Thoughts on Food Preservation and Storage in Central Anatolia
The Geoelectrical Structure of Northwestern Anatolia, Turkey
Transcript of The Geoelectrical Structure of Northwestern Anatolia, Turkey
The Geoelectrical Structure of Northwestern Anatolia, Turkey
E. U. ULUGERGERLI,1,4 G. SEYITOGLU,2 A. T. BASOKUR,1 C. KAYA,3 U. DIKMEN,1 and
M. E. CANDANSAYAR1
Abstract—The magnetotelluric method has been employed to generate a geoelectrical model that will
reveal the rich geological pattern and dynamic character of western and northwestern Anatolia, Turkey.
Magnetotelluric data were collected from 53 sites along a profile of 290 km from the Dardanelles to the
Alasehir Graben. Magnetotelluric data were in the range of 0.00055 Hz to 320 Hz. The models were
obtained through 2-D joint inversion of transverse electric and transverse magnetic modes. Lateral changes
in geoelectrical models are verified by using gravity and magnetic data. In addition, some of the
seismological data presented here agree with proposed models that suggest a brittle-ductile structure
boundary at a depth of 20 km. Generally speaking, a regional extensional regime caused reduction in the
thickness of the crust and consequent uplift towards the south. The constructed model delineates the
western part of the North Anatolian Fault Zone along the Biga Peninsula. The current patterns of volcanic
activity on the Biga Peninsula and at Kula are related to conductive spots presented in the models. The
border of the Gordes Basin, located between the Izmir - Ankara suture zone and the Menderes Massif, is
also well delineated. The North Anatolian Fault Zone presents a pattern in which density and susceptibility
anomalies attain relatively high values. Fillings covering most of the surface have lower density and
susceptibility values than those of underlying structures.
Introduction
Deep or large-scale regional structures generally control numerous geological
occurrences such as faults, horsts, grabens, magma chambers and near-surface
sedimentary basins. Realistic explanations of all such features require consistent
information that outlines the structure of upper crust. The rich geological pattern
and dynamic character of western and northwestern Anatolia (Figs. 1 and 2) have
drawn considerable attention in recent geological (e.g., OKAY et al., 1996; SEYITOGLU
and SCOTT 1994; YıLMAZ et al., 1997; ALDANMAZ et al., 2000) and geophysical (e.g.,
1 Department of Geophysical Engineering, Ankara University, 06100 Ankara, Turkey.2 Department of Geological Engineering, Tectonics Research Group, Ankara University, 06100
Ankara, Turkey.3 Department of Geophysics Engineering Sivas, Cumhuriyet University, Turkey.4 Department of Geophysics Engineering, Onsekiz Mart University, Canakkale, Turkey (currently).
Pure appl. geophys. 164 (2007) 999–10260033–4553/07/050999–28DOI 10.1007/s00024-007-0200-0
� Birkhauser Verlag, Basel, 2007
Pure and Applied Geophysics
TAYMAZ et al., 1990; HORASAN and CANıTEZ, 1995; BAYRAK et al., 2000; CAGLAR,
2001, AYDıN et al., 2005) literature.
The magnetotelluric (MT) method has been employed to outline the regional
geology of northwestern Anatolia by using 53 measurement stations along a profile
of 290 km. Time variations of magnetic and electric fields were simultaneously
recorded. Measurement sites were chosen on the basis of accessibility and the local
extent of the geological units. The measurement profile was subdivided into three
segments in order to cross the principal geological structures almost orthogonally
(Fig. 2). Actually, geological structures are always three-dimensional (3-D). How-
ever, two-dimensional (2-D) interpretation techniques may be used instead of 3-D
ones in consideration of the frequency range of the data and the main geological
features intersected; extensions of which are greater than the skin depth of the lowest
frequencies. Static shift correction was applied by using transient electromagnetic
(TEM) data (e.g., STERNBERG et al., 1988; MEJU et al., 1998). The aim was to obtain
a 2-D geoelectrical model producing a theoretical data set that fits measured data in
both transverse electric (TE) and transverse magnetic (TM) modes so as to reveal the
most likely representational setting along the profile.
A summary of other pertinent geophysical studies conducted in the region and
proposed geoelectrical models for the area are as follows. BAYRAK et al. (2000) used
Figure 1
Regional map of the Aegean Sea. Detailed map of rectangular area is given Figure 2.
1000 E. U. Ulugergerli et al. Pure appl. geophys.,
the same data that are presented in the present article but concentrated on
anisotropy. They concluded that the extensions of geological structures in western
Turkey provide opportunities for performing 2-D modeling and inversion of the
current data set. Further, BAYRAK and NALBANT (2001) derived a geoelectrical model
using these data. However, they carried out only TM mode inversion without static
shift correction. They assumed that the magnified range of apparent resistivity error
bars will reduce the static shift effects. However, enlarging the error bars and use of
Figure 2
Location of MT stations (small dots), Neogene and Quaternary basins and main basement structures in
western Turkey (after SEYITOGLU and SCOTT, 1994). Thin solid lines show the segments. Larger dots
indicate towns and cities.
Vol. 164, 2007 The Geoelectrical Structure of Northwestern Anatolia, Turkey 1001
single mode inversion, as done by BAYRAK and NALBANT (2001) will increase the
uncertainties in model space by increasing the number of possible models that
describe the observed data.
Recently, CAGLAR (2001) also proposed a geoelectrical model for the western part
of Anatolia. The data presented here somewhat cover the same geological settings as
does CAGLAR (2001)’s profile, but our current profile employs shorter station
intervals and the directions of the segments differ from those of CAGLAR (2001). The
geoelectrical models presented in CAGLAR (2001) were obtained through 2-D
inversion of TE and TM mode data, independently. Also, static shift problems were
not taken into account. BERDICHEVSKY et al. (1998) showed that single mode data
inversion is not always sufficient for obtaining a reasonable geoelectrical model and
emphasized that TE and TM mode data may be mutually complementary in order to
extract more detailed models.
GURER et al. (2001) presented results for the Gediz (Alasehir) graben. But their
profile is not in line with the current profile. TAYMAZ et al. (1990) shed some light
on the seismological activity of the Aegean region. ILKıSıK (1995) reported that high
heat flow values dominate in the region. Both papers concluded that the area is
experiencing highly active tectonism. AYDIN et al. (2005) summarized the regional
geological setting and presented Curie-point depth for Turkey. Both AYDIN et al.
(2005) and HISARLı (1995) showed that shallow Curie-point depths (8–12 km) are
well correlated with the young volcanic areas and with highs of the heat flow. In
addition, they also stated that the shallow Curie-point depths indicate thinned
crust.
SARI and SALK (1995) estimated the thickness of sediments in the central Aegean
region using gravity data. ATES et al. (1999) presented an updated gravity and
magnetic anomaly map of the region. Substantial information about geological and
geophysical research in the area may also be found in the internal-report archives and
libraries of the General Directorate of Mineral Research and Exploration of Turkey
(MTA) and the Turkish Petroleum Corporation (TPAO).
A key general result that is gleaned from these works is that the area is still
tectonically active, thus explaining earthquakes in the region and suggesting the
possibility that magma chambers and/or intrusions exist which give rise to many
hot springs, some of which are utilized as geothermal resources. A realistic
explanation for all of these occurrences demands adequate information regarding
the structure of the upper crust. This paper attempts to set forth a regional
geoelectrical model that fits both the TE- and TM-mode MT data and to interpret
the derived model in light of the regional geology. To date, apart from the articles
mentioned above, there has been no other large-scale geoelectrical model for
western Anatolia obtained from a 2-D or 3-D modeling scheme published in the
literature.
The derived 2-D geoelectrical structure is also verified by gravity and magnetic
models. 2.5-D gravity and magnetic modeling schemes are employed to obtain a
1002 E. U. Ulugergerli et al. Pure appl. geophys.,
smooth final model. Although the susceptibility model shows some discrepancies
from the geoelectrical model in the southern part of the profile, the responses of both
density and susceptibility models derived from the geoelectrical interpretation show a
reasonable fit to the observed data.
Geology
The geology of northwestern Turkey (Fig. 2) comprises an amalgamation of
microcontinents that were situated between Gondwana and Laurasia from the
Permo-Triassic until the Oligocene. The rocks exposed in the region which reflect this
complex history are divided into several zones, namely: the Sakarya zone, including
Karakaya complex; the Izmir-Ankara Suture Zone; and the Menderes Massif (OKAY
et al., 1996; OKAY and TUYSUZ 1999).
The current pattern of northwestern Turkey started to form in Late Cretaceous,
the collision of Istanbul zone and Sakarya continent created the Intra-Pontid suture.
The ophiolite obduction on Menderes - Taurus block is named Bozkır nappes. Thefinal closure of the Northern branch of Neo-Tethys occurred in Late Eocene to
Oligocene along the Izmir-Ankara suture zone and the amalgamation of western
Anatolia is completed (SENGOR and NATAL’IN 1996).
Following the Oligocene, western Turkey experienced N-S extensional tectonics
(SEYITOGLU and SCOTT, 1996; SEYITOGLU et al., 2004), and/or NNE-SSW extensional
regimes (KREEMER et al., 2004), and metamorphic core complexes, grabens, igneous
activity and geothermal fields are the main geological features of the region. Note
that the current extension rate is, approximately, 30–40 mm yr)1 in the region
(MCKENZIE, 1978; TAYMAZ et al., 1991).
A recent study (SEYITOGLU et al., 2004) indicates that in the Oligocene, Datca-
Kale main breakaway fault causes the exhumation of Menderes massif that is at the
surface during Early Miocene. At this time, due to the continuation of extensional
tectonics, major E-W (Alasehir and Menderes) and N-trending basins (i.e., Gordes,
Demirci basins) began to develop simultaneously. Basin fillings have also been
subject to research. BOZKURT and SoZBILIR (2004), using geological observations,
implied that the thickness of the Neogene sediments in the Alasehir graben is about
1.3–1.5 km. On the other hand, SARI and SALK (2006), using the gravity data,
advanced that the thickness of sedimentary cover reaches 2.5 and 3.5 km in the
Menderes graben, and 0.5 and 2.0 km in the Alasehir graben.
In the Pliocene, the youngest structures cut the older ones (i.e., Simav graben)
and mask the earlier extensional history of the region. After the Pliocene, the
southern branch of the North Anatolian Fault (NAF) affected northwestern Turkey
and structures became more complex (OKAY and SATıR, 2000).
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The geoelectrical line of this study starts at Canakkale, located in the Sakarya
Zone, passes through the Izmir-Ankara Suture Zone, and then enters the Menderes
Massif upon which the major extensional basins have developed.
Major extending structures can be grouped in three segments. The first part
consists of the branches of the NAF between Canakkale and Balıkesir. The NAF
zone has many local faults such as Etili and Yenice-Gonen faults, directions of which
vary between N50E and N70E. The Second part is the Izmir Ankara Suture Zone
between Balıkesir and Gordes. This part has no dominant features apart from the
suture itself (�N40E) and some local faults (�N70E). The last part is the western
edges of Demirci and Selendi basins which present a fan structure together with
Alasehir graben and the suture. Directions vary from N15E to N70W. All MT
stations are placed according to main tectonic units during the field trip. Structural
variations urged to divide the data set in three segments rather than to use a single
profile during the modelling study.
Seismological Background
Some findings of the geoelectrical model require comparison with seismological
data. Therefore, in order to gain some insight about tectonic activities, 886
earthquake occurrences have been evaluated. The epicenters of earthquakes with
magnitudes over 3 on the Richter scale and that occurred between 1900 and 2002 are
mainly between 2 and 35 km. The magnitudes increase with increasing depth of the
epicenters. The occurrence frequency of magnitude 5 earthquakes is less than one
year, indicating a high risk of earthquake hazard. The frequency (F) – magnitude
(M) relation for the region is given as
log F ¼ a� b�M ;
where a and b values were calculated by means of the least-squares methods and as
shown in Figure 3. The b value (defined as a tectonic parameter) may give valuable
seismological information about the region as pointed out by, for example, MOGI
(1962), SCHOLZ (1968) and WEEKS et al. (1978). In terms of absolute value, a zone
with a relatively low b value compared to the surrounding area indicates an energy-
accumulation zone, while higher b values outline energy-release zones. The
cumulative sum of the b value along the profile is presented in Figure 4. The
variation of b value decreases linearly up to 20 km, and then becomes almost
constant beyond that depth. Thus, the zone between the surface and a depth of
20 km may be defined as an active energy-release zone, while the deeper zones build
up energy and have almost constant b values. Recently, AKYOL et al. (2006) reported
that, using hypocentral distribution of the earthquakes, peak seismicity for the
western Anatolia occurs at depths of about 10 km. This result is also in accord with
Figure 4.
1004 E. U. Ulugergerli et al. Pure appl. geophys.,
Problems for Research
The area has a complex geological setting, and recent seismological activity shows
that fault zones are still active. Additionally, average heat flow is approximately
110 mW/m2 (e.g., ıLKıSıK, 1995; GURER et al., 2001; AYDıN et al., 2005; AKıN et al.,
2006) for the region and the pick values can reach as high as 229 mW/m2. High heat-
Figure 3
Selected earthquakes, epicenters of which are over 3 (+) on the Richter scale and which occurred between
1900 and 2002 (Source: DAD (Earthquake Research Center), KOERI (Bogazici University Kandilli
Observatory and Earthquake Research Center), ISC (International Seismological Center) ). Rectangles are
locations of MT stations.
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flow rates (ıLKıSıK, 1995) and many geothermal spots indicate the existence of
possible magma intrusions/chambers. ILKıSıK (1995) pointed out that the depth of the
lithosphere-asthenosphere boundary in western Anatolia is around 55±5 km.
SENGOR et al. (1985) suggested that the Palaeocene orogenic contraction thickened
the crust about 50 to 55 km in Early Miocene time. Seismological research presents
slightly different results for the western Anatolia; MINDEVALLI and MITCHELL (1989),
using surface waves, give an average crustal thickness of about 34 km while
SAUNDERS et al. (1998) found that the crust is approximately 30-km thick under
Kula, and HORASAN et al. (2002) suggest that a crustal thickness of 33 km in the
region. ZHU et al. (2006) showed that Moho depth is about 28 and 30 km around
Bozdag and Kula, respectively. In terms of local structures, ERGUN (1977) postulated
that the magnetic anomaly on the Biga peninsula originates from a source located at
5-km depth. AYDıN (1987) presented similar results (� 5 km) for the upper boundary
of the source of the magnetic anomaly around Soke.
From a geological and geophysical point of view, all of these findings indicate
very complex structural patterns and extensions that need explanation. The patterns
of basins and the source of volcanic units on the Biga Peninsula and around Kula
may be revealed by variation in electrical properties of these features which may be
explored by electromagnetic methods.
Magnetotelluric Data
Phoenix V5 MT equipment has been employed to record three orthogonal
magnetic (H) fields and two orthogonal electrical (E) field components. 100 m
dipoles, extending in N-S and E-W geomagnetic directions, and Pb-PbCl electrodes
Figure 4
Variation of b values vs. depth. 20 km may be a boundary between an active energy-release zone and an
energy accumulation zone.
1006 E. U. Ulugergerli et al. Pure appl. geophys.,
were used for E field measurements. Horizontal components of the H field were
measured with an induction coil. The vertical component of the H field was recorded
by a loop on the ground, however the data quality was insufficient at most of the
stations.
Remote reference stations were established a few hundred meters away from each
station. Unfortunately, the signal/noise ratio could not be improved because of the
short distance between the main and remote stations and high-level cultural noise at
some locations, such as those near industrial plants. Recorded time series permit the
extraction of periods up to 1800 s. The recording system calculates all sounding
parameters in real-time. The data acquisition is performed separately in two
frequency sets. The first one is a high frequency set, in a range of between 320 Hz and
7.5 Hz, and was processed using Fourier transform techniques. The low frequency
set has a range of 6 to 0.00055 Hz and was processed using the cascade decimation
(WIGHT and BOSTICK, 1980). Four impedance components and, in turn, apparent
resistivity and phase of impedance have been obtained in a range of 0.00055 Hz to
320 Hz in 40 frequencies. Station intervals were selected at 5 to 10 km, depending
upon the accessibility of the area.
The electrical field dipoles extend N-S (XY) and E-W (YX) assigned to TE and
TM modes, respectively after rotation. Before rotating the data possible strike angles
were examined. The area has a complex geological setting, thus one should not
expect any common strike angle for the whole profile. BAYRAK et al. (2000) gave a
dimensionality analysis of the data using the Mohr circle. As they stated, the data
have strong anisotropy in three depth levels; 7–8, 15–20 and 35–40 km. Note that
they obtained depth information from Bostick–Niblett transformation (NIBLETT and
SAYN-WITTGENSTEIN, 1960; BOSTICK, 1977; JONES, 1983). Swift and tipper strike
angels for 2, 7 and 80 sn are presented in Figure 5. Solid line with diamond marker
represents average geological extensions. The stations closer to main tectonic features
were selected for this purpose. The rest of the stations have some deviations from
extension of the main units. Deeper information represented with both ‘‘x’’ and ‘‘+’’
0
15
30
45
60
75
90
WA1
WA4
WA6
WA10
WA12
WA15
WA16
WA20
WA32
W2A
5
W2A
9
WA33
WA34
WA36
WA37
WA41
WA42
W4A
3
Deg
ree
Figure 5
Swift and tipper strike angles for 2, 7 and 80 sn. The solid line with a diamond marker indicates average
geological extensions. Stations closer to main tectonic units were presented.
Vol. 164, 2007 The Geoelectrical Structure of Northwestern Anatolia, Turkey 1007
symbols and the angles differ ±15� from main geological directions except that in the
southernmost of the last segment. Evaluation of tectonic information together with
strike angles led us to divide the whole MT profile into three segments and decide the
strike angle of the each segment separately. Details are given later in this section.
Subsequently, these strike angles were fixed in the GROOM-BAILEY (1989) decom-
position code to see distortions. The comparison of estimated apparent resistivities
with those from major axis values indicated that both apparent resistivity data are
equal to each other with a slight error (<% 1 average relative error per mode) where
strike angle and geological extensions are inline with each other. High frequency part
(>1 Hz) data comply with the condition in first two segments, then data deviate
from each other (up to %25 average relative error per mode). This indicates that the
strike direction changes at deeper parts. Mode switching occurred in the third
segment (e.g., WA38 to WA53) because of the large rotation angle value (�70�clockwise). Cross comparison reflects error less than �%10 relative errors per mode
up to 0.1 Hz Relative error is the ratio of differences of estimated and major axis
apparent resistivities to estimated apparent resistivity. Note that logarithms of the
apparent resistivities were used in error calculation. Decomposition without fixing
the rotation angle did not produce any single regional angle for the segments.
Details of the segments are given as follows. The first segment of the MT data,
collected along a 118-km profile (Fig. 1), began at the Dardanelles (Canakkale),
crossed Biga Peninsula, and was terminated near Balya (Balıkesir). All stations
between WA1–WA21 were rotated 20� clockwise to make the TE mode data
perpendicular to the 2-D geoelectrical section. The second part of the data, obtained
along a profile of 112 km between a point north of Balya, then to Balıkesir, Bigadicand Sındırgı, crossing margins of the Sakarya Zone and Karakaya complex. All data
between WA22–WA37 along the segment were rotated 45� clockwise to keep the TE
mode perpendicular to the 2-D section. The third segment was a 93-km-long profile
extending from Sındırgı, past Gordes and Koprubasi, to Kula. A 70� rotation angle
seemed to be reasonable for the stations between WA38–WA53. Another reason for
the large rotation angle rather than rotating 18� anti-clockwise was to maintain the
standard notation for the modes.
Central loop transient electromagnetic (TEM) measurements were completed at
each MT station in order to remove the static shift effect from the MT data and to
derive near-surface information. We used Protem Receiver and TEM57 transmitter
(Geonics) for TEM measurements. High (6.813–695 microseconds) and Medium
(35.25–2792 microseconds) time ranges were selected for data acquisition. A 1-D
model was obtained by the inversion of combined TEM data at each measurement
station. The synthetic high frequency MT data were computed from the corre-
sponding 1-D model that was inverted from the TEM data.
Both measured TE and TM apparent resistivity data are shifted towards the MT
response of the 1-D model. Note that the shifting process was performed after
rotation steps. Rotated apparent resistivity data were multiplied by a constant to
1008 E. U. Ulugergerli et al. Pure appl. geophys.,
shift towards pseudo MT data. The deviations are between 20% and 500% in linear
scale. We typically expected that the TE and TM apparent resistivity data would
remain parallel to each other in the high frequency band except under exceptional
conditions. However, one should keep in mind that the shifting process using a 1-D
model may cause information loss in the case of the existence of a superficial 2-D–3-
D structure, which leads to the departure of the TE and TM mode apparent
resistivities from each other even at very high frequencies. This condition is accepted
as a sacrifice for the methodology followed.
2-D Model
The models presented here were obtained using the WinGLink� interpretation
package consisting of a 2-D inversion code of d2inv_nlcg2_fast (MACKIE et al., 1997).
Initial models were taken as a homogeneous half space of 100 ohm-m. The first
model has 21 stations and is represented by a mesh of 55 by 95 cells. The second
model is represented by a mesh of 46 by 100 cells and has 19 stations (WA18–WA37)
overlapping with four stations of the first model. The third model is constructed from
a mesh of 52 by 93 cells and has 18 stations (WA35–WA53) overlapping with three
stations of the second segment. The left, right and bottom parts were extended
enough to eliminate boundary effects. The stations were placed at the top of each
mesh with 3- to 6-cell separations depending on the measurement intervals. TE and
TM mode apparent resistivity and phase of impedance data were inverted jointly.
The inversion process was subdivided into three inversion sessions. The maximum
number of iterations was set to 50 for each session. The software required some
additional inputs. The first one was smoothing factor, tau, which was taken as 30 for
the first 50 inversion steps then reduced in succeeding sessions. Therefore, inversion
was, at first, allowed to find a general pattern then forced to delineate the details by
using lower tau (20) values in the later steps. Error floors for all data were kept at 5%
as is the default of the code. All available frequencies were used in the inversion. The
termination error was selected as 0.1%, much lower than the recommended value of
the code, in order to force the program to further inversion steps toward the goal of
reaching the nearest minima. After each inversion session consisting of 50 iterations,
some cell resistivities were adjusted manually. This is required in order to reduce the
number of inversion sessions. One way of validating the final model is to start the
inversion with different initial guesses and to examine the consistency of the results.
Generally, if the data do not contain sufficient information to solve a group of
parameters representing a certain subsurface feature, then the outcome of each
inversion trial will depend on the initial model. On the other hand, the parameters
which have some influence on the data will keep similar parameter values after
independent inversion attempts that use a variety of initial models. Therefore, to
justify our models, all sections were also inverted with starting models of
Vol. 164, 2007 The Geoelectrical Structure of Northwestern Anatolia, Turkey 1009
homogeneous half space of 1 ohm-m (results not presented). The comparison of all
inversion outcomes of a certain section leads to estimation of the depth of
investigation (e.g., OLDENBURG and LI, 1999) and confirms the existence of some
small-scale features. As an example, the RMS value for the initial half space model of
100 ohm-m for the first segment was 35.88, and was later decreased to 5.8. The
second and third segments produced 3.71 and 3.57 RMS values, respectively (Fig. 6).
Figure 6
Geoelectrical models obtained from 2-D inversion of the MT data. Resistive crust represented with black
color. Conductive zone below the crust represents an electrical asthenosphere, while hot spots and basin
deposits are in gray tone.
1010 E. U. Ulugergerli et al. Pure appl. geophys.,
Pseudosections of apparent resistivity and phase of impedance for observed and
calculated data are given in Figure 7. Some selected stations and corresponding
representative curves along the segments are shown in Figure 8. The first curve is
close to the NAF (WA11).
Generally, all sections exhibit information for depths of less than 30 km. We
assume that the inversion results are useful for geological interpretation since the
conductive and resistive local structures appear above this level.
Results in Figure 6 show that the general pattern in all models may be examined
in three resistivity ranges from surface to base. The first level (>10 ohm-m) is related
to topography and uppermost crustal setting (gray) extending down to 3 km. The
second level (>100 ohm-m) includes crustal structure (black), and is of non-uniform
thickness. The third level (10< and <100 ohm-m) is a conductive zone which
appears in all models. In the rest of the profile the resolution decreases because of
insufficient data coverage. It is noted that the structural pattern presented here is
obtained through the smooth inversion technique. Therefore, the imaged features are
blurred pictures of sharp boundaries.
Starting from the surface and northernmost part of the first profile, the findings
are as follows (Fig. 6a). Average depth of investigation is around 25 km in this
geoelectrical model. The model begins with a conductive zone (<4 ohm-m) that
represents the effect of the Dardanelles Strait. A detailed structural pattern of the
Dardanelles could not be obtained due to an insufficient number of stations on
the western side. The center of the geoelectrical model presents distinct features. The
conductive spots (< 10 ohm-m) appear beneath the NAF and WA7-8 and WA13
below 15 km, and the second feature emerges at both sides of the Can between WA9
and WA13 (Fig. 6a). In addition, the model divided into two zones vertically. The
upper part contains resistive blocks (>100 ohm-m) and the lower part is conductive
(<100 ohm-m). The boundary between the zones is irregular.
The second geoelectrical model is reliable down to 25 km and 30 km, on the
northernmost and southernmost sides, respectively. The model begins with a
conductive zone (4-100 ohm-m) between stations WA18 and WA34. Two conductive
zones (<2 ohm-m) of the model, 10 km below stations WA18 and WA28. Resistive
blocks (>100 ohm-m) extend from WA21 to WA37 at a depth of 2–25 km.
In the third geoelectrical model, extending down to 25 km, the shallow part of the
model may be subdivided into three conductive zones. The first one (<10 ohm-m) is
delineated between WA38–41. The second one (<60 ohm-m) covers the area from
WA43 to WA48. The last one (<60 ohm-m) is the northern end of the section.
Resistive unit (>100 ohm-m) is delineated along the model at a depth of 3–15 km.
Figure 8 presents the apparent resistivities and phases of impedances for the
selected stations. Continuous curves show the calculated data while the symbols
indicate the observed data. In general, the shallow parts of the sections correspond-
ing to low periods reveal 1-D character. However, the divergence of TE and TM
mode curves indicates 2-D structures in the deeper part of the resistivity sections.
Vol. 164, 2007 The Geoelectrical Structure of Northwestern Anatolia, Turkey 1011
Density Distribution of the Area
Gravity data (Fig. 9a) have been collected at 3–5 km intervals during the course
of a national project and later processed by MTA; the results have appeared in
some publications (e.g., AKDOGAN, 1995, 2000). The aim of presenting the data
here is to justify the lateral discontinuities in the geoelectrical model rather than
proposing a new density model for the region. Bouguer gravity data have been
imaged in a band of 10 km from either side of the MT profile. A density model was
created using the 2.5-D modeling scheme of the WinGLink� package by focusing
on the lateral discontinuities between the main structures obtained from the MT
data. No density analysis of geological units was performed. The position, shape
and boundaries of the structures were generated from the geoelectrical image
obtained from the MT data. Since the software needs density values of blocks
rather than density differences, the crustal background of the model was set to
2.85 g/cm3. Consequently, a simple model response that fits the gravity data was
obtained (Fig. 10a–c) by a trial-and-error procedure. Subsidence areas were
represented by a density value less than 2.6 gr/cm3 while the density of the crust
was assigned to 2.87 gr/cm3 or larger values. The density of the deep conductive
zones was set to 2.2–2.5 gr/cm3.
Magnetization Distribution of the Area
Aeromagnetic data (Fig. 9b) were also collected and processed by MTA
(AKDOGAN, 2000). The flight altitude and record interval were 625 m and 70 m,
respectively. The profile interval was set as 1–2 km. The reduction to pole was
performed by using 55o inclination and 4o declination angles for Turkey. The same
selection steps were also applied to the data for modeling purposes. Along the MT
lines, magnetic data were selected in a band of 10 km on both sides of the profiles. A
model was created using the 2.5-D modeling scheme of the WinGLink� package.
Position, shape and boundaries of the structures were generated from the image of
the geoelectrical model of the MT data. The background of the model was set at 79.5
as SI · 4p 103. The derived elemental model is shown in Figures 10d–f. Some shallow
zones have susceptibility values of 79.5 and the crust is represented by susceptibility
values of 159 to 238.7.
Figure 7
Observed apparent resistivity and phase of impedance: a) TE mode, b) TM mode. Upper, middle and
bottom panels are for Segment 1, Segment 2 and Segment 3, respectively. Small dots indicate data.
Abscissas are relative intervals (km) of stations while ordinates are periods (sec).
b
Vol. 164, 2007 The Geoelectrical Structure of Northwestern Anatolia, Turkey 1013
10-3
10-2
10-1
100
101
102
103
104
10-2
10-1
100
101
102
103
Ap
p.R
es.(
oh
m-m
)TE-obs. TE-calc. TM-calc. TM-obs.
10-3
10-2
10-1
100
101
102
103
0
30
60
90
Ph
ase
(deg
ree)
WA11
10-3
10-2
10-1
100
101
102
103
104
10-2
10-1
100
101
102
103
Ap
p.R
es.(
oh
m-m
)
WA20
10-3
10-2
10-1
100
101
102
103
0
30
60
90
Ph
ase
(deg
ree)
10-3
10-2
10-1
100
101
102
103
104
10-2
10-1
100
101
102
103
Ap
p.R
es.(
oh
m-m
)
10-3
10-2
10-1
100
101
102
103
0
30
60
90
Ph
ase
(deg
ree)
WA34
10-3
10-2
10-1
100
101
102
103
104
Period (sec)
10-2
10-1
100
101
102
103
Ap
p.R
es.(
oh
m-m
)
WA39
10-3
10-2
10-1
100
101
102
103
Period (sec)
0
30
60
90
Ph
ase
(deg
ree)
Figure 8
Sounding curves for selected stations. Dots are observed data while solid lines are response of the 2-D
model, error bars are of observed data Abscissas are periods (sec).
1016 E. U. Ulugergerli et al. Pure appl. geophys.,
Figure 9
MT profile with (a) gravity map of western Anatolia and (b) magnetic map of western Anatolia.
Vol. 164, 2007 The Geoelectrical Structure of Northwestern Anatolia, Turkey 1017
Integration and Discussion
Evaluation of the geoelectrical models requires additional information. The main
steps are given in subsections.
Evaluation of Research Depth
Negative gravity anomalies (gray to black in Fig. 9a) indicate isostatic thickening
of the continental crust towards the east (e.g., see ATEs et al., 1999). Considering the
average asthenosphere depth (55+/-5 km; ILKıSıK. 1995) in western Anatolia, the
depths of investigations in all of these geoelectrical models never reached the upper
mantle. Therefore, both the high resistive unit (>100 ohm-m) and relatively medium
resistive level (10< and <100 ohm-m) observed throughout the majority of the
sections should be parts of the crust.
The resistive part of the crust extends from the Dardanelles to WA9 and from
WA14 to the end of the model at a depth of 3–25 km in the first segment. Then it
extends from WA21 to WA37 at a depth of 2–25 km in the second segment.
Fractured and thinned crust (>100 ohm-m) is delineated along the model at a depth
of 3–15 km in the last segment. Fragmentation and varying thickness along all
profiles are the result of tectonic activity in the region. It is observed that the crustal
thickness decreases towards the southern part of the segment. This is in accord with
regional extensional regimes (e.g., YıLMAZ et al., 2000). All extensions were observed
around the Menderes Massif, at the edge of the last segment.
Conductive Lower Crust
The conductive zone below the upper crust is subject to considerable researches
(e.g., OGAWA, 1987; HYNDMAN, 1988; JONES, 1992; NESBITT, 1993; MARQUIS et al.,
1995; UTADA et al., 1996; CAGLAR 2001; SATOH et al., 2001). WANNAMAKER et al.
(1997) did a survey in the eastern margin of the Great Basin, southwestern Utah and
eastern Nevada. Great Basin and Western Anatolia both have similar tectonic
settings. The general pattern of both areas is similar to each other. The MT method
mapped out the crust only. Both areas have low resistivity in the lower crust. SATOH
et al. (2001) presented a survey result from the Kuril Arc, Japan, and also found a
conductive layer in the lower crust.
Three reasons may be considered for the relatively low values of resistivity at this
depth; the first is the graphite-like conductive minerals, the second is the presence of
fluid trapped in the crust, and the last one is partial melting. There is no report for
Figure 10
(a–c) Gravity data along the MT profile; (d–f) Magnetic data along the MT profile. Both magnetic and
gravity data selected in a range of 10 from both sides of the profile. Abscissas are relative intervals (km) of
MT stations while ordinates are depth (m) in the lower panels and data units for the upper panels.
Susceptibility values (s) are scaled by 4p.
b
Vol. 164, 2007 The Geoelectrical Structure of Northwestern Anatolia, Turkey 1019
such a large-scale conductive minerals in the vicinity of the study area. AKYOL et al.
(2006) showed that western Anatolia is characterized by crustal velocities that are
significantly lower than average continental values. It is also noted that seismological
research (not presented) indicates that the average depth to the brittle–ductile
structural boundary is around 20 km in the study area. There are a few epicenters
below this level. Thus the conductive zone is not expected to be ductile. Curie depth
research (e.g., AYDıN et al., 2005) indicates that this depth level has low or no
magnetisation, i.e., the temperature should exceed at least 580 C. ALDANMAZ et al.
(2000) stated that geochemical analysis of the late Miocene alkaline rocks in western
Anatolia indicates that these rocks formed by partial melting of enriched astheno-
spheric mantle source. Direct contact of hot upwelling asthenospheric mantle
provides a hot thermal anomaly and initiates melting. Late Cenozoic volcanic
activity occurred along with the creation of magma chambers in the crust including a
partially melted zone. ERCAN et al. (1985) and CAGLAR (2001) also reached a similar
conclusion for western Anatolia.
Tectonic Units
The geoelectrical models cover the eastern boundary of the Sakarya continent.
The features which emerge under WA10 and WA13 in the vicinity of Can are related
to branches of the NAF. The NAF contains a few interlacing faults and consequently
is represented over a wider area and with a large vertical extension.
The western flank of the Simav fault zone (SEYITOGLU, 1997) appears around
WA33–34. The shallow part of the third model may be subdivided into three
subsidence areas. The first one (<10 ohm-m), delineated between WA38–41, is the
Gordes Basin, the border of which occurs between the Izmir - Ankara Suture Zone and
the Menderes Massif. The main fault which bounds the basin is located on its eastern
side (SEYITOGLU and SCOTT, 1994). The second one (<60 ohm-m) is theDemirci basin,
which covers the area fromWA43 toWA48. The last one (<60 ohm-m) is the northern
end of Alasehir graben. All three of the subsidence areas have irregular bottom
surfaces. Since the last profile ends in the Alasehir graben, the footwall-like structure
shows a fault character in the northern part of the graben (WA52).
Figure 11
Proposed model. White area is crust. The thick lines are main faults, + represent magma intrusions, and v
are partially melted areas. ¯ and • indicate the movement direction of the walls of the NAF.
Vol. 164, 2007 The Geoelectrical Structure of Northwestern Anatolia, Turkey 1021
Deep Hot Spots
The average heat-flow value for the study area is �25% higher than the average
of the rest of Turkey. The heat flow obtained from magnetic data, which also was
verified with available real observations, increases to 229 mW/m2 in the region (AKıN
et al., 2006). Additionally, recent heat-flow research related to Curie depth obtained
from magnetic data (e.g. AYDıN et al., 2005; SALK et al., 2005; AKıN et al., 2006)
indicates that western Anatolia has high gradient values and shallow Curie depth
values. HISARLı (1995) has estimated Curie-point depths of between 8 and 12 km. in
the Balıkesir area. TANAKA et al. (1999) states that 10 km or shallower Curie depth
values point out volcanic and geothermal fields which is the exact description of the
vicinity of the first profile. In light of this information, the conductive zone under
WA22 may be interpreted as a magma chamber that was a source of Upper
Oligocene volcanism to the NE of Edremit (e.g., YILMAZ, 1990). The second
conductive zone (<2 ohm-m) of the model, below station WA28, is related to
another conductive spot. This area also has low magnetization (Fig. 10e) and high
heat flow values (�120 mW/m2) between Balıkesir and Bigadic (AKıN et al., 2006). A
possible heater for the geothermal sites can also be connected to magma chambers on
the Biga Peninsula. This chamber could be a relict of widespread calc-alkaline
magmatism that occurred in the Early - Middle Miocene on the Biga Peninsula (e.g.,
ALDANMAZ et al., 2000).
Additional Data
Lateral variations are checked by using different methods (Fig. 10). The
branch of the NAF appears with low values in density and susceptibility models.
All sediment fillings at the surface also show low density and susceptibility values.
The third model has a highly resistive block until station WA50, indicating that
high susceptibility values could be expected in the region. Nevertheless, the
magnetic data present no anomaly along the profile. According to the geological
map, the profile passes over the ophiolites; however, the magnetic map does not
exhibit strong variations at that location. The contributions of thin ophiolites to
the data are probably removed via some filtering process applied as a part of the
data-processing scheme. Contrastingly, the Menderes Massif presents lower
susceptibility; therefore, the southernmost part of the magnetic data exhibits a
flat pattern.
Earthquakes which occurred on the NAF line up around Can, where the first
geoelectrical model also provides structural information. The seismological data
supports the electromagnetic model by indicating an active zone along the NAF.
Lower-magnitude earthquakes have occurred along the second model. Densely
occurring epicenters indicate high activity below the third segment. Horst and graben
structures in the basins are the main sources of the earthquakes.
1022 E. U. Ulugergerli et al. Pure appl. geophys.,
Geological Model
A geological model based on the MT data is presented in Figure 11. The
comparison with the regional map given in Figure 2 illustrates that all features along
the segments are sensed by the MT data and represented in the geoelectrical models.
Crust is illustrated by blank areas and the faults are delineated with thick lines, while
magma intrusions and partially melted areas are designated with patterns in
Figure 11. All basins are bounded by normal and listric faults. The fractured nature
of crust, delineated by partially melted areas, may also contain magma chambers.
Question marks indicate unresolved parts of the geoelectrical models.
Conclusions
In the proposed geoelectrical sections, generally deeper conductive parts are
related to hot areas (such as below WA22 and WA29). However, at shallow depths,
the conductive anomalies correspond to the sedimentary basins while highly resistive
regions are related to major structures.
Variations in magnetic and gravity data along the profiles also agree with the
lateral variations in geoelectrical models. Basin fillings which correspond to high
conductivities in shallower parts of the geoelectrical sections needed to be
represented by low density and susceptibility contrasts to catch local variations.
Themajor structures, sedimentary basins and igneous activity can easily be discerned
in the resistivity sections. In the Canakkale - Can area, the southern branches of the
NorthAnatolianFault are clearly visible. Farther south around Sındırgı, the Simav fault
appears as one of the main structures. The Gordes andDemirci basins are also resolved.
It is notable that the crust thins in the Alasehir Graben, one of the major E-W trending
grabens of western Turkey. The bottom depths of the basins and grabens are around
3 km. The deepest is the Gordes basin, while the Demirci basin is the shallowest.
Western Turkey has a thinned, fractured crust with extensive magmatism as is
typical for regions affected by extensional tectonics. The crustal part of the structure
extends along the model between depths of 3 and 25 km. In addition, the magmatism
which occurred in the late Oligocene caused decreasing resistivity of the crust at
greater depth.
Acknowledgements
This paper is part of the national geology and geophysics project (Naci Gorur,
coordinator) supported by TUBıTAK, Project No. YDABCAG-422/G. The MT
data were gathered by MTA as a part of a national project. We also thank
Geosystem for allowing us to use the WinGLink package. We extend thanks to
Vol. 164, 2007 The Geoelectrical Structure of Northwestern Anatolia, Turkey 1023
Dr S. Ozden (C. Onsekizmart University) for reading the manuscript and making a
number of suggestions. Editor G. Heinson and both reviewer, I. Ferguson and M.
Unsworth improved the manuscript.
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