- Cambrian Period
Oldest time division of the Paleozoic Era.During the Cambrian, 543–490 million years ago, there were widespread seas and several scattered landmasses. The largest continent was Gondwana. The average climate was probably warmer than today, with less variation between regions. There were no land plants or animals, but there were marine organisms with either shells or skeletons. Because the dominant animals were trilobites, the Cambrian is sometimes referred to as the Age of Trilobites.
* * *Introductionearliest time division of the Paleozoic Era, extending from about 542 to 488.3 million years ago. The Cambrian Period is divided into four stratigraphic series: Series 1 (542 to 521 million years ago), Series 2 (521 to 510 million years ago), Series 3 (510 to 501 million years ago), and the Furongian Series (501 to 488.3 million years ago).Rocks formed or deposited during this time are assigned to the Cambrian System, which was named in 1835 by English geologist Adam Sedgwick (Sedgwick, Adam) for successions of slaty rocks in southern Wales and southwestern England. These rocks contain the earliest record of abundant and varied life-forms. The corresponding period and system names are derived from Cambria, the Roman name for Wales. As originally described, the Cambrian System was overlain by the Silurian (Silurian Period) System, which was named, also in 1835, by Scottish geologist Roderick I. Murchison (Murchison, Sir Roderick Impey). Subsequent disagreement between Sedgwick and Murchison over the definition and placement of the Cambrian-Silurian boundary led to a bitter controversy that involved many British geologists. The problem persisted until after the deaths of both Sedgwick and Murchison in the 1870s and the eventual adoption of an intervening system, the Ordovician (Ordovician Period), which was proposed in 1879 by English geologist Charles Lapworth (Lapworth, Charles).The Cambrian world differed greatly from that of the present, but it was also quite different from the preceding Proterozoic Eon (2.5 billion to 542 million years ago) in terms of climate, geography, and life. Average global temperatures during much of the Neoproterozoic Era (1 billion to 542 million years ago) were cooler (around 12 °C [54 °F]) than the average global temperatures (around 14 °C [57 °F]) of the present day, whereas the global temperature of Cambrian times averaged 22 °C (72 °F). Low temperatures during the Neoproterozoic helped to sustain a series of worldwide events known as the Sturtian (748 to 713 million years ago), Marinoan (650 to 600 million years ago), and Gaskiers (595 to 565 million years ago) glaciations. Climate studies suggest that Cambrian temperatures were the norm for most of the Phanerozoic Eon (the last 542 million years), and these were exceeded only by a brief increase during the Permian Period near the end of the Paleozoic Era. Cooler periods, similar to the average global temperature of the present day, occurred during the end of the Ordovician, Late Carboniferous (Carboniferous Period), Early Permian, Late Jurassic (Jurassic Period), and Early Cretaceous periods (Cretaceous Period), as well as near the end of the Oligocene Epoch.Just prior to the beginning of the Neoproterozoic, Earth experienced a period of continental suturing that organized all of the major landmasses into the huge supercontinent of Rodinia. Rodinia was fully assembled by one billion years ago and rivaled Pangea (a supercontinent that formed later during the Phanerozoic Eon) in size. Before the beginning of the Cambrian, Rodinia split in half, resulting in the creation of the Pacific Ocean west of what would become North America. By the middle and later parts of the Cambrian, continued rifting had sent the paleocontinents of Laurentia (made up of present-day North America and Greenland), Baltica (made up of present-day western Europe and Scandinavia), and Siberia on their separate ways. In addition, new collisional events led to the formation of Gondwana, a supercontinent composed of what would become Australia, Antarctica, India, Africa, and South America.The tectonic events involved in the breakup of Rodinia also modified the ocean basins, forcing their expansion and flooding portions of many continents. The melting of the Varanger glaciers during the Neoproterozoic also played a role in the flooding of continents. This episode represented one of the largest and most persistent rises in sea level of the Phanerozoic Eon. Though the extent of continental flooding varied, for most continents sea level reached its maximum by the middle and later parts of the Cambrian. This flooding, combined with the elevated Cambrian temperatures and changes in Earth's geography, led to increased rates of erosion that altered ocean chemistry. The most notable result was an increase in the oxygen content of seawater, which helped set the stage for the rise and later diversification of life—an event that has come to be known as the “Cambrian explosion.”The Cambrian environmentThe geography of the Cambrian world differed greatly from that of the present day. The geographic reconstruction is based on integrated geologic and biological evidence. Fossils in continental-shelf deposits indicate the presence of at least three major faunal (faunal region) provinces (or biogeographical regions) during much of the Cambrian Period.The most distinct faunal province surrounded the continent of Laurentia. Paleomagnetic evidence indicates that Laurentia was located over the paleoequator during most or all of Cambrian time. This geographic interpretation is supported by the presence of thick, warm-water carbonate-platform deposits that accumulated in a broad belt encircling the continent. These carbonates (carbonate rock) are commonly flanked on the inner shelf by lagoonal shale and nearshore sandstone deposits. On the outer shelf, the carbonates commonly grade into laminated mudstone and shale that accumulated in deeper water. At times, two almost mutually exclusive ecosystems are separated by temperature and salinity barriers in the shallow water on the carbonate platforms. Inner restricted-shelf deposits were characterized by sparse low-diversity communities that tended to be highly endemic (confined to a particular region). Outer open-shelf deposits are characterized by high-diversity ecosystems that were widely distributed around the continent. Fossils are usually most abundant and most diverse near the outer margins of the carbonate platform. Because Laurentia remained nearly intact structurally, it is ideal for studying the relationships between Cambrian environments and communities of organisms around a low-latitude Cambrian continent.Another Cambrian faunal province surrounded the small continent of Baltica, which was located in middle to high southern latitudes. Cambrian shelf deposits of Baltica are relatively thin, rarely exceeding 250 metres (820 feet) in thickness, and are composed primarily of sandstone and shale. Seemingly as a consequence of cool-water environments, carbonate deposits are relatively minor and very thin. The wide distribution of many species from the nearshore to deep-shelf environments of Baltica suggests that no significant restrictions in shelf dispersal occurred, unlike the shallow carbonate platforms of Laurentia.The largest Cambrian faunal province is located around Gondwana, which extended from the low northern latitudes to the high southern latitudes, just short of the South Pole. The rocks and fossil assemblages of Gondwana show major changes that correspond to its great size and wide range of climates and environments. The Antarctic and Australian sectors of Gondwana rested in low latitudes during the Cambrian and have extensive carbonate deposits, although those of Antarctica are poorly exposed through the present-day polar ice cap. Differences in their fossil assemblages in addition to paleomagnetic evidence suggest that present-day North and South China were on separate tectonic plates; however, extensive carbonate deposits in both regions indicate that both plates were found in low latitudes during the Cambrian. The fossil assemblages of South China have strong similarities with those of both Australia and Kazakhstan, but details of the Cambrian geographic relationships remain unclear.Several terranes (fault-bounded fragments of the Earth's crust) seem to have been located near or attached to the margin of the northern Africa sector of Gondwana in the high southern latitudes, but many details of their Cambrian geographic relations are unknown. These terranes now make up much of southern Europe and parts of eastern North America. Cambrian deposits in all the terranes are chiefly sandstone and shale and include few or no carbonates. Their faunas closely resemble those of Baltica at generic and higher taxonomic levels, but differences at the species level suggest some geographic separation.Siberia was a separate continent located in the low latitudes between Laurentia and Gondwana. Fossil similarities between this continent and Gondwana suggest that it was positioned relatively close to the equatorial region of Gondwana. Present-day Kazakhstan seems to be composed of several microcontinental blocks that were in all likelihood separated during the Cambrian. These blocks became amalgamated after the Cambrian, and the subsequent composite continent known as Kazakhstania collided with Siberia during the late Paleozoic Era.Few Cambrian faunas from continental-slope and deep-ocean environments are known. Limited information from these is important, however, for demonstrating affinities between deep, cool-water ecosystems at all latitudes and shallow, cool-water communities of higher latitudes. There exists a close similarity between the observed distribution patterns of Cambrian and modern marine arthropods. This has been used as persuasive evidence for the existence of thermally stratified Cambrian oceans in lower latitudes with a thermocline separating warm-water from cool-water layers. This inferred thermocline and the wide oceanic separation of biogeographic regions are seen as the likely causes for the high endemism of the biological communities surrounding Laurentia. This interpretation is supported by deposits that date back to the middle of the Cambrian in northern Greenland where, within a few tens of kilometres, normal Laurentian shelf-margin trilobite (distinctive three-lobed marine arthropods) communities grade into deepwater faunas like those in the shallow-shelf deposits of Baltica. Similarly, trilobite species in later Cambrian deepwater faunas found in the western United States also appear in southeastern China, whereas shallow-water communities of the two regions have few genera in common.As large tectonic plates (plate tectonics) continued to move during the Phanerozoic Eon, terranes of various sizes were displaced. Endemic Cambrian fossils, in conjunction with other geologic evidence such as physical stratigraphy, have been useful for identifying the geographic origins of some terranes, particularly those that have undergone substantial displacement. Examples of displaced terranes include northern Scotland and west-central Argentina (Precordillera) with Laurentian fossils, eastern Newfoundland with fossils from Baltica, and southern Mexico (Oaxaca) with Gondwanan (South American) fossils.Another important consequence of continued plate movement has been the formation of large mountain ranges at the sites of plate collision. Pressure and heat generated during collisions since the Cambrian have folded (fold), faulted (fault), and metamorphosed significant volumes of Cambrian rock, especially from the outer margins and slopes of many continental shelves. No crustal rocks found in today's oceans are older than the Mesozoic Era (251 to 65.5 million years ago); most pre-Mesozoic deposits that accumulated in the deep ocean basins are thought to have been destroyed after they subducted into Earth's interior.Relatively abrupt changes in sea level may have significantly influenced Cambrian environments and life. A global drop in sea level is suggested by extensive unconformities (interruptions in the deposition of sedimentary rock). The time represented by such unconformities in sectors of Laurentia and Baltica bounding the Iapetus Ocean has been called the Hawke Bay event. An apparent absence of a coeval unconformity in western North America seems to be an anomaly. Thick uninterrupted shelf deposits in this sector of Laurentia, however, may have resulted from abnormal shelf subsidence caused by the cooling of crustal rocks following a late Precambrian plate-rifting (plate tectonics) event. The timing of unconformities found in widely separated continents cannot be correlated with precision; however, it is perhaps significant that a number of characteristic animal groups from the early portions of the Cambrian were either exterminated or severely restricted in their geographic distribution at about the same time in the world's shallow-shelf environments. Among biostratigraphically important trilobites, the olenellids (Olenellus) were exterminated near Laurentia, the holmiids went extinct at the margins of Baltica, and the redlichiids vanished from the shallow-shelf ecosystems near Gondwana. Also, diverse and abundant reef-dwelling archaeocyathans (archaeocyathid) (extinct group of sponges thought to have helped construct the first reefs) disappeared from most low-latitude warm-water continental shelves.The significant rise in sea level is suggested by rather abrupt and extensive displacements in sedimentary environments and biotas during the middle of the Cambrian (the Ptychagnostus gibbus zone). Lowland areas were flooded, as in parts of Baltica. In warm-water shelf sections of the world, coarse-grained, shallow-water, carbonate rocks were abruptly overlain by fine-grained, deeper-water, laminated limestone or shale. adaptive radiation of the pelagic agnostoid (Agnostus) trilobites was greatly accelerated in open-oceanic environments following this event, perhaps in response to newly expanded habitats.In Laurentia, a significant drop in sea level near the end of the Cambrian is suggested by both the disappearance of some faunas and a single unconformity that defines the boundary between the Dresbachian and Franconian stages, two regional stages in peripheral areas of North America. However, there is no evidence for a comparably large change in sea level at or near the Cambrian-Ordovician boundary. Associated minor unconformities have made it difficult to select a defining Global Standard Section and Point (GSSP) for the boundary, which ideally should be located in an uninterrupted stratigraphic section.Several regions of Cambrian volcanism have been identified. Australia was especially active; large areas in the northern and central regions were covered by flood basalts (basalt) during the early parts of the Cambrian with residual activity extending into the middle of the period. Basalts and mafic (mafic rock) intrusives (molten rock derived from basic magmas) in southeastern Australia formed in a volcanic island arc setting during the early and middle parts of the Cambrian. Volcanic suites of similar age are also present in New Zealand and in parts of Antarctica (northern Victoria Land, Ellsworth Mountains, and Pensacola Mountains). Other significant Cambrian volcanic deposits occurring during the early and middle parts of the period are found in southern Siberia and western Mongolia (Altai (Altai Mountains) and Sayan Mountains), eastern Kazakhstan and northwestern China (Tian Shan (Tien Shan)), and northeastern China. Cambrian volcanics are scattered along the easternmost margin of the United States, but most are probably island arc deposits that were accreted to Laurentia after the Cambrian. In the southern United States ( Oklahoma), granitic (granite) intrusives and basaltic and rhyolitic (rhyolite) extrusives are associated with a large tectonic trough that was formed by rifting, or crustal extension, throughout the first half of the period.Minor volcanic deposits, mainly ash beds and thin flows, are widely known. In general, these have received little study, but some are suitable for determination of isotopic ages. Zircons (zircon) from a lower Lower Cambrian (pretrilobite) volcanic ash bed in New Brunswick, Can., have a uranium-lead age of 531 million years. Volcanic tuffs near inferred Tommotian-Atdabanian boundaries (Russian designations for the pretrilobite and trilobite portions of the Cambrian explosion) in both Morocco and southwestern China have yielded similar dates of 521 million years.The tectonic (tectonics) history of the Precambrian is not as well-known as that of the Paleozoic. In general, however, late Precambrian history seems to have been characterized by continental fragmentation, whereas Paleozoic history was characterized by the continental accretion of terranes. The Cambrian was a period of transition between those tectonic modes, and continents were scattered, apparently by fragmentation of Rodinia. Major Cambrian and early Ordovician tectonism affected large areas of Gondwana in what are now Australia, Antarctica, and Argentina. Multiphase tectonism in Antarctica is called the Ross Orogeny, and in Australia it is known as the Delamerian Orogeny. At least some of the volcanic activity noted above, particularly that of volcanic island arcs, is evidence that seafloor spreading and crustal subduction were active geologic processes.Paleoclimate (paleoclimatology)Global climate during Cambrian time was probably warmer and more equable than today. An absence of either land or landlocked seas at the Cambrian poles may have prevented the accumulation of polar ice caps. The general absence of glacial till deposits of Cambrian age is more notable, because these deposits are common and widespread in upper Precambrian strata. They accumulated again during the Ordovician Period in northern Africa as Gondwana began to move over the South Pole. Otherwise, the presence of persistent and widespread limestone deposits found on the margins of a centralized transcontinental arc in North America, for example, indicates that a subtropical climate existed in latitudes between 30° N and 30° S. In addition, arid to semiarid conditions at latitudes around the Tropics of Cancer and Capricorn (approximately 23°27′ N and S latitude, respectively) are suggested by deposits that include sandstone with quartz grains frosted by abrasion through wind transport, ventifacts (ventifact) (wind-polished stones), and evaporites (evaporite).More sophisticated research on paleoclimates relies on the detection of changing patterns in the amounts of isotopic (isotope) oxygen, carbon, and strontium retained in limestone samples to correlate the timing of different geological events. Much remains to be accomplished regarding this promising line of research on Cambrian strata, but certain trends and events are becoming better defined. Strong reductions in isotopic carbon (13C), for example, are correlated from Lower Cambrian strata at localities as distant from one another as the Lena River area of Siberia and the Atlas Mountains of Morocco. Another substantial drop in 13C is believed to mark the transition between the early and middle parts of the Cambrian in the Great Basin of North America. Such decreases may represent a global rise in temperature occurring at the same time as a rise in global sea level. In addition, the delivery of anoxic (oxygen-depleted) ocean waters with reduced amounts of 13C also may have been aided by rising sea level.Cambrian lifeThe long history of life on Earth has been punctuated by relatively abrupt changes. Some have argued that the greatest change of all occurred in marine environments near the Precambrian-Cambrian boundary. Fossils from Cambrian rocks include the oldest representatives of most animal phyla having mineralized shells or skeletons. A lack of observed connecting links suggests that processes of biomineralization (specifically, the formation of bones, shells, and teeth) evolved independently in several phyla. Whether or not soft-bodied representatives of some of these phyla originated during the Precambrian but have no preserved record is a debated question. Nevertheless, the hard parts of Cambrian animals had a much greater potential for preservation than the soft parts, and they mark the beginning of a diverse fossil record.Fossil record of the Precambrian-Cambrian transitionThe preservation of the record of the Precambrian-Cambrian transition was significantly affected by global changes in sea level. During latest Precambrian time, the sea level was relatively low, resulting in spatially restricted oceans and expanded continents. Throughout much of the Cambrian, rising seas gradually flooded vast land areas. Sediment was eroded from the continents and deposited in adjacent seas. Because of low sea level, the sedimentary and fossil records of the Precambrian-Cambrian transition are generally most complete toward the outer margins of continental shelves. As a corollary, the time gaps, represented by the boundary surface, generally increase in landward directions. This has led to an absence or serious incompleteness of the transitional record in most areas, particularly in those of classical Cambrian studies. As a result, it is thought that this incompleteness, combined with a general deficiency in knowledge—prior to the mid-1900s—of Precambrian communities, contributed significantly to the long-held notion of an abrupt or sudden appearance of Cambrian fossils.Considering the biological importance of the Precambrian-Cambrian transition, it is somewhat surprising that the primary impetus for its detailed study came from a project designed to establish a suitable international boundary stratotype (a rock layer that serves as a benchmark of geologic time). Before the project was initiated in 1972, reasonably complete stratigraphic sections across the transition were either largely unrecognized or ignored. Since 1972, information about the transition has accumulated at an accelerating rate. Although many details remain to be learned, the general history of this momentous interval is becoming clear.The Precambrian-Cambrian biotic transition, once thought to be sudden or abrupt, has been found to include a succession of events spread over many millions of years. It commenced with the appearance of the animal kingdom (i.e., multicelled organisms that ingest food), but the date and details of that event remain obscure. At least three informal phases in the transition can be identified by progressively more diverse and complex biological communities.The earliest phase of late Precambrian (Precambrian time) age is characterized by fossils (fossil) of soft-bodied animals known from many localities around the world. Based on fossils of animal embryos, it is thought that elements of the Ediacaran fauna (Ediacara fauna) appeared as early as 590 to 600 million years ago. The fossils are predominantly the imprints of soft-bodied animals. Their extraordinary preservation, usually in sandstone or shale, was probably the result of rapid burial and protection by smothering sediment. Most of the fossils are relatively simple, and many resemble worms, sea pens, and jellyfish. Dwelling traces (fossilized burrows and other excavations) like those of modern sea anemones are also common. Placing Ediacaran fauna in higher (more generalized) taxonomic levels is controversial, however, because critical diagnostic features are not evident. Some paleontologists have assigned Ediacaran body fossils to the extant phyla Annelida (annelid), Coelenterata (cnidarian), and Arthropoda (arthropod), whereas others have regarded them as members of extinct taxonomic groups of high rank. Some adherents of this latter viewpoint have suggested that the Ediacaran fauna was terminated by a major extinction event, but direct evidence of an abrupt replacement of species has not been found in the geologic record.Other kinds of fossils also provide valuable clues about life during Ediacaran time. Photosynthetic organisms include unicellular blue-green algae (cyanobacteria) and acritarchs (probable algae), both of low diversity. Individuals of some species were probably abundant, however, and may have been an important source of food for Ediacaran animals. Hard parts of animals, primarily known from Africa and China, are mainly dwelling tubes composed of calcium carbonate and other compounds. Most were probably secreted by sessile, filter-feeding, wormlike animals. Although rare and of low diversity, these forms are significant because they signal the advent of biomineralization. The oldest unequivocal trace fossils, mainly crawling trails, are also of Ediacaran age. The trails suggest that locomotion of the trace makers was accomplished by waves of muscular contraction, like that in annelids and sea slugs, and not by legs. All but the latest Ediacaran trace fossils are relatively simple, suggesting limited and primitive behaviour patterns. Their low diversity further suggests that few kinds of mobile animals lived on the Ediacaran seafloor.The second phase of the Precambrian-Cambrian biotic transition is characterized by a marked increase in the diversity of its shelly fauna and a lack of trilobites (trilobite). It is near the lowest stratigraphic occurrence of this fauna that the Precambrian-Cambrian boundary stratotype has been placed. The fauna includes that of the Tommotian Stage, as applied in Russia, and it has often been referred to as the Tommotian fauna. It is known from many localities around the world, but time correlations lack precision. A general acceleration in biotic diversity during this second phase is the beginning of the Cambrian explosion.Fossils of the second phase, which may be locally abundant, represent several new animal groups of Paleozoic (Paleozoic Era) aspect. Calcified archaeocyathans (archaeocyathid) (extinct group of sponges (sponge) thought to have helped construct the first reefs) diversified rapidly and were the first skeletal metazoans (multicellular animals with differentiated tissues) to develop a modular growth habit. They also evolved a complex symbiotic relationship with reef-building blue-green algae. Mollusks (mollusk), preserved in both shale and limestone, include at least four classes (Monoplacophora, Gastropoda, Hyolitha, and Rostroconchia). Brachiopods (lamp shells) (lamp shells) made their appearance but are low in diversity. Several groups are represented by an astonishing array of small mineralized tubes, scales, and spicules (spicule). The presence of arthropods (arthropod), the first animals to develop legs, is indicated by characteristic trace fossils. The skeletal remains of arthropods are not preserved in the fauna, however, presumably because they were not mineralized. Other trace fossils show a marked increase in abundance and diversity as well as an expansion of behaviour patterns that reflect improvements in locomotion, greater ability to penetrate sediment, and new foraging strategies.The third phase of the Precambrian-Cambrian biotic transition commenced with the appearance of mineralized trilobite skeletons. The subsequent adaptive radiation of the trilobites was exceptional, and their remains dominate most later Cambrian deposits. For this reason, the Cambrian Period has sometimes been called the Age of Trilobites.The known Cambrian biota was restricted to marine environments. At least 11 extant animal phyla (Annelida, Arthropoda, Brachiopoda, Chordata (chordate), Ctenophora (ctenophore), Echinodermata (echinoderm), Hemichordata (hemichordate), Mollusca, Onychophora (velvet worm) [velvet worms], Porifera, and Priapulida (priapulid)), including most of those with a fossil record, first appear in Cambrian rocks. Most of these rapidly diversified as they seemingly adapted to numerous unfilled ecological niches. Another five phyla (Nemertea, Phoronida, Platyhelminthes, Pogonophora, and Sipuncula) may also trace their origin back to the Cambrian fossils, though questions still remain about them. The only extant animal phylum with a good fossil record that is not known from Cambrian rocks are the Bryozoa (moss animal) (moss animals), which first appear in rocks of Early Ordovician (Ordovician Period) age. A summary of the principal biotic groups of the Cambrian is given below.Photosynthetic organismsCambrian photosynthetic organisms, the primary food of animals, are entirely unicellular. These organisms include a variety of prokaryotic (nonnucleated) and eukaryotic (nucleated) bacteria and algae. Their evolution, like that in associated animals, shows a marked acceleration in adaptive radiation and biomineralization near the base of the Cambrian. A new calcareous bottom-dwelling (benthos) flora dominated by blue-green algae appeared. Some of these organisms formed mounds on the seafloor. Others formed small, concentrically laminated, marble- or biscuit-shaped structures called oncoids, which were locally abundant. Although it was rarely preserved, there existed a noncalcareous benthic flora that also was dominated by blue-green algae. By at least the middle of the Cambrian, some noncalcareous green algae (Chlorophyta) had become common. In North America and Siberia, the axes of one species, Margaretia dorus, exceeded 2 cm (0.8 inch) in diameter and were probably more than 1 metre (3.3 feet) in height. Such large size is attained by modern green algae only in warm, equatorial oceans. The phytoplankton, consisting of acritarchs and blue-green algae, also diversified near the base of the Cambrian. Acritarchs are widespread in many kinds of marine rocks and seem to have potential for an improved zonation of Lower Cambrian rocks. They are difficult to study, however, because of their microscopic size.Fauna (faunal region)Cambrian faunas, like those of the present day, are commonly dominated in numbers and kind by members of the phylum Arthropoda. Calcification of skeletons by the beginning of Atdabanian time contributed to an abundant fossil record of the class Trilobita, of which some details have been discussed above. Many hundreds of genera and thousands of species of Cambrian trilobites have been described worldwide. Rates of evolution in Cambrian trilobites were relatively rapid, resulting in short stratigraphic ranges and giving them much value for biostratigraphic correlation. Representatives of the class Ostracoda (mussel shrimp), characteristically enclosed by a bivalved carapace, also appeared near the base of the Atdabanian. Compared with trilobites, however, ostracods are generally rare and of low diversity throughout the Cambrian, except in some rocks of Australia and China. Extraordinary preservation at rare localities indicates that many other kinds of arthropods were at least locally more abundant and more diverse than the trilobites. These other arthropods had unmineralized skeletons, and some may represent extinct classes.Sponges (sponge) (phylum Porifera) are commonly represented in Cambrian faunas. Archaeocyathan sponges, characterized by cup-shaped skeletons with double calcareous walls and numerous pores, are abundant and diverse in some early Cambrian deposits. They have been used for provincial biostratigraphic zonation, especially in Australia and Siberia. Archaeocyathans (archaeocyathid) are common only in regions that were positioned in low latitudes during the Cambrian—Antarctica, Australia, China, Kazakhstan, Siberia, and North America. Their latitudinal distribution is similar to that of modern colonial corals, suggesting adaptations to similar ecological controls in warm shallow seas. Archaeocyathans nearly disappeared about the middle of the Cambrian, but rare species survived until much later in the period, after which the group became extinct. Other common Cambrian sponges had skeletons of siliceous (silica-derived) spicules, which readily disaggregated after death, making their identification at lower taxonomic levels difficult, if not impossible. At rare locations of exceptional preservation, where articulated skeletons and associated soft-bodied taxa and others were found, spicular sponges are second only to arthropods in species diversity. This suggests that Cambrian sponges were much more common and more diverse than is indicated by the known fossil record. Limited information indicates that species of spicular sponges evolved slowly during the Cambrian, resulting in relatively long ranges within the stratigraphic record.Brachiopod (lamp shells) shells are present in many Cambrian continental-shelf deposits. In terms of the total number of species that have been described from Cambrian rocks, brachiopods are second only to trilobites. Species diversity, however, is generally low to moderate at most localities. Phosphatic shells of the class Inarticulata are normally much more common and more diverse than are calcareous shells of the class Articulata. These abundance and diversity relationships are usually reversed in post-Cambrian rocks.The phylum Echinodermata (echinoderm) (some present-day representatives of which are sea urchins and starfish) had a major adaptive radiation during the Cambrian Period. The number of classes increased from three early in the Cambrian to eight toward the middle of the period. Only one of these, the Eocrinoidea, is known from many species, but the described record seems to be grossly incomplete. Skeletal plates in early echinoderms were not rigidly connected, and they readily disaggregated after the death of an animal. Consequently, it is rare to find articulated skeletons that can be classified to lower taxonomic levels. In some Cambrian limestones (limestone), however, skeletal plates of echinoderms are a dominant sedimentary constituent, indicating the existence of innumerable animals and suggesting far greater diversity, especially at low taxonomic levels, than has been recorded. As in some modern echinoderm species, it is common for those in the Cambrian to show evidence of a gregarious habit and patchy distribution. Most of the Cambrian echinoderms were suspension and detritus feeders, and it was only after the Cambrian that herbivores and carnivores became common. All classes of echinoderms that were present during the Cambrian, except for the Crinoidea (crinoid), subsequently became extinct.The phylum Mollusca (mollusk) also underwent significant adaptive radiation during the Cambrian, with the appearance of the classes Monoplacophora (monoplacophoran), Gastropoda (gastropod), Pelecypoda (bivalve) (synonymous with Bivalvia), Cephalopoda (cephalopod), Polyplacophora, Rostroconchia, Hyolitha, and Stenothecoida. (The latter three are now extinct.) The only molluscan class that appeared after the Cambrian is the Scaphopoda (tusk shell) (tusk or tooth shells), which originated during the Ordovician. A small variety of mollusks is present in the shelly fauna of the earliest Cambrian. Mollusk shells usually are absent or rare in later Cambrian rocks, but at a few localities they are common to abundant. The small conical shells of hyoliths are the kind most commonly preserved in Cambrian rocks.Other new Cambrian phyla largely lack biomineralization and have a poor fossil record. The Hemichordata (hemichordate) is represented by rare sessile graptolites (graptolite) (order Dendroidea) of the class Graptolithina, which appeared during the middle of the Cambrian. Appearances of the more common planktonic graptolites (order Graptoloidea) have been used as informal indicators of the Cambrian-Ordovician boundary; the formal boundary stratotype coincides with the first appearance of Iapetognathus fluctivagus, a conodont (primitive chordate with tooth-shaped fossil remains). Cambrian worm phyla (Annelida, Priapulida, and probable Pogonophora) are mainly known from localities where preservation was extraordinary. Other rarely represented phyla include the Onychophora, with leglike lobopodia (a catchall category of Cambrian life), and the Ctenophora (comb jellies).The origin of the phylum Chordata (chordate) is unclear. If primitive conodont-like fossils (paraconodonts) are included, as argued by some paleontologists, the phylum appeared during the late Precambrian. Rare soft-bodied possible chordates have been described from Lower Cambrian rocks. The oldest unequivocal chordate remains come from the Lower Cambrian of south China, where small jawless fish similar to present-day lamprey and hagfish occur as part of the Chengjiang Biota. The fossils from this Lagerstätte (a fossil-rich deposit of sedimentary rock) preserve the remains of different soft body tissues—traces of gill pouches, dorsal fins, and likely the notochord itself.Trace fossils, as discussed above, provide independent evidence of accelerated animal diversification and a distinct increase in the complexity of animal behaviour near the beginning of the Cambrian Period. Other evidence from trace fossils indicates changes in Cambrian bioturbation, the churning and stirring of seafloor sediment by animal forms. Late Precambrian (Ediacaran) trace fossils from around the world are essentially surface trails that show little evidence of sediment burrowing. Quantitative study in the western United States has shown that a significant increase in bioturbation occurs between pretrilobite (Tommotian) and trilobite-bearing (Atdabanian) Lower Cambrian rocks. Throughout the Cambrian, bioturbation was more intensive in nearshore and inner-shelf environments than in more offshore settings. The depth of bioturbation in carbonate environments of the inner shelf was consistently less than a few centimetres throughout Cambrian time.Deposits with soft-bodied organismsModern biota are largely dominated by soft-bodied organisms, whereas the fossil record is overwhelmingly dominated by the hard parts of organisms. Rare deposits of fossils with soft parts are therefore of great importance in helping to establish the original diversity and ecology of ancient communities. Among the most famous soft-bodied biota are those found in the Burgess Shale of western Canada (British Columbia), which was formed during the middle of the period, and the Chengjian Biota from southern China (Yunnan), which was formed earlier in the period. In the case of the Burgess Shale, tens of thousands of complete specimens, many with soft parts preserved in remarkable detail, were apparently buried by submarine slumping of sediment on the continental shelf of Laurentia. Fossils from the Burgess Shale have been used to demonstrate the presence of a complex community as diverse in habit, structure, and adaptation as many modern communities. If isolated, fossils with hard parts would constitute a typical Cambrian fauna, but they represent only about 40 percent of the genera in the Burgess Shale, a proportion similar to that in modern faunas on continental shelves. Approximately 15 percent of the genera known from the Burgess Shale also occur in the older Chengjian deposit. Mollusks and echinoderms appear to be the only major groups absent in the Chengjian Biota that occur in the Burgess Shale.The most celebrated invertebrate from the Burgess Shale is attributed to the genus Anomalocaris. This creature was the largest predator that swam in Cambrian seas. It was outfitted with a pair of giant flexible appendages that could grasp and move prey toward a peculiar mouth structure consisting of armoured plates arranged in a circular pattern. The articulated mouth of Anomalocaris has been described as resembling a pineapple ring with the center cut out. Trilobites with telltale scars on their carapace are believed to represent the cookie-cutter bite of Anomalocaris.A smaller relative of Anomalocaris is the bizarre Opabinia, with its five eyes mounted on an arthropod-like body and a long nozzlelike structure fitted with a single pair of claws that protrudes forward from the head. It is thought that Opabinia moved across the seafloor, using its flexible nozzle to stir up bottom sediment and grasp hidden prey with extended claws.Other less-diverse Cambrian deposits with soft-bodied organisms have been discovered in such places as South Australia, northern Greenland, Sweden, and the United States (Utah and Pennsylvania). Some of these are important in demonstrating that the biota of the Burgess Shale is unusual only in preservation and not in composition. They also demonstrate that some of the soft-bodied taxa have substantial geologic ranges and wide geographic distributions. Extraordinary preservation of arthropods dating to the later parts of the Cambrian Period in Sweden is especially notable, as the bodies and appendages remain largely uncrushed; the integument retains many fine structures, including setae (bristly hairs or organs) and pores.extinction eventsMinor extinction events occurred sporadically throughout the Cambrian Period. One near the middle of the Cambrian was apparently related to global marine regression. At least three later Cambrian events primarily affected low-latitude shelf communities and have been used in North America to define biostratigraphic units called biomeres. (Such units are bounded by sudden nonevolutionary changes in the dominant elements of a phylum.) Each of the Cambrian biomere events eliminated several trilobite families, which collectively contained most of the genera and species that were living on the continental shelves. Less attention has been paid to extinction patterns among other invertebrates, but some evidence of corresponding extinctions among brachiopods and conodonts is available. Geochemical evidence suggests that the biomere extinctions were probably caused by abrupt drops in water temperature. Oxygen isotopes from the skeletons of bottom-dwelling trilobites associated with one biomere boundary in Texas indicate a drop in water temperature of about 5 °C (9 °F) at the boundary. A comparable decrease in temperature would kill the larvae of many modern marine invertebrates that live in warm oceans. Following each Cambrian extinction, shelf environments were repopulated by low-diversity trilobite faunas of relatively simple form, which apparently emigrated from deeper and cooler off-shelf environments. In effect, every one of the biomere events was followed by an adaptive radiation of new taxa, especially among the trilobites.Cambrian rocksTypes and distributionCambrian rocks have a special biological significance, because they are the earliest to contain diverse fossils of animals (animal). These rocks also include the first appearances of most animal phyla that have fossil records. Cambrian evolution produced such an extraordinary array of new body plans that this event has been referred to as the Cambrian explosion. The beginning of this remarkable adaptive radiation has been used to divide the history of life on Earth into two unequal eons. The older, approximately three-billion-year-old Cryptozoic Eon began with the appearance of life on Earth, and it is represented by rocks with mainly bacteria, algae, and similar primitive organisms. The younger, approximately half-billion-year-old Phanerozoic Eon, which began with the Cambrian explosion and continues to the present, is characterized by rocks with conspicuous animal fossils.Rocks of Cambrian age occur on all of the continents, and individual sections may range up to thousands of metres thick. The most fossiliferous and best-studied deposits are principally from marine continental-shelf environments. Among the thicker and better-documented sections are those in the Cordilleran region (cordillera) of western North America, the Siberian Platform of eastern Russia, and areas of central and southern China. Other well-documented fossiliferous but thinner sections are located in Australia (especially in western Queensland), the Appalachian Mountains of eastern North America, Kazakhstan, and the Baltic region (most notably in Sweden).Lateral changes in the composition of Cambrian rocks resulted from regional differences in environments of deposition. Nearshore deposits are commonly composed of siliceous sandstone. This usually grades seaward into siltstone and shale, which formed by accumulation of finer-grained sediment in deeper water where the seafloor was less affected by wave action. Extensive carbonate (carbonate rock) platforms, analogous to the present-day Bahama Banks, developed along some continental shelves that were in low latitudes during Cambrian time. Rapid production of carbonate sediment in this warm, shallow-water environment resulted in massive deposits of Cambrian limestone and dolomite. Examples are exposed in the Cordilleran region of North America, in north central Australia, along the Yangtze River in central China, and along the Lena River in Siberia. Few Cambrian rocks from land environments have been documented, and most of those are of limited areal extent. They mainly represent deposits of floodplains (floodplain) and windblown sand. Without plants or animals, the desolation of Cambrian landscapes must have rivaled that of any present-day desert. In the absence of plants with roots to hold soil in place, Cambrian lands in general probably eroded more rapidly than they do now.Relative sea level rose significantly during the Cambrian, but with fluctuations. This is indicated by both the geographic distribution and the stratigraphic layering of sedimentary deposits. In North America, for example, marine deposits from earlier in the period covered only marginal areas, whereas later marine deposits covered much of the continent. Similar distributions of marine rocks are present on other continents. In stratigraphic sections from continental shelves that were located in low latitudes, it is common for a basal nearshore sandstone to be overlain by layers of more seaward shale and carbonate rocks deposited during times of high sea level. Shelf sections from high latitudes may be mostly or entirely sandstone, or a basal sandstone deposit may grade upward into shale, but most of these sections contain evidence of marine transgression. Exceptions to the general Cambrian sea-level pattern are commonly attributable either to local tectonism (tectonics) or to different rates of sediment accumulation. The most likely explanation for the general rise in Cambrian sea level seems to be increased thermal activity and related swelling of spreading ridges between lithospheric plates, which would displace vast quantities of seawater. It has been suggested that these periods of marine inundation exerted an influence on adaptive radiation (the proliferation of organic lineages) by greatly increasing the area of shallow seas where life was most abundant.Boundaries and subdivisions of the Cambrian SystemThe lower boundary of the Cambrian System is defined at a formal global stratotype section and point (GSSP), which was ratified by the International Commission on Stratigraphy (ICS) of the International Union of Geological Sciences (IUGS) in 1992. The stratotype section is located at Fortune Head on the Burin Peninsula of southeastern Newfoundland in Canada. It contains a thick and continuous marine succession of mostly shale, siltstone, and sandstone. The stratotype point, representing a moment in time, is in the lower part of the Chapel Island Formation. It coincides with the base of the remnant burrows of the fossil Trichophycus pedum and marks the first occurrence of well-developed, fairly complex metazoans (group of animals composed of multiple, differentiated cells). This is currently regarded as the most useful benchmark on which to characterize both the lower boundary of Cambrian time and the beginning of the Phanerozoic Eon. T. pedum can be found on most continents, and its chronological position puts it slightly younger than Ediacaran fossils (Ediacara fauna) (around 570 million years ago) and some 20 million years older than the small shelly fossils dated to the early parts of the Cambrian Period.While there is general agreement on the point in time picked for the beginning of the Cambrian, there is little or no agreement on how to subdivide the remaining 53 million years of Cambrian time. In most regions of the world, Cambrian rocks have been divided into lower, middle, and upper series according to regional standards and practices, but these distinctions are neither uniform nor internationally recognized. Furthermore, regional series boundaries are not necessarily synchronous with one another, owing to differences in definition and problems in correlation. Some series have been further divided into stages, but these are mostly identifiable only within individual regions. Many supplementary sections were investigated at boundary localities around the world before the stratotype was selected in Newfoundland. All these supplementary sections are important references for reconstructing the physical and biological histories of the boundary interval. Among the more thoroughly studied supplementary sections are those along the Aldan River of eastern Siberia and near the city of Kunming in the Yunnan province of southern China.The lower boundary of the Ordovician System indirectly defines the upper boundary of the Cambrian System. A formal boundary stratotype coincides with the first appearance of the conodont Iapetognathus fluctivagus. This boundary marks the base of the Tremadoc Series (Tremadocian Stage) in the Ordovician System. British geologists have traditionally assigned rocks and fossils of Tremadoc age to the Cambrian, whereas many others have assigned them to the Ordovician.Rocks in the Cambrian-type area in Wales are so poorly exposed, structurally complicated, and sparsely fossiliferous that they have had little influence on development of modern concepts of the Cambrian and its subdivisions. In fact, many rocks in the Cambrian-type area have been reassigned to either the Precambrian or the Ordovician. Rocks in Wales that are now assigned to the Cambrian System roughly correspond to Sedgwick's Lower Cambrian.Economic significance of Cambrian depositsCambrian rocks are of moderate economic importance, as they provide a variety of resources. For example, ore bodies rich in such metals as lead, zinc, silver, gold, and tungsten have secondarily replaced Cambrian carbonate rocks (carbonate rock), especially in parts of North America and Australia. Other carbonate rocks have been widely used as building stone and for making lime and portland cement. Large Cambrian phosphorite deposits are major sources of agricultural fertilizer in northern Australia, southwestern China, and southern Kazakhstan. Other Cambrian resources in China are mercury, uranium, and salt. Eastern Russia also has salt deposits of Cambrian age, as well as those of bauxite, the chief commercial source of aluminum. Some oil fields in southern Siberia produce oil (petroleum) from Lower Cambrian rocks.Correlation of Cambrian strataTime correlation of Cambrian rocks has been based almost entirely on fossils. The most common fossils in Cambrian rocks are trilobites (trilobite), which evolved rapidly and are the principal guide fossils for biostratigraphic zonation in all but rocks below the Atdabanian Stage or those of equivalent age. Until the mid-1900s, almost all trilobite zones were based on members of the order Polymerida. Such trilobites usually have more than five segments in the thorax, and the order includes about 95 percent of all trilobite species. Most polymeroids, however, lived on the seafloor, and genera and species were mostly endemic to the shelves of individual Cambrian continents. Therefore, polymeroid trilobites are useful for regional correlation but have limited value for intercontinental correlation, which has been difficult and subject to significant differences in interpretation.From the 1960s, investigators began to recognize that many species of the trilobite order Agnostida (Agnostus) have intercontinental distributions in open-marine strata. These trilobites are small, rarely exceeding a few millimetres in length, and they have only two thoracic segments. Specialized appendages, which were probably useful for swimming but unsuitable for walking on the seafloor, suggest that they were pelagic (living in the open sea). Agnostoids make up less than 5 percent of all trilobite species, but individuals of some agnostoid species are abundant. This fact, together with their wide geographic distribution and rapid evolution, makes them valuable for refined intercontinental correlation. Agnostoids first appear in upper Lower Cambrian rocks but did not become common or diversify significantly until the middle of the Cambrian. Therefore, agnostoids have their greatest biostratigraphic value in the upper half of the Cambrian System. A comprehensive trilobite zonation in Sweden has frequently been cited as a standard for correlation.Other kinds of fossils have had more limited use in Cambrian biostratigraphy and correlation. Among them are the archaeocyathan (archaeocyathid) sponges in the Lower Cambrian and brachiopods (moss animal) (moss animals) throughout the Cambrian, but use of both groups has been hampered by problems of endemism. Small mollusks (mollusk) and other small shelly fossils, mostly of problematic affinities, have been employed for biostratigraphy in the Tommotian Stage (a Russian designation for the pretrilobite portion of the Cambrian explosion), but their utility is also limited by endemism. Conodonts (conodont) appear in the uppermost Precambrian but are rare in most Cambrian rocks except those of latest Cambrian age, when adaptive radiation of conodont animals accelerated. Wide species distributions, rapid evolution, and abundance make conodonts excellent indexes for global biostratigraphy in uppermost Cambrian to uppermost Triassic (Triassic Period) rocks.Since roughly the 1980s, trace fossils have been used with limited precision to correlate uppermost Precambrian and basal Cambrian strata. Although the biostratigraphic use of such fossils has many problems, they nevertheless demonstrate progressively more complex and diverse patterns of locomotion and feeding by benthic (bottom-dwelling) marine animals. T. pedum, which initially appears in Cambrian deposits and marks the base of the period, demonstrates the first regularly branching burrow pattern.Additional ReadingStephen Jay Gould, Wonderful Life: The Burgess Shale and the Nature of History (1989); and Simon Conway Morris, The Crucible of Creation: The Burgess Shale and the Rise of Animals (1998), offer conflicting outlooks on a famous Cambrian biota and its significance in the history of life. Discovery of the oldest fossil fish is described by D.G. Shu et al., “Lower Cambrian Vertebrates from South China,” Nature, 402:42–46 (Nov. 4, 1999).C.H. Holland (ed.), Cambrian of the New World (1971), Cambrian of the British Isles, Norden, and Spitsbergen (1974), Lower Palaeozoic of the Middle East, Eastern and Southern Africa, and Antarctica (1981), and Lower Palaeozoic of North-Western and West-Central Africa (1985), are detailed surveys of Lower Paleozoic rocks. Correlation charts, explanatory notes on rocks and faunas, and extensive references are found in Reinhard Wolfart, The Cambrian System in the Near and Middle East (1983); J.H. Shergold et al., The Cambrian System in Australia, Antarctica, and New Zealand (1985); W.T. Chang, The Cambrian System in Eastern Asia (1988); Kaisa Mens, Jan Bergström, and Kasimiera Lendzion, The Cambrian System on the East European Platform (1990); and Vladimir A. Astashkin et al., The Cambrian System on the Siberian Platform (1991).Richard A. Robison Rex E. Crick
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