An Overview of Paleo-Climate Evidence in Egypt
35
oxic and suitable conditions as indicated by the increase of productivity indicators
such as Ba, P and both δ
13 C Carb and δ
13 C org , which gradually return to the background
values observed below the PETM interval.
The PETM at Dababiya GSSP can be therefore divided into four main phases
(Fig. 9): (1) pre-PETM gradual warming during the latest Paleocene), (2) PETM
main phase with methane hydrate release, (3) environmental response (weathering
and anoxia), and (4) finally, recovery phase.
7 Anthropocene Warming
In 2016, both Anthropocene Working Group (AWG) of the Subcommission on Quaternary Stratigraphy (SQS) of the International Commission on Stratigraphy (ICS),
defined the Anthropocene as the period of the commencement of significant human
impact on the Earth’s geology and ecosystems [139–142]. Human activity has had
dramatic impacts on landscape, the subsurface and Earth systems, and driving significant atmospheric, chemical, physical and biological changes. The Anthropocene
climatic changes are determined to start from the beginning of the Agricultural Revolution 12,000–15,000 years ago. The ratification process continues, and thus a date
remains to be decided definitively. The most notable environmental change occurring
on earth has a direct link with the beginning of the industrial revolution. Whereas
some recent studies linked the beginning of the Anthropocene era to begin approximately 8000 years ago with the development of agriculture and beginning of stable
humans societies. It started when the ancient farmers cleared forests to grow crops
[143, 144].
The main factor forcing the Anthropocene climate change is increasing the greenhouse gaseous due to the burning of fossil fuel. The burning of fossil fuel due to the
increased human activities push the atmospheric carbon dioxide (CO 2 ) content to
higher levels. In 2013, the CO 2 emissions increased atmospheric CO 2 concentration
by 100 ppm to reach approximately 400 ppm from 280 ppm that recorded from
Holocene or pre-industrial [145], these values continue increasing through 2015–
2016 [146] showing a rising trend above 400 ppm. This significant increases in CO 2
has a strong impact on the Earth’s climate system it is occurring much faster, with
a greater extent, than any recorded warming events during the geologic history of
the earth [147]. Most of this increase is due to the combustion of fossil fuels such
as coal, oil, and gas, although smaller fractions result from cement production and
from land-use changes (such as deforestation).
Geologically, this climate warming is commonly compared with the rapid shortterm ~5 °C warming of the PETM except that during the PETM major diversification
in marine and terrestrial life and significant species extinctions occurred only in
deep-water benthic foraminifera [148]. Therefor to get a better understanding of
the Anthropocene climatic changes we have to compare it with the different rapid
warming and mass extinction events such as Cretaceous-Paleogene mass extinction
as well as the Paleocene Eocene climatic optimum to gain insights into potential
35
oxic and suitable conditions as indicated by the increase of productivity indicators
such as Ba, P and both δ
13 C Carb and δ
13 C org , which gradually return to the background
values observed below the PETM interval.
The PETM at Dababiya GSSP can be therefore divided into four main phases
(Fig. 9): (1) pre-PETM gradual warming during the latest Paleocene), (2) PETM
main phase with methane hydrate release, (3) environmental response (weathering
and anoxia), and (4) finally, recovery phase.
7 Anthropocene Warming
In 2016, both Anthropocene Working Group (AWG) of the Subcommission on Quaternary Stratigraphy (SQS) of the International Commission on Stratigraphy (ICS),
defined the Anthropocene as the period of the commencement of significant human
impact on the Earth’s geology and ecosystems [139–142]. Human activity has had
dramatic impacts on landscape, the subsurface and Earth systems, and driving significant atmospheric, chemical, physical and biological changes. The Anthropocene
climatic changes are determined to start from the beginning of the Agricultural Revolution 12,000–15,000 years ago. The ratification process continues, and thus a date
remains to be decided definitively. The most notable environmental change occurring
on earth has a direct link with the beginning of the industrial revolution. Whereas
some recent studies linked the beginning of the Anthropocene era to begin approximately 8000 years ago with the development of agriculture and beginning of stable
humans societies. It started when the ancient farmers cleared forests to grow crops
[143, 144].
The main factor forcing the Anthropocene climate change is increasing the greenhouse gaseous due to the burning of fossil fuel. The burning of fossil fuel due to the
increased human activities push the atmospheric carbon dioxide (CO 2 ) content to
higher levels. In 2013, the CO 2 emissions increased atmospheric CO 2 concentration
by 100 ppm to reach approximately 400 ppm from 280 ppm that recorded from
Holocene or pre-industrial [145], these values continue increasing through 2015–
2016 [146] showing a rising trend above 400 ppm. This significant increases in CO 2
has a strong impact on the Earth’s climate system it is occurring much faster, with
a greater extent, than any recorded warming events during the geologic history of
the earth [147]. Most of this increase is due to the combustion of fossil fuels such
as coal, oil, and gas, although smaller fractions result from cement production and
from land-use changes (such as deforestation).
Geologically, this climate warming is commonly compared with the rapid shortterm ~5 °C warming of the PETM except that during the PETM major diversification
in marine and terrestrial life and significant species extinctions occurred only in
deep-water benthic foraminifera [148]. Therefor to get a better understanding of
the Anthropocene climatic changes we have to compare it with the different rapid
warming and mass extinction events such as Cretaceous-Paleogene mass extinction
as well as the Paleocene Eocene climatic optimum to gain insights into potential