International Archives of the Photogrammetry, Remote Sensing and Spatial Information Sciences, Vol XXXV.
point (3917 m.) in central Anatolia. Mass is approximately 2800
m higher than plateau which is 1050 meters high (figure 1).
Erciyes Mountain is independent from west, south and north
part of mountain. It has relationship between Hızır Mountain
from eastern part of mountain. Erciyes Mountain floor has
approximately circle shape (approximately 35 km. radius).
Mass raised from narrow place, which has concave shape.
Erciyes Mountain divided two main parts by Alpine Pasture
which name is Tekir Yaylası.
ESVC have unique and various morphological features. They
are parasite cones, old and new lava flows, tufas, cinder cones,
etc. Additionally some glacial morphology and valleys systems
is situated on mountain. The Erciyes glacier Occupies a
pleistocene cirque on the northwestern slopes of the Erciyes
Mountain. The glacier, which due to its existence to an
expeceptionally favourable exposition has an area of about 15
hectars. (Erine, 1951; Bakirci, 1961). It has 550 m. lenght and
50 m. thichness. The tonque of the glasier ends about 3400 m.
Erciyes glasier is going to disappear even under the one of the
effects of global warming. According to Erinc (1951) Erciyes
glasier reached 2500 m. above sea level in phase of expansion
the pleistocene.
The intercontinental transcurrent Central Anatolian Fault Zone
(CAFZ) cuts the eastern part of Anatolia, the Taurus belt and
displaces them sinistrally by up to 75 km. The CAFZ is about
730 km long and runs from Erzincan in the northeast to offshore
of Anamur country in the southwest. Its northeast and
southwest parts are linked to each other by the intervening and
actively forming transtensional Erciyes Pull-apart Basin which
is situated on Coppadocian Volcanic Plateau (CVP) and it is a
approximately 35 km wide, 120 km long and 1.2 km deep
single depression with a lazy S shape that resulted from a
relasing double bend along the CAFZ during Plio-Quaternary
times. ESVC is situated on the central part of Erciyes pull-apart
basin (Kocyigit and Erol, 2001).
The ESVC is the diagnostic feature of the Erciyes depression
occupying the central part of the depression and rising to 2840
m and 3917 m above the depression floor. It consists of six
major units. From bottom to top, these are basaltic and andesitic
lavas, deictic-rhyodacitic lava domes, olivine basalt lavas,
hyalodacitic lava domes and pumiceous ash deposits (Pasquare,
1968). ESVC commenced with eruption of basaltic fissures
coeval with the rifting of the CVP and initial subsidence of the
Erciyes depression. First phase of basaltic eruption was
followed by andesitic volcanic activity leading to emergence
and growth of the central of the mountain. Subsequently, a
series of radial dykes cut the central cone and produced a
number of dacitic-rhyodacitic exogenous lava domes shaping
the main frame of the ESVC. Growth of these domes was
followed by outflow of olivine basaltic lava streams flowing
down the slopes of main and flank cones down to the foot of
volcano. Finally, explosive volcanic activity ended in
pumiceous ash sheets in activity extending into approximately
15 000 years ago (Innocenti, et al., 1975). At last step, big
debris avalanche come into existence by collapse on peak of
mountain. Amphitheatres shaped caldera has approximately |
km radius and 2km depth (Sarikaya, et al., 2003b). Volcanic
cones preserved on southeast side of hill slope (Figure 2).
380
Part B2. Istanbul 2004
Figure 2. Perspective view of Erciyes Mountain and its caldera.
The ESVC also experienced three stage of glaciation in the Late
Pleistocene- Early Holocene times producing glacial erosion
features and deposits in crestal regions above 2700 meters. In
general, the geochemical composition of volcanic rocks
comprising the ESVC is calcalkaline (Innocenti, et al., 1975;
Batum, 1978; Ercan, 1986; Güner, et al., 1984; Kogyigit ve
Erol, 2001).
3. TECHNOLOGIES
In this investigations, morphological features are described by
both recent and traditional technologies. Topographic analysis
from maps and field studies are the most important elements in
geomorphology and volcanology. This observations and
analysis are able to improved by measure, monitor and analysis
forms of terrain using by satellite data and DTM. Image
processing systems are used to identification to morphological
units from interpretation both satellite data and DTM together.
They are also able to explain and measure aspects of
morphological features and processes (Waslh, et al., 1998). In
earthsciences, remote sensing can not only supply synoptic
views but also it supplies measurements of the terrain and its
attributes.
Satellite data have been one of the most effective data in
earthsciences since the middle of the 1970s. Satellite sensors
designs to operate in many part of portion of the
electromagnetic spectrum. Each portion of electromagnetic
spectrum is able to explain different terrain features. Remote
sensing supplies data which quality and distribution more
detailed than through traditional geomorphologic observations
and surveys in macro scales.
Additionally, Satellite data and DTM are the most acceptable
and cost effective way to understanding geomorphologic
features of terrain. Recently, satellite data and DTM are using
independently or in concert in numerous applications
(Gazioglu, et al., 2004; Gókasan, et al., 2003; Gazioglu et al.,
2002; Musial et al, 2002; Gôkasan et al, 2002: Mayer, L.
2000; Wilson and Gallant, 2000; Novak and Soulakellis, 2000;
McCullagh, 1998). Landsat ETM data were used in this study.
3.1. The DTM of Mt. Erciyes
The DTM of Mt. Erciyes estimated by digitised contour lines of
1/25 000 scale topographic maps. A digitalisation error of 0.3
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