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Joined 2026-09-21 Message
Incoming links: Permian
Paleozoic 2026-10-25
Four documented examples, each tied to its actual context, are:
- Geographic range: widespread marine bivalve genera survived the end-Cretaceous event better than geographically restricted genera. Spatial spread can reduce exposure to some geographically heterogeneous stresses, although this does not guarantee survival of a global perturbation.[ref]Selectivity of end-Cretaceous marine bivalve extinctions by David Jablonski and others. Abstract: lower extinction intensity in geographically widespread genera
- Body size: large-bodied mammals were disproportionately lost during the late Quaternary. The global analysis documents size selectivity across continents and trophic groups; this is not evidence that large body size always raises extinction risk in every geological interval.[ref]Body size downgrading of mammals over the late Quaternary by Felisa Smith and others. Abstract: size-selective losses over the studied late-Quaternary intervals
- Physiological buffering and respiratory capacity: poor capacity to tolerate elevated carbon dioxide and associated oxygen stress has been linked to higher vulnerability among end-Permian marine groups. This is a paleophysiological interpretation informed by living relatives and fossil traits, rather than a direct measurement of a fossil animal’s tolerance.[ref]Paleophysiology and end-Permian mass extinction by Andrew H. Knoll and others. Abstract and section Extinction in the oceans: hypercapnia vulnerability and physiological selectivity
- Sexual dimorphism as a proxy for male reproductive investment: greater male–female carapace differences in fossil cytheroid ostracods were associated with higher estimated extinction rates. The measured fossil trait is dimorphism; interpreting it as investment requires the biological correspondence observed in living relatives.[ref]High male sexual investment as a driver of extinction in fossil ostracods by Maria João Fernandes Martins and others. Abstract: dimorphic fossil carapaces and association with estimated extinction rates
These examples demonstrate event- and group-dependent selectivity. They do not define one universal vulnerability ranking: the bivalve study, for instance, did not find body-size selectivity at the same end-Cretaceous genus-level event.
A mass extinction is driven by changes that overwhelm organisms' physiological tolerances or destroy their food and habitat systems. Distinguish the initiating forcing from the linked environmental mechanisms: one event can generate several contributors.
- Large extraterrestrial impact. At the Cretaceous–Palaeogene boundary, the Chicxulub impact injected dust, aerosols and soot that reduced incoming sunlight and photosynthesis, disrupting food webs; rapid heating, fires and subsequent cooling added stresses. The impact is the trigger, while darkness and loss of primary production are proximate mechanisms.
- Large-scale volcanism. Eruption and intrusion of large igneous provinces, notably the Siberian Traps around the end-Permian crisis, release or mobilize gases and can produce rapid climate change. Carbon dioxide favors warming; sulfur-bearing emissions can cause shorter cooling and acid deposition. The outcome depends on rate, duration and interacting reservoirs, rather than eruption volume alone.
- Ocean anoxia and euxinia. Warming lowers oxygen solubility and can strengthen stratification; altered nutrient supply increases oxygen demand. Oxygen loss removes habitable marine volume, while sulfide in anoxic waters can be toxic. These processes contributed to the end-Permian marine crisis and can reinforce warming-driven mortality.
- Ocean ocean acidification and elevated carbon dioxide. Rapid addition of carbon dioxide changes seawater carbonate chemistry and can impair biomineralization, while high carbon dioxide also challenges physiological acid–base regulation. Susceptibility varies with physiology; this is a linked mechanism rather than proof that every calcifying group responds identically.
- Rapid cooling and eustatic sea level change. Late Ordovician glaciation and regression reduced shallow-marine habitat and changed temperatures and circulation; subsequent warming and oxygen loss introduced a different set of stresses. Habitat loss and climate change can therefore contribute in successive phases of one crisis.
These examples supply more than four drivers or contributors. The historical effects of volcanism, warming, oxygen loss and elevated carbon dioxide can act together rather than compete as mutually exclusive explanations.[ref]
Paleophysiology and end-Permian mass extinction by Andrew H. Knoll and others. Abstract and introduction: linked physiological effects of warming, anoxia, sulfide and hypercapnia
The result predicts initial failure in a uniform material under the assumed principal-stress orientations. The actual Figure 3 is a present-day NW–SE cross section through a thick, heterogeneous Alpine stack, extending to about 50 km depth. It contains near-horizontal basal stretches, curved ramps, tightly bent contacts, and steep structures in the internal zones around Viso and the Dora Maira complex. It does not show a single undeformed conjugate pair newly formed in horizontal uniform rock.
Several processes explain the departures:
- Mechanical layering and inherited weaknesses. Faults can follow weak bedding, old fault planes, or contacts with lower friction or cohesion than the surrounding rock. These can form shallow décollements linked by steeper ramps. Figure 2 explicitly distinguishes the near-surface red “geophysical bedrock” boundary at a few hundred metres from the much deeper crystalline basement beneath the Jurassic, Triassic and Permian cover. An age label or a seismic contrast alone does not establish a friction coefficient; clay-rich or evaporite detachments are possibilities to test, not lithologies proved by that drawing.
- Rotation after formation. Continuing tectonic shortening, folding, stacking and fault slip can rotate an initially optimal fault plane to steeper or shallower present-day fault dips. A steep older structure may be inherited from an earlier deformation episode rather than created at its present orientation.
- Curved faults and local stresses. Faults bend through a layered crust; local principal stress axes rotate near topography, ramps and interacting faults. The optimum angle is measured relative to the local , not necessarily to the regional horizontal direction everywhere.
- Changing strength and deformation mechanism. Spatial changes in pore fluid pressure, coefficient of friction, cohesion and temperature alter which surfaces reactivate. At depth, ductile deformation can replace frictional brittle failure, so the same new-fracture construction need not apply throughout the section.
Finally, a section shows apparent dip unless it is perpendicular to fault strike. For an ideal plane, , where is the angle between the section direction and fault strike. Obliquity can make a plane look shallower, but cannot on its own explain an apparent dip steeper than its true dip. Do not infer that each black curve is a currently active brittle earthquake fault.
Siberian Traps 2026-10-25
A large volcanic and intrusive province associated in time with the end-Permian crisis. Gas release and interactions with surrounding sediments provide mechanisms for linked warming, ocean chemical change and physiological stress during mass extinction.