Large quantities of impact-related microspherules have been found in fine-grained sediments retained within seven out of nine, radiocarbon-dated, Late Pleistocene mammoth (Mammuthus primigenius) and bison (Bison priscus) skull fragments. The well-preserved fossils were recovered from frozen “muck” deposits (organic-rich silt) exposed within the Fairbanks and Klondike mining districts of Alaska, USA, and the Yukon Territory, Canada. In addition, elevated platinum abundances were found in sediment analysed from three out of four fossil skulls. In view of this new evidence, the mucks and their well-preserved but highly disrupted and damaged vertebrate and botanical remains are reinterpreted in part as blast deposits that resulted from several episodes of airbursts and ground/ice impacts within the northern hemisphere during Late Pleistocene time (~46–11 ka B.P.). Such a scenario might be explained by encounters with cometary debris in Earth-crossing orbits (Taurid Complex) that was generated by fragmentation of a large short-period comet within the inner Solar System.
During the time period leading up to the Last Glacial Maximum (~23–19 ka B.P.), when eustatic sea level was substantially lower, Alaska and the Yukon Territory were part of the largest circumarctic area to remain unglaciated, called Beringia (Fig. 1), which extended from eastern Siberia (Chukotka) across the exposed Bering Strait region into Alaska and western Canada1,2. The glacial steppe environment of Beringia3 was a refugium for Plio-Pleistocene tundra-grassland plant communities4 as well as for the now-extinct mammalian megafauna5. Relict permafrost within the region6,7,8,9 has preserved an extraordinary frozen record of plant, pollen, insect, and vertebrate fossil remains, as well as their ancient DNA1,10,11.
Early expeditions to Alaska12,13,14 and the Yukon Territory14,15 found large quantities of megafaunal bones along beaches, riverbanks, and in minor-stream valleys8. Even greater collections of these fossils were made after industrial-scale placer-gold mining operations began in the Fairbanks and Klondike districts in the early 20th century16. Otto W. Geist undertook extensive fossil collecting in Alaska on behalf of the American Museum of Natural History (AMNH), and in a typical year (1938) shipped more than eight thousand select specimens, weighing nearly eight tons (~7257 kg), to New York City8.
The fossil bones collected included those of bison, mammoth, horse, musk ox, moose, lynx, lion, camel, mastodon, bear, and caribou, with many of these animals also appearing as frozen partial carcasses or mummies1,8,17. The three most common genera found were bison, mammoth, and horse, which represent more than 90% of Beringia’s large mammalian biomass18. Many tens of thousands of specimens were collected in the 20th century from Alaska and the Yukon Territory5,8,19, and hundreds to thousands more are still being recovered every year from mines in the Klondike district alone1.
Unfortunately, the stratigraphic context of most Beringian vertebrate fossils in museum collections is unknown because they were usually found already exhumed on beaches, riverbanks, or the floors of mining excavations7,8. Radiocarbon dates19,20 and those fossils recovered with stratigraphic information, however, indicate that the megafaunal remains are predominantly from Wisconsinan-aged deposits8,9,21,22. Furthermore, by the end of the Wisconsinan Glacial Stage (~85–11.7 ka B.P.) and Pleistocene Epoch (~2.58 Ma–11.7 ka B.P.) much of the mammalian megafauna of Eurasia and North America had become extinct. A number of causes for the Late Pleistocene extinctions have been proposed including intensive human hunting23,24, climate change20,25, and extraterrestrial impacts26,27,28, and the subject remains highly controversial29,30.
The demise of animals whose remains have been found in Beringian mucks has long been attributed to “natural deaths” in a “rigorous environment”8, and researchers have generally held to non-catastrophic or “uniformitarian concepts” in their interpretations of the causal events leading up to fossil preservation5,31. Uniformitarian explanations can often appear inadequate, however, in providing a clear picture of how, for instance, animals found as frozen carcasses were quickly killed, often dismembered, and buried without normal predation, scavenging, or decomposition prior to freezing5.
Otto Geist held a more catastrophic view, based on his observations as collector, and envisioned a rapid series of events beginning with large volcanic eruptions and dust storms depositing widespread ash and silt beds that starved the animal grazers, followed by “great winds” that stripped trees of their leaves and bark before knocking them down, and finally by floodwaters that dismembered the many carcasses while washing them along with silt and plant debris into the creek valleys32. No evidence of large-scale starvation or floodwaters has been found, and no sources of “great winds” have been identified, so the scientific community has largely dismissed such catastrophic interpretations.
Herein we present the discovery of impact-related microspherules and elevated platinum concentrations in fine-grained sediments retained within seven Late Pleistocene bison and mammoth skull fragments from Alaska and the Yukon Territory, which potentially indicate a catastrophic origin for at least part of the frozen Beringian mucks. Our results point to repeated airbursts, including ground/ice impacts, and their associated blast winds33 as major factors in the emplacement of Alaskan and Yukon mucks and their included megafaunal and botanical remains. In addition, we consider an astronomical scenario in which Late-Pleistocene episodes of terrestrial bombardment were caused by cyclic intersections with cometary debris during formation of the Taurid Complex34.
“Muck” is a miner’s term used to indicate frozen, usually dark-coloured, fine-grained sediments (silt), often containing large amounts of plant material and abundant vertebrate fossils that unconformably overlie gold-bearing gravels in stream valleys of Alaska and the Yukon Territory6,7,8,9,16. Mucks of the Fairbanks and Klondike districts are situated within the discontinuous permafrost zone (DPZ, >50% frozen ground; Fig. 1)35 and because of their high organic content8,36 emit a fetid stench upon thawing6,9,37. The silt portion of the mucks is generally inferred to be retransported (gravitationally emplaced) loess from nearby upland areas that was initially swept up by winds from glacial outwash plains and deposited across the landscape, primarily during periods of glacial expansion8,38. These loess beds have total thicknesses ranging from a few cm on ridges to >60 m at lower elevations8,39 and are generally referred to as “primary”, “upland”, or “air-fall” loess40,41 as opposed to the “muck”, “organic silts”, or “valley” and “retransported” loess of the valley bottoms9,42. Nearby volcanic centers of the Aleutians and Alaskan margin produced distal tephra beds intercalated within the mucks and primary silts, and these tephras have played an important role in determining the age and stratigraphic framework of these deposits43.
Vertebrate and plant remains
The fossil skull fragments assembled for this study are Wisconsinan in age (Table S1), so we will focus on information concerning emplacement of the corresponding Goldstream Formation (Fig. 2; see Supplementary Information, “Quaternary stratigraphy”), the equivalent King Solomon Formation (Silt unit) of the Klondike district, and their incorporated vertebrate and plant remains. Similar organic-rich loess deposits also occur in Siberia (Fig. 1) and are called “Yedoma”. Overall, the fossil bones recovered from these units show a spectrum of preservation ranging from highly weathered to exceptionally well preserved with intact ancient DNA1,7,10. The recovered mummified or “freeze-dried” partial carcasses also indicate that some part of the permafrost in the Fairbanks and Klondike areas has existed there since Wisconsinan time6,7,8,9. Moreover, soil horizons were often buried and frozen before the plant material could decompose, in some instances preserving it for >700 kyr9,35.
The remarkable preservation of vertebrate and plant remains within the mucks, however, is in stark contrast to the physical disruption and damage affecting much of this material. Much of the skeletal remains from Alaska and Yukon were disarticulated and broken prior to freezing (Fig. 3a), and the rare preserved carcasses were often mangled and torn apart5,7,8. Such dismemberment has been attributed to predators and scavengers, but these explanations raise questions including why the carcasses’ remaining fat and flesh had not been consumed5. In addition, the fine-grained character of the mucks differs markedly from that of the more massive logs, megafaunal bones and tusks enclosed within it. Although the valley-bottom mucks are thought to have accumulated from gradual downslope movement of primary upland loess by slopewash, creep, and mudflow8,42, this scenario appears inconsistent with the required rapid burial and freezing of well-preserved carcasses7,8 and plant remains9,35. Below we examine these and other paradoxes more closely, some of which amazed and bewildered early explorers, scientists, and miners venturing to the region.
Fossil bone abundance
“Fossil bones are astonishingly abundant in the frozen ground of Alaska”7, and most observers from Quackenbush14 to Péwé et al.22 have made similar remarks. The majority of Alaskan fossils have been found in creek valley bottoms8, but the fossils have not been abraded or waterworn7. Bones are generally found throughout a given valley, and have been recovered from almost all creek valleys that have been mined7 (Fig. 3a). According to Otto Geist, most of the Pleistocene bones from the Fairbanks district were found in black muck containing plant remains16.
In the Klondike district, bones are mostly found near the base of the King Solomon Formation, usually within a few decimeters of its contact with the underlying auriferous gravel beds9. At one Alaskan locality, Little Eldorado Creek, 48 bison skulls and other related skeletal remains were found within a 35–m2 area32, while at other localities bones from a mixture of species have been recovered7,8,18. Although fossil remains are more abundant at some localities than others, many individual bones, or skeletal and carcass fragments, have been found in complete isolation8,44.
Fossil bone dispersal and breakage
“The dispersal of the bones is as striking as their abundance”7 and articulated bones are scarce in Beringia with the exception of small rodent carcasses (e.g., ground squirrels, pikas, mice) found underground within their nests and burrows5,8. Moreover, not only are individual megafaunal bones found separately, or mixed together in concentrated “bone beds”, they also are often broken (Figs 3a and 4–7, S1–S4). In examining large collections of Pleistocene fossil bones at the AMNH in New York and a Yukon Government warehouse in Whitehorse, we noted that the majority had been broken, including the largest (femora and humeri), with some still containing relict marrow, supporting the lack of predation. Because the mucks have apparently remained frozen since Wisconsinian time, dispersal and breakage of bones must have occurred prior to freezing and was not a general byproduct of the mining operations.
MacPhee et al.44 attempted to explain the dismemberment of Pleistocene carcasses and the resultant dispersal and breakage of bones recovered from Yedoma deposits on Russia’s Taimyr Peninsula as being caused by movements of ice in valley bottoms during spring breakup. They suggested that exposed limbs or other body parts of partially buried carcasses could have been sheared off by moving ice, and that ice-caused push fractures could have produced forces great enough to break bones as large as mammoth femora and humeri (see Fig. 3a). They acknowledged, however, that the “exquisite condition” of carcasses and many bones argues against these remains having spent a significant amount of time at the surface or having undergone any manner of “repeated redeposition”44.
A distinctive characteristic of the Beringian mucks is their uniform fine-grain size with only a few thin layers and lenses of coarser sand and gravel near their lower contacts16. Most mineral particles of the mucks will pass through a 200-mesh (<74 μm) sieve6, and, as mentioned above, the ultimate origin of these deposits is considered aeolian7,9,22. The Wisconsinian Goldstream mucks are poorly- to well-stratified, and the layers are conformable to the valley slopes and bottoms16,42. In the Silt unit of the Klondike district, planar bedding is the most common structure, as at Quartz Creek where a 17 m-thick section contains individual beds up to 5 cm thick. The silt can also be massive (≤3 m thick) with no apparent sedimentary structures9.
The sedimentary contrast of dispersed bone clasts (e.g., megafuanal skulls, tusks), isolated rock fragments ~2–10 cm in diameter16, and logs (Fig. 3b), within a silty matrix, however, is incompatible with a fluvial origin. A complete mammoth skull including tusks can weigh 100–150 kg or more, and a large male woolly mammoth tusk can weigh up to 80 kg44. Large volumes of water moving at high velocity would be needed to move such objects any distance, for which there is no water-related sedimentological evidence, indicating that the partial frozen carcasses have not been transported any distance by fluvial processes. Dense vegetal cover and low rainfall levels in Alaska have kept slopewash to a minimum7, and downslope movements of skeletal remains by creep and solifluction would be limited to the depth of seasonal thawing6,7, which is presently <1–2 m in the Fairbanks area5.
Partial frozen carcasses
One of the most remarkable and perplexing aspects of the mucks is their preservation of frozen animal carcasses or mummies. The vast majority of megafaunal mummies in Beringia were found as partial carcasses, and the most commonly found body parts in Alaska have been isolated limbs of horses, bison, moose, and caribou5. Even the most complete mummies show signs of significant internal damage: the Siberian Berezovka mammoth had a number of broken bones (e.g., pelvis, ribs, foreleg, shoulder blade) and evidence of significant internal bleeding5,45. Notably, the well-preserved tip of a Steppe Bison’s tail (~22 cm long) was found under the sole of the mammoth’s right forefoot45. The headless Selerikan pony (Siberian) also had broken humeri and ribs, and the Steppe bison “Blue Babe” (Alaskan) had missing and broken bones including a shattered right tibia and broken right mandible5.
The nearly undamaged baby mammoth “Lyuba” from Siberia, found in 2007, also had a broken mandible46, whereas the baby mammoth “Dima”, found in 1977, showed a small wound on its right wrist and hemorrhaging of its heart muscle5. In both Dima and Lyuba, fine-grained mineral particles were found within their trachea, bronchi, and/or lung alveoli5,46. Only hide from the head, neck, and trunk, along with the attached left front leg of an Alaskan baby mammoth, “Effie”, were found at Fairbanks Creek in 19485,8. Previously, in 1941, a leg from a different mammoth with bone, hide, and hair had been found near the Effie discovery site16. Full gastrointestinal tracts (e.g., Selerikan pony) and food material between their teeth (e.g., Berezovka mammoth) indicate that death for many of these mummies was “almost instantaneous”5. Furthermore, from their thick fat deposits and recovered gut contents, it appears that many of the animals died at roughly the same times of year during the late summer or autumn seasons5. Notably, megafaunal deaths were not concentrated during the lean months of winter when they would have been subject to harsher environmental conditions8.
The Goldstream Formation contains abundant layers, lenses, and clumps of plant material derived from grasses, mosses, alder, spruce, willow, cottonwood, and birch that match the present-day flora6,8. Pollen analyses indicate that trees during the Wisconsinan glaciation were scarce in the region and that the tree line was ~600 m lower, although forested areas likely prevailed at lower elevations within the creek bottoms8. Peaty layers are common in the Goldstream muck, ranging from <0.01 to >3 m in thickness7,8, and in many places contain tree stumps rooted in place with the trunks and treetops having been “broken off and carried away”7,16. Multiple forest layers (e.g., 6 horizons within a 6-m section6) are more common within the overlying Holocene Ready Bullion Formation8 (Fig. 2).
Severely splintered tree stumps and logs are often found in the Goldstream mucks, and the splintering has been attributed to freezing7, although many frozen stumps and logs, mostly lacking their bark, are well preserved8. Other buried wood includes sticks and branches ~2–13 cm in diameter (Fig. 3b)8,16. Some of the finely comminuted plant material found throughout most of the Goldstream muck is carbonized, with the total carbon content of this material being 2.39%16. Comminution of this plant material was thought to have resulted from a combination of forest fires, frost action, and downslope transport16.
The accelerator mass spectrometer (AMS) radiocarbon dates for the Beringian megafaunal skull fragments range between ~48 and 18 ka B.P. (Table S1) and are similar to those commonly determined for megafaunal bones and carcasses recovered from Alaskan and Yukon mucks20,25,47 and Siberian Yedoma deposits5,25,47. The youngest age (18,635 ± 65 yr B.P.) is for an AMNH bison skull with a shellacked exterior (Fig. 4a). The shellacked top of the core drilled from this skull was removed before processing, but contamination of the remaining bone sample remains a possibility. The mammoth skull had also been shellacked, but its dating sample was collected from bone structures within the skull (Fig. 5a).
Magnetic fractions extracted from aliquots of bulk sediment removed from each skull ranged in size from ~5–44 g/kg, averaging 23.6 g/kg (Table S1). Upon examining each fraction for microspherules, two fractions were found to contain only rounded detrital magnetite grains (Y-404.716, Y-109-8; Fig. S4), whereas the other seven contained numerous microspherules ranging in abundance from ~1000–18,000/kg, with an average of ~8000/kg. For comparison, concentrations of magnetic spherules (~10 μm–5.5 mm in diameter) from samples of the Younger Dryas boundary layer collected at 18 sites in the northern hemisphere range from 5–4900 spherules∕kg with an average of 940/kg30. Only one rounded quasi-spherical particle was found within the magnetic separate from primary loess sample AK-915. It was lost before it could be identified, but if similar to the other recovered microspherules it was present at a much lower abundance (~17/kg) by several orders of magnitude (Table S1).
Scanning electron microscopy (SEM) images (see Supplementary Information, “Analytical methods”) for some of the 49 muck microspherules selected in our study are shown in Figs 4–7, S1–S3. Their shapes and surface textures are similar to those of microspherules associated with the Chixulub impact at ~66 Ma48, the Chesapeake Bay impact at ~35 Ma49, the Meteor Crater impact at ~50 ka B.P., the Younger Dryas boundary layer at ~13 ka B.P., the Tunguska airburst in 1908, and the Trinity atomic airburst in 194530,50. In particular, microspherules from the mammoth skull (Fig. 5b,e,g–i) show accretionary features, which form within the impact plume when partially molten and still tacky projectiles collide at low differential velocities. At higher initial velocities destructive collisions often occur resulting in particles displaying microcraters (Fig. 5e) and/or brittle fracturing30.
Energy dispersive X-ray spectroscopy (EDS) analyses (see Supplementary Information, “Analytical methods”) of the 49 microspherules indicate two distinct chemical populations: those from the mammoth skull (Fig. 5) are predominately aluminosilicate (Al2O3 = 30.7 wt.%, SiO2 = 34.4 wt.%, FeO = 23.4 wt.%, CaO = 2.9 wt.%, with all other oxides being <2.3 wt.%), whereas those from the remaining six bison skulls (Figs 4, 6–7, S1–S3) are typically iron-rich (FeO = 87.4 wt.%, Al2O3 = 2.0 wt.%, SiO2 = 2.3 wt.%, CaO = 4.0 wt.%, with all other oxides being <1.1 wt.%). Various oxides of the 49 microspherules are plotted on ternary diagrams along with those for known populations of other types of spherules. In Fig. 8a, abundances of Mg, total Fe, and Al for the 49 microspherules are compared with >700 cosmic spherules (melted micrometeorites) and micrometeorite particles from 83 sites, mostly in Antarctica and Greenland. The cosmic material tends to be significantly more enriched in MgO and depleted in Al2O3 relative to the muck microspherules. In Fig. 8b, compositions of the 49 microspherules are compared to 267 fly-ash particles and anthropogenic spherules collected at 48 sites around the world that were produced primarily by coal-fired power plants30. In this case, the fly ash is enriched in Al2O3 and far more depleted in P2O5 relative to the muck microspherules. The potential for anthropogenic contamination, however, is extremely low because it is usually restricted to near-surface deposits of industrial age (<300 yr), whereas the Beringian fossils had remained deeply buried and frozen for thousands of years.
A comparison of the muck microspherules with >10,000 volcanic samples (glass, tephra, and spherules) from 205 sites of global extent is shown in Fig. 8c. Volcanic material tends to be enriched in silica (>40 wt.%) and depleted in Fe abundances compared to the 49 microspherules. Moreover, the sediment removed from the skull fragments lacked any typical indicators of volcanic activity such as volcanic ash and/or tephra. Finally, compositions of >1000 impact-related markers (spherules, ejecta, and tektites) from 12 craters and tektite-strewn fields30 were compared to compositions of the muck microspherules (Fig. 8d). In addition, compositions of typical metamorphic rocks (P, pelitic; Q, quartzofeldspathic; C, calcareous; and B, basic) are indicated on the ternary diagram. The 49 microspherules are most similar to pelitic rocks that are chemically equivalent to clayey mudstones and shales with several having more calcareous compositions. Biasing of the microspherules toward more Fe-rich compositions (A and F), however, was caused by their magnetic separation from the bulk sediments. In summary, approximately 75–90% of the muck microspherules are dissimilar to known cosmic, anthropogenic, and volcanic spherules and related materials, and are most similar to known impact-related spherules and classes of terrestrial sediments.
Average crustal abundances are 0.51 ppb for platinum (Pt) and 0.52 ppb for palladium (Pd), based on sediment and loess data51, and average values for our primary loess samples are 1.02 ppb for Pt and 1.67 ppb for Pd, with a lower detection limit of 0.1 ppb (Table S2). For muck samples from three of the four bison skulls analysed, Pt abundances are elevated and range from ~2–4 ppb; for skull Y-404-716, in which no microspherules were found (Table S1), the sediment’s Pt content (0.90 ppb) is similar to that of the primary loess (1.02 ppb). Pd values remain relatively constant between the muck and loess samples, averaging 1.31 ppb, and the Pt/Pd ratios are thus higher for the Pt-rich muck samples. High Pt/Pd ratios suggest an influx of impact-related, Pt-enriched material from an impactor and/or from Pt-rich target rocks, possibly included within the microspherules. As an example, Andronikov et al.52 found high Pt abundances (18–460 ppb) in four of six microspherules collected from the Younger Dryas Boundary layer at Blackwater Draw, NM.
The high-temperature, melt-quenched and accretionary microspherules, and Pt enrichments associated with sediments from the megafaunal fossils of this study (Figs 4–7, S1–S3), are well-established indicators of extraterrestrial impact events30,50,53. In light of this evidence, much of the death, dismemberment, burial, and preservation of megafaunal bones and partial carcasses within the frozen Beringian mucks is perhaps better explained by the catastrophic effects of cosmic impacts rather than by more commonplace causes of mortality such as illness, accident, advanced age and/or predation. In the following discussion, we reinterpret parts of the mucks and their contents as blast deposits and attempt to resolve the apparent paradoxes and inconsistencies outlined above. Examples to be applied come from studies of blast effects associated with the ~50 ka B.P. Meteor Crater impact33, 1908 Tunguska airburst54, ≥1945 nuclear tests55, and 1980 Mount St. Helens eruption56.
The blast or shock waves associated with ground impacts or airbursts cause an almost instantaneous rise in air pressure to peak overpressures as the wave fronts expand at supersonic velocities. The subsequent mass movement of air generates blast winds, which travel more slowly than the blast waves but can be just as damaging, if not more so33,57. In general terms, the area (A) damaged by an explosion is proportional to the cube root of its yield (E) squared33, or A ∝ E 2/3. The amount of damage is also a function of the explosion’s height, and for a given yield there is an optimum blast height at which the damage is maximized. For the 1908 Tunguska airburst, the blast height was ~6–9 km58, near the optimum height for a ~10–20 megaton (MT) blast, and trees of the Siberian taiga were knocked down33 over an area of ~2150 km2. Intense thermal radiation was also associated with the Tunguska event. Within a radius of ~10–15 km from the epicenter the sides of trees facing the atmospheric impact were scorched, and ignited treetops were reported to have burned in many places for up to 24 hr54.
Kring33 quantified the air blast for the Meteor Crater impact using scaling relationships derived from nuclear bomb tests. Given an estimated explosive yield of ~20–40 MT for the impact of an ~50-m-diameter iron asteroid59, the air blast would have flattened trees within a ~16–22 km radius of ground zero, and damaged them over an area of ~4100–8500 km2. Within a radius of ~3–5 km, the ephemeral blast wind (>1000 km/hr) would likely have “scoured the surface of loose debris, plants, animals, and soil”, and, although decreasing in intensity with distance, would have remained “fairly large” up to distances of ~20–40 km33. Both types of impact events would have killed megafauna from various levels of blast injuries.
Primary blast injuries are caused by the nearly instantaneous change in environmental pressure from passage of the blast wave. In large mammals, the organs most commonly affected are the lungs, ears, bowel, and central nervous and cardiovascular systems57. The blast wave can also fracture bones and cause dismemberment including traumatic amputations and decapitations. From the exposure of a wide range of animals to nuclear tests (e.g., steers, burros, sheep, goats, monkeys, pigs, dogs, cats, rabbits, chickens, rats, hamsters, and mice), it was determined that larger animals generally endure higher overpressures better than smaller ones, and that animals affected by primary blast injuries usually die within a few minutes55.
Secondary blast injuries are associated with the subsequent blast wind and result from projectiles that have been picked up and energized by it. Sufficiently large fragments can also cause direct limb amputations and decapitations. Tertiary blast injuries result when victims are hurled against the ground or fixed objects. Often, victims tumble along the ground sustaining multiple injuries. Miscellaneous blast injuries include inhalation of dust, and burns from the explosion itself or from fires ignited by it57.
A modern example of a catastrophic explosion causing death and dismemberment of large mammals was the 1980 eruption of Mount St. Helens. An equivalent explosive yield for the eruption is estimated to have been ~35 MT, and the “blast zone” of downed trees and destroyed habitat56 covered an area >350 km2. Animals within the blast zone died from suffocation, severe blast injuries, and falling timber and/or pumice blocks60. Of the 24 sites where remains of elk (Cervus elaphys) and black-tailed deer (Odocoileus hemionus) were found, 5 were examined ~1 year later by Lyman56. All 5 sites were located ~15 km away from the Mount St. Helens vent, and at this distance mature trees had been snapped off and splintered near their base and completely stripped of their branches. The volcanic crater could not be seen from two of the sites, where intervening ridges probably acted as deflectors, but the crater was visible at the other three sites where they would have been subjected to the full force of the blast56.
Portions of cervid skeletons were found buried under ~20–60 cm of volcanic ash and no soft tissue was preserved. Long bones at the sheltered sites were not broken, but those at the exposed sites were fractured, in some cases shattered, and were generally more disarticulated and widely scattered. Bone fracturing was nonselective as unbroken examples of all skeletal elements could be found. Apparently the elk and deer at the exposed sites were engulfed in the eruption’s ash cloud, hurled along with trees, rock fragments and pumice blocks, and deposited some distance away at their recovery locations. Carnivore damage to the bones was minimal because many of the bones were buried, and scavengers within the blast zone would have been killed as well56.
The blast injuries sustained by cervids at Mount St. Helens apparently match much of the damage exhibited by the vertebrate remains found within Beringian muck and Yedoma deposits. Broken and shattered bones, especially within the frozen mummies (e.g., Berezovka mammoth, Lyuba, Blue Babe), have been attributed to retransportation and diagenetic processes5,46. Pfizenmayer45, however, noted that bleeding had occurred at the break of the Berezovka mammoth’s right foreleg, and inferred it had still been alive at the time. The mammoth, therefore, was initially thought to have fallen into a “crevasse”45, but instead could have been thrown and/or tumbled across the ground by blast winds, come to rest in a surface depression or pit, and been covered over by blast-mobilized sediment. The segment of a bison’s tail found under the Berezovka mammoth’s foot could simply have been clipped off a nearby grazer by the blast and deposited along with the mammoth’s carcass. That a healthy bull mammoth was instantly killed while grazing, subjected to multiple broken bones and internal injuries, and rapidly buried along with a body part from another animal, is consistent with the effects of a large explosive event.
The smallest frozen mummies preserved in underground nests and burrows (e.g., ground squirrels, pikas, mice) could have been killed because of their higher susceptibility to blast overpressures. At the surface, baby mammoths (e.g., Dima, Lyuba), with smaller cross sections, would have sustained less blast damage than adults. The baby mammoth Effie, however, could have been blown apart in closer proximity to an explosive center. The disarticulated and scattered bones along with partial carcasses and the relatively abundant mummified limbs are likely indicative of the damaging effects of airbursts and/or ground impacts. The overall abundance of Beringian fossil bones, often including those of different species within a single bed, do not conform with normal modes and rates of attrition, but are in accord with the expected aftermaths of cosmic impact events.
The mixture of vertebrate remains, plant debris, and loess within the Beringian mucks is consistent with ground-surface scouring, transport, and the chaotic redeposition of these materials in creek valleys by blast winds (Fig. 3b). Trees exposed to such winds would have been stripped of their branches, leaves, and bark, and either knocked down or broken off and splintered, like those found in the muck deposits. The finely comminuted plant material distributed throughout the mucks might have resulted from pulverization of less durable plant debris (leaves, grasses, bark, etc.) within turbulent blast winds, and its carbonization could have been initially caused by scorching and/or burning from intense thermal radiation associated with atmospheric passage of hypervelocity impactors. Stacked layers of killed forests indicate that creek-valley silt accumulation was not gradual or uniform, but that it was deposited cyclically in large amounts over short intervals of time. In addition, less severely injured animals could have suffocated in the dense clouds of airborne silt (e.g., Dima, Lyuba).
The buried forest layers, range of radiocarbon dates, and microspherules associated with the vertebrate fossils indicate that deposition of the Alaskan and Yukon mucks would have required more than one impact event between ~48 and 18 ka B.P. (Fig. 9; Table S1). A possible mechanism for repetitive impacts on Earth is the cyclical intersection of its orbit with meteoroid streams containing numerous objects large enough (~10–100 m) to generate Tunguska-class airbursts and ground impacts. Since the late 1970s, a group of British astronomers34,61,62 has calculated that such a scenario likely affected Earth throughout Late Pleistocene time during formation of the Taurid Complex.
The massive Taurid Complex is known to consist of several dynamically related meteoroid streams, several Apollo-type asteroids, and Comet 2 P/Encke, which has a ~5-km diameter and orbital period of 3.3 yr61,63. These objects are most likely the remnant debris of a large comet (~50–100 km) from the trans-Neptunian region that was injected into a short-period, sub-Jovian, low-inclination Earth-crossing orbit63,64 by gravitational fields of the outer planets. Such injections of large comets into the inner solar system possibly occur at a mean rate of roughly once per 30 to 100 kyr64.
Spontaneous splitting is a major factor in comet disintegration and may occur anywhere along its orbit, with some preference for near-perihelion breakup, and would lead to hierarchical fragmentation of the progenitor comet into numerous ~1 km-sized bodies in short-period orbits, many smaller objects in the ~10–100 m range, and large quantities of dust34,64. Substreams of meteoroids having similar but separate orbits within the complex are evidence of this cascading mode of fragmentation, which would likely have occurred over a period of ~10–100 kyr63,64. Using the observed dispersion of material in the Taurid Complex, Steel and Asher62 have calculated an overall age of at least 20–30 kyr, similar to the older age limit of megafaunal fossils containing impact-related microspherules. The continued dispersal of Taurid material by collisions, and by gravitational and radiative effects, has created a broad sporadic stream surrounding the complex65.
Jupiter’s gravity would predominantly cause the Taurid-object orbits to precess, and dynamical calculations have shown that Earth would encounter these orbits at ~3000 yr intervals34,64. Over the ~30-kyr period spanned by the skull-fragment ages (Table S1), it is expected that one or more encounters might have individually generated the atmospheric impact of hundreds to thousands of Tunguska-sized objects on a hemispheric scale. Such bombardment episodes could have lasted for several hours and occurred at certain times of the year, every few years, over a period of one to two centuries34,64,65.
The Late Pleistocene megafaunal extinction events appear to have occurred over a time interval between ~46 and 24 ka B.P. prior to the LGM, and again over a shorter interval between ~15 and 11 ka B.P. near the end of the Pleistocene Epoch47,66. Recently, Cooper et al.25 investigated all megafaunal species, or major clades, with comprehensive radiocarbon-dated series, to determine the timings of regional or global extinctions, and invasions or replacements by conspecific or congeneric populations (Fig. 9). They determined 31 such events widely distributed across Eurasia and North America that involved animals having diverse ecological roles and life histories25. The lack of megafaunal extinction events during the LGM, and to a lesser extent the YD stadial, suggests that cold environmental conditions were not an important driver of the extinctions, and Cooper et al.25 found that the population transitions were instead significantly correlated with rapid climate shifts associated with the Dansgaard-Oeschger (D-O) interstadial warmings (Fig. 9). Because of the apparent lack of ecological turnovers related to similar interstadial events that frequently occurred before ~46 ka, when modern humans were mostly absent from Eurasia and North America, Cooper et al.25 concluded that humans likely played a significant role in enhancing the effects of rapid climate change on Late Pleistocene megafaunal extinctions and population transitions25.
The presence of two geochemically distinct microspherule populations found by us in Late Pleistocene skull fragments points to at least two episodes of cosmic impact, and/or different target source rocks, and the skull ages (~18–48 ka B.P.; Table S1; Fig. 9) indicate that perhaps a greater number of such episodes (~2–4) occurred. It is also unclear how many separate extinction events there were both before and after the LGM. Cooper et al.25 noted a distinct cluster of events between ~37 and 32 ka, corresponding to D-O interstadials 5–7, and the question arises whether these extinctions with overlapping ages could have resulted from a single short-lived event. By comparing our 14C dates with the extinction age ranges in Fig. 9, it appears plausible that there could have been fewer discrete impact-related extinction events prior to the LGM, possibly occurring around 40–42 ka, 34–37 ka, and 27–30 ka, with another at the onset of the YD stadial (~13 ka)26,27,28.
Modern humans have also been implicated in the Late Pleistocene megafaunal extinctions23,24,25, but the temporal correspondence between these events both in Eurasia and North America seems to argue against their involvement (Fig. 9). The megafaunal extinctions and population transitions during MIS3 occurred in North America before modern humans had arrived, and in Eurasia over an extended period well after their arrival, whereas the terminal Pleistocene extinctions (MIS1-2) appear roughly coincident with modern humans’ arrival in North America, but occurred in Europe long after they had become established there. It would appear that some mechanism other than intensive human hunting drove the extinctions in both locations over the same time intervals. Moreover, the lack of evidence for ecological disturbances associated with interstadial warmings prior to ~46 ka25 suggests that rapid climate change might also have played a more limited, if any, role in the Late Pleistocene megafaunal extinctions.
The range in degree of fossil preservation, from weathered bones to frozen mummies, likely indicates the depth and/or timing of burial. Mummified carcasses and body parts were probably rapidly buried and frozen at deeper levels, whereas well-preserved bones were buried close enough to the surface to allow decomposition of the attached soft tissues before freezing, while weathered bones were exposed at the surface before burial by subsequent depositional events. Fraser and Burns9, however, noted “the position of bones of various ages near the lower contact of the Silt unit suggests…redeposition by events of considerable magnitude”. With the lack of evidence in the mucks for fluvial transport, such redeposition might have been accomplished by one or more impact-generated blast winds. During a bombardment episode, blast winds could have excavated and mixed bones of various ages, including those from animals that had already died of more common causes. Thus, the extensive breakage and disarticulation of skeletal elements in the Alaskan and Yukon mucks could have resulted from a relatively few episodes of cosmic bombardment.
Our results suggest that large amounts of melt-quenched impact spherules, associated with Pleistocene megafaunal remains, were deposited in the mucks of eastern Beringia after ~48 kyr. The SEM/EDS and Pt/Pd data we acquired indicates they are not cosmic, anthropogenic, or volcanic in origin (Fig. 8), but were most likely produced by hypervelocity airbursts and ground/ice impacts. Based on this evidence, and the damaged and disrupted character of the muck’s vertebrate and botanical material documented by others6,7,8,9, we conclude that some parts of the Beringian muck and Yedoma deposits were catastrophically emplaced during the Late Pleistocene by blast winds associated with multiple episodes of cosmic impact.
Blast winds from the impacts would have swept across the Beringian landscape flattening trees and killing, dismembering, and burying megafaunal carcasses or body parts, along with logs, branches, other plant material, with a matrix of redeposited loess in low-lying creek valleys. Normal depositional processes such as slopewash, creep, and mudflow would have continued within the valleys during the thousands or more years between blast events. The lack of microspherules in the primary loess (Table S1) indicates that it was emplaced between impact episodes and those microspherules found within the mucks were added to the remobilized primary loess as it was retransported by blast winds along with comminuted organic material and the damaged and fragmented vertebrate and plant remains.
The radiocarbon dates determined for the skull fragments of this study are too few to support any robust correlation with the Late Pleistocene extinction events25. Further studies of fossils with well-established stratigraphic contexts are needed before the actual role of impacts in driving or contributing to the megafaunal extinctions can be inferred. Elevated Pt abundances53,67 and microspherules26,30,50,52 have also been associated with the YD-onset impact event26,27,28, and our results suggest that the terminal megafaunal extinctions were the culmination at ~13 ka B.P. of a relatively small number of subsidiary episodes that occurred prior to the LGM during MIS3 (Fig. 9). Chaotically deposited arboreal plant material and the presence of megafaunal carcasses within the Ready Bullion and coeval upper Organic mucks of Alaska and the Yukon Territory (Fig. 2), respectively, suggest that extraterrestrial impacts might have continued into the Holocene Epoch.
The skull fragments assembled for this study are from Pleistocene vertebrate fossil collections curated at the American Museum of Natural History (AMNH) in New York City (Figs 4–6) and at the Yukon Government offices in Whitehorse (Fig. 7, S1–S4). Although collection locations are known for most of the fossils, they lack any useful stratigraphic information. Although the Yukon fossils had been subjected to little or no sample preparation and cleaning, the surfaces of the AMNH fossils had been cleaned and shellacked. In both cases, however, the selected skulls still contained significant amounts of host sediment, or dried muck, within them, and the included sediment was collected to determine if it contained any markers of extraterrestrial impact30,50. The fine-grained sediment was shaken from each skull onto fresh pieces of 81/2 × 11-inch (21.6 × 27.9 cm) white copier paper, and then transferred to new plastic sample bags. Bone samples for radiocarbon dating (see Supplementary Information, “Analytical methods”) were taken from seven of the nine skulls using either a small handsaw or electric drill and hole-saw. Optimum samples for dating from two of the skulls (Table S1) were not obtained because they lacked enough thick, dense, and unweathered bone.
D. Muhs (USGS) collected samples of primary loess (Gold-Hill type), of equivalent and younger age to the mucks (Table S1), at the Halfway House, Chena Hot Springs Road, and Birch Hill sections near Fairbanks, Alaska. The geochronology of the Chena Hot Springs Road and Birch Hill sections is based on correlations with dated tephra and radiocarbon dates on wood, charcoal, or organic matter from soil horizons40,41. Ages were assigned to the samples from these sections due to their close proximity to dated sediment horizons or from interpolation between them. Ages for samples from the Halfway House section were similarly assigned based on stratigraphic relations with dated tephra and geomagnetic-field-excursion horizons, and with thermoluminescence-age determinations68,69.
Magnetic separates were extracted from bulk sediment slurries using a large neodymium (NdFeB) magnet (5.15 × 2.5 × 1.3 cm) wrapped in 4-mil plastic bags30,50. Each magnetic grain fraction was dried, weighed, and sorted into four size sub-fractions of >150 μm, between 53 μm and 150 μm, between 38 μm and 53 μm, and <38 μm using a stack of ASTM sieves. Aliquots of each grain-size fraction were then examined under reflected light using a 200x–300x zoom microscope to manually count and photograph the candidate microspherules (Fig. S5). Microspherules are defined as being <2 mm in diameter, and those of this study were usually found within the smaller two size fractions of the Alaskan and Yukon muck samples. Forty-nine candidate microspherules from the mucks were mounted on SEM stubs for further analysis.
Details of the SEM and EDS techniques, AMS radiocarbon dating, and platinum and palladium analytical methods are given in the Supplementary Information, “Analytical methods”. The datasets generated and analysed during the current study are available from the corresponding author on reasonable request.
Froese, D. G. et al. The Klondike goldfields and Pleistocene environments of Beringia. GSA Today 19, 4–10 (2009).
Hoffecker, J. F., Elias, S. A. & O’Rourke, D. H. Out of Beringia? Science 343, 979–980 (2014).
Zazula, G. D. et al. Late Pleistocene steppe macrofossils in east Beringia. Nature 423, 603 (2003).
Goetcheus, V. G. & Birks, H. H. Full-glacial upland tundra vegetation preserved under tephra in the Beringia National Park, Seward Peninsula, Alaska. Quat. Sci. Rev. 20, 135–147 (2001).
Guthrie, R. D. Frozen fauna of the mammoth steppe: The story of Blue Babe (University of Chicago Press, 1990).
Tuck, R. Origin of the muck-silt deposits at Fairbanks, Alaska. Geol. Soc. Am. Bull. 51, 1295–1310 (1940).
Taber, S. Perennially frozen ground in Alaska: Its origin and history. Geol. Soc. Am. Bull. 54, 1433–1548 (1943).
Péwé, T. L. Quaternary Geology of Alaska. U.S. Geol. Surv. Prof. Pap. 835 (1975).
Fraser, T. A. & Burn, C. R. On the nature and origin of “muck” deposits in the Klondike area, Yukon Territory. Can. J. Earth Sci. 34, 1333–1344 (1997).
Shapiro, B. & Cooper, A. Beringia as an Ice Age genetic museum. Quat. Res. 60, 94–100 (2003).
Haile, J. et al. Ancient DNA reveals late survival of mammoth and horse in interior Alaska. PNAS 106, 22,352–22,357 (2009).
Maddren, A. G. Smithsonian exploration in Alaska in 1904, in search of mammoth and other fossil remains. Smithsonian Misc. Coll. 49 (1905).
Gilmore, C. W. Smithsonian exploration in Alaska in 1907 in search of Pleistocene fossil vertebrates. Smithsonian Misc. Coll. 51, 1–38 (1908).
Quackenbush, L. S. Notes on Alaskan mammoth expedition of 1907 and 1908. Am. Mus. Nat. Hist. Bull. 26, 87–130 (1909).
Dawson, G. M. Notes on the occurrence of mammoth remains in the Yukon district of Canada and in Alaska. Quart. J. Geol. Soc. London 50, 1–9 (1894).
Péwé, T. L. Geomorphology of the Fairbanks area, Alaska. Ph.D. thesis (Stanford University, 1952).
Frick, C. Alaska’s frozen fauna. Nat. Hist. 30, 71–80 (1930).
Guthrie, R. D. Paleoecology of the large-mammal community in interior Alaska during the Late Pleistocene. Am. Midland Nat. 79, 346–363 (1968).
Harington, C. R. Annotated bibliography of Quaternary vertebrates of northern North America—with radiocarbon dates (University of Toronto Press, 2003).
Guthrie, R. D. New carbon dates link climatic change with human colonization and Pleistocene extinctions. Nature 441, 207–209 (2006).
Kotler, E. & Burn, C. R. Cryostratigraphy of the Klondike “muck” deposits, west-central Yukon Territory. Can. J. Earth Sci. 37, 849–861 (2000).
Péwé, T. L., Westgate, J. A., Preece, S. J., Brown, P. M. & Leavitt, S. W. Late Pleistocene Dawson Cut Forest Bed and new tephrochronological findings in the Gold Hill Loess, east-central Alaska. Geol. Soc. Am. Bull. 121, 294–320 (2009).
Haynes, B. & Eiselt, B. S. The power of Pleistocene hunter-gatherers: Forward and backward searching for evidence about mammoth extinction in Extinctions in near time: Causes, contexts, and consequences (ed. MacPhee, R. D. E.) 71–93 (Kluwer Academic/Plenum Publishers, 1999).
Martin, P. S. Twilight of the mammoths: Ice age extinctions and the rewilding of America (University of California Press, 2005).
Cooper, A. et al. Abrupt warming events drove Late Plestocene Holarctic megafaunal turnover. Science 349, 602–606 (2015).
Firestone, R. B. et al. Evidence for an extraterrestrial impact 12,900 years ago that contributed to the megafaunal extinctions and the Younger Dryas cooling. PNAS 104, 16,016–16,021 (2007).
Kennett, D. J. et al. Shock-synthesized hexagonal diamonds in Younger Dryas boundary sediments. PNAS 106, 12,623–12,628 (2009).
Melott, A. L., Thomas, B. C., Dreschhoff, G. & Johnson, C. K. Cometary airbursts and atmospheric chemistry: Tunguska and a candidate Younger Dryas event. Geology 38, 355–358 (2010).
Surovell, T. A. et al. An independent evaluation of the Younger Dryas extraterrestrial impact hypothesis. PNAS 106, 18,155–18,158 (2009).
Bunch, T. E. et al. Very high-temperature impact melt products as evidence for cosmic airbursts and impacts 12,900 years ago. PNAS 109, E1903–E1912 (2012).
Farrand, W. R. Frozen mammoths and modern geology. Science 133, 729–735 (1961).
Keim, C. J. Aghvook, white eskimo: Otto Geist and Alaskan archaeology (University of Alaska Press, 1969).
Kring, D. A. Air blast produced by the Meteor Crater impact event and a reconstruction of the affected environment. Meteor. & Planet. Sci. 32, 517–530 (1997).
Asher, D. J., Clube, S. V. M., Napier, W. M. & Steel, D. I. Coherent catastrophism. Vist. Astron. 38, 1–27 (1994).
Froese, D. G., Westgate, J. A., Reyes, A. V., Enkin, R. J. & Preece, S. J. Ancient permafrost and a future warmer arctic. Science 321, 1648 (2008).
Sanborn, P. T., Smith, C. A. S., Froese, D. G., Zazula, G. D. & Westgate, J. A. Full-glacial paleosols in perennially frozen loess sequences, Klondike goldfields, Yukon Territory, Canada. Quat. Res. 66, 147–157 (2006).
Wilkerson, A. S. Some frozen deposits in the goldfields of interior Alaska: A study of the Pleistocene deposits of Alaska. Am. Mus. Novit. 525, 1–22 (1932).
Péwé, T. L. Origin of the upland silt near Fairbanks, Alaska. Geol. Soc. Am. Bull. 66, 699–724 (1955).
Péwé, T. L. An observation on wind-blown silt. J. Geology 59, 399–401 (1951).
Muhs, D. R. et al. Stratigraphy and palaeoclimatic significance of late Quaternary loess-palaeosol sequences of the Last Interglacial–Glacial cycle in central Alaska. Quat. Sci. Rev. 22, 1947–1986 (2003).
Muhs, D. R. et al. Paleoclimatic significance of chemical weathering in loess-derived paleosols of subarctic central Alaska. Arct., Antarc., Alp. Res. 40, 396–411 (2008).
Péwé, T. L. Quaternary Stratigraphic Nomenclature in Central Alaska. U.S. Geol. Surv. Prof. Pap. 862 (1975).
Westgate, J. A., Stemper, B. A. & Péwé, T. L. A 3 m.y. record of Pliocene-Pleistocene loess in interior Alaska. Geology 18, 858–861 (1990).
MacPhee, R. D. E. et al. Chronologies and extinction dynamics of the Late Quaternary mammalian megafauna of the Taimyr Peninsula, Russian Federation. J. Archaeol. Sci. 29, 1017–1042 (2002).
Pfizenmayer, E. W. Siberian Man and Mammoth (Blackie and Son, Ltd., 1939).
Fisher, D. C. et al. Anatomy, death, and preservation of a woolly mammoth (Mammuthus primigenius) calf, Yamal Peninsula, northwest Siberia. Quat. Int. 255, 94–105 (2012).
Harington, C. R. Late Pleistocene mummified mammals. Encycl. Quat. Sci. 3197–3202 (Elsevier, 2007).
Mathur, S. C., Gaur, S. D., Loyal, R. S., Tripathi, A. & Sisodia, M. S. Spherules from the Late Cretaceous phosphorite of the Fatehgarh Formation, Barmer Basin, India. Gondwana Res. 8, 579–584 (2005).
Glass, B. P., Huber, H. & Koeberl, C. Geochemistry of Cenozoic microtektites and clinopyroxene-bearing spherules. Geochim. Cosmochim. Acta 69, 3971–4006 (2004).
Wittke, J. H. et al. Evidence for deposition of 10 million tonnes of impact spherules across four continents 12,800 y ago. PNAS 110, E2088–E2097 (2013).
Rudnick, R. I. & Gao, S. Composition of the continental crust in The Crust (eds Holland, H. D. & Turekian, K. K.) 1–64 (Gulf Professional Publishing, 2005).
Andronikov, A. V. et al. Implications from chemical, structural and mineralogical studies of magnetic microspherules from around the lower Younger Dryas boundary (New Mexico, USA). Geografiska Annaler, Series A, Phys. Geog. 98, 1–21 (2016).
Moore, C. R. et al. Widespread platinum anomaly documented at the Younger Dryas onset in North American sedimentary sequences. Sci. Reports 7, https://doi.org/10.1038/srep44031 (2017).
Rubtsov, V. The Tunguska Mystery (Springer, 2009).
White, C. S., Jones, R. K., Damon, E. G., Fletcher, E. R., & Richmond, D. R. The Biodynamics of Air Blast, DNA 2738T (Defense Nuclear Agency, 1971).
Lyman, R. L. Broken bones, bone expediency tools, and bone pseudotools: Lessons from the blast zone around Mount St. Helens, Washington. Am. Antiq. 49, 315–333 (1989).
Covey, D. C. Blast and fragment injuries of the musculoskeletal system. J. Bone Joint Surg. 84, 1221–1234 (2002).
Turco, R. P. et al. An analysis of the physical, chemical, optical, and historical impacts of the 1908 Tunguska meteor fall. Icarus 50, 1–52 (1982).
Roddy, D. J. & Shoemaker, E. M. Meteor Crater (Barringer Meteorite Crater), Arizona: Summary of impact conditions. Meteoritics 30, 567 (1995).
Anderson, D. C. Observations on Thomomys talpoides in the region affected by the eruption of Mount St. Helens. J. Mamm. 63, 652–655 (1982).
Clube, S. V. M. & Napier, W. M. The microstructure of terrestrial catastrophism. Mon. Not. R. Astron. Soc. 211, 953–968 (1984).
Steel, D. I. & Asher, D. J. The orbital dispersion of the macroscopic Taurid objects. Mon. Not. R. Astron. Soc. 280, 806–822 (1996).
Napier, W. M. Palaeolithic extinctions and the Taurid Complex. Mon. Not. R. Astron. Soc. 405, 1901–1906 (2010).
Napier, B., Asher, D., Bailey, M. & Steel, D. Centaurs as a hazard to civilization. Astron. & Geophys. 56, 6–24 (2015).
Napier, B. & Asher, D. The Tunguska impact event and beyond. Astron. & Geophys. 50, 1–18 (2009).
Sutcliffe, A. J. On the Track of Ice Age Mammals (Harvard University Press, 1985).
Petaev, M. I., Huang, S., Jacobsen, S. B. & Zindler, A. Large Pt anomaly in the Greenland ice core points to a cataclysm at the onset of Younger Dryas. PNAS 110, 12917–12920 (2013).
Oches, E. A., Banerjee, S. K., Solheid, P. A. & Frechen, M. High-resolution proxies of climate variability in the Alaskan loess record in Dust Aerosols, Loess Soils and Global Change (ed. Busacca, A. J. et al.) 167–170 (Washington State University Miscellaneous Publication No. MISC0190, 1998).
Jensen, B. J. L., Evans, M. E., Froese, D. G. & Kravchinsky, V. A. 150,000 years of loess accumulation in central Alaska. Quat. Sci. Rev. 135, 1–23 (2016).
Ehlers, J. & Givvard, P. L. Quaternary glaciations—Extent and chronology, Part II: North America (Elsevier, 2004).
Rahmstorf, S. O. et al. A new Greenland ice core chronology for the last glacial termination. J. Geophys. Res. 111, D06102 (2006).
Svensson, A. et al. A 60,000 year Greenland stratigraphic ice core chonology. Clim. Past 4, 47–57 (2008).
Dansgaaard, W. et al. Evidence for general instability of past climate from a 250-kyr ice-core record. Nature 364, 218–2204 (1993).
Broecker, W., Bond, G., Klas, M., Clark, E. & McManus, J. Origin of the northern Atlantic’s Heinrich events. Clim. Dyn. 6, 265–273 (1992).
For their invaluable assistance we thank Grant Zazula at the Yukon Government Heritage Resources Department in Whitehorse, Ruth O’Leary and Judy Galkin at the American Museum of Natural History in New York, and Diane Tyink at the University of New Mexico, Maxwell Museum of Anthropology’s Photo Archives in Albuquerque. We are grateful to Dan Muhs (USGS) for providing the primary loess samples, and to Jennifer Parlier and David Kimbel for making many of the magnetic separates. Patrick Muffler, Carl Wentworth, Mike Clynne, Summer Praetorius (USGS), Bill Napier (U. Buckingham), Jim Kennett (UCSB), and an anonymous reviewer provided constructive reviews that significantly improved earlier versions of the manuscript. The ideas and conclusions presented in this paper are those of the authors alone, and any use of trade, firm, or product names is for descriptive purposes only and does not imply endorsement by the U.S. Government.
The authors declare that they have no competing interests.
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Hagstrum, J.T., Firestone, R.B., West, A. et al. Impact-related microspherules in Late Pleistocene Alaskan and Yukon “muck” deposits signify recurrent episodes of catastrophic emplacement. Sci Rep 7, 16620 (2017). https://doi.org/10.1038/s41598-017-16958-2