Ordovician Introduction
Charles
Lapworth (1842-1920), an English geologist, mapped out complicated
marine strata in the Southern Uplands of Scotland. His work led to
the realization that the lower Paleozoic fauna could be divided into
three stratigraphic units: Cambrian (oldest), middle (which he named
the Ordovician), and Silurian (youngest) (Lapworth Museum Website).
Lapworth is well known for determining the correct chronological
sequence of graptolites in this same location, thereby establishing
graptolites as an important index fossil (Palmer, 1999, pp 68-69).
The Ordovician period was named for the Ordovices, a Celtic tribe
living in Wales during the Roman conquest. The Ordovician period
extends from 488.3 million years to 443.7 million years ago.
Primary
Producers & Reefs
Life
thrived in shallow seas and seems to have started its foothold
on land.
Cyanobacteria, green and red algae continue to
be the dominant primary producers (photosynthesizers) (Knoll, Summons,
Waldbauer, and Zumberge, 2007, p. 148). At the beginning of the
Ordovician stromatolites continue to make up reef systems. As the
Ordovician unfolds sponges (lithistid & stromatoporoid), bryozoans,
coralline algae, and corals become major reef builders (Johnson & Stucky,
1995, p. 35) and (Webb, 2001, p. 174). As these new reefs built
vertically, new habitats became available above the sea floor.
Corals (both rugose and tabulate) become much more common during
the Ordovician.
Invertebrates
Trilobites
survived but would never regain their prominence after the final
mass extinction
of the Cambrian. (Stanley, 1987, p.65).
At up to 16 inches, Isotelus is one of the largest trilobites
known. Isotelus was a large predator in the Ordovician
seas and is
Ohio’s
state fossil. Brachiopods survive and diversify; articulate brachipods
displace inarticulate varieties as the dominant shelled organisms
of the sea
floor. Corals and echinoderms start to find success in environments
previously inhabited by sponges (Nudds & Selden, 2008, p. 56).
Overall, many animal groups that were rare in the Cambrian diversify
and become well established during the Ordovician period. Bryozoans,
sponges, crinoids, nautiloid cephalopods, conodontophoras, jawless
fish, and planktonic graptolites become much more common. Graptolites
are
thought
to be colonial hemichordates and are so widespread and varied during
the Ordovician that they can be used as index fossils to date and
correlate rock strata. Crinoids come to dominate the ocean floor. Echinoids
in the form of Sea Urchins first appear in the Ordovician. These
regular, round echinoids with pentameral symmetry had long spines
and were adapted for grazing along the sea bottom (Prothero, 2004,
p. 336). Eurypterids
and starfish make their first appearance during the Ordovician period.
Jawless Fish
Jawless fish become much more common in the Ordovician. The armored
agnathans or Ostracoderms make their first appearance during the
Ordovician. These fish had no jaws or paired fins; their body was
ell-like. Ostracoderms had skeletons made of cartilage, protective
bony shields around the head and bony scales covering the body. The
bony scales give these fossil agnathans their collective name ostracoderms
or shelly skins. Ostracoderms can be divided into two groups the
heterostracans (order Heterostraci), which appear in the Ordovician
and the cephalaspids (order Osteostraci), which appear in the Silurian.
Arandaspis is a heterostracan found near Alice Springs Australia
and is named after the Aranda, an aboriginal tribe. Arandaspis had
a streamlined body with a head sheild made of two large bony plates.
All heterostracans possessed a bony head shield, which could grow
as the fish aged (Dixon et. al, 1988, pp. 24-25). The rest of the
body was covered in bony scales arranged in oblique rows. Its jawless
mouth was near the ventral surface indicating it may have fed off
the ocean bottom. Heterostracans would diversify and become common
during the Silurian and Devonian. Today, only the hagfish and lamprey
represent the class Agnatha.
The Soom Shale
The
Soom Shale of Western Cape, South Africa is a lagerstatten representing
the Ordovician
(Selden & Nudds, p. 29). This deposit was particularly
important in establishing the nature of conodonts (phosphatic tooth
rows). The Soom shale conodont animal Promissum pulchrum revealed
conodonts to be a chordate jawless eel-like fish. The Soom shale
formed in a shallow sea filled with nekton (swimming organisms),
but relatively devoid of benthos (bottom life). Eurypterids, conodonts
and orthocones filled the predatory niches. Brachiopods and cornulitids
lived on the bottom as filter feeders (Selden & Nudds, p. 36).
Beecher’s
Trilobite Bed
Beecher’s Trilobite Bed is a fossil lagerstatten near Rome,
New York. The trilobite bed is famous for producing trilobites in
which the soft tissue anatomy has been preserved by pyrite replacement.
The first examples of trilobite antennae along with ventral anatomy
including legs, gills, and musculature have given paleontologist
a window into the anatomy of once living trilobites. Beecher’s
Trilobite bed is a 4 cm thick layer within the Frankfort Shale beds.
Evidence suggests this layer was formed from a microturbidite. Turbidites
are “marineslides”, which occur when sediment is pulled
down a slope by gravity into deeper waters. Earthquakes can trigger
Tubidites. Pyritized trilobites in Beecher’s Bed include: Triarthrus
eatoni, Triarthrus beckii, Cryptolithus bellulus, and Stenoblepharum
beecheri. Triarthrus trilobites are often found in dark mudstones
rich in sulfur, which formed in anoxic (low oxygen) environments.
Richard Forty believes these trilobites may have been the first to
use sulfur bacteria as chemoautotrophic symbionts (Forty, 2001, pp.
70-71). Triarthrus trilobites had reduced mouthparts and filamentous
structures in their ventral anatomy that could have been used to
cultivate the sulfur bacteria. These bacteria were also responsible
for facilitating the pyrite replacement of soft tissues after death.
The shale surrounding Beecher’s Trilobite Bed contains trilobite
parts, echinoderms, planktonic graptolites, articulate brachiopods,
and orthocone (straight-shelled) cephalopods (Nudds & Selden,
2008, pp. 56-71).
Evidence of Life on Land
Tantalizing
clues provide evidence that life started its invasion of land
during the Ordovician.
A variety of spores (reproductive
structures from primitive land plants) make their first appearance
in the mid-Ordovician (470 mya). One category of spore, the tetrads,
possesses a mark that indicates cell division by meiosis. Along side
these spores are bits and pieces of plant tissues. (Kenrick & Davis,
2004, pp. 19-21). Plant debris becomes more common during the late
Ordovician and Silurian. In late Ordovician rock (450 mya) from England
millipede-like trackways have been preserved (Palmer, 1999, p.
71).
Mass Extinction
The marine ecosystems experienced extinction on a global
scale towards the end of the Ordovician period. The Ordovician
extinction may be second only to the mass extinction that
would end the Paleozoic Era. Heavy extinction occurred
in the reef communities. Graptolites, bryozoans, brachiopods,
nautiloids, and trilobites were especially hard hit. Nearly
25 percent of all animal families were wiped out (Selden & Nudds,
2004, p.36). Over fifty percent of trilobite families went
extinct (Nudds & Selden, 2008, p. 69). There is evidence
of glaciation and with this a lowering of sea level, and
the expansion of cold water adapted species to lower latitudes
as the Ordovician
extinction event unfolded (Stanley, 1987, pp 71-75). An ocean
turn over may have accompanied the cooling event bringing
deep ocean water to the surface, which would have been toxic
to the sensitive shallow marine benthic community. The Ordovician
event took place over a span of 2 million years (Prothero,
2004, p. 90).
Forty, R. (2001). Trilobite:
Eyewitness to Evolution. New York:
Vintage Books.
Kazlev, M.A. (2002). Palaeos
Website. see: http://www.palaeos.com/Timescale/default.htm
Knoll,
Summons, Waldbauer, and Zumberge. (2007). The Geological Succession
of Primary Producers in the Oceans. In Falkowski, P.G. Knoll,
A.H. [Eds] Evolution of Primary Producers in the Sea.
(pp. 133-163). China: Elsevier Academic Press.
Lapworth Museum Website: http://www.lapworth.bham.ac.uk/about/Lapworth.htm
Nudds
J.R. & Selden
P.A. (2008). Fossil Ecosystems of North America: A Guide to
the Sites and Their Extraordinary Biotas. Chicago:
The University of Chicago Press.
Palmer,
D. (1999). Atlas
of the Prehistoric World. New York: Discovery
Books.
Prothero,
D.R. (2004). Bringing Fossils to Life: An Introduction
to Paleobiology [2nd edition]. New York: McGraw-Hill.
Stanley, S.M., (1987). Extinction. New York: Scientific American
Books.
Selden
P. & Nudds,
J. (2004). Evolution of Fossil Ecosystems. Chicago: The University
of Chicago Press.
USGS Publication: Major
Division of Geologic Time see: http://pubs.usgs.gov/gip/geotime/divisions.html
http://www.uga.edu/~strata/
Webb, G.E. (2001). Biologically Induced Carbonate Precipitation
in Reefs through Time. In Stanley, G.D. Jr. [Ed] The History
and Sedimentology of Ancient Reef Systems (159-203). New York: Kluwer
Academic/Plenum Publishers.