Silurian-Devonian Terrestrial Revolution

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Artist interpretation of a Devonian swamp forest scene. Artwork by Eduard Riou from The World Before the Deluge 1872 Devonianscene.jpg
Artist interpretation of a Devonian swamp forest scene. Artwork by Eduard Riou from The World Before the Deluge 1872

The Silurian-Devonian Terrestrial Revolution, also known as the Devonian Plant Explosion (DePE) [1] and the Devonian explosion, was a period of rapid colonization, diversification and radiation of land plants and fungi on dry lands that occurred 428 to 359 million years ago (Mya) during the Silurian and Devonian periods, [2] [3] [4] with the most critical phase occurring during the Late Silurian and Early Devonian. [5]

Contents

This diversification of terrestrial photosynthetic florae had vast impacts on the biotic composition of the Earth's surface, especially upon the Earth's atmosphere by oxygenation and carbon fixation. Their roots also eroded into the rocks, creating a layer of water-holding and mineral/organic matter-rich soil on top of Earth's crust (known as the pedosphere), and significantly altering the chemistry of Earth's lithosphere and hydrosphere. The floral activities following the Silurian-Devonian plant revolution also exerted significant influences on changes in the water cycle and global climate, as well as driving the biosphere by creating diverse layers of vegetations that provide both sustenance and refuge for both upland and wetland habitats, paving the way for all terrestrial and aquatic biomes that would follow. [6]

Through fierce competition for sunlight, soil nutrients and available land space, phenotypic diversity of plants increased greatly during the Silurian and Devonian periods, comparable in scale and effect to the explosion in diversity of animal life during the Cambrian explosion, [7] especially in vertical growth of vascular plants, which allowed for expansive canopies to develop, and forever altering the plant evolutions that followed. As plants evolved and radiated, so did arthropods, who became the first established terrestrial animals and some formed symbiotic coevolution with plants. [8] Herbivory, granivory and detritivory subsequently evolved independently among terrestrial arthropods (especially hexapods such as insects, as well as myriapods), molluscs (land snails and slugs) and tetrapod vertebrates, causing plants to in turn develop defenses against foraging by animals.

The Silurian and Devonian terrestrial florae were largely spore-bearing plants and significantly different in appearance, anatomy and reproductive strategies to most modern florae, which are dominated by fleshy seed-bearing angiosperms that evolved much later during the Early Cretaceous. Much of these Silurian-Devonian florae had died out in extinction events including the Kellwasser event, the Hangenberg event, the Carboniferous rainforest collapse, and the End-Permian extinction. [9] [10]

Silurian and Devonian life

Rather than plants, it was fungi, in particular nematophytes such as Prototaxites , that dominated the early stages of this terrestrial biodiversification event. Nematophytes towered over even the largest land plants during the Silurian and Early Devonian, only being truly surpassed in size in the Early Carboniferous. The nutrient-distributing glomeromycotan mycorrhizal networks of nematophytes were very likely to have acted as facilitators for the expansion of plants into terrestrial environments, which followed the colonising fungi. [11] The first fossils of arbuscular mycorrhizae, a type of symbiosis between fungi and vascular plants, are known from the Early Devonian. [12]

Land plants probably evolved in the Ordovician. [13] The earliest radiations of the first land plants, also known as embryophytes, were bryophytes, which began to transform terrestrial environments and the global climate in the Ordovician. [14] [15] [16] Baltica was a particularly important cradle for early land plant evolution, with it having a diverse flora by the Darriwilian. [17] ∆199Hg and ∆200Hg excursions reveal that land plants had already spread across much of the Earth's land surface by the Early Silurian. [18] The end of the Homerian glaciation, a glacial phase of the Early Palaeozoic Ice Age, and the corresponding period of global warming marked the first major diversification of plants that produced trilete spores. The later glaciation during the middle Ludfordian, corresponding to the Lau event, led to a major marine regression, creating significant areas of new dry land habitat that were colonised by plants, along with cyanobacterial mats. These newly created terrestrial habitats helped facilitate the global expansion and evolutionary radiation of polysporangiophytes. [19] A warming climate during the subsequent Pridoli epoch lent itself to further floral diversification. [20] During the Wenlock epoch of the Silurian, the first fossils of vascular plants appear in the fossil record in the form of sporophytes of polysporangiophytes. [21] Clubmosses first appeared during the later Ludlow epoch. [22] Palynological evidence points to Silurian terrestrial floras exhibiting little provincialism relative to present day floras that vary significantly by region, instead being broadly similar across the globe. [23] Plant diversification in the Silurian was aided by the presence of numerous small, rapidly changing volcanic islands in the Rheic Ocean that acted as natural laboratories accelerating evolutionary changes and enabling distinct, endemic floral lineages to arise. [24] Silurian plants rarely reached large sizes, with heights of 13 cm, achieved by Tichavekia grandis, being exceptionally large for the time. [25]

The Devonian witnessed the widespread greening of the Earth's surface, [26] with many modern vascular plant clades originating during this period. Basal members of Euphyllophytina, the clade that includes trimerophytes, ferns, progymnosperms, and seed plants, are known from Early Devonian fossils. [27] Lycopsids experienced their first evolutionary radiation during the Devonian period. [13] Early Devonian plant communities were generally similar regardless of what landmass they inhabited. [28]

In the Middle Devonian, euphyllophytes continued to increase in diversity. [29] The first true forest environments featuring trees exceeding eight metres in height emerged by the Middle Devonian, [30] with the earliest known fossil forest dating to the Eifelian. [31] The oldest known trees were members of the clade Cladoxylopsida. [32] Devonian swamp forests were dominated by giant horsetails (Equisetales), clubmosses, ancestral ferns (pteridophytes), and large lycophyte vascular plants such as Lepidodendrales, referred to as scale trees for the appearance of scales on their photosynthetic trunks. These lycophytes, which could grow up to 40 metres high, grew in great numbers around swamps along with tracheophytes. [9] Seed ferns and true leaf-bearing plants such as progymnosperms also appeared at this time and became dominant in many habitats, particularly archeopteridaleans, which were likely related to conifers. [33] Pseudosporochnaleans (morphologically similar to palms and tree ferns) likewise experienced a similar rise to dominance. [34] Archeopteridaleans had likely developed extensive root systems, making them resistant to drought, and meaning they had a more significant impact on Devonian soil environments than pseudosporochnaleans. [35]

The Late Devonian saw the most rapid land plant diversification of the Devonian, largely owing to the rapid radiation of pteridophytes and progymnosperms. [36] Cladoxylopsids continued to dominate forest ecosystems during the early Late Devonian. [32] During the latest Devonian, the first true spermatophytes appeared, evolving as a sister group to archaeopteridaleans or to progymnosperms as a whole. [37]

Most flora in Devonian coal swamps would have seemed alien in appearance when compared with modern flora, such as giant horsetails which could grow up to 30 m in height. Devonian ancestral plants of modern plants that may have been very similar in appearance are ferns (Polypodiopsida), although many of them are thought to have been epiphytes rather than grounded plants. True gymnosperms like ginkgos (Ginkgophyta) and cycads (Cycadophyta) would appear slightly after the Devonian in the Carboniferous. [9]

Vascular plant lineages of sphenoids, fern, progymnosperms, and seed plants evolved laminated leaves during the Devonian. Plants that possessed true leaves appeared during the Devonian, though they may have many independent origins with parallel trajectories of leaf morphologies. Morphological evidence to support this diversification theory appears in the Late Devonian or Early Carboniferous when compared with modern leaf morphologies. The marginal meristem also evolved in a parallel fashion through a similar process of modified structures around this time period. [38] In a 1994 study by Richard M Bateman and William A. Dimechele of the evolutionary history of heterospory in the plant kingdom, researchers found evidence of 11 origins of heterospory events that had occurred independently in the Devonian within Zosterophyllopsida, Sphenopsida, Progymnospermopsida. The effect of this heterospory was that it presented a primary evolutionary advantage for these plants in colonizing land. [39] The simultaneous colonization of dry land and increase in plant body size that many lineages underwent during this time was likely facilitated by another parallel development: the replacement of the ancestral central cylinder of xylem with more elongate, complex xylem strand shapes that would have made the plant body more resistant to the spread of drought-induced embolism. [40] Tracheids, tapered cells that make up the xylem of vascular plants, first appear in the fossil record during the Early Devonian. [30] Woody stems evolved during the Devonian as well, with the first evidence of them dating back to the Early Devonian. [41] Evidence of root structures appears for the first time during the Late Silurian. [42] Further appearances of roots in the fossil record are found in Early Devonian lycophytes, [43] and it has been suggested that the development of roots was an adaptation for maximising water acquisition in response to the increase in aridity over the course of the Silurian and Devonian. [44] The Early Devonian also saw the appearance of complex subterranean rhizome networks. [45]

Effect on atmosphere, soil, and climate

Deep-rooted vascular plants had drastic impacts upon soil, atmosphere, and oceanic oxygen composition. The Devonian Plant Hypothesis is an explanation about these effects upon biogeomorphic ecosystems of climate and marine environments. [6] A climate/carbon/vegetation model could explain the effects of plant colonization during the Devonian. Expansion of terrestrial Devonian flora modified soil properties, increasing silicate weathering by way of rhizosphere development as evidenced by pedogenic carbonates. [46] This caused atmospheric CO2 levels to fall from around 6300 to 2100 ppmv, although it also drastically reduced the albedo of much of Earth's land surface, retarding the cooling effects of this greenhouse gas drawdown. [47] The biological sequestration of so much carbon dioxide resulted in the beginning of the Late Palaeozoic Ice Age at the terminus of the Devonian, [48] [49] [50] together with the tectonic uplift of the continent Gondwana. [51]

Oxygen levels rose as a direct result of plant expansion. [47] With increased oxygenation came increased fire activity. [52] Earth's atmosphere first became sufficiently high in oxygen to produce wildfires in the Pridoli, when the first charcoal evidence of wildfires is recorded. [53] For most of the Early and Middle Devonian, the atmosphere was insufficiently oxygenated to enable significant fire activity. [54] By the late Famennian, however, oxygen levels were high enough to enable wildfires to occur with regularity and on large scales, [55] something which had not been previously possible due to the paucity of atmospheric oxygen. [56]

The rise of trees and forests caused greater amounts of fine sediment particles to be retained on alluvial plains, increasing the complexity of meandering and braided fluvial systems. The greater complexity of terrestrial habitats facilitated the colonisation of the land by arthropods. Additionally, the increased weathering of phosphates and quantity of terrestrial humic matter increased nutrient levels in freshwater lakes, facilitating their colonisation by freshwater vertebrates. From these lakes, vertebrates would later follow arthropods in their conquest of the land. [57]

The Devonian explosion had global consequences on oceanic nutrient content and sediment cycling, which had led to the Devonian mass extinction. The expansion of trees in the Late Devonian drastically increased biological weathering rates and the consequent riverine input of nutrients into the ocean. [58] [59] [60] The altering of soil composition created anoxic sedimentation (or black shales), oceanic acidification, and global climate changes. This led to harsh living conditions for oceanic and terrestrial life. [61]

The increase in terrestrial plant matter in swamplands explains the deposits of coal and oil that would later characterize the Carboniferous. [9]

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The Devonian is a geologic period and system of the Paleozoic era during the Phanerozoic eon, spanning 60.3 million years from the end of the preceding Silurian period at 419.2 million years ago (Ma), to the beginning of the succeeding Carboniferous period at 358.9 Ma. It is named after Devon, South West England, where rocks from this period were first studied.

<span class="mw-page-title-main">Ordovician</span> Second period of the Paleozoic Era 485–444 million years ago

The Ordovician is a geologic period and system, the second of six periods of the Paleozoic Era. The Ordovician spans 41.6 million years from the end of the Cambrian Period 485.4 million years ago (Ma) to the start of the Silurian Period 443.8 Mya.

The PaleozoicEra is the first of three geological eras of the Phanerozoic Eon. Beginning 538.8 million years ago (Ma), it succeeds the Neoproterozoic and ends 251.9 Ma at the start of the Mesozoic Era. The Paleozoic is subdivided into six geologic periods :

<span class="mw-page-title-main">Permian–Triassic extinction event</span> Earths most severe extinction event

Approximately 251.9 million years ago, the Permian–Triassicextinction event forms the boundary between the Permian and Triassic geologic periods, and with them the Paleozoic and Mesozoic eras. It is the Earth's most severe known extinction event, with the extinction of 57% of biological families, 83% of genera, 81% of marine species and 70% of terrestrial vertebrate species. It is also the greatest known mass extinction of insects. It is the greatest of the "Big Five" mass extinctions of the Phanerozoic. There is evidence for one to three distinct pulses, or phases, of extinction.

<span class="mw-page-title-main">Silurian</span> Third period of the Paleozoic Era, 443–419 million years ago

The Silurian is a geologic period and system spanning 24.6 million years from the end of the Ordovician Period, at 443.8 million years ago (Mya), to the beginning of the Devonian Period, 419.2 Mya. The Silurian is the shortest period of the Paleozoic Era. As with other geologic periods, the rock beds that define the period's start and end are well identified, but the exact dates are uncertain by a few million years. The base of the Silurian is set at a series of major Ordovician–Silurian extinction events when up to 60% of marine genera were wiped out.

<span class="mw-page-title-main">Triassic</span> First period of the Mesozoic Era 252–201 million years ago

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References

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