Burgess Shale

Burgess Shale
Stratigraphic range: Cambrian Series 3 – ~508 Ma

Ottoia, a soft-bodied worm, abundant in the Burgess Shale. (From Smith et al. 2015)
Type Geological formation
Unit of Stephen Formation
Thickness 161 meters (528 ft)[1]
Primary Shale
Coordinates 51°26′N 116°28′W / 51.433°N 116.467°W / 51.433; -116.467
Region Yoho National Park and Kootenay National Park
Country Canada
Type section
Named for Burgess Pass
Named by Charles Doolittle Walcott, 1911

Map highlighting Yoho National Park in red

The Burgess Shale Formation is a fossil-bearing deposit exposed in the Canadian Rockies of British Columbia, Canada.[2] It is famous for the exceptional preservation of the soft parts of its fossils. At 508 million years (Middle Cambrian) old,[3] it is one of the earliest fossil beds containing soft-part imprints.

The rock unit is a black shale and crops out at a number of localities near the town of Field in Yoho National Park and the Kicking Horse Pass. Another outcrop is in Kootenay National Park 42 km to the south.

History and significance

The first complete Anomalocaris fossil found.

The Burgess Shale was discovered by palaeontologist Charles Walcott on 30 August 1909,[4] towards the end of the season's fieldwork.[5] He returned in 1910 with his sons, daughter, and wife, establishing a quarry on the flanks of Fossil Ridge. The significance of soft-bodied preservation, and the range of organisms he recognised as new to science, led him to return to the quarry almost every year until 1924. At that point, aged 74, he had amassed over 65,000 specimens. Describing the fossils was a vast task, pursued by Walcott until his death in 1927.[5] Walcott, led by scientific opinion at the time, attempted to categorise all fossils into living taxa, and as a result, the fossils were regarded as little more than curiosities at the time. It was not until 1962 that a first-hand reinvestigation of the fossils was attempted, by Alberto Simonetta. This led scientists to recognise that Walcott had barely scratched the surface of information available in the Burgess Shale, and also made it clear that the organisms did not fit comfortably into modern groups.

Excavations were resumed at the Walcott Quarry by the Geological Survey of Canada under the persuasion of trilobite expert Harry Blackmore Whittington, and a new quarry, the Raymond, was established about 20 metres higher up Fossil Ridge.[5] Whittington, with the help of research students Derek Briggs and Simon Conway Morris of the University of Cambridge, began a thorough reassessment of the Burgess Shale, and revealed that the fauna represented were much more diverse and unusual than Walcott had recognized.[5] Indeed, many of the animals present had bizarre anatomical features and only the slightest resemblance to other known animals. Examples include Opabinia, with five eyes and a snout like a vacuum cleaner hose and Hallucigenia, which was originally reconstructed upside down, walking on bilaterally symmetrical spines.

With Parks Canada and UNESCO recognising the significance of the Burgess Shale, collecting fossils became politically more difficult from the mid-1970s. Collections continued to be made by the Royal Ontario Museum. The curator of invertebrate palaeontology, Desmond Collins, identified a number of additional outcrops, stratigraphically both higher and lower than the original Walcott quarry.[5] These localities continue to yield new organisms faster than they can be studied.

Stephen Jay Gould's book Wonderful Life, published in 1989, brought the Burgess Shale fossils to the public's attention. Gould suggests that the extraordinary diversity of the fossils indicates that life forms at the time were much more disparate in body form than those that survive today, and that many of the unique lineages were evolutionary experiments that became extinct. Gould's interpretation of the diversity of Cambrian fauna relied heavily on Simon Conway Morris' reinterpretation of Charles Walcott's original publications. However, Conway Morris strongly disagreed with Gould's conclusions, arguing that almost all the Cambrian fauna could be classified into modern day phyla.[6]

The Burgess Shale has attracted the interest of paleoclimatologists who want to study and predict long-term future changes in Earth's climate. According to Peter Ward and Donald Brownlee in the 2003 book The Life and Death of Planet Earth,[7] climatologists study the fossil records in the Burgess Shale to understand the climate of the Cambrian Explosion, and use it to predict what Earth's climate in the future when a warming and expanding Sun combined with declining CO2 and oxygen levels eventually heat the Earth toward temperatures not seen since the Archean Eon 3 billion years ago, before the first plants and animals appeared, and therefore understand how and when the last living things will die out. See also Future of the Earth.

After the Burgess Shale site was registered as a World Heritage Site in 1980, it was included in the Canadian Rocky Mountain Parks WHS designation in 1984.

In February 2014, the discovery was announced of another Burgess Shale outcrop in Kootenay National Park to the south. In just 15 days of field collecting in 2013, 50 animal species were unearthed at the new site.:[8])

Geological setting

Main article: Stephen Formation
Satellite image of the area.

The fossil-bearing deposits of the Burgess Shale correlate to the Stephen formation, a collection of slightly calcareous dark mudstones, about 508 million years old.[5] The beds were deposited at the base of a cliff about 160 m tall,[5] below the depth agitated by waves during storms.[9] This vertical cliff was composed of the calcareous reefs of the Cathedral Formation, which probably formed shortly before the deposition of the Burgess Shale.[5] The precise formation mechanism is not known for certain, but the most widely accepted hypothesis suggests that the edge of the Cathedral Formation reef became detached from the rest of the reef, slumping and being transported some distance — perhaps kilometers — away from the reef edge.[5] Later reactivation of faults at the base of the formation led to its disintegration from about 509 million years ago.[10] This would have left a steep cliff, the bottom of which would be protected from tectonic decompression because the limestone of the Cathedral Formation is difficult to compress. This protection explains why fossils preserved further from the Cathedral Formation are impossible to work with — tectonic squeezing of the beds has produced a vertical cleavage that fractures the rocks, so they split perpendicular to the fossils.[5] The Walcott quarry produced such spectacular fossils because it was so close to the Stephen Formation — indeed the quarry has now been excavated to the very edge of the Cambrian cliff.[5]

It was originally thought that the Burgess Shale was deposited in anoxic conditions, but mounting research shows that oxygen was continually present in the sediment.[11] The anoxic setting had been thought to not only protect the newly dead organisms from decay, but it also created chemical conditions allowing the preservation of the soft parts of the organisms. Further, it reduced the abundance of burrowing organisms — burrows and trackways are found in beds containing soft-bodied organisms, but they are rare and generally of limited vertical extent.[5] Brine seeps are an alternative hypothesis; see Burgess Shale type preservation for a more thorough discussion.


Walcott Quarry of the Burgess Shale showing the Walcott Quarry Shale Member. The white parallel vertical streaks are remnants of drill holes made during excavations in mid-1990s.

The Burgess Shale Formation comprises 10 members, the most famous being the Walcott Quarry Shale Member comprising the greater phyllopod bed.[9]

Taphonomy and diagenesis

Please expand this section[12][13][14][15][16][17]

Further information: Burgess Shale type preservation

There are many other comparable Cambrian lagerstätten; indeed such assemblages are far more common in the Cambrian than in any other period. This is mainly due to the limited extent of burrowing activity; as such bioturbation became more prevalent throughout the Cambrian, environments capable of preserving organisms' soft parts became much rarer.[5] (The pre-Cambrian fossil record of animals is sparse and ambiguous.)


The biota of the Burgess Shale appears to be typical of Middle Cambrian deposits.[5] Although the hard-part bearing organisms make up as little as 14% of the community,[5] these same organisms are found in similar proportions in other Cambrian localities. This means that there is no reason to assume that the organisms without hard parts are exceptional in any way; indeed, many appear in other lagerstätten of different age and locations.[5]

The biota consists of a range of organisms. Free-swimming (nectonic) organisms are relatively rare, with the majority of organisms being bottom dwelling (benthic) — either moving about (vagrant) or permanently attached to the sea floor (sessile).[5] About two-thirds of the Burgess Shale organisms lived by feeding on the organic content in the muddy sea floor, while almost a third filtered out fine particles from the water column. Under 10% of organisms were predators or scavengers, although since these organisms were larger, the biomass was split equally among each of the filter feeding, deposit feeding, predatory and scavenging organisms.[5]

Many Burgess Shale organisms represent stem-group members of the modern animal phyla, though crown-group representatives of certain phyla are also present.[18]

Working with the Burgess Shale

The fossils of the Burgess Shale are preserved as black carbon films on black shales, and so are difficult to photograph; however, various photographic techniques can improve the quality of the images that can be acquired.[19] Other techniques include backscatter SEM, elemental mapping and camera lucida drawing.

Once images have been acquired, the effects of decay and taphonomy must be accounted for before a correct anatomical reconstruction can be made. A consideration of the combination of characters allows researchers to establish the taxonomic affinity.

See also


  1. Lexicon of Canadian Geological Units. "Burgess Shale". Retrieved 2009-02-06.
  2. Gabbott, Sarah E. (2001). "Exceptional Preservation". Encyclopedia of Life Sciences. doi:10.1038/npg.els.0001622. ISBN 0-470-01590-X.
  3. Butterfield, N.J. (2006). "Hooking some stem-group" worms": fossil lophotrochozoans in the Burgess Shale". BioEssays. 28 (12): 1161–6. doi:10.1002/bies.20507. PMID 17120226.
  4. "Charles Walcott". Royal Ontario Museum. Retrieved 29 August 2013.
  5. 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 Briggs, D.E.G.; Erwin, D.H.; Collier, F.J. (1995), Fossils of the Burgess Shale, Washington: Smithsonian Inst Press, ISBN 1-56098-659-X, OCLC 231793738
  6. Simon Conway Morris (1998). The Crucible of Creation: The Burgess Shale and the Rise of Animals. Oxford University Press. p. 316. ISBN 0-19-286202-2.
  7. Ward, Peter Douglas; Brownlee, Donald (2003), The life and death of planet Earth: how the new science of astrobiology charts the ultimate fate of our world, Macmillan, ISBN 0-8050-7512-7
  8. "'Epic' new fossil site found in B.C. national park". Canoe.ca. Quebecor Media. 11 February 2014. Retrieved 11 February 2014.
  9. 1 2 Gabbott, S.E.; Zalasiewicz, J.; Collins, D. (2008). "Sedimentation of the Phyllopod bed within the Cambrian Burgess Shale Formation of British Columbia". Journal of the Geological Society. 165 (1): 307–318. doi:10.1144/0016-76492007-023.
  10. Collom, C. J.; Johnston, P. A.; Powell, W. G. (2009). "Reinterpretation of 'Middle' Cambrian stratigraphy of the rifted western Laurentian margin: Burgess Shale Formation and contiguous units (Sauk II Megasequence); Rocky Mountains, Canada". Palaeogeography Palaeoclimatology Palaeoecology. 277: 63–85. doi:10.1016/j.palaeo.2009.02.012.
  11. Powell, W. (2009). "Comparison of Geochemical and Distinctive Mineralogical Features Associated with the Kinzers and Burgess Shale Formations and their Associated Units". Palaeogeography Palaeoclimatology Palaeoecology. 277 (1–2): 127–140. doi:10.1016/j.palaeo.2009.02.016.
  12. Butterfield, N.J. (1990). "Organic Preservation of Non-Mineralizing Organisms and the Taphonomy of the Burgess Shale". Paleobiology. Paleontological Society. 16 (3): 272–286. JSTOR 2400788.
  13. Page, Alex; Gabbott, Sarah; Wilby, Phillip R.; Zalasiewicz, Jan A (2008). "Ubiquitous Burgess Shale–style "clay templates" in low-grade metamorphic mudrocks". Geology. Geological Society of America. 36 (11): 855–858. Bibcode:2008Geo....36..855P. doi:10.1130/G24991A.1.
  14. Orr, Patrick J.; Briggs, Derek E. G.; Kearns, Stuart L. (1998). "Cambrian Burgess Shale Animals Replicated in Clay Minerals". Science. AAAS. 281 (5380): 1173–5. Bibcode:1998Sci...281.1173O. doi:10.1126/science.281.5380.1173. PMID 9712577. Retrieved 2008-06-22.
  15. CARON, JEAN-BERNARD; JACKSON, DONALD A. (2006). "Taphonomy Of The Greater Phyllopod Bed Community, Burgess Shale". PALAIOS. Society for Sedimentary Geology. 21 (5): 451–465. doi:10.2110/palo.2003.P05-070R.
  16. Gaines, R.R.; Kennedy, M.J.; Droser, M.L. (2005). "A new hypothesis for organic preservation of Burgess Shale taxa in the middle Cambrian Wheeler Formation, House Range, Utah". Palaeogeography, Palaeoclimatology, Palaeoecology. Elsevier. 220 (1–2): 193–205. doi:10.1016/j.palaeo.2004.07.034. Retrieved 2008-06-22.
  17. Butterfield, N.J.; Balthasar, U.; Wilson, L.A. (2007). "Fossil Diagenesis In The Burgess Shale". Palaeontology. 50 (3): 537–543. doi:10.1111/j.1475-4983.2007.00656.x.
  18. e.g. Smith, Martin R.; Caron, Jean-Bernard (2015). "Hallucigenia's head and the pharyngeal armature of early ecdysozoans". Nature. 523 (7558): 75–8. doi:10.1038/nature14573. PMID 26106857.
  19. Bengtson, Stefan (2000). "Teasing Fossils out of Shales with Cameras and Computers" (PDF). Palaeontologia Electronica. 3 (1). Retrieved 3 December 2010.

Further reading

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