4 research outputs found
Brachiopods from the Silberberg Formation (Late Eocene to Early Oligocene) of Atzendorf, Central Germany
Millennial physical events and the end-Permian mass mortality in the western Palaeotethys: timing and primary causes.
This chapter focuses on the nature and pattern of four transgressiveâregressive
depositional cycles (C1âC4) across the PermianâTriassic Boundary (PTB) in the
Dolomites, on their timing and on the possible causal relationships with four massmortality
events (E0âE3), which, considered together, constitute the end-Permian
extinction event in the western Palaeotethys. The duration of the investigated interval
is ca. 200 ky; the duration of each cycle ranged from less than 20 ky to ca. 100 ky; and
the magnitude of the sea level changes ranged from 5 to 15 m. Each mass-mortality
event affecting the shallow marine environments of the western Palaeotethys corresponds
with a regressive phase lasting a few millennia. The oldest mortality event
(E0) at the top of Cycle 1 (i.e., the top of the Ostracod Unit) in the Southern Alps
is aligned with the regressive Bed 24e of the Meishan D section in the eastern
Palaeotethys; it is usually considered the actual end-Permian extinction event. The
same cooling/fall-stand has been identified in various sites along the shallow-marine
Gondwana margin. In the Southern Alps, E0 is mostly masked by stressed conditions
typical of the regional carbonate tidal flat. During the following transgression
and high-stand periods of Cycle 2 (i.e., Bulla Member), the shallow marine environment
became re-populated by ca. 200 species referred to ca. 30 genera. At the top of
Cycle 2, the sea level fell 10 m or less in a few millennia; it started the most devastating
mass-mortality event (E1) in the Southern Alps. This mortality event lasted less
than 20 millennia; it continued briefly during the trangressive phase of the following
Cycle 3âwhich brackets the Bellerophon-Werfen formational boundary (BWB).
This interval, aligned with Beds 26â27a at Meishan in the eastern Palaeotethys, was
deposited in a deeper and distal environment. About 90% of the marine skeletal
biomass disappeared at the end of E1. The acme of mortality event, E1, corresponded
with a submarine chemical-corrosion event, followed locally by subaerial exposure
and pedogenesis. The mass-mortality event on land slightly predatesâor is nearly
coevalâwith the mass-mortality event in shallow marine environments. The intensity
of submarine corrosion became almost imperceptible at the foreshoreâoffshore boundary.
The sea level rose ca. 15 m during Cycle 3 when the shallow marine environment,
mostly over-saturated in carbonate but punctuated by short periods of vadose or submarine
dissolution, transgressed rapidly more than 40km inland over the corroded bedrock,
depositing oolite shoals and microbialite. The subsequent mortality events E2 and E3
are obviously of less intensity. E2, ca. 20 ky after E1, corresponds to a regressive interval
associated with the first appearance of Hindeodus parvus (i.e., the PermianâTriassic
Boundary). It seems to be the acme of colonisation of the shallow sea floor by cyanobacteria
(stromatolites). E3, ca. 10 ky after the PermianâTriassic Boundary, corresponds
to the last occurrence of Permian-type red algae in the Dolomites area. Whereas the
end of E3 is gradual in the shoreface, it appears to have been abrupt in the lower foreshore,
probably because of general conditions of less-ventilated and suboxic conditions.
We hypothesise that a few local palaeo-environmental factors (e.g., distance of stressing
factors from the source area, the pattern of atmospheric and marine palaeocurrents,
and reduction of the shallow coastal area due to retreat of the coastline) concurred to
modulate the intensity and duration of mortality events in space and time. Data suggest
that increased warming was of primary importance in controlling the mortality tail but
doesnât allow us to confirm or deny other local or general concurrent causes, such as
up-welling of anoxic oceanic waters from the Palaeotethys. We interpret the cause of
the mass-mortality events in the Dolomites area as having been a composite âtop-downâ
mechanism with acid-rain events devastating the Permian-type life on continental and,
subsequently, in shallow marine environments during millennial periods of cooling and
regression of the Bellerophon sea. The ultimate causal factor was, very probably, large
atmospheric perturbations connected with volcanism. Most of the sparse surviving biota
disappeared immediately after the beginning of the following transgressionâbecause
of rapid global warming produced by greenhouse conditions, with only minor, repeated,
episodes of acid rains. These stressed conditions contributed to inhibiting recovery of the
long and efficient shallow-marine food chain. Because the magnitude of mass-mortality
event E0 in the Dolomites and in much of the Gondwana margin is appreciably lower
than the coeval one in Meishan, the first may have acted as refugia. Mass-mortality event
E1 affected the shallow-marine western Palaeotethys for only a few millennia after E0.
In the eastern Palaeotethys, coeval Beds 26â27a of Meishan were deposited from lower
foreshore to marine shelf, lacking any clear record of anoxic conditions. It is the same
for the coeval short-term parasequences in many sites along the Gondwana margin. We
interpret the different magnitude of extinction on the shelves as due to different levels
of temperature and excessive carbon dioxide (pCO2) in the seawater. The rapid
demise of taxa (occurring concordantly with the diachronous major mortality events)
caused local severing of food chains, mostly of small suspension feeders, resulting in the
âLilliputâ faunas (sensu Twitchett 2005) of event E2 in the Dolomites. This aligns with
Beds 27câd at Meishanâthese beds were deposited in the lower foreshore and marine
shelf environments under suboxic to dysoxic bottom conditions. It seems unlikely that
the disappearance of red algae in the western Palaeotethys was connected with dysoxic
conditions; increased temperature seems a more likely factor. Doubtless a medley of
different mechanisms, including rapid fluctuations in marine salinity, operated variously
as regards time and space and produced the end-Permian extinctionâoccurring over a
time span of less than 100 ky