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The strain history of tectonically deformed rocks may be deduced by petrofabric

study with the help of shape, orientation and axial ratio determination of deformed

minerals and grains in the rock. Under the high stress the minerals are stretched

reoriented and new growth occurred parallel to the less stress direction and

represent a distinct fabric. Thus the individual grain shapes and their orientation

constitute the rock petrofabric. Maximum deformed rocks contain paramagnetic

and ferromagnetic minerals with distinct orientation respond under the

deformational stress in which magnetic fabric study is useful to deduce the strain

pattern. The magnetic fabric study through Anisotropy of Magnetic Susceptibility

(AMS) is first time used by Graham (1954) as a petrofabric element and which

reflects the magnetic susceptibility anisotropy ellipsoid in a rock as the strain

ellipsoid.

The AMS, a physical property of the rock, represents more perfect picture

of deformation then microscopic strain fabric study. Its relationship with fabric of

the rock arises because the most magnetically susceptible minerals can have

distributions of shape orientations or lattice orientations influenced by the

kinematic history of the fabric, and the magnitude ellipsoid of susceptibility may

be a faithful representation of the total fabric (Borradaile, 1988; Aranguren, et al.,

1996). Borradaile (1988), Housen et al. (1993) and Aranguren, et al. (1996) have

shown the geometrical relationship between the magnetic foliation and field

structures and proposed the different models of the composite magnetic fabrics.

ANISOTROPY OF MAGNETIC

SUSCEPTIBILITY; STRAIN FABRIC

CHAPTER-V

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The AMS study is very useful to explain the neotectonic stresses and

active tectonics (Borradaile and Henry, 1997; Borradaile and Hamilton, 2004;

Dubey and Bhakuni, 2008). Jayangondaperumal et al. (2010b) have used AMS

fabric to understand the kinematics and infer recent tectonics in the Garhwal

Inner Lesser Himalaya.

The rocks of the area are metamorphosed under the greenschist and

amphibolite facies and contain mainly diamagnetic and paramagnetic minerals,

also explained by Agarwal et al. (2010).

The strain ratios and the orientation of the strain ellipse estimated by

different methods on the fabrics of deformed rocks by different workers.

Srivastava (2004) has used elongated porphyroblasts in augen gneisses to

determine the shape of finite strain ellipsoid, and explained multiple deformations

in the Dudatoli-Almora crystallines. Two dimensional strain estimation from

weakly deformed rocks, where it is difficult to precisely define the longer and

shorter axis of ellipse/grain, have been performed by Srivastava (1995, 2009).

In present work, the petrofabric strain is measured by using AMS

technique and correlated with strain fabric results obtained by using Rf/φ

technique (Ramsay, 1967; Dunnet 1969; Dunnet and Siddan, 1971) and also by

plotting Flinn diagram (Zingg, 1935; Flinn, 1962) of axial ratio of microscopic

elliptical markers.

Application of AMS technique and correlation with meso-microscopic

fabric is also attempted by Jayangondaperumal et al. (2010a), Devrani et al.

(2009) and Agarwal et al. (2010). Mamtani and Vishnu (2011) have investigated

the use of AMS data to provide the information about the shape of the strain

ellipsoid in the micaceous quartzites.

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5.1 ANISOTROPY OF MAGNETIC SUSCEPTIBILITY (AMS)

TECHNIQUE:

AMS technique is very sensitive to read the schistosity developed at the last

phase of deformation with early schistosity or bedding. The orientation of

principal susceptibilities represents distribution of magnetic minerals fabric in

rock; however, the rock composition and metamorphic grade may affect the

anisotropy of magnetic susceptibility and bulk susceptibility of rock type

(Borradaile and Henry, 1997; Nakamura and Borradaile, 2004). The bulk

susceptibility (Km), anisotropy susceptibility and other forms of magnetic

anisotropy commonly play a great roll to determine the state of strain and

petrofabric, and are also used as strain indicators. The AMS may be represented

by magnitude ellipsoids, geometrically shaped by three magnetic principal axes

(K1≥ K2≥K3), those are closely related to the strain axes (λ1>λ2 >λ3). There are

two elements, magnetic foliation ‘F’ (K1- K2 Plane) and magnetic lineation ‘L’ (K1)

(Tarling and Hrouda, 1993; Aubourg, et al., 2000; Sidman, et al., 2005) and their

anisotropy parameters are described by eccentricity ‘Pj’ and its shape ‘T’.

Measurement of AMS is a fast method for investigating the fabric pattern

in plastically deformed rocks, and comment about strain in them (e.g., Borradaile,

1991; Tarling and Hrouda, 1993; Nakamura and Nagahama, 1997; Borradaile

and Jackson, 2004; Mukherji et al., 2004; Mamtani and Greiling, 2005; Sen et al.,

2005; Sen and Mamtani, 2006; Mamtani and Sengupta, 2009, 2010; Majumder

and Mamtani, 2009; Agarwal et al., 2010; Vishnu et al., 2010; Pant et al., 2011). It

is the useful method in delineating the changes induced due to brittle deformation

in fractured rocks in faults/thrust zones (Ozima and Kinoshita, 1964; Hallwood et

al., 1992; Nakamura and Nagahama, 2001; Pant, et al., 2011). AMS has been

used successfully to understand deformation and tectonic setup of the Himalayan

region by earlier workers (Jayangondaperumal and Dubey, 2001; Dubey et al.,

2004; Dubey and Bhakuni, 2008; Tripathy et al., 2009; Agarwal et al., 2010;

Jayangondaperumal et al., 2010). In present work the AMS analyses of rocks

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from the NASZ (Pancheshwar-Seri-Seraghat-Dwarahat- Gairsen region) are

performed with the aim of evaluating the deformation and tectonics of the region

(Fig. 1). Field and AMS data are compared, and data from thermal

demagnetization of some samples are presented to evaluate the magnetic

carriers of the AMS.

Detail study has been done of the structures along the NASZ, by carrying out the

AMS analysis, which is a useful tool to study fabrics in tectonites.

5.1.1 AMS Parameters

All minerals have magnetic properties at temperatures above absolute

zero (0 K) (Tarling and Hrouda, 1993). The results of the AMS data for all

transects of the area are given in table I, II, III and IV. The magnetic susceptibility

(K) is defined as the ratio between the induced magnetization (M) of the

specimen and the applied magnetic field (H).

K = M/H

The AMS is a second rank tensor with three principal axes (K1≥K2≥K3),

where K1 is the magnetic lineation and K3 is normal to the magnetic foliation

(Tarling and Hrouda, 1993). The bulk magnetic susceptibility ‘Km’ is the arithmetic

mean of the principal susceptibilities (Km = K1+K2+K3/3).

The magnitude of anisotropy is expressed by ‘Pj’ parameter based on

logarithmic values of susceptibility (Jelinek, 1981; Tarling and Hrouda, 1993;

Sidman et al., 2005).

Pj = exp√ [2 {(η1- ηm)2 +( η2- ηm) 2+( η3- ηm) 2}]

Where η1= In K1

η2 = In K2

η3 = In K3

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ηm= (η1+ η2+ η3)/3

The shape of the anisotropy ellipsoid or eccentricity of the ellipsoid is given

by the shape parameter ‘T’ (Jelinik, 1981; Hrouda, 1982; Borradaile, 1988).

T= [2 In (K1/K2)/In (K1/K2)]-1

The value of T varies from -1 to +1. T>0 implies the oblate shape, whereas T<0

suggests the prolate shape of magnetic susceptibility ellipsoids.

5.2 METHODOLOGY

Oriented rock samples were collected from the area across the NAT. 316 cores

(25.4 mm x 22 mm) from 65 oriented rock specimens were obtained for AMS

analysis. AMS data were generated in the Palaeomagnetic Lab of the Wadia

Institute of Himalayan Geology, Dehradun, India. To determine the AMS, each

core was analyzed in 15 different directions with reference to the north using a

KLY-3 Kappabridge (AGICO, Czech Republic), which has a sensitivity of 2 x 10-6

(SI) and accuracy of 0.1%. AMS study of the specimens of the area revealed the

mean susceptibility values <800 x 10-6 SI, and has been grouped according to

their mean magnetic susceptibility ranges in five groups (i) >500 x 10-6 (SI), (ii)

500-300 x 10-6 (SI), (iii) 300-200 x 10-6 (SI), (iv) 200-100 x 10 -6 (SI) and (v) 100-

10 x 10-6 (SI). These low susceptibilities indicate a minor contribution from

ferromagnetic minerals (Rochette, 1987). In AMS study, the knowledge of

magnetic carriers is very important for reliable results. The recognition of these

magnetic carriers was done in our samples through petrography and

thermomagnetic curves. In order to constrain the ferromagnetic and

paramagnetic contribution, 10 samples of various mean susceptibilities (Gh25, D3,

S5, C105, Gh12, D2, C38, S4, C72 and C10 in order of decreasing susceptibility) were

selected and examined through measuring temperature variation of the bulk

magnetic susceptibility on the samples by using TSD-2 Schonstedt thermal

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demagnetizer and temperature variation of susceptibility by using the

Kappabridge (Jelinek and Pokorny, 1997) (Table 5).

In addition to the AMS, the petrofabric strain study with the help of Rf/φ and

Flinn plots was carried out of 13 samples across the NASZ. In this petrofabric

measurement the elliptically deformed feldspar and quartz grains have been used

for strain analysis at the microscopic level. For which sections were prepared by

cutting the specimens in XZ and YZ directions. The mineral elongation lineation

direction is the X-direction of finite strain ellipsoid (Lister and Hobbs, 1980; Joy

and Saha, 2000; Joshi and Tiwari, 2004; Bhattacharya and Weber, 2004),

foliation plane is XY plane and Z is perpendicular the XY plane. The Rf/φ and

Flinn plots are prepared by using the versatile Windows based software, the

“Window32.Bit Platform” developed by Roday (2003).

5.3 AMS STUDY

5.3.1 Petrography and Magnetic Mineralogy

Debacker et al. (2010, 2011), Mamtani and Vishnu, (2011) investigated the

magnetic properties of a variety of lithostratigraphic units of the Brabant Massif.

Magnetic techniques employed are the determination of (a) magnetic

susceptibility (MS, for methodology, see Ellwood et al., 2000 and references

therein), (b) the temperature-dependent variation in MS within the “room

temperature interval” (for methodology, see Herbosch et al., 2008 and Debacker

et al., 2009, 2010), (c) the anisotropy of magnetic susceptibility (AMS) at room

temperature (for methodology, see Jelinek and Pokorny, 1997), (d) the magnetic

mineralogy by means of a stepwise thermal demagnetisation of a three-axis

isothermal remnant magnetism (for methodology, see Lowrie, 1990).

In present work the magnetic mineral study was done by means of

petrography and stepwise thermal demagnetization method (for methodology,

see Lowrie, 1990).

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Each rock unit in the NASZ shows intense deformation and attendant

recrystallization. Petrographic study shows that the mylonitic to proto-mylonite

rocks consist of fine to medium grained quartz, K-feldspar and some amount of

muscovite and biotite. Ultra-mylonitized granite-gneiss contains very fine and lineated

grains of quartz, feldspar, muscovite and biotite with very small ferromagnetic

(pyrrhotite) minerals (Fig. 5.1 a). Schists are mainly composed of biotite,

muscovite, chlorite and garnet (Fig. 5.1 b). Garnet in schists is associated with

quartz, muscovite, biotite, chlorite and plagioclase minerals. Almora quartzite

often displays schistosity that is defined by micaceous minerals. Quartzarenite of

the Rautgara Formation dominantly consists of quartz (diamagnetic minerals)

with <10% paramagnetic minerals. However, at the NAT contact the

metasedimentary rocks are characterized by the presence of biotite and

muscovite (>10%). Thin sections of fractured rocks along the fault zone exhibit

nucleation of very fine grained (~6μm) iron oxides in the micro veinlets intruded

along the microfractures (Fig. 5.1 c, d).

A simple thermal heating of rock sample may cause of not only magnetic

phase transformation but it can change the magnetic mineral grain size. Since

under the different successively applied heating treatment the rock is not

modified, and measurement gives accurate data to determine the magnetic

carriers.

The thermal magnetic heating curves of ten samples represent to discrete

susceptibility and temperature determinations (up to 750°C), which have direct

relation with magnetic carriers and used to identify the magnetic minerals in the

rock specimen (Fig. 5.2). It is noted that samples C105, D2, C38, S4, C72, C10 and

Gh8 contain paramagnetic minerals. Samples D3, S6 and Gh12 show sudden

decrease in susceptibility around 300 to 380°C; this may be due to presence of

some monoclinic pyrrhotite (Dekkers, 1988, 1989; Aubourg et al., 2000). Sample

C105 shows an increase in susceptibility at ~500°C, suggesting that magnetite has

possibly formed during experiment at this temperature (Hrouda, 1994; Hrouda et

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al., 1999). The rock units contain predominantly phyllosilicates, which are the

paramagnetic minerals and main source of AMS in schist and gneissic rocks.

Phyllosilicates are important and strongly anisotropic component of tectonites,

and their contribution to AMS has been well documented by Henry (1990, 1992),

Borradaile and Werner (1994), Borradaile (2001), Borradaile and Jackson (2009).

The growth of phyllosilicates (i.e. biotite >10%) controls the magnetic

susceptibility of the rock unit in highly sheared quartzarenite along the thrust/fault

contact (samples C64, C61, C100 and D2). Similarly, the nucleation of iron oxides

(very fine grain magnetite) along the microfractures is found (samples C73, C75,

C98 and C100).

Figure 5.1: Microphotographs showing (a) magnetic mineral vein within quartz and mica grains aggregate, (b) garnet, quartz, mica and feldspar minerals in the garnet mica schist, (c) and (d) veins of iron oxide minerals along the micro-fractures in quartzo-feldspathic rock. Scale bar 1mm.

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Figure 5.2: Thermal demagnetization plots of magnetic susceptibility (Km) of 10 core samples at different temperatures up to 750º C.

5.3.2 Analytical Results of AMS study

Petrography and thermal demagnetization studies reveal that the most samples

are not significantly influenced by ferromagnetic minerals. However, there are

some samples of ultra-mylonitized granite (Gh12, S6, C98 and D3) from the sharp

contact of the fault plane show relatively high susceptibility with high degree of

anisotropy which is due to presence of ferromagnetic minerals (pyrrhotite,

magnetite). Mylonitized, proto-mylonitized and ultra-mylonitized granite rocks

exposed along the NAT have high magnetic susceptibility (200 – 796 x 10-6 SI),

whereas schistose rocks have relatively low susceptibility (70 – 337 x 10-6 SI).

However the specimens G25 and C105 those have relatively high susceptibility

(Tables I, II, III and IV) due to the presence of porphyroblasts of garnet. Garnet is

characterized by volume susceptibility of the same magnitude as biotite. Although

it does not contribute to anisotropy, it may influence bulk susceptibility (Hrouda

and Ullemeyer, 2001). In general quartzarenite gives negative susceptibility

(contains diamagnetic minerals i.e. quartz) (Gh10). In the study area due to

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presence of mica content and growth of very fine grain iron oxides, it is giving

positive susceptibility (3 - 192.8 x 10-6 SI) and in some samples it is cause of

high susceptibility with high anisotropy. Few specimens of quartzarenite are

giving high anisotropy (~1.3) with low susceptibility (1 - 8 x 10-6 SI) (Tables I, II, III

and IV), which is due to presence of very thin discrete layers (<20µm) of very fine

grain iron oxide along the microfractures in the specimens (D8A, D36, S8, D25, D5

and C81).

AMS data represents well defined magnetic foliations in the rocks of the

Saryu Formation and shows association to field foliations and deformation in the

area. In thin sections, Shape Preferred Orientation (SPO) is commonly inclined to

the compositional layering, and AMS data are inferred to give resultant schistosity

due to superimposition of crystal orientation on compositional layering.

As early described the whole area is divided into four sectors and AMS

study is taken up accordingly and each sector described in detail domain-vise.

I. Pancheshwar-Seri Sector

Eastern part of the NASZ is studied by taking various traverses across the NAT in

Pancheshwar-Seri sector (Fig 5.3):

The Pancheshwar area comprises N-S and ENE-WSW trending fault

across the NAT inferred by geomorphic and structural data, and strongly

supported by the AMS fabric data of the area. Magnetic foliation planes do vary

with the NAT trend and field foliation, whereas they are showing good

relationship with the N-S and ENE-WSW oriented faults. Due to limited approach

along the ENE and WSW oriented fault plane only two samples were collected,

which are giving N-S (P1 specimen) and ENE-WSW (P2 specimen) magnetic

foliation plane orientation respectively away and near the fault plane trace (ENE-

WSW). Here N-S orientation of the magnetic foliation plane in P1 specimen

represents the impact of the N-S oriented fault (Fig 5.4a).

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Fig

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5.3

: G

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Figure 5.4: (a) Lower hemisphere equal area projections of magnetic and field foliation at different sites in Pancheshwar domain, (b) Pj vs. Km, (c) T vs. Km and (d) Jelinek plot (T vs. Pj) for all samples of the NASZ, Pancheshwar-Seri sector. T= shape parameter and Km= mean susceptibility; Pj =corrected degree of magnetic anisotropy.

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P3a, P3b and P4 samples were taken along the N-S oriented fault plane

and across the NAT, represent parallel to sub-parallel magnetic foliation

orientations with the fault plane. Magnetic lineations are horizontal to sub-

horizontal, gently plunging towards N (samples P3a, P3b, P4) and W (sample P2).

However somewhere they lie on the intersection of field foliation and magnetic

foliation plane (P2, P4). In figure 5.3 b, Pj vs. Km plot of the granitic gneiss shows

inverse relationship between the values of Pj and Km. The AMS data for mica

schist, micaceous quartzite, granitic gneiss and mylonites lie in neutral to oblate

field (T=1 and T>0) (Fig. 5.4 c, d), which is due to development of flaky

micaceous minerals and may be also due to flattening strain (Mukherji et al.,

2004; Mamtani and Sengupta, 2010; Vishnu et al., 2010).

In Netra domain, the strike of magnetic foliation plane do vary from WNW-

ESE to NW-SE, which are parallel- sub parallel to the NAT trend and making low

angle with field foliation. Magnetic lineations are horizontal to sub-horizontal,

whereas magnetic foliations do vary from gentle to steeply dipping (Fig. 5.5 a). P j

vs. Km plot of the granitic gneiss shows inverse relationship, whereas schist and

ultramylonites representing positive relation between the values of Pj and Km (Fig.

5.5 b). In T vs. Km and Pj vs. T plots data lie completely in oblate field (T>0) (Fig.

5.5 c, d).

In the Ghat domain the geomorphic and structural data inferred NW-SE

trending fault parallel to the NAT (in SW of the NAT) (Fig. 5.6 a). Magnetic

lineations are gentle to steeply plunging towards WSW to SSE directions.

Magnetic foliation planes are vertical to sub-vertical and variably oriented from N-

S to ENE-WSW whereas near the NAT and its subsidiary fault plane, they show

parallel to sub-parallel orientation with the NAT and NW-SE oriented fault (Fig.

5.6 a).

Pj vs. Km plot shows inverse relationship in the granitic gneiss and

protomylonite units (Fig. 5.6 b). Highly sheared quartzarenite represents prolate

to oblate field in the T vs. Km and Pj vs. T plots. The data of granitic gneiss, mica

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bearing quartzite and mylonite lie in the neutral to oblate and oblate field,

respectively. Here micaceous quartzite (Saryu Fm.) is showing high anisotropy

with high susceptibility (Fig. 5.6 c, d).

Figure 5.5: (a) Lower hemisphere equal area projections of magnetic and field foliation at different sites in Netra domain, (b) Pj vs. Km, (c) T vs. Km and (d) Jelinek plot (T vs. Pj) for all samples of the domain in the NASZ, Pancheshwar-Seri sector. T= shape parameter and Km= mean susceptibility; Pj =corrected degree of magnetic anisotropy.

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Figure 5.6: (a) Lower hemisphere equal area projections of magnetic and field foliation at different sites in Ghat domain, (b) Pj vs. Km, (c) T vs. Km and (d) Jelinek plot (T vs. Pj) for all samples of the domain in NASZ, Pancheshwar-Seri sector. T= shape parameter and Km= mean susceptibility; Pj =corrected degree of magnetic anisotropy.

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Figure 5.7: (a) Lower hemisphere equal area projections of magnetic and field foliation at different sites in Rameshwar domain, (b) Pj vs. Km (c), T vs. Km and Jelinek plot (T vs. Pj) for all samples of the domain in the NASZ, Pancheshwar-Seri sector. T= shape parameter and Km= mean susceptibility; Pj =corrected degree of magnetic anisotropy.

The Rameshwar area is characterized by two faults trending NNE-SSW and

NE-SW. The magnetic foliation planes varyingly oriented ESE-WNW to NNW-

SSE. Near NAT, the magnetic foliations are trending parallel to the NAT plane,

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whereas in the proximity of the faults their orientation swings from ESE-WNW

through NW-SE to NNW-SSE. At and around the intersection area of the fault

planes, the strike of magnetic foliation planes are NW-SE and NNW-SSE, where

minimum magnetic axes (K3) on an average oriented towards NE and

representing σ1 of the conjugate set of the faults (Fig. 5.7 a). Pj and Km plot is

giving independent values of mylonite, schist and granitic gneiss (Fig.5.7 b). T vs.

Km and Pj vs. T plots are showing prolate to oblate shape of magnetic ellipsoids

(Fig. 5.7 c, d).

II. Seri-Seraghat Sector

This sector of the NASZ is characterized by superposed transverse Rantoli fault

(Valdiya, 1976) or Saryu River Fault (Pant et al., 2007) which coincide with the

trend of the NAT (Fig. 5.8).

At the NW terminal part of the Rantoli Fault the NAT swings from SW to

SSE orientation and coincides with NNW-SSE trend of the fault. Here the

magnetic foliations show parallelism with the NAT and become parallel/sub-

parallel to the Rantoli Fault as moving toward the Fault plane. Stereo projections

show that the magnetic foliations are vertical to sub-vertical, and lineations (K1)

are horizontal near the Fault plane (Fig. 5.9 a), however near the NAT contact

they are gently dipping (with variable orientation) (Fig. 5.9 a). Pj and Km plot

shows positive relationship in the schist and micaceous quartzite (Fig. 5.9 b). T

vs. Km and Pj vs. T plots show prolate to oblate shape of magnetic ellipsoids (Fig.

5.9 c, d).

In the Naichun-Rantoli area the AMS data shows that the magnetic

foliations dominantly represent to NNW-SSE oriented Rantoli Fault. Near the fault

plane the magnetic foliation are parallel to sub-parallel to the Fault plane and

trending NNW-SSE to N-S, whereas one specimen (S7) away from the fault plan

giving WNW-SES trend. Magnetic foliation planes are steeply inclined with

horizontal magnetic lineation except one specimen S6 (gently plunging) (Fig. 5.10

a).

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Figure 5.8: Geological map of the Seri-Seraghat sector showing distribution of various lithounits and position of AMS samples.

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Figure 5.9: (a) Lower hemisphere equal area projections of magnetic and field foliation at different sites in the Sartola- Nali domain, (b) Pj vs. Km, (c) T vs. Km and (d) Jelinek plot (T vs. Pj) for all samples of the domain in the NASZ, Seri-Seraghat sector. T= shape parameter and Km= mean susceptibility; Pj =corrected degree of magnetic anisotropy.

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Figure 5.10: (a) Lower hemisphere equal area projections of magnetic and field foliation at different sites in the Naichun- Rantoli domain, (b) Pj vs. Km, (c) T vs. Km and (d) Jelinek plot (T vs. Pj) for all samples of the domain in the NASZ, Seri-Seraghat sector. T= shape parameter and Km= mean susceptibility; Pj =corrected degree of magnetic anisotropy.

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Mica bearing quartzarenite shows high anisotropy with positive susceptibly

(Fig. 5.10 b). Pj and Km data of proto-mylonite, mylonite to ultramylonites explain

the decrease in the susceptibility with increase in anisotropy (proto-mylonite to

mylonite) and then increase in susceptibility with increase in anisotropy (mylonite

to ultramylonites) (Fig. 5.10 b). Here plots are showing positive relationship in the

data of schist and micaceous quartzite. Km vs. T and Pj vs. T plots are

representing neutral to oblate shape of magnetic ellipsoids (T=0 and T>0) (Fig.

5.10 c and d).

III. Seraghat-Dwarahat Sector

Seraghat-Dwarahat sector comprises a large area, has been further subdivided

for detail study into two regions i.e. Seraghat-Someshwar and Someshwar-

Dwarahat.

(i) Seraghat-Someshwar Domain

This region is characterized by NNW-SSE oriented Takula Fault and NE-

SW oriented Rasiyari Fault, however the fabrics of the rock units are dominatingly

controlled by the NAT. the detail AMS study is done across the NAT (Fig. 5.11).

Sampling in the Kaphligair area was carried out across the NAT and along

the Rasiyari fault. Here the magnetic foliation planes have parallel to sub-parallel

orientation with the NE-SW oriented fault plane. Magnetic lineations are

horizontal to gently plunging with vertical magnetic foliation planes (Fig. 5.12 a).

Similar to other area, here AMS data of mylonite in plot Pj vs. Km shows inverse

relation ship (Fig. 5.12 b). In Km vs. T and Pj vs. T plots data lie in oblate (T>0) to

prolate field (T<0) (Fig. 5.12 c, d).

The Kanarichhina area is mainly deducing the NAT dominating AMS

results. Magnetic foliations are steeply inclined, parallel to sub-parallel to the NAT

and lineation gentle to steeply plunging with variable orientations (Fig. 5.13 a).

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Fig

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Figure 5.12: (a) Lower hemisphere equal area projections of magnetic and field foliation at different sites in the Kaphligair region, (b) Pj vs. Km, (c) T vs. Km and (d) Jelinek plot (T vs. Pj) for all samples of the region in the NASZ, Seraghat-Someshwar domain. T= shape parameter and Km= mean susceptibility; Pj =corrected degree of magnetic anisotropy.

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Figure 5.13: (a) Lower hemisphere equal area projections of magnetic and field foliation at different sites in the Kanarichhina region, (b) Pj vs. Km, (c) T vs. Km and (d) Jelinek plot (T vs. Pj) for all samples of the region in the NASZ, Seraghat-Someshwar domain. T= shape parameter and Km= mean susceptibility; Pj =corrected degree of magnetic anisotropy.

Magnetic foliation orientations in the Saryu rock units support N-S or

NNW-SSE compression in the area. Similar to other area, AMS data of proto-

mylonite and mylonite in the Pj vs. Km plot infers inverse relation ship, whereas

schist and mica bearing quartzarenite show positive relation ship between Pj and

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Km (Fig. 5.13 b). In Km vs. T and Pj vs. T plots data lie in oblate (T>0) to prolate

field (T<0) (Fig. 5.13 c, d).

(ii) Someshwar-Dwarahat Domain

The Someshwar-Dwarahat is characterized by NNE-SSW trending faults

in Binta-Bagwalipokhar and Someshwar-Ranman areas. AMS study is carried out

precisely in detail, along these faults and across the NAT (Fig. 5.14).

A NNE-SSW oriented fault is passing along the Gagas river across the

NAT and termed Gagas River Fault (Kothyari and Pant, 2008). AMS data

represent vertical to sub-vertical magnetic foliations and gentle to steeply

plunging magnetic lineations with varying orientations. Magnetic foliation planes

near the fault trace are parallel/sub-parallel to the fault, whereas at the vicinity of

the NAT they are parallel/ sub-parallel to the thrust plane (Fig. 5. 15 a). Figure

5.15 b shows inverse relation ship in the Pj and Km data of protomylonite and

mylonite units, whereas mica-bearing quartzite and micaceous-quartzarenites

giving positive relation. In Km vs. T and Pj vs. T plots data lie in oblate (T>0) to

prolate field (T<0) (Fig. 5.15 b, d).

Someshwar-Manan segment is characterized by a NNE-SSW/ Manan

Fault across the NAT. Here magnetic foliations are parallel/ sub-parallel to the

fault trace (NNE-SSW), whereas at the terminal part, magnetic foliations is sub-

parallel (WNW-ESE) to the NAT (ENE-WSW). Magnetic foliation planes show

high angle with the field foliation along the fault trace and at the terminal part they

are at low angle (D25) (which seems to be slightly rotated ENE-WSW to WNW-

ESE due to the movement along the fault) (Fig. 5.16 a). Here also granitic gneiss,

proto-mylonite and mylonite show inverse relationship between Pj and Km (Fig.

5.15 b). In Km vs. T and Pj vs. T plots data lie in oblate (T>0) to prolate field (T<0)

(Fig. 5.16 c, d).

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Fig

ure

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Figure 5.15: (a) Lower hemisphere equal area projections of magnetic and field foliation at different sites in the Binta-Lodh region, (b) Pj vs. Km, (c) T vs. Km and (d) Jelinek plot (T vs. Pj) for all samples of the region in the NASZ, Someshwar-Dwarahat domain, T= shape parameter and Km= mean susceptibility; Pj =corrected degree of magnetic anisotropy.

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Figure 5.16: (a) Lower hemisphere equal area projections of magnetic and field foliation at different sites in the Someshwar-Manan region, (b) Pj vs. Km, (c) T vs. Km and (d) Jelinek plot (T vs. Pj) for all samples of the region in the NASZ, Someshwar- Dwarahat domain. T= shape parameter and Km= mean susceptibility; Pj =corrected degree of magnetic

anisotropy.

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IV. DWARAHAT-GAIRSEN SECTOR

Besides the Seraghat-Seri Sector the northwestern margin of the Almora

Nappe is also superposed by a transverse Chaukhutiya Fault that coincides with

the northeastern margin of the NAT (Valdiya, 1976; Kothyari and Pant, 2008,

Pant et al., 2011). Based upon the homogeneity of structures and tectonites, the

Chaukhutiya Fault is sub-divided into the three domains (Fig. 5.17).

In and around Dwarahat region, the NASZ is relatively narrow. Magnetic

lineations and foliations near the thrust plane are vertical to sub-vertical (Fig. 5.18

a). Magnetic foliations are characterized by variation in their orientations from E-

W to NNE-SSW and magnetic lineation from W to SW, as the trace of the NAT

swings from E-W to NNW-SSE (Fig. 5.18 a). Magnetic lineations in the ultra-

mylonite (sample D3), lie at the intersection of the field and magnetic foliations.

The ultra-mylonites located at the sharp contact of NAT yield high Km and Pj

values, as shown by sample D3 (Fig. 5.18 b). Granite-gneiss and schistose rocks

show linear inverse relationship between Pj and Km values, whereas the

ultramylonite represents totally independent Pj and Km (Fig. 5.18 b). Here the

data, except the ultramylonite sample (D3), falls within the field of lower

amphibolite facies (Borradaile and Henry, 1997; Nakamura and Borradaile,

2004). The shape of the AMS ellipsoid varies from oblate (T>0) to prolate (T<0)

as shown by plots (T vs. Km and T vs. Pj) (Fig. 5.18 c, d). The schist of the Saryu

Formation and mica-bearing quartzarenite of the Rautgara Formation have oblate

shape of stain ellipsoids, whereas mylonite and ultramylonites of the Saryu

Formation show prolate to oblate shapes of AMS ellipsoids.

In Chaukhutiya-Masi area, samples were taken across the NAT, where

magnetic foliations are vertical to sub-vertical (Fig. 5.19a). The strike of magnetic

foliations vary from ESE-WNW to NW-SE and magnetic lineation from SE to

WNW (except C98 sample). The NW-SE orientation of magnetic foliations is sub-

parallel to the trend of the Chaukhutiya Fault.

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Structural data and geomorphic features represent the E-W oriented

subsidiary brittle faults Ramganga (near Chaukhutiya) and Mahalchauri faults,

their presence are also supported by AMS data (Kothyari, 2008; Pant et al.,

2011).

The magnetic foliation planes are parallel to the Ramganga Fault plane

(Fig. 5.19a). Magnetic lineations are gently plunging in the rock units of the Saryu

Formation and horizontal in the mica-bearing quartzarenite of the Rautgara

Formation. Magnetic lineations at the junction of the Chaukhutiya and Ramganga

faults (sample C98) lie at the intersection of the field foliation and magnetic

foliations (Fig. 5.19 a). In figure 5.19 b, Pj vs. Km plot of the schist rocks shows

inverse relationship between the values of Pj and Km. The ultramylonitized granite

(specimen C98) yields high Km with high Pj value may be due to presence of minor

ferromagnetic minerals (pyrrhotite and magnetite) along with paramagnetic

minerals. On the other hand the data of micaceous quartzite reveals positive

relationship between Km and Pj values. The AMS data for mica schist, micaceous

quartzite and mylonites lie completely in oblate field (T>0). The quartzarenite

(Rautgara Formation) shows a less anisotropy (Pj), and symmetry shows more

neutral (T = 0) to prolate (T<0) shapes of magnetic ellipsoid (Fig. 5.19c and d).

In the Panduakhal region the magnetic foliations are sub-vertical to vertical

having a general E-W orientation with E to ESE plunging magnetic lineation. Near

the Mahalchauri Fault, the lineations are horizontal (samples C76 and C81). The E-

W orientation of magnetic foliations is parallel to the axial plane orientation and to

the Mahalchauri Fault plane, and also varies with orientation of field foliation (Fig.

5.20 a). This variation is inferred to be due to the growth of some magnetic

minerals in the E-W direction due to later influence of deformation that developed

the magnetic foliation trending E-W. Plot Pj vs. Km illustrates inverse relation in

schist rocks and positive in micaceous quartzite, which is similar to the

Chaukhutiya area. It suggests that the anisotropy is high in proximity of NAT

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plane and is low away from it (Fig. 5.20 b). Data of Pj, Km and T fall in oblate field

(Fig. 5.20 c, d), which is due to development of flaky micaceous minerals.

In Gairsen-Dewalikhal section samples were collected from a narrow shear

zone across the NAT (Fig. 5.21). This domain shows identical orientations of field

and magnetic foliations. The magnetic foliations are nearly parallel to the field

foliations (except specimen C57). Similar magnetic foliations in the Gairsen area

show E-W to NW-SE swing in their orientations and become parallel to thrust

plane towards the NAT. The magnetic lineations vary from E to W and NNW to

SSE in the rock units of the Saryu Formation whereas in the quartzarenite, it is

vertically dipping. The magnetic lineations in the samples C55, C56 and C60 lie at

the intersection of the field foliation and the magnetic foliations. In the Dewalikhal

area it shows WNW-ESE orientation, which is sub-parallel to the NW-SE oriented

NAT plane. Besides this the magnetic lineations show ESE orientation in the

rocks of the Saryu Formation and WNW orientation in the quartzarenite (Fig.

5.21).

In the Gairsen area, mica schists show inverse relationship, however

quartzarenite of the Rautgara Formation show positive relationship between Km

and Pj (Fig. 5.22 a). In the Pj vs. Km plot, there is a positive relationship in

micaceous quartzite (Saryu Formation) that is similar to other domain while mica-

bearing quartzarenite (Rautgara Formation) do not show any such relationship

(Fig. 5.23 a).

In the both regions of NW terminal of the NAT, T vs. Pj plots represent

that the mylonitized granite gneiss and mica schist have oblate AMS ellipsoids

(Gairsen region) and micaceous quartzite and quartzarenite have AMS ellipsoid

that vary from oblate to prolate (Dewalikhal region) (Figs. 5.22 c, d and 5.23 c, d).

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Figure 5.17: Geological map of the Dwarahat-Gairsen sector showing distribution of various lithounits and position of samples collected for AMS study.

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Figure 5.18: (a) Lower hemisphere equal area projections of magnetic and field foliation at different sites in the Dwarahat domain, (b) Pj vs. Km, (c) T vs. Km and (d) Jelinek plot (T vs. Pj) for all samples of the domain in the NASZ, Dwarahat-Gairsen sector. T= shape parameter and Km= mean susceptibility; Pj =corrected degree of magnetic anisotropy.

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Figure 5.19: (a) Lower hemisphere equal area projections of magnetic and field foliation at different sites in the Chaukhutiya domain, (b) Pj vs. Km, (c) T vs. Km and (d) Jelinek plot (T vs. Pj) for all samples of the domain in the NASZ, Dwarahat-Gairsen sector. T= shape parameter and Km= mean susceptibility; Pj =corrected degree of magnetic anisotropy.

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Figure 5.20: (a) Lower hemisphere equal area projections of magnetic and field foliation at different sites in the Panduakhal domain, (b) Pj vs. Km, (c) T vs. Km and (d) Jelinek plot (T vs. Pj) for all samples of the domain in the NASZ, Dwarahat-Gairsen sector. T= shape parameter and Km= mean susceptibility; Pj =corrected degree of magnetic anisotropy.

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Figure 5.21: Lower hemisphere equal area projections of magnetic and field foliation at different sites in the Gairsen and Dewalikhal domains, Dwarahat-Gairsen sector.

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Figure 5.22: In the Gairsen domain (a) Pj vs. Km plot showing negative relation (arrow) in granitic gneiss and schist, (b) Pj vs. Km (c) T vs. Km and (d) Jelinek plot (T vs. Pj) for all samples of the domain in the NASZ, Dwarahat-Gairsen sector. T= shape parameter and Km= mean susceptibility; Pj =corrected degree of magnetic anisotropy.

Figure 5.23: In the Dewalikhal domain (a) Pj vs. Km plot showing positive relation (arrow) in micaceous quartzite, (b) Pj vs. Km, (c) T vs. Km and (d) Jelinek plot (T vs. Pj) for all samples of the domain, Dwarahat-Gairsen sector in the NASZ. T= shape parameter and Km= mean susceptibility; Pj =corrected degree of magnetic anisotropy.

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5.4 RF/Φ AND FLINN PLOTS TECHNIQUE

Rf/φ plots are prepared, by using the data obtained through measuring the

axial ratios (Rf) and angle (φ) between the long axis and principal extension

direction, of two dimensional sections (i.e. XZ, YZ) (Figs. 5.24, 5.25, 5.26 and

5.27). In three dimensional strain studies, only two sections are required to

determine the three principal strain ratios (Dunnet, 1969; Ramsay and Huber,

1983). For three dimension value X/Y ratio is obtained from other two ratios i.e.

X/Z and Y/Z. Flinn (1962, 1978) plots are prepared by taking the axial ratio X/Y

and Y/Z in order to find shape anisotropy in strain ellipsoid across the NAT (Fig.

5.28). Rock units of the area are polymineralic and individual mineral grain

behaves differently under the stress, and strain accumulation is variable at grain

level. So it is tough to find out that which grains are giving accurate finite strain

data, however after some limitation it is useful to determine the average finite

strain in a particular rock unit.

5.4.1 RESULTS

In order to compare the AMS strain fabric only three but significant samples

of protomylonite to ultramylonite (especially of mylonitised granitic gneiss) from

each sector, are analyzed by this method (Rf/φ), and representative plots are

shown (Figs. 5.24, 5.25, 5.26 and 5.27). The major objective was to compute the

strain variation across the NAT plane with this method and compare with the

AMS stain data.

The Harmonic mean (H) (Lisle, 1977) of ‘RS’ values thus obtain by this

method, gives more accurate strain values then geometric mean and arithmetic

mean, checked by Srivastava (2004).

The Strain ellipsoid ratios (X > Y > Z) measured from the NASZ are shown

below:

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Sectors Strain ellipsoid ratios

Pancheshwar-

Seri

Protomylonite 1.45 : 1.2 : 1

Mylonite 2: 1.3 : 1

Ultramylonite 2: 1.12 :1

Seri- Seraghat Protomylonite 1.45 : 1.11 : 1

Mylonite 1.98 : 1.7 : 1

Ultramylonite 3.2 : 2.9 :1

Seraghat-

Dwarahat

Protomylonite 1.5 : 1.5 :1

Mylonite 1.92 : 1.2 :1

Ultramylonite 2.03 : 1.2 : 1

Dwarahat-

Gairsen sector

Protomylonite 1.74 : 1.57 : 1

Mylonite 2.11 : 1.57 :1

Ultramylonite 3.11 : 3 : 1

The above strain estimation represent that the mylonites to ultramylonites

across the NAT show high strain ratio of major and minimum axes of strain

ellipses. Here high strain ratio explained by intensely stretched and elongated

grains of quartz and feldspars in the mylonites and ultramylonites.

.

The strain ellipsoids shown on Flinn plots, determined from elliptical grains of

quartz and feldspars. Data of specimens of Pancheshwar-Seri and Seraghat-

Dwarahat sectors are falling flattening (k<1) to constriction (k>1) field. Whereas

strain ellipsoid of the Seri-Seraghat and Dwarahat- Gairsen sectors lying

dominatingly in flattening field (Fig. 5.28 b and d).

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Figure 5.24: Rf/φ plots in XZ and YZ section of the Pancheshwar-Seri sector of the samples

taken across the NAT.

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Figure 5.25: Rf/φ plots in XZ and YZ section of the Seri-Seraghat sector of the samples taken across the NAT.

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Figure 5.26: Rf/φ plots in XZ and YZ section of the Seraghat-Dwarahat sector of the samples taken across the NAT.

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Figure 5.27: Rf/φ plots in XZ and YZ section of the Dwarahat-Gairsen sector of the samples taken across the NAT

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Figure 5.28: Flinn plots of the samples taken across the NAT of (a) Pancheshwar-Seri, (b) Seri-Seraghat, (c) Seraghat-Dwarahat and (d) Dwarahat-Gairsen sectors.

5.5 DISCUSSION

Magnetic fabrics can reflect the shearing, folding and later faulting impacts in the

rocks (Hallwood et al., 1992; Tarling and Hrouda, 1993; Nakamura and

Nagahama, 2001; Mamtani and Sengupta, 2010). Petrography and magnetic

mineralogy (high temperature demagnetization curves) reveals that the

anisotropy is controlled mostly by paramagnetic minerals and also yielded

negligible contribution of ferromagnetic minerals. The study area is traversed by

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two regional transverse faults (NNW-SSE oriented Rantoli and Chaukhutiya

faults) and numbers of subsidiary faults (relatively small scale and variably

oriented). Through magnetic fabric study their tectonic impacts on the

surrounding rocks can be easily observed. Sub-vertical to vertical magnetic

foliation planes with their variable orientations represent the superimposition of

later developed fabrics due to continuous horizontal compressional forces.

Parallel to sub-parallel magnetic foliation planes to the transverse faults with

steep dip and horizontal to gently plunging magnetic lineations, represent the

effect of the strike slip movement of NNW-SSE oriented Rantoli and Chaukhutiya

faults along the NAT. Magnetic foliations remain parallel to the field foliations

along with steep magnetic lineation at the terminal part of the transverse fault,

also proves rotational movement along the faults. In the Central part of

transverse faults the variation in attitudes of magnetic foliation and field foliation

manifests high impact of the transverse faults and their subsidiary faults, contrary

to this in the terminal parts of the transverse faults the parallelism of magnetic

foliation with field foliation is noted. This indicates that the impact of faulting is

negligible in the terminal parts. Parallelism of magnetic foliation planes with

subsidiary faults also reflecting their tectonic impact on the magnetic fabric of the

nearby rock units. Whereas their parallelism with the NAT trend show thrusting

effect on the magnetic fabric of the rock units near the NAT.

The clusters of magnetic axes (K1, K2 and K3) are well defined in the rocks

of the Saryu Formation as well as in the highly sheared micaceous quartzarenites

of the Rautgara Formation (Gh16, S4, S8, D37, J20, G30, D8, D25, C61, C64, and C100),

as shown by stereoplots, whereas less deformed quartzarenite rock samples

away from the NAT have almost randomly oriented axes (samples Gh10, Gh5, D5,

C81 and C65), e.g. mixed maximum, intermediate and minimum axes and shows

no significant results in fabric study.

Schists are showing positive as well as negative relation between Pj and

Km. Positive relation is due to the growth of very fine grain iron oxides and

negative relation is due to alteration of paramagnetic minerals as strain

increases, which is verified by the petrography study. Granitic gneiss and proto-

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mylonite to mylonite in the study area, are consistently showing negative relation

between Pj and Km due to the decreasing the size of the paramagnetic minerals

on increasing the strain near the thrust plane. High Km value of ultramylonitized

granite is a consequence of the presence of ferromagnetic minerals (pyrrhotite,

size < 0.1mm). High Pj value at the NAT plane is due to the localization of high

strain in the rocks of the contact. Pj values across the NAT represent the

increasing amount of degree of anisotropy as well as increasing strain towards

the NAT plane.

Rf /φ plots are giving high Rs values, obtained in the ultramylonites rock

due to the presence of highly stretched and elongated grains of quartz (quartz

ribbons) and feldspars at the vicinity of the NAT, and low values are from a

distant area from the NAT in the shear zone. it represent high strain in the central

part of the NASZ.

Highly fractured and sheared rocks in the fault zones show distinct

magnetic foliations, which are parallel or sub-parallel to the fault plane. Their

parallel orientations are due to the development of fractures parallel to the fault

zone and growth of very fine grain iron oxides along the microscopic fractures,

which have changed the magnetic properties drastically. These results of

fractured rocks are significant in finding out the effects of the main transverse

faults as well as of the small scale subsidiary faults (Nakamura and Nagahama,

2001).

The plots of magnetic parameters (T vs. Pj) show dominating oblate

magnetic ellipsoids in the central part of the transverse faults, and prolate to

oblate magnetic ellipsoids in terminals of the transverse faults and along the

NAT. In comparison to AMS fabric the Flinn plot of axial ratio studied at

microscopic level also show the similar results. Therefore it is inferred that

deformation was mostly of flattening in the central part and constrictional in

terminal parts of the transverse faults. Whole study along the NASZ represents

the dominating oblate shape magnetic ellipsoid in the transverse faults area is the

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cause of flattening strain, whereas prolate to oblate shape in other parts of the

NASZ is due to constrictional to flattening strain. In addition to this Rf /φ plot

represents high strain value at the contact of NAT, which decreases away from

the NAT plane, whereas φ angle decreases towards the NAT contact or at the

center of the NASZ.

5.6 CONCLUSION

Magnetic fabric studies along the NASZ and associated transverse faults

reveal the finite-strain in ductile to brittle fields of deformation. The steep

magnetic foliations are interpreted to be on account of regional compression.

Strike of the magnetic foliations and plunge direction of magnetic lineations are

parallel/ sub-parallel to the NAT trace but where the transverse faults are

encountered they become parallel to sub-parallel to these faults. AMS results

revealed a strong strike-slip movement with rotational component especially

along the Rantoli and Chaukhutiya faults. Detail study along the transverse faults

also explains that they are more active in the Central part, whereas there is a little

effect in terminal parts. However near the NAT trace in the Pancheshwar-Seri

and Seraghat-Dwarahat sectors, AMS study and classical strain study (Rf / φ)

revealed the dominating effect of thrusting.

Km value decreases and anisotropy increases in the magnetic fabric of the

granitic gneiss and proto-mylonite to mylonite as moving towards the NAT

contact and proved the high strain near the thrust plane. High susceptibility in

ultramylonites indicates the presence of the pyrrhotite ferromagnetic minerals

within the lattice of paramagnetic minerals. Similarly RS values obtained in Rf/ φ

strain analysis are showing increasing strain value toward the NAT plane within

NASZ.

Dominating oblate magnetic ellipsoids indicate that strain was dominantly

flattening type along the transverse faults, and prolate to oblate magnetic and

micro-fabric strain ellipsoids along the NAT imply constrictional as well as

flattening strain and thrusting effects.

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TABLE 1: AMS data from rocks of the Pancheshwar-Seri sector of study area under low

temperature: Km (10-6 SI), mean magnetic susceptibility; K1, K2 and K3, are maximum,

intermediate and minimum susceptibility axes respectively; L and F are the intensity of

magnetic lineation and foliation respectively ; Pj, corrected anisotropy degree; T- shape

factor.

Sample

No

KLF

LF-normed principal

Susceptibilitie

LF-A factors

MS principal

LF-AMS principal

direction

K1 K2 K3 Pj L T K1 K2 K3

Dec. Inc. Dec. Inc. Dec. Inc.

GH1AA 4.596 1.2242 1.1833 0.5926 2.268 1.035 0.906 163 9 72 5 316 79

GH1AB 4.174 1.2083 1.0614 0.7303 1.687 1.138 0.485 273 7 178 34 13 55

GH1AC 5.060 1.1465 1.0882 0.7653 1.552 1.054 0.742 325 25 65 20 189 57

GH1AD 2.429 1.2558 1.0549 0.6893 1.854 1.191 0.419 123 21 223 25 359 57

GH1AE 1.563 1.3440 0.9590 0.6971 1.928 1.401 -0.028 201 27 293 2 27 63

GH1BA 32.45 1.0656 1.0259 0.9085 1.181 1.039 .564 242 30 300 4 45 63

GH1BD 37.90 1.0889 1.0151 0.8960 1.218 1.073 0.280 266 36 1 7 100 53

GH1BE 34.98 1.0714 1.0454 0.8831 1.234 1.025 0.746 270 24 1 4 100 65

GH1BF 32.69 1.0911 1.0357 0.8731 1.263 1.054 0.532 253 31 355 21 114 52

GH2A 88.71 1.0593 1.0476 1.0476 1.210 1.011 0.871 143 57 273 23 13 23

GH2B 63.38 1.1002 1.0638 0.8361 1.349 1.034 0.755 275 0 184 74 5 16

GH2C 96.55 1.0652 1.0355 0.8993 1.199 1.029 0.667 170 65 271 271 3 24

GH2D 65.55 1.0766 1.0653 0.8581 1.292 1.011 0.907 123 61 268 24 5 14

GH2E 99.81 1.0820 1.0259 0.8920 1.221 1.055 0.449 179 62 274 3 5 28

GH2F 119.2 1.0498 1.0430 0.9072 1.179 1.007 0.910 169 69 268 3 359 21

GH3A 140.6 1.0782 1.0224 0.8994 1.205 1.205 0.413 251 43 341 0 72 47

GH3B 149.6 1.0660 1.0341 0.8999 1.198 1.031 0.641 225 41 322 8 60 48

GH3C 152.3 1.0634 1.0393 0.8973 1.202 1.023 0.730 229 32 322 5 61 57

GH3D 150.9 1.1080 0.9993 0.8927 1.241 1.109 0.045 262 40 160 13 56 47

GH3E 138.9 1.0564 1.0337 0.9099 1.175 1.022 0.708 250 27 158 4 59 63

GH3F 143.8 1.0777 1.0393 0.8830 1.237 1.037 0.636 283 34 141 6 52 45

GH4A 125.8 1.0607 1.0340 0.9053 1.185 1.026 0.679 192 44 320 33 70 28

GH4B 117.0 1.0424 1.0237 0.9339 1.125 1.018 0.672 305 23 196 37 59 44

GH4C 118.6 1.0669 1.0212 0.9119 1.176 1.045 0.442 167 15 272 44 63 42

GH4D 150.1 1.0422 1.0154 0.9424 1.110 1.026 0.484 273 36 167 21 53 46

GH4E 120.3 1.0459 1.0289 0.9251 1.143 1.016 0.733 158 12 258 42 55 46

GH4F 133.5 1.0436 1.0181 0.9383 1.118 1.025 0.534 173 22 279 33 56 48

GH5A 41.48 1.0489 1.0151 0.9360 1.124 1.033 0.424 261 80 95 10 5 2

GH5B 54.31 1.0101 0.9977 0.9922 1.019 1.012 -0.383 11 3 281 10 118 80

GH5C 65.81 1.0200 1.0077 0.9723 1.051 1.012 0.490 273 40 90 50 182 2

GH5D 59.74 1.0147 0.9974 0.9879 1.028 1.017 -0.279 269 12 21 59 173 28

GH5E 72.53 1.0070 0.9971 0.9958 1.012 1.010 -0.772 14 13 180 77 283 3

GH5F 66.77 1.0055 1.0019 0.9926 1.014 1.004 0.444 201 12 298 29 92 58

GH9A 273.1 1.0241 1.0170 0.9589 1.075 1.007 0.788 92 17 314 68 187 14

GH9B 260.4 1.0165 1.0111 0.9724 1.050 1.005 0.757 89 30 315 50 193 24

GH9C 288.1 1.0172 1.0158 0.9669 1.059 1.001 0.946 98 29 324 51 201 23

GH9D 287.2 1.0175 1.0129 0.9696 1.055 1.005 0.813 290 12 39 57 193 31

GH9E 260.0 1.0181 1.0107 0.9711 1.052 1.007 0.692 94 14 337 62 191 24

GH7A 198.6 1.0331 1.0003 0.9666 1.069 1.033 0.030 274 12 182 8 60 75

GH7B 167.0 1.0272 1.0250 0.9478 1.096 1.096 0.947 311 25 210 21 86 56

GH7C 188.5 1.0329 1.0130 0.9541 1.086 1.020 0.510 276 11 186 1 89 79

GH7D 158.8 1.0403 1.0085 0.9511 1.095 1.032 0.308 173 2 263 18 78 72

GH7E 197.3 1.0291 1.0035 0.9674 1.064 1.026 0.185 278 12 187 6 72 76

GH8A 74.60 1.0356 0.9929 0.9715 1.067 1.043 -0.320 176 3 269 36 82 54

GH8B 69.31 1.0394 0.9970 0.9636 1.079 1.043 -0.100 180 14 274 14 46 70

GH8C 69.23 1.0380 0.9987 0.9633 1.078 1.039 -0.034 175 15 268 10 31 72

GH8D 88.50 1.0425 0.9978 0.9596 1.086 1.045 -0.057 174 16 270 20 50 64

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Continue…………

GH8E 77.36 1.0365 0.9989 0.9647 1.074 1.038 -0.030 178 18 274 18 46 64

GH8F 87.91 1.0338 1.0021 0.9641 1.072 1.032 0.106 176 19 274 22 48 60

GH8G 81.12 1.0351 0.9990 0.9659 1.072 1.036 -0.027 179 17 275 21 53 63

GH10A -7.258 -0.8181 -1.0019 -1.179 1.443 1.178 0.107 258 54 99 34 2 10

GH10B -8.453 -0.9466 -0.9867 -1.0668 1.129 1.081 -0.306 148 68 272 16 7 15

GH10C -5.364 -0.2268 -1.2209 -1.5523 1.135 1.271 0.750 183 52 277 4 10 38

GH10D -5.465 -0.7728 -0.9774 -1.2498 1.617 1.279 -0.023 337 44 104 33 215 29

GH12A 442.1 1.0551 1.0348 0.9101 1.174 1.020 0.736 263 76 95 13 4 3

GH12B 475.9 1.0610 1.0448 0.8942 1.208 1.015 0.820 274 21 101 69 5 2

GH12C 538.2 1.0765 1.0625 0.8610 1.285 1.013 0.883 91 34 270 56 0 1

GH12D 447.0 1.0598 1.0374 0.9028 1.190 1.022 0.734 275 7 103 83 5 1

GH12E 535.6 1.0752 1.0622 0.8626 1.281 1.012 0.889 94 22 275 68 184 0

GH13A 413.1 1.0772 1.0341 0.8887 1.225 1.042 0.576 119 15 224 45 16 41

GH13B 318.3 1.0414 1.0298 0.9288 1.134 1.011 0.803 158 46 254 6 349 43

GH13C 407.0 1.0766 1.0268 0.8965 1.209 1.048 0.483 126 31 235 29 359 46

GH13D 407.7 1.0788 1.0274 0.8938 1.216 1.050 0.480 129 36 238 24 353 45

GH13E 373.6 1.0535 1.0328 0.9138 1.167 1.020 0.721 124 6 221 51 29 39

GH14AA 164.9 1.0598 1.0113 0.9289 1.143 1.048 0.289 272 41 166 18 58 44

GH14AB 88.41 1.0357 1.0135 0.9508 1.093 1.022 0.492 277 21 174 30 37 51

GH14AC 144.1 1.0436 1.0387 0.9177 1.157 1.005 0.927 312 6 216 45 48 44

GH14AD 165.1 1.0335 1.0214 0.9451 1.102 1.012 0.736 284 18 185 27 43 57

GH14AE 164.4 1.0343 1.0225 0.9433 1.106 1.012 0.751 288 17 188 29 44 56

GH15A 318.9 1.0571 1.0304 0.9125 1.170 1.026 0.653 201 21 292 5 35 69

GH15B 267.3 1.0535 1.0282 0.9183 1.158 1.025 0.645 175 15 272 23 55 62

GH15C 306.3 1.0462 1.0380 0.9157 1.161 1.008 0.882 204 25 300 13 54 61

GH15D 260.1 1.0565 1.0252 0.9183 1.159 1.030 0.572 173 15 270 24 54 61

GH15E 291.6 1.0482 1.0278 0.9240 1.145 1.020 0.687 175 15 270 20 50 64

GH15F 256.5 1.0551 1.0271 0.9177 1.160 1.027 0.615 181 19 277 19 19 63

GH16AA 174.4 1.0178 1.0141 0.9681 1.057 1.004 0.855 120 8 15 62 214 27

GH16AB 174.0 1.0161 1.0137 0.9702 1.053 1.002 0.895 113 22 350 54 215 27

GH16AC 71.02 1.0098 1.0062 0.9840 1.028 1.003 0.730 75 57 316 18 216 27

GH16AD 70.76 1.0103 1.0060 0.9837 1.029 1.004 0.676 89 44 319 33 209 28

P1A 312.0 1.0987 1.0858 0.8155 1.402 1.012 0.921 1 1 271 2 125 87

P1B 290.1 1.0416 1.0189 0.9396 1.115 1.022 0.573 190 9 280 0 13 81

P1C 319.2 1.0439 1.0233 0.9328 1.128 1.020 0.645 13 1 283 7 115 83

P1D 314.9 1.0434 1.0285 0.9281 1.136 1.014 0.755 350 2 259 21 85 69

P1E 345.5 1.0598 1.0278 0.9124 1.171 1.031 0.591 360 2 270 1 149 88

P1F 310.6 1.0540 1.0262 0.9198 1.155 1.027 0.608 357 3 265 28 94 62

P2A 133.8 1.0480 1.0104 0.9416 1.115 1.037 0.316 284 16 20 20 159 64

P2B 119.8 1.0363 1.0156 0.9481 1.098 1.020 0.548 297 20 33 16 158 64

P2C 140.9 1.0535 1.0134 0.9331 1.132 1.039 0.362 291 23 29 16 150 61

P2D 118.8 1.0475 1.0089 0.9436 1.112 1.038 0.281 279 20 18 25 154 58

P2E 146.4 1.0538 1.0113 0.9349 1.129 1.042 0.311 295 19 30 15 155 66

P2F 130.3 1.0447 1.0201 0.9352 1.124 1.024 0.569 297 21 33 15 156 64

P3AA 174.4 1.0431 1.0297 0.9272 1.138 1.013 0.780 353 9 246 62 88 26

P3AB 198.7 1.0438 1.0283 0.9279 1.137 1.015 0.746 353 15 243 53 93 33

P3AC 207.3 1.0327 1.0215 0.9458 1.101 1.011 0.753 353 16 239 54 93 31

P3AD 162.7 1.0430 1.0271 0.9299 1.133 1.015 0.733 5 11 136 74 272 12

P3AE 198.9 1.0404 1.0346 0.9250 1.142 1.006 0.905 344 38 202 45 90 20

P3AF 163.3 1.0377 1.0207 0.9416 1.110 1.017 0.659 3 5 117 78 272 11

P3BA 189.9 1.0509 1.0295 0.9195 1.155 1.021 0.692 173 4 265 29 77 61

P3BB 202.3 1.0519 1.0317 0.9164 1.161 1.020 0.718 190 20 291 29 70 54

P3BC 206.8 1.0439 1.0394 0.9167 1.159 1.004 0.933 315 38 199 30 82 38

P3BD 177.5 1.0526 1.0315 0.9159 1.162 1.021 0.708 348 7 250 47 84 42

P3BE 202.9 1.0522 1.0304 0.9174 1.159 1.021 0.694 172 0 262 35 82 55

P4A 290.2 1.0315 1.0251 0.9435 1.105 1.006 0.861 205 7 295 2 39 82

P4B 341.7 1.0410 0.9996 0.9594 1.085 1.041 0.005 267 61 148 15 51 24

P4C 347.5 1.0323 1.0048 0.9629 1.073 1.027 0.222 282 66 155 15 60 18

P4D 373.1 1.0359 1.0001 0.9641 1.074 1.036 0.020 269 57 142 21 43 24

P4E 416.5 1.0399 1.0052 0.9549 1.090 1.035 0.205 276 69 158 10 65 18

P4F 395.4 1.0325 1.0051 0.9623 1.074 1.027 0.237 257 68 154 5 62 21

Estelar

164

TABLE 2: AMS data from rocks of the Seraghat-Seri sector of study area under low temperature: Km (10-6 SI), mean magnetic susceptibility; K1, K2 and K3, are maximum, intermediate and minimum susceptibility axes respectively; L and F are the intensity of magnetic lineation and foliation respectively ; Pj , corrected anisotropy degree; T- shape factor.

Sample

No

KLF

LF-normed principal

Susceptibilitie

LF-A factors

MS principal

LF-AMS principal

direction

K1 K2 K3 Pj L T K1 K2 K3

Dec. Inc. Dec. Inc. Dec. Inc.

S1A 294 1.042 1.012 0.945 1.105 1.029 0.406 111 33 206 8 309 55

S1B 355 1.053 1.003 0.944 1.115 1.049 0.121 119 3 227 10 352 49

S1C 314 1.052 1.004 0.944 1.115 1.048 0.144 98 34 199 15 309 52

S1D 374 1.068 1.015 0.918 1.167 1.052 0.330 124 35 216 3 311 55

S1E 330 1.092 0.989 0.919 1.188 1.103 0.143 111 31 205 6 305 58

S2A 190.5 1.0316 1.0121 0.905 1.06 1.03 0.10 307 10 228 46 60 36

S2B 201.6 1.0264 1.0115 0.962 1.07 1.015 0.547 152 11 254 47 52 41

S2C 221 1.0553 1.0006 0.944 1.118 1.055 0.044 322 22 146 68 53 31

S2D 219.6 1.032 1.0166 0.952 1.09 1.015 0.63 320 26 188 54 62 23

S2E 200 1.029 1.0066 0.964 1.068 1.022 0.32 319 6 223 44 55 45

S3A 27.10 1.0779 0.9726 0.9495 1.144 1.108 -0.621 172 18 8 71 263 5

S3B 43.09 1.0858 0.9877 0.9415 1.161 1.116 -0.542 166 15 54 55 266 31

S3C 49.01 1.0843 0.9283 0.9464 1.156 1.119 -0.648 162 18 322 71 70 6

S3D 58.3 1.06 0.9700 0.9597 1.112 1.083 -0.596 166 17 340 73 75 2

S3E 25.03 1.0353 0.9896 0.9751 1.064 1.046 -0.507 162 32 13 54 261 15

S3F 79.28 1.0702 0.9765 0.9533 1.130 1.096 -0.583 165 18 41 60 263 23

S4A 171.4 1.0424 1.0002 0.9574 1.089 1.042 0.027 33 26 275 44 143 35

S4B 195.1 1.0627 0.9831 0.9542 1.118 1.081 -0.447 15 33 239 48 121 23

S4C 150.8 1.0339 1.0074 0.9587 1.080 1.026 0.312 32 30 267 45 142 30

S4D 183.7 1.0415 1.0069 0.9515 1.096 1.034 0.252 27 37 266 34 148 34

S4E 172.1 1.0453 0.9991 0.9555 1.094 1.046 -0.007 26 27 271 41 139 38

S5A 487.3 1.0354 1.0101 0.9545 1.087 1.025 0.392 184 10 281 36 81 53

S5B 472.6 1.0292 1.0099 0.9609 1.019 1.019 0.449 358 7 261 44 95 45

S5C 423.7 1.0278 1.0072 0.9650 1.066 1.020 0.466 186 2 278 44 94 46

S5D 479.5 1.0286 1.0105 0.9608 1.073 1.018 0.480 3 2 271 47 94 43

S5E 487.0 1.0348 1.0093 0.9559 1.084 1.025 0.370 183 6 278 39 86 50

S6A 507.0 1.1359 1.0558 0.8083 1.431 1.076 0.570 54 43 146 7 262 25

S6B 296.4 1.1043 1.0308 0.8648 1.287 1.071 0.437 63 45 333 0 238 25

S6C 580.8 1.1631 1.0610 0.7759 1.529 1.096 0.546 61 42 155 9 266 26

S6D 301.3 1.1096 1.0436 0.8468 1.328 1.063 0.546 58 45 148 8 257 27

S6E 796.2 1.1793 1.0691 0.7515 1.606 1.103 0.565 62 42 156 9 267 26

S7A 219.9 1.0346 1.0239 0.9414 1.109 1.010 0.780 98 25 265 65 5 5

S7B 195.4 1.0352 1.0202 0.9446 1.103 1.015 0.682 104 24 261 64 10 9

S7C 195.8 1.0347 1.0227 0.9426 1.107 1.012 0.748 104 22 258 66 10 9

S7D 227.3 1.0305 1.0133 0.9562 1.082 1.017 0.551 107 37 262 51 8 12

S7E 179.8 1.0297 1.0232 0.9471 1.098 1.006 0.847 114 44 279 45 17 8

S8A 3.40 1.059 1.0433 0.918 1.318 1.023 0.704 115 16 26 44 200 28

S8B 8.454 1.1596 1.023 0.805 1.435 1.123 0.278 305 6 35 8 220 30

S8C 3.905 1.1432 1.006 0.841 1.445 1.125 0.14 319 13 40 76 231 6

S8D 10.13 1.058 1.0343 0.913 1.312 1.023 0.704 145 22 36 44 236 28

S9A 201.7 1.0316 1.0121 0.965 1.06 1.04 0.12 330 7 220 55 61 35

S9B 211 1.0264 1.0105 0.962 1.06 1.016 0.547 154 8 256 47 54 46

S9C 212 1.0553 1.0013 0.940 1.109 1.049 0.044 332 15 156 68 63 1

S9D 214 1.028 1.0105 0.949 1.09 1.014 0.63 330 14 208 54 72 23

S9E 221 1.0352 1.0060 0.970 1.068 1.024 0.33 328 8 232 48 64 43

Estelar

165

TABLE 3: AMS data from rocks of the Seraghat-Dwarahat sector of study area under low temperature: Km (10-6 SI), mean magnetic susceptibility; K1, K2 and K3, are maximum, intermediate and minimum susceptibility axes respectively; L and F are the intensity of magnetic lineation and foliation respectively ; Pj, corrected anisotropy degree; T- shape factor.

Sample

No

KLF

LF-normed principal

Susceptibilitie

LF-A factors

MS principal

LF-AMS principal

direction

K1 K2 K3 Pj L T K1 K2 K3

Dec. Inc. Dec. Inc. Dec. Inc.

D8A 7.400 0.5997 0.9511 1.4492 1.417 1.524 0.045 269 5 116 85 360 2

D8B 7.826 0.9108 0.9578 1.1314 1.255 1.181 -0.536 94 16 296 73 185 6

D8C 8.241 0.8892 0.9281 1.1827 1.360 1.274 -0.700 95 63 269 27 0 2

D8D 7.650 0.6797 0.9312 1.2120 1.111 1.324 0.052 254 6 121 86 359 3

D8E 7.813 0.9123 0.9461 1.2451 1.241 1.161 -0.516 96 18 292 71 189 5

D9Aa 3.338 0.8245 0.9953 1.1802 1.432 1.186 0.050 113 67 253 18 347 14

D9Ab 2.162 0.7110 1.1102 1.1788 1.737 1.062 0.763 106 63 260 24 355 11

D9Ac 1.214 0.6822 0.9632 1.3545 1.985 1.406 0.006 93 51 231 31 334 21

D9Ad 1.213 0.6824 0.9622 1.3535 1.974 1.400 0.010 91 50 221 30 333 20

D9Ae 2.213 0.7452 1.0012 1.1623 1.748 1.084 0.783 110 65 258 25 345 15

D9Ba 600.4 1.0539 0.9798 0.9663 1.098 1.076 -0.680 186 57 3 33 94 1

D9Bb 591.8 1.0488 0.9819 0.9693 1.088 1.068 -0.674 182 61 356 29 88 3

D9Bc 568.8 1.0548 0.9805 0.9647 1.100 1.076 -0.636 191 55 340 31 79 15

D9Bd 571.3 1.0494 0.9817 0.9689 1.089 1.069 -0.670 187 51 348 37 85 9

D9Be 593.2 1.0492 0.9815 0.9682 1.089 1.071 -0.662 185 58 351 30 82 5

D25A 7.46 -0.9496 -0.9923 -1.0581 1.115 1.066 -0.188 285 81 99 9 190 1

D25B 8.93 -0.9496 -0.9937 -1.0566 1.113 1.063 -0.150 96 66 297 22 204 8

D25C 7.334 -0.9661 -0.9990 -1.0349 1.071 1.036 -0.025 295 1 32 85 205 5

D25D 9.843 -0.8396 -1.0734 -1.0870 1.238 1.013 0.903 51 2 158 82 320 8

D25E 9.698 -0.8615 -0.9561 -1.1824 1.281 1.237 -0.342 337 9 243 23 87 65

D25F 5.94 -0.9828 -0.9948 -1.0224 1.041 1.028 -0.386 306 65 98 22 192 10

D27A 532.4 1.0168 0.9927 0.9905 1.029 1.024 -0.831 142 77 38 3 308 12

D27B 503.9 1.0136 0.9944 0.9920 1.024 1.019 -0.772 95 62 237 23 334 15

D27C 512.4 1.0128 0.9923 0.9923 1.042 1.032 -0.781 139 74 41 8 310 13

D27D 513.9 1.0132 0.9933 0.9943 1.032 1.021 -0.780 96 65 241 24 337 14

D28A 10.223 1.2933 1.0473 -0.6594 1.01 1.235 0.748 65 7 156 6 289 81

D28B 30.235 1.1232 1.0232 0.2318 1.023 1.224 0.657 60 9 155 7 284 70

D28C 15.435 1.1034 1.0112 -0.5612 1.032 1.101 -0.342 62 8 155 5 285 75

D29A 301.6 1.0317 1.0170 0.9513 1.090 1.014 0.647 238 6 52 83 147 1

D29B 228.7 1.0495 1.0057 0.9448 1.112 1.044 0.190 219 5 67 85 309 2

D29C 291.6 1.0323 1.0151 0.9413 1.100 1.032 0.447 226 6 58 84 149 1

D29D 295.7 1.0395 1.0157 0.9428 1.110 1.041 0.390 220 6 64 86 310 1

D31A 102.9 1.0345 0.9964 0.9692 1.068 1.038 -0.151 23 23 70 50 257 31

D31B 184.1 1.0244 1.0095 0.9661 1.063 1.015 0.498 200 32 316 35 80 38

D31C 111.2 1.1010 0.9629 0.9629 1.189 1.143 -0.152 180 9 88 48 280 52

D31D 110.7 1.0330 0.9973 0.9697 1.065 1.036 -0.115 21 12 132 58 284 29

D36A 26.62 1.0908 1.0450 0.8642 1.281 1.044 0.632 87 69 274 21 183 3

D36B 25.33 1.0762 1.0309 0.8929 1.216 1.044 0.540 86 71 275 19 184 3

D36C 41.26 1.2897 1.0963 0.6140 1.182 1.176 0.562 94 13 4 2 265 77

D36D 30.56 1.0306 1.0068 0.9626 1.072 1.024 0.315 292 25 39 31 170 48

D36E 35.39 1.0577 0.9794 0.9629 1.105 1.080 0.638 286 13 20 14 154 70

D37A 14.76 1.0956 1.0040 0.9005 1.217 1.091 0.110 282 62 185 4 93 28

D37B 9.567 1.0697 0.9797 0.9506 1.130 1.092 -0.490 280 41 137 43 28 19

D37C 5.990 1.1899 0.9668 0.8432 1.415 1.231 -0.206 89 38 278 51 183 5

D37D 11.60 1.0521 0.9904 0.9575 1.100 1.062 -0.282 257 9 14 71 164 17

D37E 7.765 1.3070 1.0833 0.6097 1.214 1.207 0.508 91 61 278 29 187 3

D37F 12.93 1.1098 0.9736 0.9165 1.216 1.140 -0.368 342 1 252 3 98 87

D37G 5.120 1.1670 0.9920 0.8410 1.388 1.176 0.009 95 56 270 34 182 2

D37H 5.200 1.1633 0.9591 0.8776 1.334 1.213 -0.370 91 59 236 26 334 15

D39A 248.4 1.0510 1.0103 0.9387 1.122 1.040 0.302 225 13 44 77 135 0

D39B 287.9 1.0450 1.0189 0.9360 1.122 1.026 0.541 238 21 64 68 329 2

D39C 248.4 1.0401 1.0054 0.9545 1.090 1.035 0.209 48 10 208 80 317 4

D39D 275.0 1.0345 1.0123 0.9532 1.089 1.022 0.470 47 14 200 74 315 7

Estelar

166

Continue………

D41A 203.8 1.0499 1.0166 0.9336 1.129 1.033 0.451 217 50 36 40 126 0

D41B 179.1 1.0564 1.0082 0.9354 1.131 1.048 0.233 218 36 53 53 313 7

D41D 221.3 1.0584 1.0005 0.9411 1.125 1.058 0.041 214 29 30 60 123 2

D41C 217.8 1.0537 1.0120 0.9342 1.130 1.041 0.329 218 49 55 40 318 9

D49A 220.4 1.0472 1.0289 0.9239 1.145 1.018 0.720 258 40 96 49 356 9

D49B 206.5 1.0450 1.0260 0.9290 1.135 1.019 0.688 259 50 94 39 358 7

D49C 232.2 1.0451 1.0297 0.9252 1.142 1.015 0.755 266 44 99 45 2 7

D49D 267.3 1.1374 0.9590 0.9036 1.270 1.186 -0.483 264 57 356 1 86 33

G17A 7.234 1.0948 0.9936 0.9116 1.201 1.102 -0.060 266 31 65 57 170 10

G17B 16.75 1.0676 1.0342 0.8982 1.202 1.032 0.632 109 59 247 24 345 18

G17C 12.52 1.0688 1.0342 0.8990 1.18 1.036 0.630 122 44 235 34 342 16

G17D 9.234 1.0875 0.0801 0.9012 1.200 1.045 0.060 168 42 64 55 172 12

G25A 800.6 1.0160 1.0041 0.9799 1.038 1.012 0.350 153 74 55 2 324 16

G25B 753.4 1.0229 1.0044 0.9726 1.052 1.018 0.276 187 74 47 12 314 10

G25C 782.7 1.0197 1.0034 0.9769 1.044 1.016 0.251 185 69 321 15 54 14

G25D 780.6 1.0196 1.0041 0.9759 1.048 1.019 0.250 163 70 51 5 320 14

G25E 766.4 1.0189 1.0039 0.9744 1.050 1.016 0.266 177 71 50 10 318 12

G30A 19.55 1.0639 0.9791 0.9570 1.118 1.087 -0.568 112 15 358 57 211 28

G30B 23.61 1.0747 1.0101 0.9152 1.176 1.064 0.228 262 3 19 84 171 5

G30C 15.48 1.0516 0.9871 0.9614 1.097 1.065 -0.412 63 17 330 11 208 70

G30D 21.23 1.0721 0.9850 0.9522 1.121 1.085 -0.213 120 12 359 60 215 24

G30E 23.21 1.0739 1.0012 0.9215 1.152 1.074 0.221 255 5 20 79 177 8

G31A 288.4 1.0790 0.9987 0.9223 1.170 1.080 0.015 227 46 39 44 133 4

G31B 267.6 1.0474 1.0196 0.9330 1.129 1.027 0.535 198 67 48 20 314 11

G31C 286.6 1.0598 1.0351 0.9051 1.186 1.024 0.701 215 52 49 37 314 7

G33A 581.1 1.0614 1.0281 0.9105 1.176 1.032 0.584 58 52 301 19 199 31

G33B 595.4 1.0719 1.0011 0.9270 1.157 1.071 0.059 122 46 276 41 18 13

G33C 585.1 1.0644 1.0271 0.9125 1.166 1.042 0.054 60 53 299 20 197 30

G33D 589.4 1.0709 1.0201 0.9220 1.147 1.051 0.044 120 48 285 35 20 25

J4A 387.0 1.0617 1.0129 0.9254 1.150 1.048 0.315 141 16 42 27 257 58

J4B 372.2 1.0563 1.0054 0.9383 1.126 1.051 0.166 153 10 61 11 284 75

J4C 329.1 1.0636 1.0242 0.9122 1.174 1.039 0.508 130 25 30 19 267 58

J4D 367.2 1.0296 1.0251 0.9453 1.101 1.004 0.898 157 24 53 30 279 51

J4E 392.4 1.0563 1.0135 0.9302 1.138 1.042 0.348 144 19 46 22 271 60

J5A 202.9 1.0590 1.0095 0.9315 1.138 1.049 0.254 158 28 256 14 9 58

J5B 186.5 1.0600 1.0236 0.9164 1.164 1.036 0.520 175 25 266 3 2 65

J5C 194.3 1.0566 1.0071 0.9363 1.129 1.049 0.207 166 33 73 4 337 56

J5D 200.3 1.0784 1.0215 0.9000 1.204 1.056 0.401 153 26 55 16 297 59

J5E 200.0 1.0552 1.0087 0.9361 1.129 1.046 0.247 352 31 86 8 189 58

J6A 206.9 1.0755 1.0516 0.8729 1.258 1.023 0.785 324 6 56 19 217 70

J6B 230.8 1.0571 1.0470 0.8959 1.204 1.010 0.884 347 16 83 20 221 63

J6C 236.5 1.0693 1.0465 0.8841 1.232 1.022 0.774 329 9 63 21 217 67

J6D 195.6 1.0635 1.0508 0.8857 1.227 1.012 0.868 355 15 87 7 201 73

J6E 219.0 1.0686 1.0399 0.8915 1.216 1.028 0.700 353 13 87 19 230 67

J9A 662.2 1.0240 1.0109 0.9652 1.064 1.013 0.565 180 53 291 16 32 33

J9B 668.6 1.0204 1.0120 0.9676 1.059 1.008 0.690 309 8 212 44 47 45

J9C 667.2 1.0488 0.9886 0.9627 1.092 1.061 -0.379 354 53 182 37 89 4

J9D 617.3 1.0169 1.0102 0.9729 1.049 1.007 0.699 184 61 288 7 21 27

J9E 701.7 1.0322 1.0161 0.9516 1.090 1.016 0.613 243 55 149 3 57 35

J10A 167.6 1.0397 1.0329 0.9274 1.137 1.007 0.884 262 0 172 40 352 50

J10B 176.2 1.0572 1.0149 0.9278 1.143 1.042 0.374 102 15 203 35 352 50

J10C 164.0 1.0608 1.0218 0.9175 1.163 1.038 0.484 131 34 241 28 1 44

J10D 148.9 1.0528 1.0255 0.9217 1.151 1.027 0.605 144 38 246 14 352 48

J10E 155.0 1.0400 1.0255 0.9344 1.123 1.014 0.738 150 41 249 10 351 47

J16A 280.9 1.0973 1.0178 0.8850 1.244 1.078 0.301 269 31 168 18 52 54

J16B 276.4 1.1433 0.9746 0.8821 1.299 1.173 -0.231 152 29 244 4 341 61

J16C 277.4 1.1122 0.9674 0.9204 1.217 1.150 -0.474 266 3 359 44 173 46

J16D 289.8 1.0899 1.0423 0.8678 1.273 1.046 0.608 142 4 236 42 47 47

J20A 23.81 1.0549 1.0449 0.9002 1.195 1.010 0.880 127 40 261 40 14 25

J20B 26.47 1.0532 1.0315 0.9152 1.164 1.021 0.704 140 16 267 65 45 19

J20C 22.18 1.0599 1.0038 0.9363 1.132 1.056 0.122 135 30 265 48 28 26

J20D 28.33 1.0567 1.0397 0.9036 1.188 1.016 0.793 134 32 267 55 34 20

Estelar

167

TABLE 4: AMS data from rocks of the Dwarahat-Gairsen sector of study area under low temperature: Km (10-6 SI), mean magnetic susceptibility; K1, K2 and K3, are maximum, intermediate and minimum susceptibility axes respectively; L and F are the intensity of magnetic lineation and foliation respectively ; Pj, corrected anisotropy degree; T- shape factor.

Sample

No

KLF

LF-normed principal

Susceptibilitie

LF-A factors

MS principal

LF-AMS principal

direction

K1 K2 K3 Pj L T K1 K2 K3

Dec. Inc. Dec. Inc. Dec. Inc.

D1A 245.8 1.0407 1.0338 0.925 1.141 1.007 0.887 136 56 254 18 354 28

D1B 275 1.0377 1.0249 0.937 1.117 1.012 0.756 226 54 97 25 355 25

D1C 287.7 1.0379 1.0313 0.931 1.13 1.006 0.883 242 32 109 48 349 24

D1D 282.7 1.0388 1.0315 0.93 1.132 1.007 0.874 153 63 261 9 355 25

D1E 285.6 1.0368 1.0311 0.932 1.127 1.006 0.895 245 31 115 47 353 27

D2A 262.7 1.0393 1.0157 0.945 1.104 1.023 0.517 360 19 168 70 268 4

D2B 281.4 1.0437 0.9835 0.973 1.079 1.061 -0.687 81 78 194 5 285 11

D2C 291.2 1.0474 0.9835 0.969 1.086 1.065 -0.621 80 81 191 3 282 9

D3A 596.5 1.0527 0.9847 0.963 1.67 1.069 -0.494 194 58 349 30 86 12

D3B 632.3 1.0323 1.0176 0.95 1.793 1.015 0.653 201 26 53 59 298 14

D3C 533.4 1.0409 1.0241 0.935 1.781 1.016 0.698 202 66 32 24 300 4

D3D 560.5 1.0454 1.0025 0.952 1.509 1.043 0.104 226 44 40 46 133 3

D3E 525.6 1.0585 0.9911 0.95 1.615 1.068 -0.221 214 49 56 39 317 11

D3F 557.9 1.049 0.9984 0.953 1.66 1.051 -0.025 209 39 27 51 118 1

D3G 550.7 1.0393 1.0096 0.951 1.76 1.029 0.347 219 43 26 46 123 6

D4A 208.3 1.0447 0.9901 0.965 1.084 1.055 -0.358 251 52 101 34 1 15

D4B 267.1 1.0553 0.9972 0.948 1.114 1.058 -0.052 258 22 351 6 96 67

D4C 130.4 1.0515 1.0033 0.945 1.113 1.048 0.118 214 25 120 7 15 63

D5A 13.13 1.058 1.0343 0.908 1.318 1.023 0.704 145 34 16 44 256 28

D5B 7.454 1.1696 1.023 0.807 1.455 1.143 0.278 304 5 35 8 181 81

D5D 3.965 1.1427 1.0066 0.851 1.345 1.135 0.14 321 14 140 76 231 0

C10A 57.09 1.1175 1.0271 0.856 1.314 1.088 0.369 296 41 193 15 87 45

C10B 50.82 1.0364 1.0347 0.929 1.134 1.002 0.971 44 73 272 11 179 12

C10C 51.35 1.042 1.0319 0.926 1.14 1.01 0.835 69 59 274 28 178 11

C10D 60.95 1.0393 1.0324 0.928 1.135 1.007 0.883 337 78 89 5 180 11

C10E 59.64 1.0373 1.0247 0.938 1.116 1.012 0.756 68 54 267 34 171 9

C11A 61.51 1.054 1.0475 0.898 1.198 1.006 0.922 88 11 340 57 185 31

C11B 64.04 1.1705 1.0412 0.788 1.201 1.124 0.408 132 42 296 47 35 8

C11C 64.27 1.0523 1.0419 0.906 1.183 1.01 0.868 323 46 102 36 208 22

C11D 55.42 1.0566 1.0466 0.897 1.202 1.01 0.884 77 36 310 40 192 30

C11E 67.79 1.0534 1.0526 0.894 1.208 1.001 0.99 300 38 60 32 176 35

C38A 189.4 1.0373 0.9946 0.968 1.072 1.043 -0.217 266 71 76 18 167 3

C38B 199.8 1.0428 0.9949 0.962 1.084 1.048 -0.172 94 71 285 19 193 3

C38C 176.1 1.029 0.9972 0.974 1.057 1.032 -0.137 96 69 289 21 198 4

C38D 182.4 1.0321 0.9972 0.971 1.063 1.035 -0.121 93 65 288 25 196 6

C38E 180.8 1.0318 0.995 0.973 1.061 1.037 -0.243 92 73 288 17 196 4

C54A 78.73 1.0609 1.0389 0.9 1.196 1.021 0.745 108 19 235 61 11 22

C54B 79.02 1.0465 1.0403 0.913 1.167 1.006 0.836 164 60 260 4 353 30

C54C 93.15 1.043 1.0322 0.925 1.143 1.01 0.827 114 33 246 46 6 26

C54D 92.69 1.0473 1.0431 0.91 1.174 1.004 0.942 100 17 255 71 8 7

C54E 83.07 1.049 1.0356 0.915 1.163 1.013 0.812 236 53 108 25 5 25

C56A 70.72 1.0571 1.0415 0.902 1.192 1.015 0.813 151 29 325 61 59 2

C56B 70.05 1.0604 1.0421 0.898 1.201 1.018 0.791 153 32 323 58 60 4

C56C 72.86 1.0529 1.043 0.904 1.186 1.009 0.876 153 24 297 61 56 15

C56D 71.12 1.0527 1.0447 0.903 1.189 1.008 0.901 187 70 326 16 60 13

C56E 67.66 1.1122 0.996 0.892 1.247 1.117 0.601 186 79 356 11 87 2

C56F 73.85 1.067 1.0345 0.899 1.201 1.031 0.64 154 49 322 41 57 6

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Continue…………………

C57A 192.6 1.02 1.009 0.971 1.053 1.011 0.558 327 65 84 12 178 22

C57B 193.5 1.0216 1.0097 0.969 1.058 1.012 0.557 296 43 74 39 183 22

C57C 165.9 1.0266 1.0106 0.963 1.069 1.016 0.509 79 60 280 29 185 9

C57D 196.7 1.025 1.0128 0.962 1.069 1.012 0.622 275 1 182 69 6 21

C57E 167.8 1.0203 1.0057 0.974 1.049 1.015 0.377 297 47 86 16 189 16

C60A 172.7 1.0326 1.0021 0.965 1.07 1.03 0.11 327 6 228 56 60 34

C60B 201.6 1.0264 1.0115 0.962 1.07 1.015 0.547 152 11 254 47 52 41

C60C 221 1.0553 1.0006 0.944 1.118 1.055 0.044 322 22 146 68 53 1

C60D 219.6 1.032 1.0166 0.952 1.09 1.015 0.63 320 26 188 54 62 23

C60E 200 1.029 1.0066 0.964 1.068 1.022 0.32 319 6 223 44 55 45

C61A 17.7 1.1111 1.0537 0.835 1.355 1.054 0.628 294 55 194 7 99 34

C61B 7.35 1.0576 0.9985 0.944 1.12 1.059 -0.01 316 76 97 11 189 9

C61C 26.53 1.1161 1.049 0.835 1.358 1.064 0.573 263 78 86 12 356 1

C61D 15.64 1.057 1.0189 0.924 1.149 1.037 0.454 309 76 77 9 168 11

C61E 11.21 1.0353 0.9958 0.969 1.069 1.04 -0.173 249 73 354 5 86 17

C61F 57.64 1.0858 1.0166 0.898 1.213 1.068 0.308 271 86 96 4 6 0

C61G 22.26 1.0293 1.0214 0.949 1.094 1.008 0.81 339 68 81 5 173 22

C62A 102.3 1.1212 1.1091 0.77 1.534 1.011 0.943 126 65 272 21 8 13

C62B 46.36 1.0681 1.0387 0.893 1.212 1.028 0.688 154 46 271 24 19 34

C62C 54.08 1.1048 1.0505 0.845 1.33 1.052 0.625 266 35 135 43 17 27

C62D 50.13 1.0818 1.0594 0.859 1.291 1.021 0.819 162 44 272 20 20 39

C62E 49.81 1.0786 1.0564 0.865 1.276 1.021 0.811 154 38 265 25 19 42

C63A 61.87 1.0294 1.0221 0.949 1.195 1.007 0.825 116 22 282 67 24 5

C63B 54.06 1.0239 1.0078 0.968 1.159 1.016 0.433 94 27 282 63 186 3

C63C 60.75 1.0281 1.0241 0.948 1.196 1.004 0.904 288 9 115 80 18 1

C63D 104.8 1.0587 1.0541 0.887 1.223 1.004 0.951 292 11 122 79 22 2

C63E 122.9 1.0752 1.0663 0.859 1.291 1.008 0.926 121 63 280 25 13 8

C63F 75.01 1.0469 1.0367 0.916 1.16 1.01 0.852 107 82 278 8 8 1

C65A 12.758 1.3128 1.0796 0.608 1.228 1.216 0.492 82 40 205 33 320 32

C65B 19.672 1.4463 1.1184 0.435 1.35 1.293 0.572 174 1 264 25 82 65

C65C 13.05 1.0604 1.027 0.913 1.671 1.032 0.574 157 59 276 17 15 26

C65D 26.25 1.1255 1.0265 0.848 1.635 1.096 0.35 153 48 40 19 295 36

C70A 217.4 1.0796 1.042 0.878 1.121 1.036 0.656 77 71 305 13 212 14

C70B 158.4 1.0452 1.0313 0.924 1.146 1.013 0.784 92 58 233 26 332 18

C70D 215.9 1.0801 1.0399 0.88 1.2 1.039 0.629 107 53 305 36 209 9

C70E 243.5 1.141 1.0474 0.812 1.12 1.089 0.497 102 46 314 39 210 16

C71A 113.4 1.0365 1.0314 0.932 1.127 1.005 0.907 55 45 284 33 175 26

C71B 151.4 1.0441 1.0223 0.934 1.126 1.021 0.622 41 65 284 12 189 22

C71C 116.8 1.0402 1.0332 0.927 1.138 1.007 0.883 352 65 98 7 191 24

C71D 146 1.0539 1.03 0.916 1.162 1.023 0.673 140 68 260 11 354 18

C71E 111.1 1.0472 1.0305 0.922 1.148 1.016 0.746 350 68 105 9 198 19

C72A 105.9 1.0733 1.0531 0.874 1.255 1.019 0.815 90 80 281 10 191 2

C72B 101.4 1.0692 1.055 0.876 1.25 1.013 0.866 97 71 283 19 192 2

C72C 113.1 1.0712 1.0616 0.867 1.27 1.009 0.915 102 86 259 4 350 2

C72D 108.4 1.0685 1.0613 0.87 1.263 1.007 0.934 57 84 282 4 192 4

C72E 110.9 1.0696 1.06 0.87 1.263 1.009 0.913 99 73 281 17 190 0

C72F 112.1 1.0646 1.0587 0.877 1.247 1.005 0.944 99 21 274 69 8 2

C73A 14.864 1.0976 1.0613 0.841 1.336 1.034 0.747 110 53 254 31 355 17

C73C 16.18 1.1237 1.0647 0.812 1.4 1.055 0.668 108 48 263 39 4 13

C73D 16.16 1.1086 1.0457 0.846 1.329 1.06 0.568 117 39 259 45 10 20

C73E 14.773 1.1593 1.0035 0.837 1.386 1.155 0.113 115 40 259 44 9 19

C75A 13.82 1.0441 1.0208 0.935 1.22 1.023 0.591 281 54 114 36 20 6

C75B 10.55 1.0303 1.0214 0.948 1.096 1.009 0.792 300 34 103 55 204 8

C75D 11.74 1.0497 1.0234 0.927 1.141 1.026 0.591 242 77 123 7 31 12

C75E 107.8 1.1817 1.1267 0.692 1.809 1.049 0.822 271 38 96 52 3 3

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C76A 291.3 1.0629 0.9884 0.949 1.122 1.075 -0.278 83 31 322 41 197 33

C76B 308.3 1.046 0.993 0.961 1.089 1.053 -0.226 95 9 324 77 187 10

C76C 273.3 1.0426 0.9994 0.958 1.088 1.043 -0.002 92 16 317 68 187 14

C76D 200.6 1.0817 0.9832 0.935 1.16 1.1 -0.312 103 18 323 67 198 14

C76E 309.8 1.0478 0.9909 0.961 1.091 1.057 -0.294 108 46 268 42 8 10

C81A 13.14 1.058 1.0343 0.908 1.318 1.318 0.204 81 65 269 24 180 4

C81B 7.453 1.1696 1.023 0.807 1.401 0.704 0.278 301 81 95 8 186 4

C81C 3.965 1.1427 1.0066 0.851 1.345 0.278 0.14 70 74 288 11 199 11

C88A 78.31 1.0566 1.019 0.924 1.148 1.037 0.458 85 65 274 24 182 4

C88B 80.42 1.0688 1.0151 0.916 1.17 1.053 0.331 301 81 95 8 186 4

C88C 78.45 1.0746 0.9775 0.948 1.14 1.099 -0.511 72 76 297 10 205 10

C88D 80.54 1.065 1.0195 0.915 1.169 1.045 0.423 63 85 273 5 183 3

C88E 78.14 1.0604 1.0196 0.92 1.158 1.04 0.447 291 76 101 13 191 2

C88F 72.33 1.0648 1.0147 0.92 1.16 1.049 0.339 123 75 283 14 14 5

C92A 212.3 1.0388 1.0242 0.937 1.118 1.014 0.726 148 67 281 16 16 16

C92B 177.4 1.0219 1.0168 0.961 1.07 1.005 0.837 128 40 277 46 24 16

C92C 196.6 1.0244 1.0145 0.961 1.071 1.01 0.697 176 79 79 1 349 11

C92D 235.9 1.0328 1.0221 0.945 1.102 1.01 0.765 116 14 253 71 23 12

C92E 282.9 1.0602 1.0379 0.902 1.192 1.022 0.737 268 34 125 50 11 18

C93A 22.572 1.2207 1.0157 0.764 1.204 1.202 0.616 171 39 273 14 19 47

C93B 36.58 1.0762 1.06 0.864 1.278 1.015 0.862 280 28 159 44 30 33

C93C 13.11 1.0647 1.0321 0.903 1.191 1.032 0.622 173 39 275 15 21 47

C93D 11.6 1.0899 1.0781 0.832 1.358 1.011 0.919 265 46 145 26 37 32

C93E 15.43 1.0763 0.9989 0.925 1.164 1.077 0.016 271 24 155 44 20 36

C93F 21.64 1.0906 1.0004 0.909 1.2 1.09 0.053 253 44 115 38 6 22

C96A 49.83 1.2372 0.9825 0.78 1.586 1.259 0 125 46 312 44 219 3

C96B 51.2 1.1816 1.0436 0.775 1.543 1.132 0.412 153 61 299 25 36 14

C96C 53.29 1.1513 1.0348 0.814 1.426 1.113 0.385 141 60 296 28 32 11

C96D 51.53 1.2096 0.9886 0.802 1.509 1.223 0.019 130 41 304 49 38 3

C96E 51.76 1.2183 1.0917 0.69 1.828 1.116 0.614 201 76 295 1 25 14

C97A 29.04 1.1581 0.9923 0.85 1.363 1.167 0.003 170 75 300 10 32 11

C97B 25.34 1.2658 0.9174 0.817 1.574 1.38 -0.469 79 37 290 49 181 16

C97C 31.86 1.1519 1.0076 0.841 1.372 1.143 0.151 131 64 358 19 262 18

C97D 20.73 1.2168 1.006 0.777 1.568 1.21 0.151 86 57 237 30 335 13

C97E 22.06 1.261 0.9824 0.757 1.667 1.284 0.022 123 74 233 6 324 15

C98A 410 1.1406 1.0934 0.766 1.549 1.043 0.788 98 77 270 13 1 2

C98B 451.3 1.1438 1.0914 0.765 1.553 1.048 0.767 266 31 86 59 176 0

C98C 564.2 1.161 1.1122 0.727 1.678 1.044 0.817 311 81 89 7 179 6

C98D 526.4 1.1394 1.1036 0.757 1.576 1.032 0.844 95 55 267 34 359 4

C98E 545.2 1.1743 1.1209 0.705 1.759 1.048 0.818 99 64 271 26 2 3

C98F 478.5 1.137 1.0891 0.774 1.524 1.044 0.776 89 65 268 37 0 3

C98G 617.6 1.1533 1.1041 0.743 1.624 1.045 0.802 94 53 268 37 0 3

C98H 457.9 1.1236 1.0915 0.785 1.49 1.029 0.838 97 52 269 38 2 4

C100A 201.9 1.0321 1.0003 0.968 1.067 1.032 0.029 85 48 273 41 180 4

C100B 184.3 1.028 0.9939 0.978 1.052 1.034 -0.356 84 45 272 45 178 4

C100C 192.8 1.03 0.9985 0.972 1.06 1.032 -0.064 83 60 276 29 183 5

C100D 172 1.0226 0.9987 0.979 1.045 1.024 -0.077 83 62 280 27 186 7

C100E 180.1 1.0278 0.9948 0.978 1.052 1.033 -0.301 83 55 270 35 177 3

C105A 331.9 1.0175 1.0125 0.97 1.054 1.005 0.793 90 64 249 25 343 8

C105B 359.6 1.0167 1.0115 0.972 1.051 1.005 0.776 201 81 68 6 337 7

C105C 276.7 1.0179 1.0158 0.966 1.061 1.002 0.921 248 2 4 85 157 5

C105D 318.3 1.0254 1.0168 0.958 1.077 1.008 0.753 66 43 256 47 161 5

C105E 290.9 1.0203 1.0116 0.968 1.058 1.009 0.674 237 48 77 40 339 10

C105F 400.5 1.0252 1.0158 0.959 1.075 1.009 0.725 252 66 86 24 354 5

Estelar

170

TABLE 5: Thermal demagnetization data of magnetic susceptibility of 10 core samples at different temperatures up to 750º C

Sample No. and Magnetic Susceptibility (Km)

Temp.

ºC D3 S6 C105 Gh12 D2 C38 C72 Gh8 S3 C10

25 637.5 612.4 305.2 556.3 277.3 100.5 106.9 45.4 35.8 57.01

100 660.5 634.3 315.4 534.6 257.9 186.4 110.3 44.36 34 58.31

200 676.4 639.1 313.3 547.2 286.7 188.3 110 77.2 45.3 58.8

300 678.9 552.2 315.4 543.9 292.8 188.4 110.3 81.1 45.1 58.65

400 541.1 511.5 312.1 470.3 285.9 186.7 110.5 87.3 46.38 56.8

500 521.6 535.7 329.5 463.3 292.1 182.3 111.6 69.3 55.4 60.2

550 517.5 523.3 343.2 468.2 292.4 177.9 121.3 68.9 57.8 59

600 549.5 534.3 321.8 453.1 305.5 166.7 148.6 67.8 55.3 50.24

650 576.9 538.2 361 443.7 337.9 166.8 128.7 68.2 52.76 63.89

700 650.3 574.3 511.4 413.2 323.9 170.9 117.3 66.3 49.89 58.38

750 649.8 587.9 586.1 425.9 302.6 166.9 107.3 66.2 52.47 58.02

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