J.R. Patterson , J.B. Jago , G.A. Brock , and J.G. Gehling 2007. Taphonomy and palaeoecology of the emuellid trilobite Balcoracania dailyi (Early Cambrian, South Australia). Palaeogeography, Palaeoclimatology, Palaeoecology 157: 213–225. Google Scholar

  47. G.J. Retallack 1990. Soils of the Past. 520 pp. Unwin Hyman, Boston. Google Scholar

  48. A.J. de Ricqlès 1980. Tissue structures of dinosaur bone: functional significance and possible relation to dinosaur physiology. In : D.K. Thomas and E.C. Olson (eds.), A Cold Look at the Warm-blooded Dinosaurs , 104–140. Westview Press, Boulder. Google Scholar

  49. B.T. Roach and D.L. Brinkman 2007. A reevaluation of cooperative pack hunting and gregariousness in Deinonychus antirrhopus and other nonavian theropod dinosaurs. Bulletin. Peabody Museum of Natural History 48: 103–138. Google Scholar

  50. R.R. Rogers 1990. Taphonomy of three dinosaur bone beds in the Upper Cretaceous Two Medicine Formation of northwestern Montana: evidence for drought-related mortality. Palaios 5: 394–413. Google Scholar

  51. M.J. Ryan , A.P. Russell , D.A. Eberth , and P.J. Currie 2001. The taphonomy of a Centrosaurus (Ornithischia: Ceratopsidae) bone bed from the Dinosaur Park Formation (Upper Campanian), Alberta, Canada, with comments on cranial ontogeny. Palaios 16: 482–506. Google Scholar

  52. P.M. Sander 1992. The Norian Plateosaurus bonebeds of central Europe and their taphonomy. Palaeogeography, Palaeoclimatology, Palaeoecology 93: 255–299. Google Scholar

  53. P.M. Sander , C. Peitz , F. Jackson , and L. Chiappe 2008. Upper Cretaceous titanosaur nesting sites and their implications for sauropod reproductive biology. Palaentographica A 284: 69–107. Google Scholar

  54. B. Scherzer 2008. Taphonomy of the Sun River Bonebed, Late Cretaceous (Campanian) Two Medicine Formation of Montana. 108 pp. Unpublished Master's thesis, Montana State University, Bozeman. Google Scholar

  55. B. Scherzer and D.J. Varricchio 2005. Taphonomy of a juvenile lambeosaur bonebed in the Two Medicine Formation of Montana. Journal of Vertebrate Paleontology 25: 110A. Google Scholar

  56. H.L. Schwartz and D.D. Gillette 1994. Geology and taphonomy of the Coelophysis quarry, Upper Triassic Chinle Formation, Ghost Ranch, New Mexico. Journal of Paleontology 68: 1118–1130. Google Scholar

  57. P. Shipman 1975. Implications of drought for vertebrate fossil assemblages. Nature 257: 667–668. Google Scholar

  58. S.E. Speyer 1991. Trilobite taphonomy: a basis for comparative studies of arthropod preservation, functional anatomy and behavior. In : S.K. Donovan (ed.), The Process of Fossilization , 194–219. Columbia University Press, New York. Google Scholar

  59. S.E. Speyer and C.E. Brett 1985. Clustered trilobite assemblages in the Middle Devonian Hamilton Group. Lethaia 18: 85–103. Google Scholar

  60. E.C. Stirling 1894. The recent discovery of fossil remains of Lake Callabonna, South Australia. Nature 50: 184–188. Google Scholar

  61. C.A. Suarez , M.A. Suarez , D.O. Terry Jr. , and D.E. Grandstaff 2007. Rare earth element geochemistry and taphonomy of the Early Cretaceous Crystal Geyser Dinosaur Quarry. Palaios 22: 500–512. Google Scholar

  62. M.A. Suarez , C.A. Suarez , J.I. Kirkland , L.A. González , D.E. Grandstaff , and D.O. Terry Jr. 2007. Sedimentology, stratigraphy, and depositional environment of the Crystal Geyser Dinosaur Quarry, east-central Utah. Palaios 22: 513–527. Google Scholar

  63. J.B. Thorbjarnarson and G. Hernandez 1993. Reproductive ecology of the Orinoco crocodile (Crocodylus intermedius) in Venezuela. II. Reproductive and social behavior. Journal of Herpetology 27: 371–379. Google Scholar

  64. O. Tinn and T. Meidla 2003. Ontogeny and thanatocoenoses of early Middle Ordovician palaeoscope ostracode species Brezelina palmata (Krause, 1889) and Ogmoopsis bocki (Öpik, 1935). Journal of Paleontology 77: 64–72. Google Scholar

  65. D.J. Varricchio and J.R. Horner 1993. Hadrosaurid and lambeosaurid bone beds from the Upper Cretaceous Two Medicine Formation of Montana: taphonomic and biologic implications. Canadian Journal of Earth Sciences 31: 997–1006. Google Scholar

  66. D.J. Varricchio , A. Martin , and Y. Katsura 2007. First trace and body fossil evidence of a burrowing, denning dinosaur. Proceedings of the Royal Society of London B 274: 1361–1368. Google Scholar

  67. M.R. Voorhies 1969. Taphonomy and population dynamics of an early Pliocene vertebrate fauna, Knox County, Nebraska. University Wyoming Contributions to Geology, Special Paper 1: 1–69. Google Scholar

  68. M.R. Voorhies 1985. A Miocene rhinoceros herd buried in volcanic ash. National Geographic Society Research Reports 19: 671–688. Google Scholar

  69. J. Weigelt 1989. Recent Vertebrate Carcasses and their Paleobiological Implications. 188 pp. University of Chicago Press, Chicago. Google Scholar

  70. P.D. White , D.E. Fastovsky , and P.M. Sheehan 1998. Taphonomy and suggested structure of the dinosaurian assemblage of the Hell Creek Formation (Maastrichtian), eastern Montana and western North Dakota. Palaios 13: 41–51. Google Scholar

  71. J.W. Wilson 1993. Histological techniques. In : P. Leiggi and P. May (eds.), Vertebrate Paleontological Techniques , 205–234. Cambridge University Press, Cambridge. Google Scholar

  72. L. Zanno and G. Erickson 2006. Ontogeny and life history of Falcarius utahensis, a primitive therizinosauroid from the Early Cretaceous of Utah. Journal of Vertebrate Paleontology 26:143A. Google Scholar

  73. Q. Zhao , P.M. Barrett , and D.A. Eberth 2007. Social behaviour and mass mortality in the basal ceratopsian dinosaur Psittacosaurus (Early Cretaceous, People's Republic of China). Paleontology 50: 1023–1029. Google Scholar

David J. Varricchio, Paul C. Sereno, Zhao Xijin, Tan Lin, Jeffery A. Wilson, and Gabrielle H. Lyon "Mud-Trapped Herd Captures Evidence of Distinctive Dinosaur Sociality," Acta Palaeontologica Polonica 53(4), 567-578, (1 December 2008). https://doi.org/10.4202/app.2008.0402
Published: 1 December 2008
JOURNAL ARTICLE
12 PAGES


SHARE
ARTICLE IMPACT
Back to Top