Paleoserenomyces

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Paleoserenomyces
Scientific classification OOjs UI icon edit-ltr.svg
Domain: Eukaryota
Kingdom: Fungi
Division: Ascomycota
Class: Sordariomycetes
Order: Phyllachorales
Family: incertae sedis
Genus:† Paleoserenomyces
Currah, Stockey & LePage 1998
Species:
†P. allenbyensis
Binomial name
†Paleoserenomyces allenbyensis
Currah, Stockey & LePage 1998

Paleoserenomyces is an extinct monotypic genus of pleosporale fungus of uncertain family placement. When described it contained the single species Paleoserenomyces allenbyensis. The genus is solely known from the Early Eocene, Ypresian aged, Princeton Chert deposit of the Allenby Formation. Palaeoserenomyces is one of only three described fossil fungus species found in the Princeton Chert, being a tar spot like parasite of the fossil palm Uhlia allenbyensis , and is host for the hyperparasite Cryptodidymosphaerites princetonensis .

Contents

History and classification

The type series of fossils were first identified in serial thin section cellulose acetate peels of Uhlia allenbyensis fossils. The peels were made with hydrofluoric acid and mounted in Eukitt mounting material, than affixed to microscope slides using double sided tape. The holotype and paratype microscope slides were accessioned into the University of Alberta palaeobotanical collections and the formal description of the new genus and species was published by Randolph Currah, Ruth Stockey, and Ben LePage (1998) in the journal Mycologia . [1] The researchers formed the genus name as combination of the name Serenomyces , a modern genus of phaeochoraceous sac fungi, plus the prefix paleo- denoting its status as a fossil. They chose the specific epithet allenbyensis as a reference to the mining ghost town of Allenby in Canada that is also the namesake of the type locality's parent formation. [1]

The family affiliation of P. allenbyensis is undetermined, with Currah, Stockey, and LePage (1998) only assigning to the order Phyllachorales [1] a placement which is used by some fungal databases [2] while other databases only place the genus to the division Ascomycota. [3] [4]

Description

Paleoserenomyces allenbyensis stromata are darker in coloration than the Uhlia allenbyensis host cells, from which the infections can be present on either the upper or lower leaf surface. The individual stomata are around 3 mm (0.12 in) thick and up to 13 cm (5.1 in) long. Stromata cell walls comprise an inner layer of column shaped cells, round in cross-section, and an outer layer of infected leaf epidermal tissue. [1] They are polyloculate, with the 240–480 μm (0.0094–0.0189 in) around by 180–240 μm (0.0071–0.0094 in)-thick locules formed in a layer within the stromata. Each locule has an aperture formed on the tip of a round umbo, and the locule walls are formed of two to four layers of hyphae. None of the described fossil material had any sexual or asexual cells present, possibly dues to parasitization of the locules by Cryptodidymosphaerites princetonensis . [1]

Distribution

Close up of Princeton Chert outcrop showing volcanic ash (white layer at base), peaty coal (dark layer), and Chert layers (grey). Layer 36 is labelled. Princeton Chert sequence .jpg
Close up of Princeton Chert outcrop showing volcanic ash (white layer at base), peaty coal (dark layer), and Chert layers (grey). Layer 36 is labelled.

Paleoserenomyces is known exclusively from the Princeton Chert, a fossil locality in British Columbia, Canada, [1] which comprises an anatomically preserved flora of Eocene Epoch age, with rich species abundance and diversity. The chert is located in exposures of the Allenby Formation on the east bank of the Similkameen River, 8.5 km (5.3 mi) south of the town of Princeton, British Columbia. [5]

Notable in conjunction with the coal seams of the Allenby Formation are sections of chert which formed during silica-rich periods. The rapid cyclical changes from coal to chert and back are not noted in any other fossil locality in the world. An estimated 49 coal-chert cycles are known, though the exact conditions for this process are not well understood. Silica-rich volcanic episodes in the region during deposition would have been needed for formation of the cherts, while slowly moving waters and gently subsiding terrains would be needed for the peats and fens to accumulate. Rates of organic deposition in swamps have been estimated at approximately 0.5–1 mm (0.02–0.04 in) in modern temperate climates, this suggests the time needed for each 10–20 cm (4–8 in) chert layer would be at least 100 years or more, with the full sequence of cycles taking place over no more than 15,000 years. [6]

The Allenby Formation is one of the southern-most of the Eocene Okanagan Highlands Lagerstätten in British Columbia, with the Canadian Penticton Group at the international border and the Klondike Mountain Formation of Republic, Washington in northern Ferry County to the south. The highlands, including the Allenby Formation, have been described as one of the "Great Canadian Lagerstätten" [7] based on the diversity, quality and unique nature of the biotas that are preserved. The Eocene Okanagan Highlands temperate-subtropical biome preserved across a large transect of lakes recorded many of the earliest appearances of modern genera, while also documenting the last stands of ancient lines. [7]

Paleoecology

Paleoserenomyces allenbeyensis was a parasitic fungus, invading the surface cells of Uhlia allenbyensis palm leaves resulting in areas considered to be similar to modern "tar spot" infections on leaves. Within the tissues of P. allenbeyensis, the hyperparasitic fungus, Cryptodidymosphaerites princetonensis would invade cells and develop within the stromata locules. The layered parasitic symbiosis of the palm and fungus suggests the relation between certain palms and tar spot forming Phyllachorales existed from at least 50  million years ago. [1]

Paleoenvironment

The Princeton chert preserves an aquatic system with silica rich slow moving waters which was likely a peat–fen ecosystem. While other fossil producing areas of the Allenby Formation are likely the product of deep water deposition and diatomite sedimentation, the chert layers originate from shallow waters, as evidenced by plant and animal fossils. [6] The Okanagan Highland sites, such as the Princeton chert represent upland lake systems that were surrounded by a warm temperate ecosystem with nearby volcanism. [7] The highlands likely had a mesic upper microthermal to lower mesothermal climate, in which winter temperatures rarely dropped low enough for snow, and which were seasonably equitable. [8] The Okanagan Highlands paleoforest surrounding the lakes have been described as precursors to the modern temperate broadleaf and mixed forests of Eastern North America and Eastern Asia. Based on the fossil biotas the lakes were higher and cooler than the coeval coastal forests preserved in the Puget Group and Chuckanut Formation of Western Washington, which are described as lowland tropical forest ecosystems. Estimates of the paleoelevation range between 0.7–1.2 km (0.43–0.75 mi) higher than the coastal forests. This is consistent with the paleoelevation estimates for the lake systems, which range between 1.1–2.9 km (1,100–2,900 m), which is similar to the modern elevation 0.8 km (0.50 mi), but higher. [8]

Estimates of the mean annual temperature have been derived from climate leaf analysis multivariate program (CLAMP) analysis and leaf margin analysis (LMA) the Princeton paleoflora. The CLAMP results after multiple linear regressions for Princeton's gave a 5.1 °C (41.2 °F), and the LMA returned a mean annual temperature of 5.1 ± 2.2 °C (41.2 ± 4.0 °F). This is lower than the mean annual temperature estimates given for the coastal Puget Group, which is estimated to have been between 15–18.6 °C (59.0–65.5 °F). The bioclimatic analysis for Princeton suggest mean annual precipitation amount of 114 ± 42 cm (45 ± 17 in). [8] The warm temperate uplands floras of the Allenby Formation and greater highlands in association with downfaulted lacustrine basins and active volcanism are noted to have no exact modern equivalents. This is due to the more seasonally equitable conditions of the Early Eocene, resulting in much lower seasonal temperature shifts. The highlands, however, have been compared to the upland ecological islands in the Virunga Mountains within the Albertine Rift of the African rift valley. [9]

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<span class="mw-page-title-main">Princeton Chert</span> Fossilized Flora

The Princeton Chert is a fossil locality in British Columbia, Canada, which comprises an anatomically preserved flora of Eocene Epoch age, with rich species abundance and diversity. It is located in exposures of the Allenby Formation on the east bank of the Similkameen River, 8.5 km (5.3 mi) south of the town of Princeton, British Columbia.

<span class="mw-page-title-main">McAbee Fossil Beds</span> Fossil bed in the Interior of British Columbia

<span class="mw-page-title-main">Allenby Formation</span>

The Allenby formation is a sedimentary rock formation in British Columbia which was deposited during the Ypresian stage of the Early Eocene. It consists of conglomerates, sandstones with interbedded shales and coal. The shales contain an abundance of insect, fish and plant fossils known from 1877 and onward, while the Princeton Chert was first indented in the 1950's and is known from anatomically preserved plants.

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<i>Comptonia columbiana</i> Extinct species of sweet fern

Comptonia columbiana is an extinct species of sweet fern in the flowering plant family Myricaceae. The species is known from fossil leaves found in the early Eocene deposits of central to southern British Columbia, Canada, plus northern Washington state, United States, and, tentatively, the late Eocene of Southern Idaho and Earliest Oligocene of Oregon, United States.

<i>Amia</i>? <i>hesperia</i> Extinct species of ray-finned fishes

Amia? hesperia is an extinct species of bony fish in the bowfin family, Amiidae. The species is known from fossils found in the early Eocene deposits of northern Washington state in the United States and southeastern British Columbia. The species is one of eight fish species identified in the Eocene Okanagan Highlands paleofauna.

<i>Equisetum similkamense</i> Extinct species of fern in the family Equisetacae

Equisetum similkamense is an extinct horsetail species in the family Equisetaceae described from a group of whole plant fossils including rhizomes, stems, and leaves. The species is known from Ypresian sediments exposed in British Columbia, Canada. It is one of several extinct species placed in the living genus Equisetum.

The paleoflora of the Eocene Okanagan Highlands includes all plant and fungi fossils preserved in the Eocene Okanagan Highlands Lagerstätten. The highlands are a series of Early Eocene geological formations which span an 1,000 km (620 mi) transect of British Columbia, Canada and Washington state, United States and are known for the diverse and detailed plant fossils which represent an upland temperate ecosystem immediately after the Paleocene-Eocene thermal maximum, and before the increased cooling of the middle and late Eocene to Oligocene. The fossiliferous deposits of the region were noted as early as 1873, with small amounts of systematic work happening in the 1880-90s on British Columbian sites, and 1920-30s for Washington sites. A returned focus and more detailed descriptive work on the Okanagan Highlands sites revived in the 1970's. The noted richness of agricultural plant families in Republic and Princeton floras resulted in the term "Eocene orchards" being used for the paleofloras.

<i>Fagus langevinii</i> Fossil species of beech tree

Fagus langevinii is an extinct species of beech in the family Fagaceae. The species is known from fossil fruits, nuts, pollen, and leaves found in the early Eocene deposits of South central British Columbia, and northern Washington state, United States.

<i>Plecia canadensis</i> Extinct species of flies

Plecia canadensis is an extinct species of Plecia in the fly family Bibionidae. The species is solely known from Early Eocene sediments exposed in central southern British Columbia. The species is one of twenty bibionid species described from the Eocene Okanagan Highlands paleofauna.

<span class="mw-page-title-main">Eocene Okanagan Highlands</span>

The Eocene Okanagan Highlands or Eocene Okanogan Highlands are a series of Early Eocene geological formations which span a 1,000 km (620 mi) transect of British Columbia, Canada, and Washington state, United States. Known for a highly diverse and detailed plant and animal paleobiota the paleolake beds as a whole are considered one of the great Canadian Lagerstätten. The paleobiota represented are of an upland subtropical to temperate ecosystem series immediately after the Paleocene–Eocene thermal maximum, and before the increased cooling of the middle and late Eocene to Oligocene. The fossiliferous deposits of the region were noted as early as 1873, with small amounts of systematic work happening in the 1870–1920s on British Columbian sites, and 1920–1930s for Washington sites. Focus and more detailed descriptive work on the Okanagan Highland sites started in the late 1960s.

The paleofauna of the Eocene Okanagan Highlands is comprised of Early Eocene arthropods, vertebrates, plus rare nematodes and molluscs found in geological formations of the northwestern North American Eocene Okanagan Highlands. The highlands lake bed series' as a whole are considered one of the great Canadian Lagerstätten. The paleofauna represents that of a late Ypresian upland temperate ecosystem immediately after the Paleocene-Eocene thermal maximum, and before the increased cooling of the middle and late Eocene to Oligocene. The fossiliferous deposits of the region were noted as early as 1873, with small amounts of systematic work happening in the 1880-90s on British Columbian sites, and 1920-30s for Washington sites. Focus and more detailed descriptive work on the Okanagan Highlands site started in the last 1970's. Most of the highlands sites are preserved as compression-impression fossils in "shales", but also includes a rare permineralized biota and an amber biota.

Uhlia is an extinct genus of coryphoid palm containing a single species Uhlia allenbyensis. The species is known from permineralized remains recovered from the Princeton Chert in British Columbia, Canada. Leaves of Uhlia have "tar spot"-like fungal infections of the extinct ascomycete Paleoserenomyces, which in turn are hyperparasitized by the ascomycete Cryptodidymosphaerites.

Cryptodidymosphaerites is an extinct monotypic genus of pleosporale fungus of uncertain family placement. When described it contained the single species Cryptodidymosphaerites princetonensis. The genus is solely known from the Early Eocene, Ypresian aged, Princeton Chert deposit of the Allenby Formation. Cryptodidymosphaerites is one of only three described fossil fungus species found in the Princeton Chert, and is a hyperparasite of Palaeoserenomyces allenbyensis, itself a tar spot-like parasite of the fossil palm Uhlia.

Eoseira is an extinct genus of diatoms belonging to the family Aulacoseiraceae and containing the single species Eoseira wilsonii. The species is dated to the Early Eocenes Ypresian stage and have only been found at the type locality in east central British Columbia.

<i>Plecia avus</i> Extinct species of March fly

Plecia avus is an extinct species of Plecia in the March fly family Bibionidae and is solely known from Early Eocene sediments exposed in central southern British Columbia. The species is one of twenty bibionid species described from the Eocene Okanagan Highlands.

References

  1. 1 2 3 4 5 6 7 Currah, R.S.; Stockey, R.A.; LePage, B.A. (1998). "An Eocene Tar Spot on a Fossil Palm and its Fungal Hyperparasite". Mycologia. 90 (4): 667–673. doi:10.1080/00275514.1998.12026955.
  2. ↑ "Paleoserenomyces allenbyensis". The Kalgutkar and Jansonius Database of Fossil Fungi. AASP – The Palynological society. Retrieved 27 February 2022.
  3. ↑ Bensch, K. "Paleoserenomyces". Mycobank. International Mycological Association (IMA) and the Westerdijk Fungal Biodiversity Institute. Retrieved 27 February 2022.
  4. ↑ Bensch, K. "Paleoserenomyces allenbyensis". Mycobank. International Mycological Association (IMA) and the Westerdijk Fungal Biodiversity Institute. Retrieved 27 February 2022.
  5. ↑ Miller, C. (1975). "Silicified Cones and Vegetative Remains of Pinus from the Eocene of British Columbia". Contributions from the Museum of Paleontology, University of Michigan. 24 (10): 101–118.
  6. 1 2 Mustoe, G. (2010). "Cyclic Sedimentation in the Eocene Allenby Formation of South-central British Columbia and the Origin of the Princeton Chert Fossil Beds". Canadian Journal of Earth Sciences. 48 (1): 25–43. doi:10.1139/e10-085.
  7. 1 2 3 Archibald, S.; Greenwood, D.; Smith, R.; Mathewes, R.; Basinger, J. (2011). "Great Canadian Lagerstätten 1. Early Eocene Lagerstätten of the Okanagan Highlands (British Columbia and Washington State)". Geoscience Canada. 38 (4): 155–164.
  8. 1 2 3 Greenwood, D.R.; Archibald, S.B.; Mathewes, R.W; Moss, P.T. (2005). "Fossil Biotas from the Okanagan Highlands, Southern British Columbia and Northeastern Washington State: Climates and ecosystems across an Eocene landscape" (PDF). Canadian Journal of Earth Sciences. 42 (2): 167–185. Bibcode:2005CaJES..42..167G. doi:10.1139/e04-100.
  9. ↑ DeVore, M. L.; Nyandwi, A.; Eckardt, W.; Bizuru, E.; Mujawamariya, M.; Pigg, K. B. (2020). "Urticaceae leaves with stinging trichomes were already present in latest early Eocene Okanogan Highlands, British Columbia, Canada". American Journal of Botany. 107 (10): 1449–1456. doi: 10.1002/ajb2.1548 . PMID   33091153. S2CID   225050834.
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