Transcript Presentation

The lithosphere and the soil as power equipment and hazard
4.
Useful and harmful impacts of lithospheric
processes for the humanity – case studies
Minoan eruption
Geographical position of Santorini
Tectonic profile of the Aegean Sea (TIBALDI ET AL. 2008)
Spreading of the volcanic ash of the Thera
Geological profile of Thera
The radiocarbon dates have significant implications for the accepted
chronology of Eastern Mediterranean cultures. The Minoan eruption is a
key marker for the Bronze Age archaeology of the Eastern
Mediterranean world. It provides a fixed point for aligning the entire
chronology of the second millennium BCE in the Aegean, because evidence
of the eruption is found throughout the region. Despite this evidence, the
exact date of the eruption has been difficult to determine. For most of
the twentieth century, archaeologists placed it at approximately 1500
BCE, but this date appeared to be too young as radiocarbon dating
analysis of an olive tree buried beneath a lava flow from the volcano
indicates that the eruption occurred between 1627 BCE and 1600 BCE
with a 95% degree of probability.
Eruption
of
Vesuvius in AD 79
Mount
In the year of 79 AD,
Mount Vesuvius erupted in
one of the most
catastrophic and famous
eruptions in European
history. Historians have
learned about the eruption
from the eyewitness
account of Pliny the
Younger, a Roman
administrator and poet.
Geographical position of Vesuvius
Map of the Vesuvius
Model of the Vesuvius type explosion
3D model of the explosion of Vesuvius
at 79 AD
Mount Vesuvius spawned a deadly cloud of volcanic gas, stones, ash and
fumes to a height of 20.5 miles, spewing molten rock and pulverized
pumice at the rate of 1.5 million tons per second, ultimately releasing a
hundred thousand times the thermal energy released by the Hiroshima
bombing. The towns of Pompeii and Herculaneum were obliterated and
buried underneath massive pyroclastic flows. An estimated 16,000
people died from the eruption.
The 79 AD eruption was preceded by a powerful earthquake seventeen
years beforehand on 5 February, AD 62, which caused widespread
destruction around the Bay of Naples, and particularly to Pompeii. Some
of the damage had still not been repaired when the volcano erupted.
The deaths of 600 sheep from "tainted air" in the vicinity of Pompeii
reported by Seneca the Younger leads Haraldur Sigurdsson to compare
them to similar deaths of sheep in Iceland from pools of volcanic carbon
dioxide and to speculate that the earthquake of 62 was related to new
activity by Vesuvius
1755 Lisbon earthquake
The 1755 Lisbon earthquake, also
known as the Great Lisbon
Earthquake, occurred in the
Kingdom of Portugal on Saturday, 1
November 1755, the holiday of All
Saints' Day, at around 09:40 local
time. In combination with
subsequent fires and a tsunami,
the earthquake almost totally
destroyed Lisbon and adjoining
areas. Seismologists today
estimate the Lisbon earthquake
had a magnitude in the range 8.5–
9.0) on the moment magnitude
scale, with its epicentre in the
Atlantic Ocean about 200 km
west-southwest of Cape St.
Vincent. Estimates place the death
toll in Lisbon alone between 10,000
and 100,000 people, making it one
of the deadliest earthquakes in
history.
The spread of tsunami waves at the Lisboa earthquake,
1755
Size and frequency of earthquakes at Cape St. Vincente
Although seismologists and
geologists had always agreed
that the epicentre was in the
Atlantic to the West of the
Iberian Peninsula, its exact
location has been a subject of
considerable debate. Early
theories had proposed the
Gorringe Ridge until
simulations showed that a
source closer to the shore of
Portugal was required to
comply with the observed
effects of the tsunami. A
seismic reflection survey of
the ocean floor along the
Azores-Gibraltar fault has
revealed a 50 km-long thrust
structure southwest of Cape
St. Vincent, with a dip-slip
throw of more than 1 km, that
might have been created by
the primary tectonic event.
2004 Indian Ocean earthquake and tsunami
The 2004 Indian Ocean earthquake was an undersea megathrust
earthquake that occurred at 00:58:53 UTC on Sunday, 26 December
2004, with an epicentre off the west coast of Sumatra, Indonesia. The
quake itself is known by the scientific community as the Sumatra–
Andaman earthquake. The resulting tsunami was given various names,
including the 2004 Indian Ocean tsunami, South Asian tsunami,
Indonesian tsunami, and the Boxing Day tsunami.
With a magnitude of Mw 9.1–9.3, it is the third largest earthquake ever
recorded on a seismograph. The earthquake had the longest duration of
faulting ever observed, between 8.3 and 10 minutes. It caused the entire
planet to vibrate as much as 1 centimetre and triggered other
earthquakes as far away as Alaska. Its epicentre was between Simeulue
and mainland Indonesia. The plight of the affected people and countries
prompted a worldwide humanitarian response.
Movement of the lithosphere
plates at the Sumatra
earthquake, 2004
3D model of movement of the tsunami wave
Spreading of the tsunami wave at Sumatra
Geothermal energy
Geothermal energy is thermal
energy generated and stored in
the Earth. Thermal energy is the
energy that determines the
temperature of matter. The
Geothermal energy of the Earth's
crust originates from the original
formation of the planet (20%) and
from radioactive decay of
minerals (80%). The geothermal
gradient, which is the difference
in temperature between the core
of the planet and its surface,
drives a continuous conduction of
thermal energy in the form of
heat from the core to the
surface.
Distribution of thermal water of East Hungary
Even though geothermal power is globally sustainable, extraction must still be
monitored to avoid local depletion. Over the course of decades, individual wells
draw down local temperatures and water levels until a new equilibrium is reached
with natural flows. The three oldest sites, at Larderello, Wairakei, and the
Geysers have experienced reduced output because of local depletion. Heat and
water, in uncertain proportions, were extracted faster than they were
replenished. If production is reduced and water is reinjected, these wells could
theoretically recover their full potential. Such mitigation strategies have
already been implemented at some sites. The long-term sustainability of
geothermal energy has been demonstrated at the Lardarello field in Italy since
1913, at the Wairakei field in New Zealand since 1958, and at The Geysers field
in California since 1960.
Magmatic metallogeny
The largest ore deposits of Hungary can be
bite to the pegmatite – hydrothermal mart of
magmatic system.
On the area of Matra Mountains can be found
two important ore deposits.
Hazánk érctelepeinek legnagyobb része is magmás környezetben, a
pegmatitos- hidrotermás rendszerben képződtek.
A Mátra területén kettő, kiemelkedően fontos ércképződési folyamat
játszódott le a földtörténet során.
1. In the region of Recsk and Parádfürdő, ore enrichments in genetic
relationship are known on the surface as well as at shallow and deep levels.
This is associated with the Oligocene magmatism. On the surface, in the
Parádfürdő district, a hydrothermal, low sulphidisation ore deposits of
gold (-silver) in veins associated with shallow depth quartz-porphyre
intrusion is known. To the stratovolcanic levels of the Lahóca Hill at
Recsk, an ore deposit of Cu, Au and Ag starting at a meso-epithermal
temperature
is
related.
This
energetic-luzonitic-bournonitic-pyritic
siliceous massive ore formation in hydrothermal explosive breccias
provided the most important ore material to the mining at Lahóca.
Geological map of ore deposit of Cu -Au-Ag at Recsk
2. Following the extinction of volcanic activity taking place in the Western
and Central Mátra during the Mid-Miocene, a post-volcanic activity along
with tectonic movements began resulting in the formation of hydrothermal
lithologic deformation and ore-bearing veins. In the GyöngyösorosziMátrakeresztes-Mátraszentimre area of nearly 30 km2, Hungary’s largest
occurrence of lead-zinc ore in veins was explored. The ore-bearing veins of
the ore deposits in the Central Mátra were exposed by several smaller study
adits and the deep adit of Parádsasvár. In the vein filling, predominantly
spharelite and wurtzite and marginally galenite and chalcopyrite as well as
rich disseminated pyrite are typical ore minerals
Map of ore deposit of Cu –Zn-Pb
at Gyöngyösoroszi
REFERENCES
BÁLDI T. (2003). A történeti földtan alapjai. Nemzetei Tankönyvkiadó, Budapest, p.
312.
BÁLDI T. (1991). Elemző (általános) földtan I.-II. Nemzeti Tankönyvkiadó,
Budapest, p. 797.
BALOGH K. (1991). Szedimentológia I-II-III Akadémiai Kiadó Budapest
HARTAI É. (2003). A változó Föld. Egyetemi tankönyv. Miskolci Egyetemi Kiadó, p.
192.
HAAS J. (1998). Karbonátszedimentológia. ELTE Eötvös Kiadó, Budapest, p. 147.
KUBOVICS I. (2008). Általános kőzettan. A földövek kőzettana
Mundus Magyar Egyetemi Kiadó p. 652.
TÖRÖK Á. (2007). Geológia mérnököknek. Műegyetemi Kiadó, Budapest, p. 383.
Thank you for your attention!