Conodont biostratigraphy

Conodonts are an extinct class of animals whose feeding apparatuses called teeth or elements are common microfossils found in strata dating from the Stage 10 of the Furongian, the fourth and final series of the Cambrian, to the Rhaetian stage of the Late Triassic. These elements can be used alternatively to or in correlation with other types of fossils (graptolites, trilobites, ammonites, ...) in the subfield of the stratigraphy named biostratigraphy.

Paleozoic conodonts

Cambrian conodonts

It has been suggested that Eoconodontus notchpeakensis can be a marker of Stage 10, the final stage of the Cambrian.^[1]

In 2006, a working group proposed the first appearance of Cordylodus andresi. Currently the first appearance of E. notchpeakensis is favored by many authors because it is globally widespread and is independent of facies (known from continental rise to peritidal environments).

The Eoconodontus notchpeakensis proposal would also incorporate a non-biostratigraphic marker to correlate the beginning of Stage 10 globally. A carbon isotope excursion (the HERB-event) occurs in the lower part of the E. notchpeakensis range.

Approximate protoconodont / paraconodont / euconodont zones of the Cambrian Period
Series / Epoch	Age /Stage	South China^[2]^[3]	Western North America^[4]^[5]^[1]^[6]	Australia^[7]
Furongian	"Stage 10"	upper Cordylodus lindstromi	Cordylodus lindstromi sensu lato (upper sz)	Cordylodus lindstromi (in part)
		lower Cordylodus lindstromi	Cordylodus lindstromi sensu lato (lower sz)	Cordylodus prolindstromi
		Cordylodus intermedius	Cordylodus intermedius (Clavohamulus hintzei sz)	Hirsutodontus simplex (Clavohamulus hintzei sz)
		Cordylodus intermedius	Cordylodus intermedius (Hirsutodontus simplex sz)	Hirsutodontus simplex (Hirsutodontus simplex sz)
		Cordylodus proavus	Cordylodus proavus (Clavohamulus elongatus sz)	Cordylodus proavus (Clavohamulus elongatus sz)
			Cordylodus proavus (Fryxellodontus inornatus sz)	Cordylodus proavus (Fryxellodontus inornatus sz)
			Cordylodus proavus (Hirsutodontus hirsutus sz)	Cordylodus proavus (Hirsutodontus hirsutus sz)
		Eoconodontus	Eoconodontus (Cambrooistodus minutus sz)	Hispidodontus discretus
			Eoconodontus (Cambrooistodus minutus sz)	Hispidodontus appressus
			Eoconodontus (Eoconodontus notchpeakensis sz)	Hispidodontus resimus
	(debated)	Proconodontus	Proconodontus muelleri	Teridontus nakamurai
	(debated)	Proconodontus	Proconodontus posterocostatus	Teridontus nakamurai
	Jiangshanian	Proconodontus tenuiserratus	Proconodontus tenuiserratus
	Jiangshanian	Westergaardodina cf. calix - Prooneotodus rotundatus
	Paibian	Westergaardodina lui - Westergaardodina ani
Miaolingian	Guzhangian	Westergaardodina matsushitai - Westergaardodina grandidens
		Westergaardodina quadrata
		Shandongodus priscus - Hunanognathus tricuspidatus
	Drumian	Gapparodus bisulcatus - Westergaardodina brevidens
	Wuliuan
Series 2	"Stage 4"
Series 2	"Stage 3"
Terreneuvian	"Stage 2"
Terreneuvian	Fortunian

Ordovician conodonts

Early Ordovician

The base of the Tremadocian, the lowest stage of Ordovician, is defined as the first appearance of Iapetognathus fluctivagus at the GSSP section in Newfoundland.

No conodont species is associated with the Floian, the second stage of the Ordovician.

Middle Ordovician

The base of the Dapingian, the third stage of the Ordovician, is defined as the first appearance of Baltoniodus triangularis.

The base of the Darriwilian, the fourth stage of the Ordovician, lies just above the North Atlantic Microzarkodina parva conodont zone. The base also lies in the upper part of the North American Histiodella altifrons conodont zone.

The Whiterock Stage refers mainly to the early Middle Ordovician in North America. It is often used in the older literature in a global sense. The Whiterock Stage is given a range from 471.8 (ca. 472) to 462 m.y.a., spanning close to 10 million years. Officially its start is defined by the potentially lowest occurrence of the conodont Protoprioniodus aranda or Baltoniodus triangularis.

Late Ordovician

No conodont species is associated with the Sandbian, the Katian, nor with the Hirnantian, the fifth, sixth and seventh and final stages of the Ordovician.

Baltoniodus gerdae has been found in the early Sandbian Bromide Formation, in Oklahoma, United States.

Silurian conodonts

Llandovery

The Llandovery epoch lasted from 443.8 ± 1.5 to 433.4 ± 2.8 mya, and is subdivided into three stages: the Rhuddanian, lasting until 440.8 million years ago, the Aeronian, lasting to 438.5 million years ago, and the Telychian.

The Telychian (Late Llandovery) of Estonia can be defined by five conodont zones (Pterospathodus eopennatus ssp. n. 1, P. eopennatus ssp. n. 2, P. amorphognathoides angulatus, P. a. lennarti and P. a. lithuanicus).^[8]

Wenlock

The Wenlock, which lasted from 433.4 ± 1.5 to 427.4 ± 2.8 mya, is subdivided into the Sheinwoodian (to 430.5 million years ago) and Homerian ages.

The Sheinwoodian (Wenlock) is defined between the acritarch biozone 5 and the last appearance of Pterospathodus amorphognathoides. The global boundary stratotype point is in Hughley Brook in Apedale, U.K.

Ludlow

The Ludlow, lasting from 427.4 ± 1.5 to 423 ± 2.8 mya, comprises the Gorstian stage, lasting until 425.6 million years ago, and the Ludfordian stage.

Přídolí

Devonian conodonts

Early Devonian

The Early Devonian lasts from 419.2 ± 2.8 to 393.3 ± 2.5 and begins with the Lochkovian stage, which lasts until the Pragian. This spans from 410.8 ± 2.8 to 407.6 ± 2.5, and is followed by the Emsian, which lasts until the Middle Devonian begins, 393.3± 2.7 million years ago.

Middle Devonian

The Middle Devonian comprises two subdivisions, the Eifelian giving way to the Givetian 387.7± 2.7 million years ago.

Late Devonian

Finally, the Late Devonian starts with the Frasnian, 382.7 ± 2.8 to 372.2 ± 2.5, followed by the Famennian subdivision, the beginning and end of which are marked with extinction events. This lasted until the end of the Devonian, 358.9± 2.5 million years ago. During that stage, a biologic event occurred (Upper Kellwasser Extinction of all Ancyrodella and Ozarkodina and most Palmatolepis, Polygnathus and Ancyrognathus). The Famennian (372.2 ± 1.6 mya) is defined by a GSSP Golden Spike located at Coumiac quarry, Montagne Noire, France where there is a biologic abundant occurrence of Palmatolepis triangularis.

Carboniferous conodonts

Mississippian (also known as Lower Carboniferous)

The Tournaisian, the oldest age of the Mississippian contains eight conodont biozones:

the zone of Gnathodus pseudosemiglaber and Scaliognathus anchoralis
the zone of Gnathodus semiglaber and Polygnathus communis
the zone of Dollymae bouckaerti
the zone of Gnathodus typicus and Siphonodella isosticha
the zone of Siphonodella quadruplicata and Patrognathus andersoni (upper zone of Patrognathus andersoni)
the lower zone of Patrognathus andersoni
the zone of Patrognathus variabilis
the zone of Patrognathus crassus

The Visean, the second age of the Mississippian, contains four conodont biozones:

the zone of Lochriea nodosa
the zone of Lochriea mononodosa
the zone of Gnathodus bilineatus
the zone of Gnathodus texanus

The Serpukhovian, the third or youngest age of the Mississippian, includes four conodont biozones:

the zone of Gnathodus postbilineatus
the zone of Gnathodus bollandensis
the zone of Lochriea cruciformis
the zone of Lochriea ziegleri

Pennsylvanian (also known as Upper Carboniferous)

The Bashkirian, the oldest age of the Pennsylvanian, contains six biozones based on conodont index fossils:

the zone of Neognathodus atokaensis
the zone of Declinognathodus marginodosus
the zone of Idiognathodus sinuosus
the zone of Neognathodus askynensis
the zone of Idiognathoides sinuatus
the zone of Declinognathodus noduliferus

The base of the Moscovian, the second stage in the Pennsylvanian, is close to the first appearances of the conodonts Declinognathodus donetzianus and Idiognathoides postsulcatus. A proposal is to use the first appearance of the conodont Diplognathodus ellesmerensis, but since the species is rare and its evolution relatively unknown, it has not been accepted yet. The Moscovian can biostratigraphically be divided into five conodont biozones:

the zone of Neognathodus roundyi and Streptognathodus cancellosus
the zone of Neognathodus medexultimus and Streptognathodus concinnus
the zone of Streptognathodus dissectus
the zone of Neognathodus uralicus
the zone of Declinognathodus donetzianus

The top of the Kasimovian, the third stage in the Pennsylvanian, is close to the first appearance of the conodont Streptognathodus zethus. The Kasimovian is subdivided into three conodont biozones:

the zone of Idiognathodus toretzianus
the zone of Idiognathodus sagittatus
the zone of Streptognathodus excelsus and Streptognathodus makhlinae

The base of the Gzhelian, the youngest age of the Pennsylvanian, is at the first appearance of Streptognathodus zethus. The top of the stage (the base of the Permian system) is at the first appearance of Streptognathodus isolatus within the Streptognathus "wabaunsensis" chronocline. The Gzhelian stage is subdivided into five biozones, based on the conodont genus Streptognathodus:

the zone of Streptognathodus wabaunsensis and Streptognathodus bellus
the zone of Streptognathodus simplex
the zone of Streptognathodus virgilicus
the zone of Streptognathodus vitali
the zone of Streptognathodus simulator

Permian conodonts

Cisuralian

The base of the Asselian stage is at the same time the base of the Cisuralian series and the Permian system. It is defined as the place in the stratigraphic record where fossils of Streptognathodus isolatus first appear. The top of the Asselian stage (the base of the Sakmarian stage) is at the first appearance of conodont species Streptognathodus postfusus. The Asselian contains five conodont biozones:

the zone of Streptognathodus barskovi
the zone of Streptognathodus postfusus
the zone of Streptognathodus fusus
the zone of Streptognathodus constrictus
the zone of Streptognathodus isolatus

The base of the Sakmarian stage is laid with the first appearance of Streptognathodus postfusus in the fossil record. The top of the Sakmarian (the base of the Artinskian) is defined as the place in the stratigraphic record where fossils of Sweetognathus whitei and Mesogondolella bisselli first appear.

The base of the Artinskian stage is defined as the place in the stratigraphic record where fossils of Sweetognathus whitei and Mesogondolella bisselli first appear. The top of the Artinskian (the base of the Kungurian) is defined as the place in the stratigraphic record where fossils of Neostreptognathodus pnevi and Neostreptognathodus exculptus first appear.

The base of the Kungurian stage is defined as the place in the stratigraphic record where fossils of Neostreptognathodus pnevi and Neostreptognathodus exculptus first appear. The top of the Kungurian (the base of the Roadian and the Guadalupian series) is defined as the place in the stratigraphic record where fossils of Jinogondolella nanginkensis first appear. The Kungurian contains three conodont biozones:

the zone of Neostreptognathodus sulcoplicatus
the zone of Neostreptognathodus prayi
the zone of Neostreptognathodus pnevi

Guadalupian

The base of the Roadian is defined as the place in the stratigraphic record where fossils of Jinogondolella nankingensis first appears. The top of the Roadian (the base of the Wordian stage) is at the first appearance of fossils of Jinogondolella aserrata.

The base of the Wordian stage is defined as the place in the stratigraphic record where fossils of Jinogondolella aserrata first appear. The top of the Wordian (the base of the Capitanian stage) is defined as the place in the stratigraphic record where Jinogondolella postserrata first appears.

The base of the Capitanian stage is defined as the place in the stratigraphic record where fossils of Jinogondolella postserrata first appear. The top of the Capitanian (the base of the Wuchiapingian and Lopingian series) is defined as the place in the stratigraphic record where Clarkina postbitteri postbitteri first appears. The Capitanian contains three conodont biozones:

the zone of Clarkina postbitteri hongshuiensis
the zone of Jinogondolella altudaensis
the zone of Jinogondolella postserrata

Lopingian

The base of the Wuchiapingian stage is defined as the place in the stratigraphic record where Clarkina postbitteri postbitteri first appears. The top of the Wuchiapingian (the base of the Changhsingian) is at the first appearance of conodont species Clarkina wangi.

The base of the Changhsingian stage is at the first appearance of Clarkina wangi. The top of the Changhsingian (the base of the Induan stage and the Triassic system) is at the first appearance of Hindeodus parvus.

Mesozoic conodonts

Early Triassic

The base of the Induan stage (which is also the base of the Lower Triassic series, the base of the Triassic system and the base of the Mesozoic erathem) is defined as the place in the fossil record where Hindeodus parvus first appears.

The base of the Olenekian is at the lowest occurrence of Neospathodus waageni. It is defined as ending near the lowest occurrences of Chiosella timorensis.

Middle Triassic

The base of the Anisian stage (also the base of the Middle Triassic series) is sometimes laid at the first appearance of Chiosella timorensis in the stratigraphic record. The top of the Anisian (the base of the Ladinian) is at the first appearance of Neogondolella praehungarica.

The Ladinian is defined by the first appearance of Budurovignathus praehungaricus.

Upper Triassic

The top of the Carnian (the base of the Norian) is at the conodont biozones of Metapolygnathus communisti or Metapolygnathus primitius.

The Norian stage begins at the base of the conodont biozones of Metapolygnathus communisti and Metapolygnathus primitius. The top of the Norian (the base of the Rhaetian) is close to the first appearance of Misikella spp. and Epigondolella mosheri.

The Alaunian, also known as "Middle Norian", is a sub-age in the Upper Triassic. It begins with the first appearance of Cypridodella multidentata. The stage ends with the first appearance of Cypridodella bidentata.

References

^ ^a ^b Miller, James F.; Evans, Kevin R.; Freeman, Rebecca L.; Loch, James D.; Ripperdan, Robert L.; Taylor, John F. (2018). "Combining biostratigraphy, carbon isotope stratigraphy and sequence stratigraphy to define the base of Cambrian Stage 10". Australasian Palaeontological Memoirs (51): 19–64.
^ Dong, Xiping; Repetski, John E.; Bergström, Stig M. (2004). "Conodont Biostratigraphy of the Middle Cambrian through Lowermost Ordovician in Hunan, South China". Acta Geologica Sinica - English Edition. 78 (6): 1185–1206. Bibcode:2004AcGlS..78.1185D. doi:10.1111/j.1755-6724.2004.tb00776.x. ISSN 1000-9515.
^ Dong, Xi-ping; Zhang, Huaqiao (2017). "Middle Cambrian through lowermost Ordovician conodonts from Hunan, South China". Journal of Paleontology. 91 (S73): 1–89. Bibcode:2017JPal...91S...1D. doi:10.1017/jpa.2015.43. ISSN 0022-3360.
^ Miller, J. F. (1988). "Conodonts as biostratigraphic tools for redefinition and correlation of the Cambrian–Ordovician Boundary". Geological Magazine. 125 (4): 349–362. Bibcode:1988GeoM..125..349M. doi:10.1017/S0016756800013029. ISSN 0016-7568.
^ Miller, James F.; Ethington, Raymond L.; Evans, Kevin R.; Holmer, Lars E.; Loch, James D.; Popov, Leonid E.; Repetski, John E.; Ripperdan, Robert L.; Taylor, John F. (2006). "Proposed stratotype for the base of the highest Cambrian stage at the first appearance datum of Cordylodus andresi, Lawson Cove section, Utah, USA". Palaeoworld. 15 (3–4): 384–405. doi:10.1016/j.palwor.2006.10.017.
^ Miller, James F. (2020). "Study and Use of Upper Cambrian to Lower Ordovician conodonts in central, southern, and western Laurentia, 1933–2018". Palaeobiodiversity and Palaeoenvironments. 100 (1): 95–133. Bibcode:2020PdPe..100...95M. doi:10.1007/s12549-019-00380-9. ISSN 1867-1594.
^ Shergold, John H.; Nicoll, Robert S.; Laurie, John R.; Radke, Bruce M. (1991). "The Cambrian - Ordovician boundary at Black Mountain, western Queensland: Sixth International Symposium on the Ordovician System, Guidebook for Field Excursion 1". Bureau of Mineral Resources, Geology and Geophysics (48): 1–50.
^ An updated Telychian (Late Llandovery, Silurian) conodont zonation based on Baltic faunas. Peep Männik, Lethaia, Volume 40, Issue 1, pp. 45–60, March 2007, doi:10.1111/j.1502-3931.2006.00005.x

External links

"The Most Useful Fossils in the World". PBS Eons. March 26, 2018 – via YouTube.

[:0-1] Miller, James F.; Evans, Kevin R.; Freeman, Rebecca L.; Loch, James D.; Ripperdan, Robert L.; Taylor, John F. (2018). "Combining biostratigraphy, carbon isotope stratigraphy and sequence stratigraphy to define the base of Cambrian Stage 10". Australasian Palaeontological Memoirs (51): 19–64.

[2] Dong, Xiping; Repetski, John E.; Bergström, Stig M. (2004). "Conodont Biostratigraphy of the Middle Cambrian through Lowermost Ordovician in Hunan, South China". Acta Geologica Sinica - English Edition. 78 (6): 1185–1206. Bibcode:2004AcGlS..78.1185D. doi:10.1111/j.1755-6724.2004.tb00776.x. ISSN 1000-9515.

[3] Dong, Xi-ping; Zhang, Huaqiao (2017). "Middle Cambrian through lowermost Ordovician conodonts from Hunan, South China". Journal of Paleontology. 91 (S73): 1–89. Bibcode:2017JPal...91S...1D. doi:10.1017/jpa.2015.43. ISSN 0022-3360.

[4] Miller, J. F. (1988). "Conodonts as biostratigraphic tools for redefinition and correlation of the Cambrian–Ordovician Boundary". Geological Magazine. 125 (4): 349–362. Bibcode:1988GeoM..125..349M. doi:10.1017/S0016756800013029. ISSN 0016-7568.

[5] Miller, James F.; Ethington, Raymond L.; Evans, Kevin R.; Holmer, Lars E.; Loch, James D.; Popov, Leonid E.; Repetski, John E.; Ripperdan, Robert L.; Taylor, John F. (2006). "Proposed stratotype for the base of the highest Cambrian stage at the first appearance datum of Cordylodus andresi, Lawson Cove section, Utah, USA". Palaeoworld. 15 (3–4): 384–405. doi:10.1016/j.palwor.2006.10.017.

[6] Miller, James F. (2020). "Study and Use of Upper Cambrian to Lower Ordovician conodonts in central, southern, and western Laurentia, 1933–2018". Palaeobiodiversity and Palaeoenvironments. 100 (1): 95–133. Bibcode:2020PdPe..100...95M. doi:10.1007/s12549-019-00380-9. ISSN 1867-1594.

[7] Shergold, John H.; Nicoll, Robert S.; Laurie, John R.; Radke, Bruce M. (1991). "The Cambrian - Ordovician boundary at Black Mountain, western Queensland: Sixth International Symposium on the Ordovician System, Guidebook for Field Excursion 1". Bureau of Mineral Resources, Geology and Geophysics (48): 1–50.

[8] An updated Telychian (Late Llandovery, Silurian) conodont zonation based on Baltic faunas. Peep Männik, Lethaia, Volume 40, Issue 1, pp. 45–60, March 2007, doi:10.1111/j.1502-3931.2006.00005.x

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