Magnetic Properties of Neogene Regional Dikes from East Iceland

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LICENTIATE T H E SI S Per Eriksson Magnetic Properties of Neogene Regional Dikes from East Iceland with Special Reference to Magma FlowMagma to Reference Special with Iceland DikesfromEast Regional Neogene of Properties Magnetic PerEriksson

Department of Chemical Engineering and Geosciences Division of Applied Geophysics Magnetic Properties of Neogene Regional ISSN: 1402-1757 ISBN 978-91-7439-191-6 Dikes from East Iceland with Special Luleå University of Technology 2010 Reference to Magma Flow

Per Eriksson

SWEDISH STUDIES ON ICELANDIC GEOLOGY

Dissertation presented to the Faculty in Candidacy for the Degree of Licentiate of Technology at the Division of Applied Geophysics Department of Chemical Engineering and Geosciences at Luleå University of Techonology Sweden

Magnetic properties of Neogene regional dikes from east Iceland with special reference to magma ﬂow

Examinans Per I. Eriksson

Thesis Supervisors Examinator Discutant Prof. Sten-Åke Elming Prof. Sten-Åke Elming Dr. Håkan Mattsson Dr. Morten S. Riishuus Dr. Freysteinn Sigmundsson

November 2010 Printed by Universitetstryckeriet, Luleå 2010

ISSN: 1402-1757 ISBN 978-91-7439-191-6 Luleå 2010 www.ltu.se THESIS SUMMARY

This thesis deals with rock magnetic measurements on Neogene dikes from the eastern fjords of Iceland. A vast amount of dikes generally striking north-north-east occur as swarms in the glacially eroded lava pile. They are considered as the underlying extensions of fissure swarms in active volcanic systems which like the dike swarms converge at central volcanoes. The dike swarms and associated central volcanoes are uncovered by ca. 1500 m of glacial erosion, leaving the upper parts of these igneous units bare. Two research papers have been prepared based on field studies and measurements of rock magnetism on carefully chosen occurrences of Icelandic dikes in order to test contradicting models of dike origin. The manuscripts are included in the thesis. The first is a detail study of a single composite dike, with a core of fine grained quartz-porphyry surrounded by dolerite margins. The core of the dike was sampled in three locations, separated by ∼12 km and measured for magnetic remanence and anisotropy of magnetic susceptibility. Magma flow direction in this dike was interpreted using the mirror imbrication of the minor susceptibility axes from each margin of the quartz-porphyry core of the dike. The flow regime in all three locations showed a marked flow component from north to south, supported by field evidence in the form of parabolically aligned enclaves, and shear folds. Statistical procedures of bootstrapping was utilized to define the flow and handle imbrication in both the vertical and horizontal plane thus defining direction and inclination of flow. The main contribution of this paper was to prove that anisotropy of magnetic susceptibility used to infer flow direction may give consistent and reliable results, and to present new ways (to use old techniques) to define magma flow directions. The same technique used to infer flow in paper one has sub-sequentially been applied to a far larger set of mafic dikes, extending northeast from the exhumed Álftafjörður central volcano. The second paper documents that the flow regimes from the mafic dikes showed a predominantly horizontal flow from the central volcano, supporting tectonic models that suggest shallow magma chambers to be the source of the dikes. The thesis further discusses the results from these studies in comparison to other studies on Icelandic dikes where the magma flow is determined by the direction of the major susceptibility axis. TABLE OF CONTENTS

1 Preface 2

2 Introduction 3

3 General Geology of Iceland 5 3.1Tectonics...... 7 3.2Bedrock...... 7 3.3DikeFormation...... 9 3.4ErosionalDepth...... 10

4 The Aims of the Study 13 4.1 Methods ...... 13 4.2Samplecollection...... 14

5 Theory on Rock Magnetic Properties 16 5.1MagneticPropertiesofOxideMinerals...... 17 5.2 Anisotropy of Magnetic Susceptibility ...... 19 5.3MagmaFlowFabrics...... 22 5.4SourcesofError:ADiscussion...... 27

6 Propagation of Flow in a Single Composite Dike 30

7 Emplacement of the Álftafjörður Dike Swarm 34

8 Comparison Between this Work and Other AMS Studies 37

9 Perspectives of Future Work 40

10 Sammanfattning av Avhandlingen på Svenska 44

11 Acknowledgements 46

Thesis Bibliography 47 Appendices

I Appendix – Paper 1 In review for Journal of Volcanology and Geothermal Research II Appendix – Paper 2 To be submitted to Journal of Structural Geology III Appendix – Tables Tables A–D containing data used in thesis PREFACE

HE work here presented commenced in June in the year 2007 and ﬁnished Tin November in the year of 2010. The work that underlies and merits this dissertation has been carried out at the Nordic Volcanological Center at the Institute of Earth Sciences, University of Iceland, Reykjavík, where I have been employed as a research fellow for some time. Much of the ideas for the research presented here originate at this institute whereas the expertise on and laboratory facilities for the magnetic techniques used have been supplied from Luleå University of Technology in Sweden, where this study was originally initiated.

The process of understanding not only the complicated theory of rock magnetism, demagnetization techniques, the stability of the magnetic remanence and the subtle yet profound difference between study of remanence and of susceptibility with all the problematic non-simplicity of the latter ﬁeld has been a time-consuming and sometimes frustrating work. Nevertheless, I am pleased to present this thesis and of the underlying work and I may contently say that my understanding of both the nature of rock magnetism and its uses within geology as well as the nature of scientiﬁc inquiry itself has broadened. During the study many questions has been raised, not only regarding methods used but also on epistemology.

I hope that this thesis will not only be valuable to geologists interested in dike propagation in volcanic systems but also to geology students using anisotropy of magnetic susceptibility for the historical oversight on the matter.

Per Eriksson, Hortlax November 2010

2 MAGNETIC PROPERTIES OF NEOGENE REGIONAL DIKES FROM EAST ICELAND WITH SPECIAL REFERENCE TO MAGMA FLOW

Figure 1 – View of the north side of Fáskrúðsfjörður in east Iceland close to the fjord inlet. This plate illustrates the fjord landscape of east Iceland, carved out by glacial erosion since the onset of glaciations since the Plio-Pleistocene (Geirsdóttir, 1990; Geirsdóttier and Eiríksson, 1994; Geirsdóttir et al., 2007; Eiríksson, 2008). The gentle dip of the lava pile toward the paleo-rift axis caused by burial, loading and subsequent transportation by the extensive rifting is evident (Pálmason, 1986). The dikes visible in the mountain sides represent the downward continuation of the ﬁssure swarms stretching from central volcanoes and neatly converge to a density maximum in the middle of the ﬁgure, note also that the density of dikes diminish with altitude (Bodvarsson and Walker, 1964; Helgason and Zentilli, 1985).

INTRODUCTION

HE aims of this study has been to test models of and to quantify fossilized Tﬂow directions in dikes using anisotropy of magnetic susceptibility (AMS) measurements, and to increase the knowledge on the mode of emplacement of dikes in the crust. The origin of dikes in the volcanic systems of Iceland is currently debated. Models explaining the origins of regional dike swarms as processes related to shallow magma chambers situated under central volcanoes have been proposed (Gudmundsson, 1983; Sigurdsson and Sparks, 1978; Sigurdsson, 1987; Buck et al.,

3 2006; Paquet et al., 2007). Models explaining the origin of regional dikes from deep magma reservoirs has also been proposed (Gudmundsson, 1990, 1995). A combination of the two models were laid out by Walker (1992). These models differ among other things in which mode the propagation of flow in the dikes take. One method applied to obtain magma flow directions in dikes, and thus possibly constrain these models, is anisotropy of magnetic susceptibility measurements from dike margins. AMS defines an average of the spatial distribution of magnetic minerals, given that absence of magnetic interactions (Tarling and Hrouda, 1993; Cañón-Tapia, 1996, 2001). Ideally, AMS measures the magnetic mineral fabric, in itself imposed by the chain silicate mineral fabric and thus reflecting the silicate fabric (Hargraves et al., 1991). When magma flows in a dike it acts like an laminar flow trough a pipe conduit (Blanchard et al., 1979; Coward, 1980; Philpotts and Philpotts, 2007). At the margins of the dike simple shear stress regimes form alignment of minerals and vesicles in a pattern (Gay, 1968; Ghosh and Ramberg, 1976; Shelley, 1985), enabling absolute flow direction to be discerned.

This thesis will treat the geology of Iceland, then shortly describe the underlying reasons for this study. The justiﬁcation is followed by a theory section where the theoretical background and method of the sampling and analytical work is presented, some methodological remarks are also made. The major results from the two manuscripts are then presented followed by a discussion comparing this work with other modern works that apply AMS to study propagation of Neogene dikes in Iceland. Future prospects for research is also discussed. The discussion is focused on work that has been performed in Iceland, but the implications, especially when discussing methods to infer ﬂow, is aimed at a wider audience.

4 GENERAL GEOLOGY OF ICELAND

CELAND is situated at the junction between an elevated oceanic plateau Iand the Mid-Atlantic-Ridge. The oceanic plateau, sometimes referred to as the Greenland-Iceland-Faroe ridge stretch from the east coast of Greenland towards the Iceland plateau, and continues east of Iceland, underlies the Faroe islands and disappears under the oceanic sediments around Scotland (Saemundsson, 1986; Sigmundsson, 2006; Sandwell and Smith, 2009). This marine ridge and plateau framework is depicted in Figure 2. The Mid-Atlantic-Ridge is a slow spreading

+UDG 1

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Figure 2 – Low resolution free air gravimetric map over the sea ﬂoor of the north Atlantic. 1. Greenland–Iceland ridge or ocean plateau east of Greenland. 2. Iceland plateau. 3. V-shaped ridges at the Reykjanes extensive ridge axis. 4. Iceland. 5. Iceland–Faroes ridge. 6. Faroe Islands. Figure created from data by Sandwell and Smith (2009). extensional margin between the Eurasian and the North-American tectonic plates. The ridge is constituted by the Reykjanes ridge segment south of Iceland which traverses on land from the tip of the Reykjanes peninsula across Iceland in a branched manner and emerges as the Kolbinsey ridge north of the Tjörnes fracture zone in the north (Figure 3, Sigmundsson, 2006). The various segments on land of the

5 Mid-Atlantic-Ridge provides an extensional stress regime causing faulting, block rotations and the formations of graben structures along the segments (Saemundsson, 1979, 1986; Sigmundsson et al., 2008). The cause of the excessive volcanism needed to generate the igneous rock formations in such a rate that the ridge spreading transport is overcome and the sea mount thus produced arise above sea level, is debated. It is generally accepted that the land mass is formed due to the additive interaction effect between the adiabatic decompressional melting along the Mid-Atlantic-Ridge and an increased melt generation with its locus under the northwest corner of Vatnajökull (Saemundsson, 1979). The presently favored explanation of the increased melt generation is a mantle plume (Bijwaard and Spakman, 1999; Bjarnason, 2008; Bjarnason and Schmeling, 2009), remelting of prior continental crust has also been suggested (Lundin and Doré, 2005; Foulger and Anderson, 2005; Du et al., 2006).

7M|UQHVIUDFWXUH]RQH

19=

6QDHIHOOVQHV

+RIV M¸ONXOO

:9= 9DWQDM¸NXOO

(95= 1HRJHQHODYDSLOH !0D 1 53 3OLR3OHLVWRFHQHH[WUXVLYHV 0D 5H\NMDQHVSHQLQVXOD 6,)= 1HRYROFDQLF=RQH 0D

NP +RORFHQHVDQGXUGHSRVLWVDQGODYDV

9HVWPDQQDH\MDU )LVVXUHVZDUP

Figure 3 – Map of the major geological sub-divisions in Iceland and delineated fissure swarms within the neovolcanic zone. The fissure swarms follow the different ridge segments dividing Iceland. The fissure swarms strike obliquely to the plate boundaries (no shown explicitly) and are arranged en echelon. The Reykjanes ridge goes on land at the tip of the Reykjanes peninsula and off land at the Tjörnes fracture zone. Abbreviations: RP, Reykjanes Peninsula, WVZ, Western Volcanic Zone, EVRZ, East Volcanic Rift Zone, SIFZ, South Iceland Flank Zone, NVZ, North Volcanic Zone. 6 TECTONICS

The stress regime that Iceland is subjected to is governed by the extensional nature of the Mid-Atlantic-Ridge. The ridge represent the separation between the North-American plate which lies west of the ridge and the Eurasian plate that lies east of it. The movement of the plates are fundamentally caused by plate pull of the subjected slabs in subduction zones, allowing mantle material to rise under the ridge axis (Spence, 1987; Conrad and Lithgow-Bertelloni, 2002; Collins, 2003). Presently the two plates move from each other with a velocity of ca. 10 mm per year (Geirsson et al., 2006). The deformation pattern is on land complicated by the branched manner the rift axis develops into (e.g. Keiding et al., 2009). The spatial extension of the fissure swarms delineate the major stress directions (Figure 3). The fissure swarms generally strike NNE, indicating a minor stress component in that direction, with the exception of the fissure swarms at the Reykjanes ridge (Geirsson et al., 2006).

BEDROCK

The exposed bedrock formed by the excessive volcanism can be divided into four zones (Figure 4). The Neogene lava pile, the Plio-Pleistocene extrusive rocks, the upper Pleistocene hyaloclastites and the Holocene lava ﬁelds and sediments. The zones differ in emplacement time as well as in structure. The correspondence between these epochs and those issued by the international stratigraphy commission (ISC) is somewhat arbitrary (Jóhannesson and Sæmundsson, 1998). The upper Pleistocene coincide with the onset of the Bruhnes magnetic epoch, while the division between the Plio-Pleistocene and the Neogene bedrock is based on stratigraphical hiatuses from north and west Iceland (Sigmundsson, 2006). The Holocene lava ﬁelds are generally emplaced along the plate boundary, since melt generation is largest along the Mid-Atlantic-Ridge. Off-rift volcanic systems occur but account to a lesser extent for total extruded magma volumes (Sigmarsson et al., 2008). The continuous emplacement of new lavas bury the older units which sink down into the lithosphere (Pálmason, 1986). The spreading across the rift axis transports the volcanic units east and westwards where they are subjected to erosion and eventually post-glacial uplift

7 (Pálmason, 1986). Hence, the zonation is broadly parallel to the present rift axis albeit complicated by rift jumps (Garcia et al., 2003; Harðarson et al., 2008). The melt generated, is channeled and concentrated in discrete volcanic systems, which consist of a central volcano, with or without an underlying shallow magma chamber, a ﬁssure swarm some 10 − 20 km in width and up to 150 km in length aligned oblique to the ridge axis and arranged en echelon (Saemundsson, 1986; Sigmundsson, 2006). The underlying cause of the surface ﬁssures is considered to be swarms of dike intrusions, referred to as regional dikes. Around the central volcano igneous, intrusive bodies in varying size and composition often assemble in the crust including sills, laccoliths, plugs and domes (Cargill et al., 1928; Walker, 1958, 1960, 1963; Gibson and Walker, 1963; Walker, 1964; Bodvarsson and Walker, 1964; Carmichael, 1964; Gibson et al., 1966; Gibson, 1966). If a shallow magma chamber is present cone sheets often form around it as well as radial dikes (Gudmundsson, 1995, 2006).

The Neogene bedrock consists of monotonous, far stretched layers of tholeiitic to olivine tholeiitic lava, interspersed by thin horizons of paleosols, volcaniclastic and ﬂuvial sediments and lignite layers (e.g. Walker, 1958; Saemundsson, 1979; Roaldset, 1983; McDougall et al., 1984), occasionally carrying plant fossils (Grímsson and Denk, 2005; Grímsson et al., 2007; Grímsson, 2007). The oldest rocks above sea level has an age of 15 − 16 Ma (Moorbath et al., 1968; Hardarson and Fitton, 1997). Exhumed central volcanoes are visible in the fjord landscape of east, north-west and north Iceland and occur as assemblages of felsic intrusives, extrusives and in minor extent gabbroic bodies, potentially overlying solidiﬁed magma chambers (Walker, 1963, 1966; Carmichael, 1967; Walker, 1974, 1975; Helgason and Zentilli, 1985; Duncan and Helgason, 1998; Klausen, 2004, 2006; Harðarson et al., 2008; Burchardt and Gudmundsson, 2009). The accompanying regional dikes, local cone sheets and volcaniclastic deposits are also present. The chemical and isotopic composition of the Neogene lava pile is much more uniform than the volcanics from the Plio-Pleistocene and the neo-volcanic zone (Hardarson and Fitton, 1997; Kitagawa et al., 2008). The Plio-Pleistocene zone is characterized by sub-glacial volcanic deposits including hyaloclastite ridges, tuyas

8 and tindars, i.e. table mountains. Breccia and glassy tuff deposits are also common (Walker, 1965; Jakobsson and Gudmundsson, 2008). The neo-volcanic zone contains the presently active volcanic systems with ﬁssure swarms and surface expressions in the form of central shield or strato volcanoes, calderas or explosions craters and lava ﬁelds (Sigmundsson, 2006; Thordarson and Höskuldsson, 2008).

/HJHQG *ODFLHUV 6DQGXUILHOGV +RORFHQH +LVWRULFDOODYDV +RORFHQH 3UHKLVWRULFODYDV +RORFHQH +\DORFODVWLWHV 83OHLVWRFHQH ([WUXVLYHV 3OLR3OHLVWRFHQH 100 km ([WUXVLYHV 3OLRFHQH 1HRJHQHODYDDQGLQWUXVLYHV

Figure 4 – Outline of the geological sub-divisions of Iceland, bathymetry omitted. Explanation to legend: Glaciers, presently existing glaciers. Holocene sediments, sediment strata mainly generated trough jökulhlaups during the Holocene. Historical lavas, (<1000 years) extrusive mafic to intermediate post-glacial lavas. Prehistoric lavas, (>1000 years) maficto intermediate post-glacial lava fields. Hyaloclastite, basic and intermediate hyaloclastite ridges and mountains, pillow lavas, and associated sediments (< 0.8 m.y.) Extrusive volcanic rocks of mafic to intermediate composition with intercalated sediments of Plio- to Pleistocene age (0.8-3.3 m.y.). Neogene rocks (3.3–16 Ma), volcanic extrusives of mafictofelsic composition with intercalated sediments, major intrusions and tabular intrusives.

DIKE FORMATION

In east Iceland the occurrences of regional dikes and remnants of exhumed central volcanoes are prominent (Figure 5). There is a clear trend and density distribution of the exposed dikes, converging around exhumed central volcanoes and striking NNE (Walker, 1974). The formation mode of regional dikes is debated and has been

9 discussed since the beginning of the last century (Guppy and Hawkes, 1925). Models obtained from studying active volcanic systems, i.e. diking events, propose sub-horizontal diking directions from shallow magma chambers under central volcanoes as seismic or deformation data seems to support this (Einarsson and Brandsdottir, 1978; Brandsdóttir and Einarsson, 1979; Hamling et al., 2009). Lateral diking has likewise been supported by structural studies on dikes (Gudmundsson, 1983; Helgason and Zentilli, 1985; Paquet et al., 2007). In one historic diking event a laterally intruding dike which pierced a magma chamber has been discerned by geochemical evidences (Sigurdsson and Sparks, 1978; Sigurdsson, 1987). These evidences, albeit anecdotal has been used to create models which explain the regional dikes as a consequence of lateral diking from a magma chamber (e.g. Buck et al., 2006). Models which favor vertical dike intrusion from deep magma reservoirs has been inferred from the regional structure of the active fissure swarms (Gudmundsson, 1983, 1990, 1995; Tentler, 2005; Tentler and Temperley, 2007). Their finding seems to be supported by some magma flow studies on regional dikes (Craddock et al., 2008; Kissel et al., 2010). A third diking model incorporating both reservoirs and shallow magma chambers was proposed by Walker (1992). The difference in time between the emplacement of the dikes and the lavas has proven small Kissel et al. (e.g. 2010). If the volcanic systems that creates the dikes is formed in a on rift system this should be expected. The possibility also exists that volcanic systems may form off rift, i.e. offset from the rift axis lavas into far older bedrock, which would make the volcanic products substantially younger than the bedrock.

EROSIONAL DEPTH

The level of erosion, that has exposed the felsic intrusions within the central volcano area and the accompanying regional dike swarms, has been constrained from horizontal zonations of zeolites (Walker, 1960, 1964, 1974; Neuhoff et al., 1999) and decreasing dike dilatation with altitude (Walker, 1958; Bodvarsson and Walker, 1964; Helgason and Zentilli, 1985). The zeolite zonation suggests that the bedrock at sea level has been subjected to ca. 1500 m of burial (Walker, 1974; Neuhoff et al., 1999).

10 Figure 5 – Structural map over the occurrence of dikes in east Iceland and their relative occurrence per km longitude. The names in roman capitals and brackets denote exhumed central volcanoes. The map is redrawn and modiﬁed from a map presented to Þorbjörn Sigurgeirsson by G. P. L. Walker ca. 1960. 11 This is at the upper part of the crust, which extends down to at least 25 km (Bjarnason and Schmeling, 2009). The shallow magma chambers in the active central volcanoes of Iceland are generally located at a depth between 2.5 − 6.5 km (Sigmundsson, 2006). This would place a potential origin of the dikes in the form of a shallow magma chamber at least 1 km below available sampling locations, if the same depth is assumed for Neogene volcanic systems as for recent. However, the fossil magma chambers of some exhumed central volcanoes in the Neogene zone, such as the well exposed Austurhorn and Vesturhorn intrusions, must have been emplaced much further up in the crust if they only suffered 1500 m of erosion to be exposed (Roobol, 1974; Thorarinsson and Tegner, 2009).

12 THE AIMS OF THE STUDY

HE potential of discerning magma flow from the anisotropy of magnetic Tsusceptibility allow us to inquire how regional dikes in fossil volcanic systems have intruded at the present level of exposure. This would increase the knowledge on diking modes thus testing the two models of dike intrusion. Moreover, the spatial distribution of flow directions along the dike swarm extending from an exhumed central volcano can be examined. Only a few cases of diking have been observed, for example the Krafla rifting episode (1974 − 1985) and the turmoil in Afar 2006 − 2007 (Einarsson and Brandsdottir, 1978; Brandsdóttir and Einarsson, 1979; Hamling et al., 2009). By necessity these observations are inferred from seismic or various geodetic techniques and therefore the trajectory of the vertical flow component remains elusive. Since AMS studies require a high degree of precision in both the measurements and the orientation of the samples the relative values of the vertical and horizontal flow components can be discerned. The fjords of east Iceland offers the potential to constrain both the relative occurrence of vertical to horizontal flows in dikes and the spatial distribution of these flows along a fissure swarm.

METHODS

Fossilised magma flow directions can be identified from several different features in the rock. Classic methodology uses field observations like slickensides, vesicle lineation and deformation, folds, drag folds, crystal tiling, branching, grooves, sigma or delta shaped crystal growth, wall rock foliation, enclaves or xenolith tiling, Riedel fractures, gashes, fractures and plumose fractures (Coward, 1980; Varga et al., 1998; Nicolas, 1992; Correa-Gomes et al., 2001; Philpotts and Philpotts, 2007). Modern methods use thin sections from oriented samples to provide statistical fabric evaluations based on image analyses (Allard and Benn, 1989). Evaluation of the anisotropy of magnetic susceptibility as a proxy for bulk mineral fabric has also been applied (Bascou et al., 2005; Aubourg et al., 2008; Craddock et al., 2008; Kissel et al., 2010). Such studies are often combined with thin section analysis (Philpotts and Asher, 1994; Elming and Mattsson, 2001; Aubourg et al., 2002;

13 Geoffroy et al., 2002; Poland et al., 2004; Plenier et al., 2005; Sen and Mamtani, 2006; Geshi, 2008). Techniques expanded from anisotropy of magnetic susceptibility measurements include measurements of anisotropy of anhysteretic remanent magnetization and anisotropy of isothermal remanence (Raposo et al., 2007; Raposo and Berquó, 2008; Chadima et al., 2009; Borradaile and Jackson, In press).

In this thesis anisotropy of magnetic susceptibility has been used to infer mineral fabrics from which flow directions is deduced. The AMS method has the advantage of being able to infer flow even if visible features like vesicle lineation or other flow related features are lacking. The mafic dikes generally lack these kind of features and even if such features would be available, the dikes are in general only exposed in one plane whereas magnetic studies offers three dimensional visualization. One requirement that limits the use of magnetic susceptibility studies as well as with thin section analysis is that samples have to be collected close to the dike margin, something which is not always possible, even in the well exposed geology of Iceland. In comparison to thin sections analysis the sampling and analytical measurements required to obtains the anisotropy of magnetic susceptibility is fast, hence a large number of dikes may be examined. The acquisition of orientated cores for AMS studies also enables paleomagnetic studies to be conducted contemporaneously. Moreover while one thin section sample only show preferred grain orientations in one plane, one AMS sample gives a three-dimensional image. Polished cubes to use with reflected light microscopy may be an alternative to thin sections, giving a three dimensional image. The accuracy of the AMS measurement is remarkable and differences down to 10−8 SI can be detected with the Kappabridge instrument. The accuracy of determining fabric properties in thin sections, especially if a fabrics is to be constrained in three dimensions would not achieve anything near such accuracy.

SAMPLE COLLECTION

Samples for magnetic studies were collected using a portable 1” core drilling machine. The cores were orientated using sun and magnetic compasses. From west Iceland 127 samples were collected from 7 maﬁc dikes. From east Iceland 793

14 samples were collected from 49 maﬁc dikes. These samples have been collected from the margins of the dikes, in average 8 samples per margin, with the exception of 23 samples in east Iceland and 7 samples from west Iceland that were collected as sections across dikes. Additionally, 103 samples have been collected from the Streitishvarf composite dike in three of its seven outcrops where both the margins were exposed. 42 samples were collected from the margins and 61 samples were collected in section. Data from these collections is available in appendix III.

15 THEORY ON ROCK MAGNETIC PROPERTIES

AGNETIC properties are in the strict sense intrinsic in all physical bodies. MSubstances that acquire remanent magnetizations in ambient terrestrial temperatures and ﬁelds are however restricted to ferrous, ferric and anti-ferrous compounds (Dunlop and Özdemir, 1997). The ferro-magnetic compounds generally consist of elemental metals, while ferri-magnetic compounds generally are oxides containing iron and/or other metals. In anti-ferro-magnetic compounds the net magnetization caused, by magnetic ordering of its metal ions is cancelled out, and therefore no remanent magnetization is detectable in these compounds (Dunlop and Özdemir, 1997). The occurrence of these compounds in a rock is determined by the oxygen fugacity prevalent in the rock during its magmatic phase. Since iron is the fourth most abundant element in the Earths crust the occurrence of magnetic compounds are generally attributed to this element. Iron forms compounds in three buffer systems depending on oxygen fugacity (Lindsley, 1991). At low oxygen fugacity iron occurs in its native state (Fe 0). Whence the fugacity is increased in silicate systems such as most igneous rocks, iron will be incorporated into silicates as a divalent (ferrous) ion. The reaction takes place in the Quartz-Iron-Fayalite buffer.

−−−− 0 + + Fe2SiO4 2Fe SiO2 O2

At higher oxygen fugacity iron will appear as both divalent (ferrous) and trivalent (ferric) ions and be form magnetite. The reaction is governed by the Fayalite-Magnetite-Quartz buffer:

+ −−−− + 2Fe3O4 3SiO2 3Fe2SiO4 O2

At still higher oxygen fugacities the iron will be oxidized into the trivalent (ferric) state and forms hematite:

−−−− + 6Fe2O3 4Fe3O4 O2

16 Most basaltic rocks reflect the Fayalite-Magnetite-Quartz buffer and hence contains magnetite (Lindsley, 1991). The occurrence of other metals, specifically titanium does complicate the final mineralogy in the magnetite spinel crystal structure by forming a range of minerals (Dunlop and Özdemir, 1997). The results of low temperature oxidation or devitrification also alter the magnetic mineralogy (Dunlop and Özdemir, 1997).

MAGNETIC PROPERTIES OF OXIDE MINERALS

Crustal rocks do not generally contain native iron, the few rocks that do contain iron are restricted to meteorites and on rare occasions basalts, which have intruded carbon rich sediment. The magnetic properties observed in igneous rocks have therefore most likely their origin in ferrimagnetic minerals. This includes magnetite and hematite, minerals with ferrimagnetic properties belong to the iron oxide and iron sulphide mineral suites (Lindsley, 1991; Dunlop and Özdemir, 1997). Not all of the iron oxides and iron sulphides are ferri-magnetic. The ferri-magnetic properties are produced by electron spin structures on the atomic level which are crucially dependent on crystal structure and atomic radii. Incorporation of other metal ions such as titanium into magnetite disturb this ordering in general by weakening the magnetic moment and the exchange forces and lowering the temperature in which the compound can remain permanently magnetized (Dunlop and Özdemir, 1997).

In igneous rocks the ferri-magnetic oxides occur as accessory minerals mainly of the titanomagnetite mineral suite, the titanohematite or hemoilmenite suite, the titanomaghemite suite and as terrestrial pyrrhotite, a mixture of the iron sulphides − Fe7S8 and Fe9S10 of which the former are ferrimagnetic. Fe Cr spinel minerals or chromites can be ferrimagnetic depending on composition. Chromites are generic to submarine gabbros and peridotite, whereas the other magnetic minerals are more widely dispersed in igneous units (Lindsley, 1991; Dunlop and Özdemir, 1997). In Table 1 the mentioned mineral suites with ferri-magnetic properties are listed. The compositions for which ferri-magnetism is obtained are denoted in the caption. The range of oxides that have ferri-magnetic properties carry remanent

17 Name of mineral suite Chemical formula Titanomagnetite Fe3-xTixO4 2+ 3+ 4+ 2– Titanohematite Fe2y Fe2-2yTiy O3 3+ 2+ 4+ 2– Titanomaghemites Fe[2-2k+z(1+k)]RFe(1+k)(1-z)RTikR 3(1-R)O4 3+ 2+ 2– Magnetite-Maghematite Fe2+2z/3Fe1-z z/3O4 Pyrrhotite Fe1-mS −−−− Chromites FeCr2O4 Fe3O4 Table 1 – The symbol denotes a lattice vacancy. Parameters for titanomagnetite x ≈ 0.6,x≈ 1.0, titanohematite 0.5 < y < 1, 0 < z < 1, titanomaghemites 0 < k < 1, = 8 < < . < < . R (8+z(1+x) , magnetite-maghemaite 0 z 1 and pyrrhotite 0 10 m 0 14. Chromites often contain the ions Mg 2+,Mn 2+,Ni 2+ or Ti 4+. magnetizations of varying stability depending on grain sizes and crystallographic properties. The stability of the magnetic remanence is crucial for paleomagnetic reconstructions and determinations of paleomagnetic pole position (Dunlop and Özdemir, 1997).

The ferri-magnetic minerals are also characterised by a high magnetic susceptibility compared to the common rock-forming minerals such as silicate and carbonate minerals, which are either dia or para-magnetic compounds even if containing iron (Tarling and Hrouda, 1993). The absolute values of susceptibility varies amongst the α oxide minerals. The common mineral magnetite ( Fe3O4) can generate the highest γ value of mass susceptibility, followed by maghemite ( Fe2O3), titanomaghemite 3+ 2+ 4+ 2– (Fe[2-2k+z(1+k)]RFe(1+k)(1-z)RTikR 3(1-R)O4 ) and pyrrhotite (Fe7S8). The other common mineral hematite has a far lower susceptibility range than magnetite (Tarling and Hrouda, 1993). If they are both present in a rock, the magnetic fabric will be dominated by magnetite if the mineral exceeds 5wt% of the iron oxide fraction in the rock (Ute and Norbert, 2008).

Magnetite and ulvöspinel are the end members of the titanomagnetite suite. Hematite and ilmenite are analogue end members of the titanohematite suite. As they crystallise the minerals in both suites converge to end member compositions. Intermediate compositions can only be preserved by rapid cooling. Maghemite is formed by weathering or low temperature oxidation of magnetite or titanomagnetite, a process that takes place on mineral surfaces (Ade-Hall et al., 1971; Petersen, 1976;

18 Dunlop and Özdemir, 1997). Like pyrrhotite, maghemite is a common mineral in igneous rocks in Iceland (Steinthorsson et al., 1992). Under normal circumstances magnetite is the dominating magnetic mineral in the basalt and will thus determine magnetic properties of the rock.

The Curie and Néel temperatures are deﬁned as the point where the magnetic exchange or super-exchange interactions between the electrons become uncoupled, which preclude any ferro, ferri or anti-ferrimagnetic behavior. The Curie temperature is used to describe this behavior in ferro and ferri-magnetic compounds, whereas the Néel temperature is restricted to describe anti-ferrimagnetic compounds. Magnetic electron coupling is lost in an narrow temperature-interval, which is indicated by a sharp drop in magnetic susceptibility of the sample. Thus measurements of temperature/susceptibility variations can therefore possibly indicate the oxide mineralogy of the rock (Tauxe, 1998). In Table 2 mass susceptibility and Curie/Néel temperature is listed for selected ferri-magnetic minerals.

ANISOTROPY OF MAGNETIC SUSCEPTIBILITY

The volume magnetic susceptibility is dimensionless in Système International (SI) and determines the strength of magnetization when a material is subjected to a magnetic field. Described in a vector space the susceptibility becomes a symmetric tensor of the second order and is independent to the magnetising field strength for low fields (<23.9 kA/m Tarling and Hrouda, 1993).

M = χH (1) where M is the magnetization of the body, χ is susceptibility and H is the external ﬁeld. Due to crystallographic properties, spatial distribution, shape and size of magnetic minerals in the rock matrix the susceptibility will be directionally anisotropic (Nicolas, 1992; Dunlop and Özdemir, 1997).

In iron oxide grains there are two sources for an anisotropic response to

19 Chemical compositions and mass suceptibility of rocks and accessory minerals

Mineral/Rock Chemical Compositions Density (ρ) Mass Susceptibility (χ) Curie Temperature R Name (103Kg/m3)(10−8m3/Kg)(°C) Magnetite Fe3O4 5.18 20 000 – 110 000 580 1,2 γ Maghemite Fe2O3 4.90 40 000 – 50 000 590–695 1,2 (250-850) α ∗ Hematite Fe2O3 5.26 10 – 760 675 1,2 a ∼ Titanomagnetite Fe3-xTixO4 4.98 2500 – 12 000 180 1,2 3+ 2+ 4+ Titanomaghemite Fe[2-2x+z(1+x)]RFe(1+x)(1-z)R TixR 3(1-R) 4.99 57 000 160–440 1,2 2– 4+ 2– O4 TixR 3(1-R)O4 Ulvöspinel Fe2TiO4 4.78 100 –150 1,3 Ilmenite FeTiO3 4.72 46 – 80 000 –200 1,2 Natural pyrrhotite(s) Fe1-xS 4.62 10 – 30 000 325 1,4,5 Hexagonal pyrrhotite Fe S8 4.62 69 000 320 1,6 7 ∗ Monoclinic pyrrhotite Fe9S10 4.62 3800 315 1,7 Chromite FeCr2O4 4.80 63 – 2500 –185 1,2

Andesite 57–63% SiO2 2.61 6500 – 1,8 Basalt 45–52% SiO2 2.99 8.4 – 6100 – 1,8 Dolerite 45–52% SiO2 2.91 35 – 5600 – 1,8 Granite >69% SiO2 2.64 0 – 1900 – 1,8 Rhyolite >72% SiO2 2.52 10 – 1500 – 1,8

Table 2 – Chemical composition for selected minerals and silica content for selected rock types given with bulk mass susceptibility and Curie temperatures for the minerals. Values of mass susceptibility measured in weak magnetic field, room temperature and atmospheric pressure. Mass susceptibility can be derived from volume susceptibility by χ = κ/ρ. Curie temperature given in °C ∗ Denotes Neél temperature, inversion temperatures given in brackets. aValues given for x ∼ 0.6. R: references, (1.) Hunt et al. (1995), (2.) Dunlop and Özdemir (1997), (3.) Akimoto (1962), (4.) Dekkers (1989), (5.) Pickler and Edelman (2007), (6.) O’Reilly et al. (2000), (7.) Bennett and Graham (1981), (8.) Le Maitre (2004). 20 magnetizations. The first is determined by the geometry of the crystalline structure and the strength of the micro-magnetic exchange forces in the crystal. The joint effect of crystal and exchange structure influence the electron spin directions. Therefore the spin axes and with that the magnetization, align more easily along certain axes than others, so called easy axes or easy planes. Magnetizations can be forced trough hard crystallographic axes but this require additional energy. This kind of crystallographic anisotropy is strong in hematite and pyrrhotite but almost non-existent in magnetite (Tarling and Hrouda, 1993; Dunlop and Özdemir, 1997). The second source is the shape of the grains themselves, non-equant grains become polarized when subjected to a magnetic field. The polarization strength is determined by the distance between the poles i.e. determined by shape of the grain. The anisotropy of titanomagnetite is determined almost entirely by this factor, while the shape anisotropy of hematite is negligible. Titanomagnetites and titanomaghemites behave very similar to magnetite due to the similarities in crystal structure (Dunlop and Özdemir, 1997).

The anisotropy of the magnetic susceptibility can be visualized in a shape ellipsoid, which main axes corresponds to the major, intermediate and minor axes of the susceptibility tensor so that χa > χb > χc. To fully describe the shape of the ellipsoid two additional parameters are used, the shape parameter T and the corrected anisotropy degree Pj (Jelínek, 1981). The shape parameter is expressed by:

2η − η − η T = b a c − 1(2) ηa − ηc where ηi = ln(χi). Values of T where −1 ≤ T < 0 correspond to prolate ellipsoids, T ≈ 0 corresponds to sphericals and 0 > T ≤ 1reﬂects oblate ellipsoids. The corrected anisotropy degree PJ is given by: 2 2 2 Pj = exp 2((ηa − ηm) +(ηb − ηm) +(ηc − ηm) ) (3)

√ where ηm = 3 η1 · η2 · η3. PJ describes the magnitude of anisotropy that the shape ellipsoid exhibits. PJ ranges from 1 and upwards but generally does not exceed 1.1

21 (10%) for pristine igneous rocks whereas metamorphic rocks may yield substantially higher values (Tarling and Hrouda, 1993).

MAGMA FLOW FABRICS

The origin of the magnetic fabric i.e. the axes of the susceptibility ellipsoid and their relative distribution is caused by the spatial, directional and crystallographic distribution of minerals in a rock as described above. The views on the correspondence between the bulk mineral fabric, i.e. alignment of early forming silicate minerals especially in the form of plagioclase laths, and the principal axes of the susceptibility ellipsoid has undergone some change since the use of susceptibility measurements on rocks was first proposed in the 1950s (Graham, 1954). Note that measurements of magnetic susceptibility on rocks were performed long before Graham, e.g. Rucker and White (1898). Lineation of the minerals caused by magma flow was first thought to be interpretable through the combined shape anisotropy affect of likewise flow aligned elongated magnetite grains. The lineation was to be represented by the major susceptibility axis or the intermediate axis when the major failed to give satisfactory result (Khan, 1962). The ambiguity was explained due to rolling of magnetite grains perpendicular to the flow direction in a viscous medium, something which is still being examined (Cañón-Tapia and Chavez-Alvarez, 2004). Khan (1962), who was the first to publish results on AMS from various igneous units, mentioned that “The anisotropy of the dikes, ring dikes, and cone sheets examined is not easily explained [...] as there is no simple relationship between the flow direction and the principal susceptibility directions”. This did not hinder scientist from eagerly conducting studies during the 1970-90s on dikes with the assumption that the major axis is a direct proxy of flow sense by (mis-)quoting Khan (1962). The coincidental relation between the long axis of magnetite grains and the major susceptibility axis is in agreement with the results from metamorphic rocks that Khan (1962) based this conclusion from, but not from pristine igneous rocks which tend to have subhedral magnetite (Haggerty, 1991). Iron oxides are among the latest minerals to form when a magma crystallizes (Ariskin, 1998), and any rolling by crystals within the magma can only be valid while they are non-interacting. Strong crystal interactions in laminar

22 ﬂows and thus prevention of free movement occur however relatively rapid at only 8% crystal content (Komar, 1972). Modern studies have showed a spatial congruence between the AMS, including the major axis and the petrofabric, interpreted as a consequence of emplacement deformation i.e. Olivier et al. (2010). This does in itself not imply rolling of magnetic grains.

Iron oxides as they occur in pristine igneous rocks are often dendritic and subhedral. Yet, they are still an intrinsic part of the magma they crystallize from. Since the iron and sulﬁde oxides crystallize late their growth is constrained by the previous silicate mineral fabric. Thus their growth is not random, but an image of the silicate fabric (Hargraves et al., 1991; Bascou et al., 2005).

Given the presumption that the major axis was directly indicative of flow direction the occurrence of magnetic fabrics that could not be interpreted as an image of magma flow, i.e. fabrics where the major axis is perpendicular to dike margin, became increasingly troublesome (e.g. Rochette et al., 1991, 1992, 1999; Borradaile and Gauthier, 2003). A division into normal, inverse and intermediate fabrics was made (Rochette et al., 1992). Explanations were sought from the effect of magnetically single-domain grains which will not be magnetised along their maximum length axis by low field strengths (Potter and Stephenson, 1988; Ferré, 2002), and in combined internal fabrics (Stephenson, 1994; Cañón-Tapia, 1996; Callot and Guichet, 2003). Mineral behavior in laminar viscous flow was also examined (Jezek et al., 1994; Iezzi and Ventura, 2002; Marques and Coelho, 2003; Cañón-Tapia and Chavez-Alvarez, 2004). The possibility of turbulent magma flow to account for anomalous fabrics in dikes is unlikely since such flow regimes would not generate consistent magnetic fabrics over an entire sampling site, which usually covers an area of at least 5 m2. Turbulent flows can occur, however it is an unlikely outcome of magma fluid mechanics, and they require relatively thick dikes (> 11 m Petcovic and Dufek, 2005). The effect of single-domains grains has not been successful in explaining the inverse fabrics (Cañón-Tapia, 2004). Since the interpretation of inverse and intermediate magnetic fabrics has proved troublesome,

23 thin section analyses were performed to look for eventual lineation of silicate minerals and their relation to the major axes of the susceptibility ellipsoid or the length axis of opaque minerals (Geoffroy et al., 2002; Poland et al., 2004; Archanjo et al., 2002; Archanjo and Launeau, 2004; Plenier et al., 2005).

A consistency between the mineral foliation plane and the magnetic foliation plane was discovered by Geoffroy et al. (2002, 2007). Hence, the plane of flow should be indicated by the minor susceptibility axis, if this axis show a polar distribution. The original suggestion to use the minor axis came from Halvorsen (1974). The implication of the results of Geoffroy et al. (2002) is that magnetic minerals (and hence magnetic susceptibility) become foliated parallel to the flow plane. Hence, this orientation can be used to determine the absolute flow direction if the geometry of the dike is known. A slightly oblique magnetic foliation to the dike trend has also been noted by Olivier et al. (2010). When magma intrudes into the crust as a tabular body such as a dike we can envisage that a velocity gradient across the dike develops in a zone nearest to the dike walls, analogue to a laminar flow in a pipe. The simple shear zones near the dike wall will direct the mineral fabric into a foliation sub-parallel and also imbricated away from the dike margin (Figure 6). The simple shear zones will develop irrespective of flow type (Newtonian, pseudo-plastic or Binghamian Blanchard et al., 1979; Shelley, 1985; Ildefonse et al., 1992; Arbaret et al., 1996; Dragoni et al., 1997). Thus if both the margins are accessible in field, sampling along both of them and subsequent AMS measurement will delineate the foliation planes and the absolute flow direction can be defined.

The assumption omitted in the previous discussion is that for these flow profiles to be preserved the flowmustcontaincrystalstoalignwithflow, flowingliquiddono preserve the flow profile whence the flow has halted. When the magma intrudes it generally consists of a large melt fraction, never the less shear induced fabrics still form due to interaction of early forming mineral grains, even at low (8%) concentration (Komar, 1972; Arbaret et al., 1996). Also omitted from the discussion is the distance from the margin to to which the simple shear zone is formed, and to

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Figure 6 – Velocity profiles for different types of laminar flow regimes and the resulting shear planes. (a) Velocity profiles for Newtonian and pseudo-plastic flows. Laminar flow is retained across the dike. (b) Binghamian velocity profile, laminar flow is only retained at the margins. (c) Conceptual model of resulting shear imposed mineral fabric according to Shelley (1985). The planes will be imbricated away from the margins and towards the flow (1). Shear zones develop where the stresses are readjusted (2). Shelley (1985) unfortunately do not state the respective size of each zone. what extent the imbricated fabrics is retained after the magmatic flow has ended. If the flow is Newtonian the flow parabola should be preserved across the dike (e.g. Coward, 1980). Some authors have given suggestions on suitable sampling distances of 5–10 cm (e.g. Varga et al., 1998). These estimates are unfortunately not constrained by any detailed analysis. If there is a compaction of the magma in the central part of the dike, or if the flow is Binghamian, the distance from the margin to which the flow imbrication is preserved is presently not constrained.

The previous discussion has outlined how flow fabrics is imposed, post-magmatic stresses may also affect the mineral fabric. Tectonic or local stress may while the dike is solidifying alter the original fabric (e.g. Just et al., 2004; Hamilton et al., 2004; Borradaile and Jackson, 2004). The occurrence of columnar jointing of tabular basaltic bodies is well known. The columns form as a consequence of cooling stress which may or may not affect the mineral fabric (Ellwood and Fisk, 1977; Ellwood, 1979). If several impositions of fabrics is present in a rock it may be difficult to to separate tectonic fabrics from flow fabrics using using only magnetic techniques. Hence, misinterpretations may occur if there is no other geological information

25 available or the data deviates signiﬁcantly from the theoretical models of ﬂow. In any case the magnetic fabric must be compared to some other geological information to delineate from where the magnetic fabric originates.

Another criticism is the unanimity between the lineation or foliation of the major silicate phases, preferably plagioclase laths, and the magnetic minerals and the AMS ellipsoid. In igneous rocks the oxide minerals are generally octahedral, fine-granular association of anhedral crystals or massive. In rare cases the magnetite may form dendritic or skeletal crystals (Hurlbut and Klein, 1985; Anthony et al., 1997). The magnetite grains may also mostly interact and consists of different populations of either single pseudo-single or multi-domain grains of which the latter responds distinctively different to an applied magnetic field from the two other grain sizes (Potter and Stephenson, 1988). Therefore it may prove difficult as long as the crystals are not anhedral to achieve a reliable spatial dimensional comparison between the oxides and the silicates in pristine igneous rocks, hence the source of the specific fabric may often be obscured. It must also be noted that single- and multi-domain grains have different susceptibilities, in the order of 1.7 times higher susceptibility for 90% titanomagnetite multi-domain configuration, disregarding grain size (Tarling and Hrouda, 1993). Single- and multi-domain fabrics can potentially be discerned using anisotropy of anhysteric remanence (AARM Borradaile and Jackson, In press). The directions of the magnetic susceptibility tensor can of course be compared to silicate mineral shapes and eventual lineation in thin section analysis, but the underlying reason why the magnetic fabric does or does not correspond to silicate fabric will be very difficult to determine. Furthermore alternating field demagnetization has been shown to on occasion alter the magnetic fabric, which most likely is caused by the resetting of magnetic interactions between grains. If grains are interacting thus altering an original magmatic fabric they may not reflect the silicate fabric. When faced with anomalous magnetic fabrics in respect to the flow theory it will be impossible without advanced laboratory analyses and further labor intensive work to delineate single-domain fabrics, stress fabrics or magnetic interaction fabrics. Those efforts may nullify the (apparent) advantage in making AMS measurements

26 instead of orientated thin section analyses, or polished cubes. Note that the sufficient accuracy and possibility to determine fabric parameters in three dimensions may not be achieved using thin sections or polished cubes. It is also impossible to know in advance if the normal AMS fabrics are really normal, reflecting a flow imposed silicate fabric and not a product of magnetic interaction or intersecting magnetic fabrics.

SOURCES OF ERROR:ADISCUSSION

Given the problematisation of the use of AMS in the prior discussion, ways to repudiate them may be sought in common scientific practice. I will give a theoretical example and the methodology of that example is to be discussed. The example is analogue to our presented study. Assume that a collection of samples from a number of dikes have been collected and measured for AMS. 10% of the samples were shown to be oblate. Some of the samples were then demagnetized using AF-demagnetization and measured for AMS again. Some (10%) but not all of the samples that were demagnetized changed fabrics after the demagnetization. Two problems arise from this, first, in which extent can the rest of the sample series be expected to act in the same way in regard to demagnetization (this is the problem of inductive logic). The second is which fabric corresponds to the actual petrofabric, prolate or oblate, if any of them do? We can of course reject the samples which do not corresponds to our original envisioned model of flow-imposed fabric imbrication. This requires an active choice, but if we makes choices about which data is suitable to infer our results from, what separates our results from those of soft sciences, e.g. humanists, economists, theologians. It may be objected that the measurements we perform are near indisputable (since they are in essence mathematical) whereas those of human sciences may always be subjected to bias and influence during the ’measurement’. So while there in human sciences always are two acts of choices (during data collection and during interpretation) the natural scientists have only one stage of choice-making (during interpretation). Let us try to constrain our choices and examine the difference between the human sciences and natural science further. A few polished cubes are produced from both the samples that changed magnetic fabric after demagnetization

27 and those that did not. The three dimensional fabric of the plagioclase laths, considered to reflect flow imposition, is determined. It turns out that in 90% of the prolate samples that did not change fabric, the plagioclase laths are to 90% confidence parallel to the major susceptibility axis. Note that the problem of inductive logic remains since not all samples are tested. The major axis should be parallel to flow but only if the right samples are used to infer flow. The problem can be described as dependent variables. In a sample suite 10% of the samples are oblate, 10% change fabric, 10% of the prolate fabrics are not reflecting flow and the flow can be determined to a 90% confidence in the rest. The probabilities P1,2,3,4 = 90% all need to be fulfilled such that:

P1(0.9) · P2(0.9) · P3(0.9) · P4(0.9)=0.66

The probability that we will obtain the correct flow sense from a sample is now only 66%. To build arguments on each other with lower confidence degrees than in this example will naturally yield lower probabilities. In this example the reliance on whether the plagioclase laths really reflect flow, and to which degree is not discussed. Neither is which magnetic minerals and in which domain state that the magnetic fabric originates from. The ramifications of including additional inquiries should be obvious. In terms of the results in our two papers the low ratio of fabrics that fitted the model of flow imposed imbrications along the margins can be explained in the same way. We do not know if other stresses were active during or after magma emplacement, i.e. transtensional dike openings, magma compaction, columnar jointing stress fields, regional stress fields, slipping, etc. The length into the dike which the imbrication may be preserved is presently unknown. The relation between the silicate mineral fabric and the magnetic fabric is presently not fully constrained. The influence or disturbance by single-domain grains on the magnetic fabric in a natural mixture of grains as occur in a rock is also presently not fully constrained.

The point of this discussion is to show that if some measure cannot directly be inferred with negligible error, the side arguments to support the original measure will amass making the venture difﬁcult if not hopeless. If one is to do studies which will

28 be successful in relation to its aim, and thus reliable, one should only use techniques that up to the present have proved to give indisputable results.

29 PROPAGATION OF FLOW IN A SINGLE COMPOSITE DIKE

HIS is a short summary of the major results in paper I. The reason to perform Tthis study were to test the reproducability of AMS in one single igneous unit, and to support the interpretation of AMS with field evidence. Field relations which enables us to infer flow in dikes is usually scarce, especially in maficdikes.The Streitishvarf dike has been studied in relation to various inquiries such as structural (Guppy and Hawkes, 1925; Guðmundsson, 1985), petrochemical and mineralogical (Gunn and Watkins, 1969; Watkins and Haggerty, 1968) and volcanological (Gibson and Walker, 1963; Gibson et al., 1966; Walker, 1966). The Streitishvarf dike outcropping in easternmost Iceland, is one of a relatively few number of composite dikes (Gibson and Walker, 1963), it is conspicuous with reference to both its size and length. The dike was sampled in three of its seven presently known outcrops. The three sites (I, II and III) were named after geographical names as the Streitishvarf, Hökulvík and Hellufjall outcrops. The outcrops are separated by 12 km in length and samples were collected from the quartz-porphyry core at each site. Additional samples were collected both from the margins and across the inner part at Streitishvarf as well as six samples from the dolerite margin juxtaposed to the quartz porphyry core at Streitishvarf.

The magnetic fabric were detemined through AMS measurements. When interpreting the magnetic fabric in relation to magma flow the suggestions by Geoffroy et al. (2002) on using the minor axis and margin samples to infer flow were followed. In all three outcrops the margin samples showed mirror image imbrication, that indicated a marked flow component from north to south. This was confirmed by parabolic alignment of enclaves and flow banding in the Streitishvarf outcrop. The study of the mafic enclaves and their relationship with the host quartz-poprhyry at Streitishvarf, showed features only attributable to a contemptuously origin from two co-existing liquids. These features include round forms on the enclaves, crenulated interfaces towards the quartz-porphyry, back-veining from and mechanical mixing with the quart porphyry. The enclaves showed a strong alignment parallel to the dike trend,

30 and were visible a foliation parallel to dike trend. The maﬁc enclaves are described as xenoliths by some authors. They are clearly not and are important for understanding the emplacement of this composite dike.

Additional ﬁeld studies tracked the dike further up on the slopes of Hellufjall at ca. 300 − 400 m elevation, and revealed an outcrop previously unknown in literature. A possible physical connection between the dike and the Sandfell laccolith, just north of the Hellufjall outcrop remain speculative. No outcrop on the mountain ridge separating the two fjords was found, and no continuation of the dike in the valley by Sandfell north of the Hellufjall ridgeline was found. If the dike continues north of Hellufjall it must do so below the present erosional level.

It was noted that the minor axis was imbricated both with the respect to the vertical and the horizontal plane. To address this imbrication the flow was determined using the lines of intersection between the planes perpendicular to the minor axes from both margins. The results were bootstrapped in order to obtain a statistical estimate on the mean direction of these intersection lines (Efron and Tibshirani, 1986; Constable and Tauxe, 1990; Henry, 1997). The imbrication line is thus a measure of both the strike and dip of the flow direction as long as criteria for equal and symmetric angular imbrication of the magnetic foliation planes is met. The indicated flow directions are significantly different when comparing the three sites. At the outcrops the dip angle was 47◦ at Streitishvarf, 64◦ at Hökulvík and 31◦ at Hellufjall. In all the sites the flow is nort-to-south directed. The flow dips are different from each other, but the site with steep dip, Hökulvík, was sampled at a higher altitude than the other sites, ca. 150 m. A model to encompass the possible flow trajectories was generated (Figure 7). The models is based on work suggesting that this kind of composite dike is created when a mafic dike pierces a felsic magma reservoir (Gibson and Walker, 1963; Blake et al., 1965; Wiebe and Ulrich, 1997). The felsic magma will, whence disturbed in its chamber by the mafic dike intrusion become mobilized, allowed to rise and escape through the pathway created by the mafic dike. The origin of the two dike units thus differ, and their flow directions may even be perpendicular. In the paper the

31 source of both the quartz-porphyry and the dolerite margins is argued to come from presently undescribed (but not unknown) central volcanoes. The felsic magma is argued to come from a volcanic system separate from but close to the Reyðarfjörður central volcano. The main arguments is that the timing differ between the activity of the Reyðarfjörður central volcano and the emplacement of the composite dike by >1 m.y. The Reyðarfjörður system has traditionally been inferred as the mother-system to the Sandfell laccolith juxtapozed the Streitishvarf dike (Gibson et al., 1966). The maﬁc dike is argued to have come from a submerged volcanic center south of Streitishvarf. This is the only possible system in the trajectory of the dike that cannot be ruled out from age estimations. The central volcanoes of Breiðdalsvík and Þingmúli is ruled out as they are offset north-west of the dike, and the Álftafjörður system is ruled out on basis of its likely emplacement age.

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Figure 7 – Geological model of the dike intrusion, including the dike’s relation to the paleosurface and the Sandfell laccolith. The maﬁc dike is argued to have intruded from the south (black curved arrows), piercing a speculative magma reservoir here centered under Fáskrúðsfjörður allowing the felsic magma to rise and expand to the south (dotted line and small arrows). 33 EMPLACEMENT OF THE ÁLFTAFJÖRÐUR DIKE SWARM

HIS is a short summary of the major results in paper II. The purpose for this Tstudy was to obtain flow directions in a larger quantity of mafic dikes belonging to the Álftafjörður volcanic system. Decisive flow regimes in dikes offers constraints to tectonic models used to explain the origin of dike swarms as noted in the chapter on geology. The Álftafjörður central volcano, exposed in the field as assemblages of felsic extrusives and intrusions of different sorts, has a dike swarm associated with it (Figure 8). It extends north-north-east from the central volcano, with a trajectory towards the Reyðarfjörður volcanic complex. The dike swarm is significantly offset east of the Þingmúli and Breiðdalsvík dike swarms.

The sub-vertical dikes strike NNE and they were sampled at different distances from the central volcano. The samples were collected from the margins and the flow directions was determined in the same mode as for the Streitishvarf composite dike. Previous studies on Icelandic dikes in east Iceland include those performed by Craddock et al. (2008) and Kissel et al. (2010). Neither of these authors sampled the Álftafjörður dike swarm. Kissel et al. (2010) collected dikes close to Reyðarfjörður and Craddock et al. (2008) sampled dikes dispersed across the whole east coast. These two authors used the major axis to infer flow, which suggested vertical flow regimes only. In the present study the absolute majority, 10 out of 15 flow regimes, were sub-horizontal, directed to the north from the Álftafjörður central volcano. Four flow regimes were directed from north to south, towards the central volcano. An explanation for these anomalous flow regimes were found in a diking model favoring lateral diking from shallow magma chambers (Figure 9). Seven dikes with possible transtensional magnetic fabrics were found, i.e. parallel imbrications. These dikes were exposed on a line striking NNE. Such a conspicuous spatiality of occurrence may indicate that this axis was the inflection line in a regional transtensive stress regime at the time of the dikes creation.

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NP Figure 9 – Diking model which explains the origin of a regional dike swarm through lateral propagation of dikes from a shallow magma chamber (A). A large-scale crenulation forces the magma down again at B giving rise to downwards dipping flow. At C a fissure eruption occur which allows both steep inclinations and back-flow. At the propagating tip of the magma flow (D) the direction of flow will be difficult to asses due to conflicting flow regimes.

From a geological viewpoint these results are interesting since they clearly attribute diking and thus crustal dilatation to shallow magma chamber processes. It thus seems like volcanoes are very important key features to understand if regional and global (in the case of Mid-Ocean-Ridges) geological evolution are to be explained. Some caution should be preserved in relation to these results since it will be showed in the following chapter that the ﬂow directions obtained are much dependent on which method used to infer the ﬂow.

36 COMPARISON BETWEEN THIS WORK AND OTHER AMS

STUDIES

NLY a few studies using anisotropy of magnetic susceptibility (AMS) Oon Icelandic rocks have been published. They include some of the ﬁrst studies made using the AMS technique. Ellwood and Fisk (1977), Ellwood (1978) and Ellwood (1979) measured anisotropy of magnetic susceptibility on various igneous units from Iceland such as sub-aerial lavas, deep sea lavas, dikes, sills and basalt columns. Unfortunately the sampling scheme as well as locations of the dikes was not stated. The concept of imbrication was also unknown at the time. Notably is that two of the ﬁve dikes sampled by Ellwood (1978) clearly show an imbrication pattern (cf. Tarling and Hrouda, 1993, p. 121).

Two additional magnetic studies, both on maﬁc dikes, have been made in recent years (Craddock et al., 2008; Kissel et al., 2010). In both of these studies the major susceptibility axis was used as a direct proxy to magma ﬂow, disregarding imbrication. Craddock et al. (2008) sampled thin dikes, in general <1 m wide, using a cubic sampling scheme across the dikes. In total 13 dikes from both northwest and east Iceland were sampled. Craddock et al. (2008) concluded that 10 of the 13 dikes had sub-vertical major susceptibility axes implying vertical emplacement.

Kissel et al. (2010) sampled sections across 27 dikes around Reyðarfjörður in east Iceland. The dikes were in general around 1.5 or 5 m wide. Kissel et al. (2010) report the presence of two kinds of fabrics normal and inverse, where the ﬁrst are characterized by vertical major axis lacking imbrication and the minor axis perpendicular to dike wall. The minor axis do however show imbrication, which is disregarded by Kissel et al. (2010) who conclude that the magma ﬂows was vertical based on interpretation of the major axis in dikes carrying a normal fabric. The inverse fabric is characterized by the inverse relation between the major and minor susceptibility axis.

37 The imbrication model using the minor axis is favored in this thesis based partly on the results by Geoffroy et al. (2002) (see also Philpotts and Philpotts, 2007). Neither Craddock et al. (2008) nor Kissel et al. (2010) acknowledges the findings by Geoffroy et al. (2002), who demonstrated large discrepancies between the major silicate mineral lineation and that of the major susceptibility axis, concluding that the major axis should not be used as a flow indicator. Nonetheless, the relation between the actual petrofabric and the susceptibility ellipsoid is not proved either by Kissel et al. (2010); Craddock et al. (2008) or us. In other studies congruence between the major axis and the silicate fabric have been shown (e.g. Aubourg et al., 2002; Poland et al., 2004). When interpreting flow via either the minor or major susceptibility axis the frequency of dikes that have fabrics not interpretable as flow is high.

If the results of Kissel et al. (2010) are recalculated using the intersection line the flow implications are completely different. Craddock et al. (2008) did unfortunately not offer sufficient data to perform recalculations. Three examples from the data by Kissel et al. (2010) outline this (Table 3). First if the minor axis of dike IC06, a normal type dike, is mirrored and the intersection line is calculated for the margin pair, it results in a purely horizontal flow without vertical component whereas Kissel et al. (2010) use the major axis and conclude that the flow is vertical. Note that since both margins are lumped together by Kissel et al. (2010) the flow calculated from the intersection line, will be directed either north-to-south or south-to-north depending on which configuration of margins is used. The second example is a dike with composite fabric where the margin has been recalculated assuming that the flow should be upwards directed. The results indicate a predominantly horizontal flow when using the intersection line whereas Kissel et al. (2010) interprets the flow as vertical. Note that the major axis is inclined towards north. The third example is from dike IC11 where the values are taken from Figure 9 in Kissel et al. (2010). Note that here values for each margin are available. As they are parallel they could be interpreted as an effect of transtensive dike opening, and no flow could be calculated (Lefort et al., 2006). Kissel et al. (2010) interprets the flow in this dike dike as having

38 a marked vertical flow component. This does not mean that a flow might not be vertical in transtensive stress regimes, in fact, if regional stress governs the dike opening the flow should be more or less vertical.

Kissel et al. (2010) Eriksson Dike Strike κa κc Flow E W Flow Inclination IC06 0 149/89 81/0 Up 279/0 81/0 N-S 0◦ IC01c 350 75/83 283/6 Up 283/6 57/6 S-N +15◦ IC11 35 360/84 279/9 ; 95/12 Up - - Transtension - Table 3 – Susceptibility axis data and interpretation by Kissel et al. (2010) together with recalculation using the intersection line method and its interpretation. Bootstrapping is not applied and only the mean direction is used. Dike name according to Kissel et al. (2010). Strike in degrees. Major and minor axis directions as declination/inclination. Interpretation of ﬂow regime. Mirrored margins pairs for calculating the intersection line and its interpretation.

The discrepancy between flow interpretations using either the minor or major susceptibility axis is of course not restricted to Icelandic dikes but is likewise valid for all studies where the margins of dikes have been sampled in order to define flow. Recent work where the major axis has been used to infer flow include those of Varga et al. (2008); Craddock et al. (2008); Raposo and Berquó (2008); Geshi (2008); Curtis et al. (2008) and Kissel et al. (2010) amongst others. See also Elming and Mattsson (2001); Cañón-Tapia (2004); Cañón-Tapia and Herrero-Bervera (2009); Chadima et al. (2009) and Borradaile and Jackson (In press). In this thesis the use of the minor axis has been favored and argumented for, but it should be noted that the supremacy of any of the susceptibility axes as a proxy to flow is an open question and not yet settled. The AMS data from the dikes sampled in relation to this thesis contains a number fabric that could be interpreted as sub-vertical and sub-horizontal flow if the major susceptibility axis were to be used as a flow proxy. The data also contains a large number of inverse fabrics (in reference to the major susceptibility axis). If the major axis had been used the flow implications should have been less homogeneous and indicated both vertical and horizontal flow. Note that this differs from the results by Craddock et al. (2008) and Kissel et al. (2010) who concluded solely vertical flow regimes.

39 PERSPECTIVES OF FUTURE WORK

HE scientific field investigating anisotropy of magnetic susceptibility in rocks Tand its implications would benefit from more work aimed at giving a better understanding for AMS as a petrofabric indicator. It has been shown in this thesis, using the imbrication model with the minor axis, that the method result in predominantly horizontal flow regimes. Horizontal flow regimes were also indicated in dikes from a similar rift environment in Greenland (Callot et al., 2001; Callot and Geoffroy, 2004). The results by Geoffroy et al. (2002); Bascou et al. (2005) and Olivier et al. (2010) imply the use of the minor susceptibility axis is more probably the correct way to determine flow directions since these authors have compared the AMS fabric with petrographical fabric investigations. The implication of this, is that volcanic systems with shallow magma chamber account for both regional diking and regional dilatation in rift environments. This contradicts the interpretations by both Craddock et al. (2008) and Kissel et al. (2010), who suggested vertical magma movements from studies of Neogene dikes. Examples of sub-horizontal flows using the major axis as proxy do exists (e.g. Varga et al., 2008, cf. Philpotts and Philpotts, 2007). The congruence between the major axis and the silicate fabric is supported by thin section analysis and surface lineations (e.g. Varga et al., 1998; Aubourg et al., 2002; Poland et al., 2004 and Aubourg et al., 2008). The inverse relation between the silicate lineation and the major susceptibility axis is shown by Archanjo et al. (2002), indicating that even if the AMS and the oxide minerals coincide spatially the distribution of magnetic grains might well be perpendicular to bulk silicate fabric.

The situation is complicated by various types of uncompliant fabrics, such as the inverse fabrics where no possible ﬂow regime could have generated them, as well as the compound fabrics of Kissel et al. (2010) where both normal and inverse type fabrics exists in the same dike and where the inverse is reversed into a normal type fabric whence heated, implying that they are not independent of each other. It is further known that demagnetization of samples sometimes causes changes of the

40 magnetic fabric (Park et al., 1988). Aubourg et al. (2008) have showed substantial changes in the magnetic fabric subsequent to AF-demagnetization, resulting in an inverse fabric in relation to the dike margins, but also that this was in accordance with the silicate fabric. The underlying reason for features such as inverse fabrics and changes in AMS subsequent to demagnetization or heating is not clear. The suggestion by Potter and Stephenson (1988) of single-domain type fabrics have not proven successful in explaining the inverse fabrics (Cañón-Tapia, 2004). The standard use of anhysteric remanent magnetization techniques (ARM) has been suggested to remove the potential effect of true single domain grains (Chadima et al., 2009).

After almost 50 years of work in this scientific field, there is thus still no certainty in which way the axes of the susceptibility ellipsoid relate to the actual petrofabric. In fact, there seems to be no assurance that flow must accord to a simple laminar flow model, but the flow can change along the strike of a dike forming complicated flow patterns (Philpotts and Asher, 1994).

If any future work would be done on these dikes in relation to determining indisputable flow directions, and the challenges raised when applying the method is to be resolved some suggestions on how to accomplish that are here presented. (1) The relation between the AMS and the silicate petrofabric must be constrained. This is to be done to determine whether the magnetic fabric is reflected in the silicate fabric. In order to determine this thin sections in suitable cuts may be studied or polished cubes where the silicate and oxide fabric may be quantifiable with statistical methods. ARM could be applied to delineate any possible single-domain texture. Other ways to link the magnetic and mineral fabric would be to measure the samples using neutron diffraction, X-ray texture goniometry or seismic velocity (van der Pluijm et al., 1994; Hansen et al., 2004; Feinberg et al., 2006). If a very reliable relation between the AMS and the actual petrofabric of the dikes studied in the present work could be achieved, a consensus of which method to use when inferring flow in dikes might also be achieved. That work might answer question like if the margin samples and the minor axis is to be used or if it is sufficient to collect a few samples from the central

41 core. The central core might also generally be subject to compaction and of little use for flow determinations as shown in paper I. A second important issue is (2) how to handle potential changes in the AMS subsequent to demagnetization or heating. In order to constrain this samples from each dike should be demagnetized and heated, the changes studied and the relation to the actual petrofabric determined. This might result in that all samples in future studies must be treated by either heating or be demagnetized in order to constrain the ideal AMS for flow interpretations. The study might even show that it is not possible to determine in advance, by applying or not applying demagnetization techniques, when AMS reflects the actual petrofabric. Other techniques as mentioned above might then be necessary as standard use to support or replace the use of AMS. These two issues must be resolved before any successful geological interpretation can be made. With the present knowledge interpretations given from the AMS data cannot be maintained without additional evidences e.g. in the form of indisputable field relations. The AMS results cannot be generalized in terms of flow directions, the natural scientist have in principle three choices on which susceptibility axis that is to reflect silicate mineral fabric, omitting the challenges raised by fabric alteration, single-domain grains, tectonic stress etc. In addition to the questions raised above it would benefit the scientific inquiry to (3) determine to which distance from the margin into the dike the simple shear zones develop and is retained. It is likely that the distance can be correlated to magma viscosity, i.e. magma chemistry, which is also to be examined. As noted in the theory section some suggestions of a sampling distance of at most 10 cm is suggested, but no detailed work has been performed to constrain these estimates. Such work may also explain some of the anomalous fabrics acquired when the sampling distance is evaluated to a well constrained model.

The results presented in manuscript I can be seen as a successful study, the consistency of AMS is tested on three separate outcrops, and the flow implications supported by undeniable field evidence. The suggestion is that (4) analogue studies to test the consistency of AMS should be done on mafic dikes where field relations enables us to aprioriinfer flow directions. The consistency of AMS could be tested

42 on e.g. 50 location on a 100 m outcrop. (5) Studies could also be done on other units such as a cone sheet, where the flow would be opposite to dip, or a radial dike. The problem may be to find such a wide sampling site where the margins of the igneous units can be inferred. Suggestion (3) should be dealt with before attempting these studies. When reliable flow directions are possible to obtain the presently sampled dikes which carry flow fabrics could be matched with chemical signatures, preferentially trace element ratios. Dikes spurring from the same magma chamber, or at least the same magma batch should chemically resemble each other. The magnetic polarity of the dikes in question might also help delineating different generations.

43 SAMMANFATTNING AV AVHANDLINGEN PÅ SVENSKA

Sammanfattning

Denna avhandling behandlar magnetiska egenskaper hos regionala Isländska gångbergarter från de östra fjordarna i landet. Ett stort antal av dessa gångar går att ﬁnna i det glacialt eroderade landskapet från den Neogena perioden. Gångarna bildar långträckta stråk vilka i allmänhet stryker mot NNE. Dessa gångar anses vara en underjordisk fortsättning i den övre delen av jordskorpan, av de långsträckta förkastningssprickor vilka likt gångarna sammanstrålar mot centralvulkaner i nu aktiva vulkansystem. Gångarna och centralvulkanerna har bägge blivit avtäcka genom istida nednötning av berggrunden till en utsträckning av 1500 m, vilket lämnat de övre delarna av dessa magmatiska kroppar synliga i landskapet.

Två manuskript har skrivits om dessa Isländska gångar. Det första manuskriptet omfattar en detaljerad studie av en kompositgång, bestående av en kärna av finkornig kvartsporfyr omgiven av dolerit. Kärnan i denna gång har blivit provtagen på tre ställen vilka åtskiljs från varandra av 12 km i längd. Provernas magnetiska susceptibilitet och anisotropin av denna har sedan analyserats. Riktning av fossilerat magmaflöde i denna gång har sedan bestämts från tolkningar av minimumaxeln hos den magnetiska susceptsellipsoiden och dess geometriska förhållande till gångens respektive sidor. Flödesriktningen i alla de tre provtagningsställena visade på en horizontell flödeskomponent från norr till syd, vilket stöds av fältrelationer i form av mafiska enklaver vilka lineerats av magmaflöde till formen av en paraboloid. Statistiska metoder användes för att definera flödesriktningen i det geometriska rummet vilket gett oss både riktning och lutning av flödet.

Det huvudsakliga vetenskapliga bidraget från det första manuskriptet var att tydliggöra att magnetisk susceptibilitet kan användas för att ta fram flödesriktningar. Ny tillämpning av metodik för att bättre kvantifiera flöde introducerades också. Denna nygamla teknik har sedan använtes för att bestämma magmaflöden i ett betydligt större antal av mafiska gångar, vilka

44 sträcker sig ut mot nordöst från den nu slocknade Álftafjörður-vulkanen. De flödesriktningar vilka definierades i de mafiska gångarna var företrädesvis horizontella, riktade bort från centralvulkanen. Detta stöder tektoniska modeller vilka söker förklara uppkomsten av de mafiska gångarna genom att härleda dem till intrusioner från ytliga magmakammare. Tilläggsvis har resultaten i dessa studier jämnförts med andra internationella studier vilka söker bestämma riktningen på magmaflöde genom användning av maximumaxeln i susceptibilitetsellipsoiden.

45 ACKNOWLEDGEMENTS

First of all I wish to thank my thesis supervisor Sten-Åke Elming (LTU) and co-supervisors Morten S. Riishuus (HÍ) and Freysteinn Sigmundsson (HÍ). I also wish to thank the Nordic Volcanological Center for having funded most of my research and granted me access to their facilities and personnel. Furthermore I wish to present my gratitude to persons which have contributed to this thesis in various ways. Rósa Ólafsdóttir and Benedikt G. Ófeigsson (HÍ) is acknowledged for preparing maps for the author as well as Árni Vésteinsson at Landhelgisgæsla Íslands, Sjómælingasvið. Birgir V. Óskarsson, Þorsteinn Jónsson (HÍ) and Kate Smith (HÍ) is acknowledged for support during field work. Gylfi Sigurðsson (HÍ) for help in technical matters. Leó Kristjánsson (HÍ), Níels Óskarsson (HÍ) and Sigurður Steinþórsson (HÍ) for discussions on scientific matters. Tommy Lindgren is acknowledged for preparing computer software and help in technical matters. I also wish to thank Ingi Þorleifur Bjarnason (HÍ) and Anders Schomacker (NTNU) for enjoyable discussions. And at last Marie and Jakob Kløve Keiding (GFZ), Hanna Sisko Kaasalainen (HÍ), Gabrielle Stockmann (HÍ), Erik Sturkell (GU), Eva Lindblom (UU) for the company and social life they provided under the hard years of research.

Afﬁliations: LTU: Luleå University of Technology, HÍ: Nordic Volcanological Center at the University of Iceland, NTNU: Norwegian University of Science and Technology, GFZ: German Research Centre for Geosciences, Potsdam, GU: University of Gothenburg, Sweden. UU: University of Uppsala, Sweden.

46 THESIS BIBLIOGRAPHY Balsley, J.R., Buddington, A.F., 1960. Magnetic susceptibility anisotropy and fabric of some Adirondack granites and orthogneisses. American Ade-Hall, J.M., Palmer, H.C., Hubbard, T.P., 1971. The Journal of Science 258-A, 6–20. magnetic and opaque petrological response of basalts to regional hydrothermal alteration. Geophysical Journal Bascou, J., Camps, P., Dautria, J.M., 2005. Magnetic of the Royal Astronomical Society 24, 137–174. versus crystallographic fabrics in a basaltic lava flow. Journal of Volcanology and Geothermal Research 145, Akimoto, S., 1962. Magnetic properties of 119–135. FeO–Fe2O3–TiO2 system as a basis of rock magnetism. Journal of the Physical Society of Japan 17, Bennett, C.E.G., Graham, J.W., 1981. New 1598–1611. observations on natural pyrrhotites – Magnetic transition in hexagonal pyrrhotite. American Allard, B., Benn, K., 1989. Shape preferred-orientation Mineralogist 66, 1254–1257. analysis using digitized images on a microcomputer. Computers & Geosciences 15, 441–448. Bijwaard, H., Spakman, W., 1999. Tomographic evidence for a narrow whole mantle plume below Anthony, J.W., Bideaux, R.A., Blahd, K.W., Nichols, Iceland. Earth and Planetary Science Letters 166, M.C., 1997. Handbook of Mineralogy – Halides, 121–126. Hydroxides, Oxides. Mineral Data Publishing. Bjarnason, I.Þ., 2008. An Iceland hotspot saga. Jökull Arbaret, L., Diot, H., Bouchez, J.L., 1996. Shape 58, 3–16. fabrics of particles in low concentration suspensions: 2D analogue experiments and application to tiling in Bjarnason, I.T., Schmeling, H., 2009. The lithosphere magma. Journal of Structural Geology 18, 941–950. and asthenosphere of the Iceland hotspot from surface waves. Geophysical Journal International 178, Archanjo, C.J., Araújo, M.G.S., Launeau, P., 2002. 394–418. Fabric of the Rio Ceará-Mirim maficdikeswarm (northeastern Brazil) determined by anisotropy of Blake, D.H., Elwell, R.W.D., Gibson, I.L., Skelhorn, magnetic susceptibility and image analysis. Journal of R.R., Walker, G.P.L., 1965. Some relationships Geophysical Research, Solid Earth 107, 2046. resulting from the intimate association of acid and basic magmas. Quarterly Journal of the Geological Archanjo, C.J., Launeau, P., 2004. Magma flow Society of London 121, 31–49. inferred from preferred orientations of plagioclase of the Rio Ceara-Mirim dyke swarm (NE brazil) and its Blanchard, J.P., Boyer, P., Gagny, C., 1979. Un AMS significance. Geological Society of London, nouveau critere de sens de mise en place dans une Special Publications 238, 285–298. caisse filonienne: Le "pincement" des mineraux aux epontes: Orientation des minéraux dans un magma en Ariskin, A.A., 1998. Calculation of titanomagnetite écoulement. Tectonophysics 53, 1–25. stability on the liquidus of basalts and andesites with special reference to tholeiitic magma differentiation. Bodvarsson, G., Walker, G.P.L., 1964. Crustal drift in Geochemistry International, Translated from Iceland. Geophysical Journal of the Royal Geokhimiya 36, 18–27. Astronomical Society 8, 285–300.

Aubourg, C., Giordano, G., Mattei, M., Speranza, F., Borradaile, G.J., Gauthier, D., 2003. Interpreting 2002. Magma flow in sub-aqueous rhyolitic dikes anomalous magnetic fabrics in ophiolite dikes. Journal inferred from magnetic fabric analysis (ponza island, of Structural Geology 25, 171–182. w. italy). Physics and Chemistry of the Earth 27, 1263–1272. Borradaile, G.J., Jackson, M., 2004. Anisotropy of magnetic susceptibility (AMS): magnetic petrofabrics Aubourg, C., Tshoso, G., Le Gall, B., Bertrand, H., of deformed rocks. Geological Society, London, Tiercelin, J.J., Kampunzu, A.B., Dyment, J., Modisi, Special Publication 238, 299–360. M., 2008. Magma flow revealed by magnetic fabric in the Okavango giant dyke swarm, Karoo igneous Borradaile, G.J., Jackson, M., In press. Structural province, northern Botswana. Journal of Volcanology geology, petrofabrics and magnetic fabrics (AMS, and Geothermal Research 170, 247–261. AARM, AIRM). Journal of Structural Geology . Brandsdóttir, B., Einarsson, P., 1979. Seismic activity Carmichael, I.S.E., 1967. The mineralogy of Þingmúli, associated with the September 1977 deflation of the a tertiary volcano in eastern iceland. The American Krafla central volcano in northeastern Iceland. Journal Mineralogist 52, 1815–1841. of Volcanology and Geothermal Research 6, 197–212. Cañón-Tapia, E., 1996. Single-grain versus distribution Buck, R.W., Einarsson, P., Brandsdóttir, B., 2006. anisotropy: a simple three-dimensional model. Physics Tectonic stress and magma chamber size as controls on of the Earth and Planetary Interiors 94, 149–158. dike propagation: Constraints from the 1975-1984 krafla rifting episode. Journal of Geophysical Cañón-Tapia, E., 2001. Factors affecting the relative Research, Solid Earth 111, B12404. importance of shape and distribution anisotropy in rocks: Theory and experiments. Tectonophysics 340, Burchardt, S., Gudmundsson, A., 2009. Infrastructure 117–131. of the Geitafell volcano, Southeast Iceland, in: Thordarsson, T., Self, S., Larsen, G., Rowland, S.K., Cañón-Tapia, E., Herrero-Bervera, E., 2009. Sampling Hoskuldsson, A. (Eds.), Studies in Volcanology: The strategies and the anisotropy of magnetic susceptibility Legacy of George Walker. Geological Society of of dykes. Tectonophysics 466, 3–17. London, pp. 349–368. Chadima, M., Cajz, V., Týcová, P., 2009. On the Callot, J.P., Geoffroy, L., 2004. Magma flow in the East interpretation of normal and inverse magnetic fabric in Greenland dyke swarm inferred from study of dikes: Examples from the eger graben, NW bohemian anisotropy of magnetic susceptibility: Magmatic massif. Tectonophysics 466, 47–63. growth of a volcanic margin. Geophysical Journal International 159, 816–830. Chadima, M., Hrouda, F., 2006. Remasoft 3.0 a user-friendly paleomagnetic data browser and analyzer. Callot, J.P., Geoffroy, L., Aubourg, C., Pozzi, J.P., Travaux Géophysiques XXVII, 20–21. Mege, D., 2001. Magma flow directions of shallow dykes from the East Greenland volcanic margin Collins, W.J., 2003. Slab pull, mantle convection, and inferred from magnetic fabric studies. Tectonophysics Pangaean assembly and dispersal. Earth and Planetary 335, 313–329. Science Letters 205, 225–237.

Callot, J.P., Guichet, X., 2003. Rock texture and Conrad, C.P., Lithgow-Bertelloni, C., 2002. How magnetic lineation in dykes: a simple analytical model. mantle slabs drive plate tectonics. Science 298, Tectonophysics 366, 207–222. 207–209.

Cañón-Tapia, E., 1996. Single-grain versus distribution Constable, C., Tauxe, L., 1990. The bootstrap for anisotropy: a simple three-dimensional model. Physics magnetic susceptibility tensor. Journal of Geophysical of the Earth and Planetary Interiors 94, 149–158. Research 95, 8383–8395. Cañón-Tapia, E., 2004. Anisotropy of magnetic Correa-Gomes, L.C., Souza, C.R., Martins, C.J.F.N., susceptibility of lava flows and dykes: A historical Oliveira, E.P., 2001. Development of symmetrical and account. Geological Society of London, Special asymmetrical fabrics in sheet-like igneous bodies: The Publication 238, 205–225. role of magma flow and wall-rock displacements in Cañón-Tapia, E., Chavez-Alvarez, J., 2004. Theoretical theoretical and natural cases. Journal of Structural aspects of particle movement in flowing magma: Geology 23, 1415–1428. implications for the anisotropy of magnetic susceptibility of dykes. Geological Society of London, Coward, M.P., 1980. The analysis of flow profiles in a Special Publication 238, 227–249. basaltic dyke using strained vesicles. Journal of the Geological Society of London 137, 605–615. Cargill, H.K., Hawkes, L., Ledeboer, J.A., 1928. The major intrusions of south-eastern Iceland. Quarterly Craddock, J.P., Kennedy, B.C., Cook, A.L., Pawlisch, Journal of the Geological Society of London 84, M.S., Johnston, S.T., Jackson, M., 2008. Anisotropy of 505–535. magnetic susceptibility studies in Tertiary ridge-parallel dykes (Iceland), Tertiary margin-normal Carmichael, I.S.E., 1964. The petrology of Þingmúli, a Aishihik dykes (Yukon), and Proterozoic Tertiary volcano in eastern Iceland. Journal of Kenora-Kabetogama composite dykes (Minnesota and Petrology 5, 435–460. Ontario). Tectonophysics 448, 115–124. Curtis, M.L., Riley, T.R., Owens, W.H., Leat, P.T., columnar basalt. Earth and Planetary Science Letters Duncan, R.A., 2008. The form, distribution and 35, 116–122. anisotropy of magnetic susceptibility of Jurassic dykes in H.U. Sverdrupfjella, Dronning Maud Land, Elming, S.Å., Mattsson, H., 2001. Post Jotnian basic Antarctica. Implications for dyke swarm emplacement. intrusions in the Fennoscandian shield, and the break Journal of Structural Geology 30, 1429–1447. up of Baltica from Laurentia: a palaeomagnetic and AMS study. Precambrian Research 108, 215–236. Dekkers, M.J., 1989. Magnetic properties of natural pyrrhotite II high- and low-temperature behaviour of Feinberg, J.M., Wenk, H.R., Scott, G.R., Renne, P.R., jrs and TRM as function of grain size. Physics of the 2006. Preferred orientation and anisotropy of seismic Earth and Planetary Interiors 57, 266–283. and magnetic properties in gabbronorites from the Bushveld layered intrusion. Tectonophysics 420, Dragoni, M., Lanza, R., Tallarico, A., 1997. Magnetic 345–356. anisotropy produced by magma flow: Theoretical model and experimental data from Ferrar dolerite sills Ferré, E.C., 2002. Theoretical models of intermediate (Antarctica). Geophysical Journal International 128, and inverse AMS fabrics. Geophysical Research 230–240. Letters 29, 1127.

Du, Z., Vinnik, L., Foulger, G., 2006. Evidence from Foulger, G., Anderson, D.L., 2005. A cool model for P-to-S mantle converted waves for a flat "660-km" the Iceland hotspot. Journal of Volcanology and discontinuity beneath Iceland. Earth and Planetary Geothermal Research 141, 1–22. Science Letters 241, 271–280. Garcia, S., Arnaud, N.O., Angelier, J., Bergerat, F., Duncan, R.A., Helgason, J., 1998. Precise dating of the Homberg, C., 2003. Rift jump process in northern Holmatindur cooling event in eastern Iceland: Evidence iceland since 10 Ma from 40Ar/39Ar geochronology. for mid-Miocene bipolar glaciation. Journal of Earth and Planetary Science Letters 214, 529–544. Geophysical Research, Solid Earth 103, 12397–12404. Gay, N.C., 1968. Pure shear and simple shear Dunlop, D.J., Özdemir, Ö., 1997. Rock Magnetism. deformation of inhomogeneous viscous fluids. 1. Cambridge University Press. Theory. Tectonophysics 5, 211–234. Efron, B., Tibshirani, R., 1986. Bootstrap methods for Geirsdóttier, Ä., Eiríksson, J., 1994. Growth of an standard errors, confidence intervals, and other intermittent ice-sheet in Iceland during the late measures of statistical accuracy. Statistical Science 1, Pliocence and early Pleistocene. Quaternary Research 54–75. 42, 115–130. Einarsson, P., Brandsdottir, B., 1978. Seismological Geirsdóttir, Ä., 1990. Diamictites of late pliocene age evidence for Lateral magma intrusion during the July in western Iceland. Jökull 40, 3–25. 1978 deflation of the Krafla volcano in NE-Iceland. University of Iceland, Reykjavik. Geirsdóttir, Ä., Miller, G.H., Andrews, J.T., 2007. Eiríksson, J., 2008. Glaciation events in the Glaciation, erosion, and landscape evolution of iceland. Pliocene–Pleistocene volcanic succession of Iceland. Journal of Geodynamics 43, 170–186. Jökull 58, 315–329. Geirsson, H., Ärnadóttir, T., Völksen, C., Jiang, W., Ellwood, B.B., 1978. Flow and emplacement direction Sturkell, E., Villemin, T., Einarsson, P., Sigmundsson, determined for selected basaltic bodies using magnetic F., Stefánsson, R., 2006. Current plate movements susceptibility anisotropy measurements. Earth and across the Mid-Atlantic Ridge determined from 5 years Planetary Science Letters 41, 254–264. of continuous GPS measurements in Iceland. Journal of Geophysical Research 111, B09407. Ellwood, B.B., 1979. Anisotropy of magnetic susceptibility variations in Icelandic columnar basalts. Geoffroy, L., Aubourg, C., Callot, J.P., Barrat, J.A., Earth and Planetary Science Letters 42, 209–212. 2007. Mechanisms of crustal growth in large igneous provinces: The north Atlantic province as a case study. Ellwood, B.B., Fisk, M.R., 1977. Anisotropy of Geological Society of America, Special Paper 430, magnetic susceptibility variations in a single icelandic 747–774. Geoffroy, L., Callot, J.P., Aubourg, C., Moreira, M., Gudmundsson, A., 1995. Infrastructure and mechanics 2002. Magnetic and plagioclase linear fabric of volcanic systems in Iceland. Journal of Volcanology discrepancy in dykes: A new way to define the flow and Geothermal Research 64, 1–22. vector using magnetic foliation. Terra Nova 14, 183–190. Gudmundsson, A., 2006. How local stresses control magma-chamber ruptures, dyke injections, and Geshi, N., 2008. Vertical and lateral propagation of eruptions in composite volcanoes. Earth-Science radial dikes inferred from the flow-direction analysis of Reviews 79, 1–31. the radial dike swarm in Komochi Volcano, central Japan. Journal of Volcanology and Geothermal Gunn, B.M., Watkins, N.D., 1969. The petrochemical Research 173, 122–134. effect of the simultaneous cooling of adjoining basaltic and rhyolitic magmas. Geochimica et Cosmochimica Ghosh, S., Ramberg, H., 1976. Reorientation of Acta 33, 341–356. inclusions by combination of pure shear and simple shear. Tectonophysics 34, 1–70. Guppy, E.M., Hawkes, L., 1925. A composite dyke from Eastern Iceland. Quarterly Journal of the Gibson, I.L., 1966. The crustal structure of Eastern Geological Society of London 81, 325–341. Iceland. Geophysical Journal of the Royal Astronomical Society 12, 99–102. Guðmundsson, Á., 1985. Samsetti gangurinn á streitishvarfi við breiðdalsvík. Náttúrufræðingurinn 54, Gibson, I.L., Kinsman, D.J.J., Walker, G.P.L., 1966. 135–148. Geology of the Fáskrúðsfjörður area, Eastern Iceland. Societas Scientarium Islandica, Greinar IV, 1–52. Haggerty, S.E., 1991. Oxide textures, a mini atlas, in: Ribbe, P.H. (Ed.), Oxide minerals: Petrologic and Gibson, I.L., Walker, G.P.L., 1963. Some composite magnetic significance. Mineralogical Society of rhyolite/basalt lavas and related composite dykes in America, pp. 129–219. eastern Iceland. Proceedings of the Geologists’ Association 74, 301–318. Halvorsen, E., 1974. The magnetic fabric of some dolerite intrusions, northeast Spitsbergen; implications Graham, J.W., 1954. Magnetic susceptibility for their mode of emplacement. Earth and Planetary anisotropy, an unexploited petrofabric element. Science Letters 21, 127–133. Geological Society of America Bulletin 65, 1257–1258. Hamilton, T.D., Borradaile, G.J., Lagroix, F., 2004. Sub-fabric identification by standardization of AMS: an Grímsson, F., 2007. The Miocene floras of Iceland – example of inferred neotectonic structures from Origin and evolution of fossil floras from North-West Cyprus. Geological Society, London, Special and westward Iceland. Ph.D. thesis. University of Publication 238, 527–540. Iceland. Hamling, I.J., Ayele, A., Bennati, L., Calais, E., Grímsson, F., Denk, T., 2005. Fagus from the Miocene Ebinger, C.J., Keir, D., Lewi, E., Wright, T.J., Yirgu, of Iceland: systematics and biogeographical G., 2009. Geodetic observations of the ongoing considerations. Review of Palaeobotany and Dabbahu rifting episode: new dyke intrusions in 2006 Palynology 134, 27–54. and 2007. Geophysical Journal International 178, 989–1003. Grímsson, F., Denk, T., Símonarson, L.A., 2007. Middle Miocene floras of Iceland – the early Hansen, A., Chadima, M., Cifelli, F., Brokmeier, H.G., colonization of an island? Review of Palaeobotany and Siemes, H., 2004. Neutron pole figures compared with Palynology 144, 181–219. magnetic preferred orientations of different rock types. Physica B: Condensed Matter 350, 120–122. Gudmundsson, A., 1983. Form and dimensions of dykes in eastern Iceland. Tectonophysics 95, 295–307. Harðarson, B.S., Fitton, J.G., Hjartarson, Ä., 2008. Tertiary volcanism in Iceland. Jökull 58, 161–178. Gudmundsson, A., 1990. Emplacement of dikes, sills and crustal magma chambers at divergent plate Hardarson, B.S., Fitton, G.J., 1997. Mechanisms of boundaries. Tectonophysics 176, 257–275. crustal accretion in Iceland. Geology 25, 1043–1046. Hargraves, R.B., Johnson, D., Chan, C.Y., 1991. southwest Iceland. Journal of Geophysical Research Distribution anisotropy: The cause of AMS in igneous 114, B09306. rocks ? Geophysical Research Letters 18, 2193–2196. Khan, M.A., 1962. The anisotropy of magnetic Helgason, J., Zentilli, M., 1985. Field characteristics of susceptibility of some igneous and metamorphic rocks. laterally emplaced dikes: Anatomy of an exhumed Journal of Geophysical Research 67, 2873–2885. Miocene dike swarm in Reydarfjördur, Eastern Iceland. Tectonophysics 115, 247–274. Kissel, C., Laj, C., Sigurdsson, H., Guillou, H., 2010. Emplacement of magma in Eastern Iceland dikes: Henry, B., 1997. The magnetic zone axis: A new Insights from magnetic fabric and rock magnetic element of magnetic fabric for the interpretation of the analyses. Journal of Volcanology and Geothermal magnetic lineation. Tectonophysics 271, 325–331. Research 191, 79–92.

Hunt, C.P., Moskowitz, B.M., Banergee, S.K., 1995. Kitagawa, H., Kobayashi, K., Makishima, A., Magnetic properties of rocks and minerals, in: Rock Nakamura, E., 2008. Multiple pulses of the mantle Physics and Phase Relations – A Handbook of Physical plume: Evidence from Tertiary Icelandic lavas. Journal Constants. American Geophysical Union, pp. 189–204. of Petrology 49, 1365–1396.

Hurlbut, C.S., Klein, C., 1985. Manual of Mineralogy. Klausen, M., 2004. Geometry and mode of John Wiley and Sons. emplacement of the Thverartindur cone sheet swarm, SE Iceland. Journal of Volcanology and Geothermal Iezzi, G., Ventura, G., 2002. Crystal fabric evolution in Research 138, 185–204. lava flows: results from numerical simulations. Earth and Planetary Science Letters 200, 33–46. Klausen, M.B., 2006. Geometry and mode of emplacement of dike swarms around the Ildefonse, B., Launeau, P., Bouchez, J.L., Fernandez, Birnudalstindur igneous centre, SE Iceland. Journal of A., 1992. Effect of mechanical interactions on the Volcanology and Geothermal Research 151, 340–356. development of shape preferred orientations: a two-dimensional experimental approach. Journal of Komar, P.D., 1972. Mechanical interactions of Structural Geology 14, 73–83. phenocrysts and flow differentiation of igneous dikes Jakobsson, S.P., Gudmundsson, M.T., 2008. Subglacial and sills. Geological Society of America Bulletin 83, and intraglacial volcanic formations in iceland. Jökull 973–988. 58, 179–196. Le Maitre, R.W., 2004. Igneous rocks – A Jelínek, V., 1981. Characterization of the magnetic classification and glossary of terms. volume 2nd ed. fabric of rocks. Tectonophysics 79, T63–T67. Cambridge University Press.

Jezek, J., Melka, R., Schulmann, K., Venera, Z., 1994. Lefort, J.P., Aïfa, T., Hervé, F., 2006. Structural and The behaviour of rigid triaxial ellipsoidal particles in AMS study of a Miocene dyke swarm located above viscous ﬂows–modeling of fabric evolution in a the Patagonian subduction, in: Hanski, Mertanen, multiparticle system. Tectonophysics 229, 165–180. Rämö, Vuollo (Eds.), Dyke swarms: time markers of crustal evolution. Taylor & Francis, pp. 225–241. Jóhannesson, H., Sæmundsson, K., 1998. Geological map of Iceland, 1:500 000, bedrock geology. Icelandic Lindsley, D.H. (Ed.), 1991. Oxide Minerals: Petrologic Institute of Natural History, Reykjavík 2nd ed. and Magnetic Signiﬁcance. volume 25 of Reviews in Mineralogy. Just, J., Kontny, A., De, Wall, H., Hirt, A.M., Martin-Hernandez, F., 2004. Development of magnetic Lundin, E.R., Doré, A.G., 2005. Fixity of the Iceland fabrics during hydrothermal alteration in the “hotspot” on the Mid-Atlantic Ridge: Observational soultz-sous-forets granite from the EPS-1 borehole, evidence, mechanisms, and implications for Atlantic upper rhine graben. Geological Society, London, volcanic margins. Geological Society of America Special Publication 238, 509–526. Special Paper 388, 627–651.

Keiding, M., Lund, B., Ärnadœttir, T., 2009. Marques, F.O., Coelho, S., 2003. 2-D shape preferred Earthquakes, stress, and strain along an obliquely orientations of rigid particles in transtensional viscous divergent plate boundary: Reykjanes peninsula, flow. Journal of Structural Geology 25, 841–854. McDougall, I., Kristjansson, L., K., S., 1984. Philpotts, A.R., Asher, P.M., 1994. Magmatic Magnetostratigraphy and geochronology of Nortwest flow-direction indicators in a giant diabase feeder dike, Iceland. Journal of Geophysical Research 89, Connecticut. Geology 22, 363–366. 7029–7060. Philpotts, A.R., Philpotts, D.E., 2007. Upward and Moorbath, S., Sigurdsson, H., Goodwin, R., 1968. downward flow in a camptonite dike as recorded by K-Ar ages of the oldest exposed rocks in Iceland. Earth deformed vesicles and the anisotropy of magnetic and Planetary Science Letters 4, 197–205. susceptibility (AMS). Journal of Volcanology and Geothermal Research 161, 81–94.

Neuhoff, P.S., Fridriksson, T., Arnorsson, S., Bird, Pickler, C., Edelman, N., 2007. Determining the Curie D.K., 1999. Porosity evolution and mineral paragenesis and Néel Temperature of Minerals. during low-grade metamorphism of basaltic lavas at Teigarhorn, Eastern Iceland. American Journal of Plenier, G., Camps, P., Henry, B., Ildefonse, B., 2005. Science 299(6), 467–501. Determination of flow directions by combining AMS and thin-section analyses: implications for oligocene Nicolas, A., 1992. Kinematics in magmatic rocks with volcanism in the Kerguelen archipelago (southern special reference to gabbros. Journal of Petrology 33, Indian ocean). Geophysical Journal International 160, 891–915. 63–78. van der Pluijm, B.A., Ho, N.C., Peacor, D.R., 1994. Olivier, B., Michal, B., Hervé, D., 2010. Magma flow High-resolution X-ray texture goniometry. Journal of and feeder chamber location inferred from magnetic Structural Geology 16, 1029–1032. fabrics in jotunitic dykes (Rogaland anorthosite province, SW Norway). Tectonophysics 493, 42–57. Poland, M.P., Fink, J.H., Tauxe, L., 2004. Patterns of magma flow in segmented silicic dikes at Summer O’Reilly, W., Hoffmann, V., Chouker, A.C., Soffel, Coon volcano, Colorado: AMS and thin section H.C., Menyeh, A., 2000. Magnetic properties of analysis. Earth and Planetary Science Letters 219, synthetic analogues of pyrrhotite ore in the grain size 155–169. range 1–24 μm. Geophysical Journal International 142, 669–683. Potter, D.K., Stephenson, A., 1988. Single-domain particles in rocks and magnetic fabric analysis. Pálmason, G., 1986. Model of crustal formation in Geophysical Research Letters 15, 1097–1100. Iceland, and application to submarine mid-ocean Raposo, M.I.B., Berquó, T.S., 2008. Tectonic fabric ridges, in: Vogt, P.R., Tucholke, B.E. (Eds.), The revealed by AARM of the proterozoic maficdike geology of North America, Volume M. Geological swarm in the Salvador city (Bahia state): São Francisco Society of America, pp. 87–97. craton, NE Brazil. Physics of the Earth and Planetary Interiors 167, 179–194. Paquet, F., Dauteuil, O., Hallot, E., Moreau, F., 2007. Tectonics and magma dynamics coupling in a dyke Raposo, M.I.B., D’Agrella-Filho, M.S., Pinese, J.P.P., swarm of Iceland. Journal of Structural Geology 29, 2007. Magnetic fabrics and rock magnetism of 1477–1493. Archaean and Proterozoic dike swarms in the southern São Francisco Craton, Brazil. Tectonophysics 443, Park, J.K., Tanczyk, E.I., Desbarats, A., 1988. 53–71. Magnetic fabric and its significance in the 1400 ma mealy diabase dykes of labrador, canada. Journal of Roaldset, E., 1983. Tertiary (Miocene-Pliocene) Geophysical Research, Solid Earth 93, 13,689–13,704. interbasalt sediments, NW– and W–iceland. Jökull 33, 39–56.

Petcovic, H.L., Dufek, J.D., 2005. Modeling magma Rochette, P., Aubourg, C., Perrin, M., 1999. Is this flow and cooling in dikes: Implications for magnetic fabric normal? a review and case studies in emplacement of Columbia river flood basalts. Journal volcanic formations. Tectonophysics 307, 219–234. of Geophysical Research 110, ARTN B10201. Rochette, P., Jackson, M., Aubourg, C., 1992. Rock Petersen, N., 1976. Notes on the variation of magnetism and the interpretation of anisotropy of magnetization within basalt lava flows and dikes. Pure magnetic susceptibility. Reviews of Geophysics 30, and Applied Geophysics 114, 177–193. 209–226. Rochette, P., Jenatton, L., Dupuy, C., Boudier, F., Sigurdsson, H., Sparks, S.R.J., 1978. Lateral magma Reuber, I., 1991. Diabase dikes emplacement in the flow within rifted Icelandic crust. Nature 274, 126–130. oman ophiolite: A magnetic fabric study with reference to geochemistry, in: Peters, T., Nicolas, A., Coleman, Spence, W., 1987. Slab pull and the seismotectonics of R. (Eds.), Ophiolite Genesis and Evolution of the subducting lithosphere. Reviews of Geophysics 25, Oceanic Lithosphere. Ministry of Petroleum and 55–69. Minerals, Sultanate of Oman, pp. 55–82. Stacey, F.D., Joplin, G., Lindsay, J., 1960. Magnetic Roobol, M., J., 1974. The geology of the Vesturhorn anisotropy and fabric of some foliated rocks from S.E. intrusion, SE Iceland. Geological Magazine 111, Australia. Pure and Applied Geophysics 47, 30–40. 273–286.

Rucker, A.W., White, W.H., 1898. On the Steinthorsson, S., Helgason, Ö., Madsen, M.B., determination of the magnetic susceptibility of rocks. Bdener, K.C., Bentzon, M.D., Mørup, S., 1992. Proceedings of the Royal Society of London, Series A Maghemite in Icelandic basalts. Mineralogical 63, 460–466. Magazine 56, 185–199.

Saemundsson, K., 1979. Outline of the geology of Stephenson, A., 1994. Distribution anisotropy: two Iceland. Jökull 29, 7–28. simple models for magnetic lineation and foliation. Physics of the Earth and Planetary Interiors 82, 49–53. Saemundsson, K., 1986. Subaerial volcanism in the western North Atlantic, in: Vogt, P.R., Tucholke, B.E. Tarling, D.H., Hrouda, F., 1993. The Magnetic (Eds.), The Geology of North America, Volume M, The Anisotropy of Rocks. Chapman & Hall. Western North Atlantic Region. Geological Society of America, pp. 69–86. Tauxe, L., 1998. Paleomagnetic Principles and Sandwell, D.T., Smith, W.H.F., 2009. Global marine Practice. Kluwer Academic Publishers. gravity from retracked geosat and ERS-1 altimetry: Ridge segmentation versus spreading rate. Journal of Tentler, T., 2005. Propagation of brittle failure Geophysical Research 114, B01411. triggered by magma in Iceland. Tectonophysics 406, 17–38. Sen, K., Mamtani, M.A., 2006. Magnetic fabric, shape preferred orientation and regional strain in granitic Tentler, T., Temperley, S., 2007. Magmatic fissures and rocks. Journal of Structural Geology 28, 1870–1882. their systems in Iceland: A tectonomagmatic model. Tectonics 26, ARTN TC5019. Shelley, D., 1985. Determining paleo-flow directions from groundmass fabrics in the Lyttelton radial dykes, New Zealand. Journal of Volcanology and Geothermal Thorarinsson, S., Tegner, C., 2009. Magma chamber Research 25, 69–79. processes in central volcanic systems of Iceland: constraints from layered gabbro of the Austurhorn Sigmarsson, O., Maclennan, J., Carpentier, M., 2008. intrusive complex. Contributions to Mineralogy and Geochemistry of igneous rocks in iceland: a review. Petrology 158, 223–244. Jökull 58, 139–160. Thordarson, T., Höskuldsson, Ä., 2008. Postglacial Sigmundsson, F., 2006. Iceland Geodynamics – Crustal volcanism in Iceland. Jökull 58, 197–228. Deformation and Divergent Plate Tectonics. Springer Verlag. Ute, F., Norbert, R.N., 2008. Mineral magnetic Sigmundsson, F., Símonarson, L.A., Sigmundsson, O., properties of artificial samples systematically mixed Ingólfsson, Ó. (Eds.), 2008. Jökull Special Issue – The from haematite and magnetite. Geophysical Journal dynamic geology of Iceland. volume 58. International 175, 449–461. Jarðfræðafélag Íslands. Varga, R.J., Gee, J.S., Staudigel, H., Tauxe, L., 1998. Sigurdsson, H., 1987. Dyke injection in Iceland: A Dike surface lineations as magma flow indicators review, in: Halls, H.C., Fahrig, W.F. (Eds.), Mafic dyke within the sheeted dike complex of the Troodos swarms, Geological Association of Canada Special Ophiolite, Cyprus. Journal of Geophysical Research, Paper 34, pp. 55–64. Solid Earth 103, 5241–5256. Varga, R.J., Horst, A.J., Gee, J.S., Karson, J.A., 2008. Walker, G.P.L., 1974. The structure of Eastern Iceland, Direct evidence from anisotropy of magnetic in: Krístjansson, L. (Ed.), Geodynamics of Iceland and susceptibility for lateral melt migration at superfast the North Atlantic Area, NATO Advanced Study spreading centers. Geochemistry, Geophysics, Institutes Series, Volume C11. Reidel Publishing Geosystems (G3) 9, Q08008. Company, Holland, pp. 177–188.

Walker, G.P.L., 1958. Geology of the Reyðarfjörður area, Eastern Iceland. Quarterly Journal of the Walker, G.P.L., 1975. Intrusive sheet swarms and the Geological Society of London 114, 367–391. identity of crustal layer 3 in Iceland. Journal of the Geological Society of London 131, 143–161. Walker, G.P.L., 1960. Zeolite zones and dike distributions in relation to the structure of the basalts of Eastern Iceland. Journal of Geology 68, 515–528. Walker, G.P.L., 1992. "coherent intrusion complexes" in large basaltic volcanoes – a new structural model. Walker, G.P.L., 1963. The Breiðdalur central volcano, Journal of Volcanology and Geothermal Research 50, Eastern Iceland. Quarterly Journal of the Geological 41–54. Society of London 119, 29–63.

Walker, G.P.L., 1964. Geological investigations in Watkins, N.D., Haggerty, S.E., 1968. Oxidation and Eastern Iceland. Bulletin of Volcanology 27, 351–363. magnetic polarity in single Icelandic lavas and dikes. Geophysical Journal of the Royal Astronomical Society Walker, G.P.L., 1965. Some aspects of Quaternary 15, 305–315. volcanism. Transactions of Leicester Literary & Philosophical Society 59, 25–40. Wiebe, R.A., Ulrich, R., 1997. Origin of composite Walker, G.P.L., 1966. Acid volcanic rocks in Iceland. dikes in the Gouldsboro granite, coastal Maine. Lithos Bulletin of Volcanology 29, 375–402. 40, 157–178. Part I Appendix – Paper 1

Eriksson, P.I., Riishuus, M.S., Sigmundsson, F., Elming, S.Å. (in review) ’Magma ﬂow directions inferred from ﬁeld evidence and magnetic fabric studies of the Streitishvarf composite dike, East Iceland’ Journal of Volcanology and Geothermal Research.

1 Magma ﬂow directions inferred from ﬁeld evidence and 2 magnetic fabric studies of the Streitishvarf composite 3 dike in east Iceland

4 November 18, 2010

1. Per I. Eriksson a,b,∗ 2. Morten S. Riishuus a 5 3. Freysteinn Sigmundsson a 4. Sten-Åke Elming b

a 6 Afﬁliations: Nordic Volcanological Center, Institute of Earth Sciences, University of b 7 Iceland. Division of Applied Geophysics, Department of Chemical Engineering and 8 Geosciences, Luleå University of Technology. 9 ∗ 10 Corresponding author, e-mail: [email protected] telephone: (+46) ??? ???? ???. 11 Current address: Department of Applied chemistry and Geoscience, Luleå University of 12 Technology, 971 87 Luleå, Sweden.

13 Abstract

14 Anisotropy of magnetic susceptibility (AMS) and rock magnetic studies have been 15 undertaken on three outcrops separated by 12 km along strike (NNE–SSW) on the 16 Streitishvarf composite dike in east Iceland. Samples for this study have been 17 collected from the inner granophyric part of the dike, which show clear field evidence 18 of a lateral flow component from north to south at one of the sites. This flow 19 component is consistent with margin AMS results from all three sites. The −2 20 granophyre has a substantial bulk magnetic susceptibility (10 SI) mainly carried by 21 magnetically soft titanium-poor titanomagnetite (MDF ca. 15 mT). The ferrimagnetic 22 grains yield a characteristic remanent magnetization in all three sites which gives a ◦ ◦ 23 virtual geomagnetic pole at latitude 52.6 S and longitude 319.6 E. The degree of 24 anisotropy is low (PJ = 1.033) and the magnetic fabrics shifts from oblate to prolate 25 shapes depending on dike margin and outcrop. The magnetic fabric has been 26 interpreted according to the imbrication model, using the minor susceptibility axis as 27 shear plane indicator. The absolute directions given by the minor susceptibility are 28 then quantified using vector algebra. The magma flow is indicated as an upward ◦ 29 directed flow, flowing from north to south with an inclination between 30 − 64 , with ◦ 30 a 95% confidence ellipse of 3 − 9 . A model for the intrusion of the Streitishvarf dike 31 has been constructed where magma pocket with felsic magma is punctured by a mafic 32 dike, enabling the felsic magma to rise and extent to the south within the pathway 33 created. The results of this study confirm the applicability of AMS in studies of 34 magma flow directions in igneous dikes of felsic composition in Iceland. 35 36 Key words: AMS; magnetism; anisotropy; composite dike; Iceland; magma 37 propagation

38 1 Introduction

39 The understanding of magma propagation in igneous dikes is important for our

40 understanding of volcanism and crustal dilatation (e.g. Brooks and Nielsen, 1978; Buck

1 41 et al., 2006; Paquet et al., 2007). The dikes represent feeder channels for magma from its

42 source to alternate crustal levels. Magma movement can potentially be inferred by

43 anisotropy of magnetic susceptibility (AMS), where the susceptibility relates the induced

44 magnetization a rock acquires due to a weak external ﬁeld. Due to preferred spatial

45 distributions of minerals, grain shapes and crystallographic properties the susceptibility

46 will in most cases be directionally anisotropic, and is thus a proxy of the petrofabric

47 (Tarling and Hrouda, 1993). Igneous rocks may have fabrics related to magma ﬂow

48 (Nicolas, 1992) and studies on maﬁc dikes have been carried out in several geological

49 provinces in order to deﬁne magma movement directions (e.g. Herrero-Bervera et al.,

50 2001; Callot and Geoffroy, 2004; Raposo et al., 2007; Aubourg et al., 2008; Soriano et al.,

51 2008). Similar studies have been conducted on felsic dikes (e.g. Walderhaug, 1993;

52 Aubourg et al., 2002; Poland et al., 2004; Chadima et al., 2009). Few studies of anisotropy

53 of magnetic susceptibility (AMS) have been published on Icelandic dikes (Ellwood, 1978,

54 1979; Craddock et al., 2008; Kissel et al., 2010). Here we present AMS data from a single

55 composite dike in east Iceland sampled in three outcrops separated by ∼12 km along

56 strike. We use imbrication of magnetic foliation planes to infer ﬂow at each of these three

57 outcrops. The availability of recurrent sampling locations on the same dike with exposed

58 margins is very rare in Iceland, but, here we are able to test the reproducibility of AMS as

59 well as make estimations of absolute ﬂow directions along strike of the dike. The AMS

60 results and available ﬁeld evidence is used to constrain a geological model for the

61 emplacement of the felsic part of the dike.

2 62 2 General geology

63 The bedrock of east Iceland is of Neogene age and consists of a gently dipping pile of

64 ﬂood basalts (Fig. 1a Walker, 1958; Gibson et al., 1966; Saemundsson, 1979; Hardarson

65 and Fitton, 1997). The age of the oldest lavas visible above sea level is sparsely

66 constrained, but should not exceed 13.5 Ma for the easternmost promontory (Watkins and

67 Walker, 1977; Mussett et al., 1980; Kristjansson et al., 1995). The lava pile is interrupted

68 by now exhumed volcanic centers with accompanying regional dike swarms (e.g. Walker,

69 1963; Carmichael, 1964; Walker, 1966; Carmichael, 1967; Walker, 1974; Paquet et al.,

70 2007). These exhumed central volcanoes occur in the ﬁeld as ensembles of major felsic

71 intrusions, felsic extrusives, volcaniclastics and occasionally gabbroic bodies (Walker,

72 1966). The vast majority of the dikes are maﬁc, but felsic and composite dikes do occur,

73 especially in the vicinity of volcanic centers (Gibson and Walker, 1963). The composite

74 dikes are characterized by outer maﬁc margins and an inner felsic core; several are found

75 in between Reyðarfjörður and Breiðdalsvík (Fig. 1b; Gibson and Walker, 1963; Gibson

76 et al., 1966; Walker, 1966). Both the lavas and the exhumed volcanic centers have been

77 buried and tilted 5–10° westwards subsequent to emplacement due to the spreading

78 accommodated across the rift axis (Fig. 1b, Bodvarsson and Walker, 1964; Saemundsson,

79 1979; Pálmason, 1986). Subsequent glacial erosion and isostatic rebound have uncovered

80 and uplifted the remains. The crust has suffered ca. 1500 m of erosion from the

81 paleosurface (Walker, 1960; Gibson et al., 1966; Neuhoff et al., 1999).

3 82 2.1 General ﬁeld relations of the composite dike

83 Gibson et al. (1966) mapped six composite dikes, including the Streitishvarf dike, forming

84 a NNE–SSW trending swarm centered around Sandfell, a rhyolitic oligoclase porphyry

85 laccolith (Hawkes and Hawkes, 1933). The outcrops appear from the south shore of

86 Breiðdalsvík to the north shore of Reyðarfjörður (Fig. 1b). The Streitishvarf composite

87 dike can be traced from the south slopes of Hellufjall in the north to the south side of the

88 Streitishvarf cape. The geological features of this composite dike have been described by

89 Guppy and Hawkes (1925), Gunn and Watkins (1969) and Gudmundsson (1985). The dike

90 is mentioned in a broader context by Gibson et al. (1966), Walker (1966) and Watkins and

91 Haggerty (1968).

93 The Streitishvarf dike outcrops in several areas along the coastline, spanning 14.7 km from

94 the southernmost to the northernmost outcrop (Fig. 1b). We have sampled three localities,

95 where both margins of the dikes were exposed, Streitishvarf (I), Hökulvík (II) and

96 Hellufjall (III). The dike disappears into the sea south of Streitishvarf. In the north the dike

97 disappears in the mountain side of Hellufjall, where we have traced the dike as high up as

98 400–450 m a.s.l. on the mountainside. No outcrop of the dike was found along the

99 mountain ridge between Hellufjall (859 m) and Miðfell (769 m) or further north into the

100 valley southeast of Sandfell. At present, no ﬁeld evidence is known for a connection

101 between the dike and the Sandfell laccolith. The felsic part of the dike widens with altitude

102 from ca. 8 m at sea level to between 25–35 m at 700 m altitude (Guppy and Hawkes, 1925;

103 Gudmundsson, 1985) and also along strike at sea level, from 8–10 m in the south to ∼30 m

104 in the north (Fig. 1c). Recently, the Sandfell laccolith was dated at 11.7 ± 0.1Mausing

4 40 39 105 Ar/ Ar on ground mass (Martin et al. 2010 (in prep.)). The Streitishvarf outcrop of the

238 206 106 composite dike was dated to 10.7 ± 0.2Mausing U/ Pb on zircon crystals and to

40 39 107 10.1 ± 0.2Mausing Ar/ Ar on ground mass (using the Taylor Creek Rhyolite sanidine

108 (TCr-2) at 28.34 Ma as monitor age Renne et al., 1998).

109 2.2 Streitishvarf locality

110 The Streitishvarf locality (site I, Fig. 1b and 2) is characterized, much like the other two

111 localities, Hökulvík (II) and Hellufjall (III), by a inner felsic part surrounded by thick

112 maﬁc margins. The dike is about 26 m wide in total with the felsic core 10 m thick. The

113 maﬁc and felsic parts are separated by a thin zone (15–50 cm) of intermediate, hybrid rock

114 which is a mixing product between the felsic and maﬁc magma (Gunn and Watkins, 1969).

115 The hybrid rock reveals ﬂow banding (Fig. 3a). The hybrid character continues some

116 distance into the mafic margins evident by a few darker maficenclaves.Themaficrockis

117 characterized as an aphyric single-pyroxene tholeiite, where plagioclase and pyroxene

118 form an inter-granular to subophitic relationship (Gunn and Watkins, 1969). Our

119 petrographical studies on the felsic rock indicate that it is holocrystalline with a porphyritic

120 texture including ca. 5% phenocrysts of mostly sanidine, a few crystals of clouded

121 orthoclase and ferroaugite in reaction with amphibole. Other workers report quartz in

122 phenocryst assemblages in the ground-mass, 5–10% phenocrysts of mostly sanidine and

123 quartz with lesser amounts of cloudy orthoclase in a matrix of feldspars and quartz (Guppy

124 and Hawkes, 1925; Gunn and Watkins, 1969; Martin and Sigmarsson, 2010). The

125 preferred petrogenetic model for the origin of the felsic magma is according to Martin and

126 Sigmarsson (2010) partial melting and and fractional crystallization based on oxygen

5 127 isotope systematics and Th concentrations. The felsic rock will henceforth be referred to as

128 a quartz-porphyry, while the maﬁc rock will be referred to as a dolerite. Tiny opaque cubes

129 of titanomagnetite(s) (on average 7.5μm) occur in the ground mass and more seldom larger

130 cubes (on average 22.5μm) occur which crowd amphibole rims of clinopyroxene or appear

131 as inclusions in sanidine. The opaques cubes are homogeneous and lack exsolution

132 features.

133

134 Doleritic enclaves are found both in the quartz-porphyry and hybrid rocks. Field relations

135 from Streitishvarf reveal magma mixing, crenulated margins on the enclaves, back

136 veining/micro intrusions from the quartz-porphyry and ﬂow banding connecting to the

137 maﬁc enclaves (Fig. 4). The quartz-porphyry, including enclaves, has been cross cut by at

138 least one generation of micro faults. The enclaves are often platy or rod-like with slender

139 dimensions, often aligned by ﬂow movements (Figs. 3a-b and 4b), while others have more

140 globular shapes. The ﬂat surfaces of the enclaves seem to be foliated parallel to the dike

141 plane and show a strong preferred orientation (cf. Figs. 3a and 4b). Slightly offset from the

142 center of the dike, there is a zone showing parabolic ﬂow banding in a horizontal cut,

143 indicating a horizontal component of ﬂow from the north to the south (Fig. 3b). The

144 parabolic outline indicate that, at least in that zone, the ﬂow regime of the magma was

145 Newtonian (Coward, 1980). Given that the quartz-porphyry was emplaced as one unit the

146 stress regime at the margins should be characterized by simple shear. No obvious ﬁeld

147 relations, other than the parabolic zone, such as internally chilled margins or ﬂow banding

148 support a staged intrusion of the central quartz-porphyry in any outcrop. The dolerite

149 margins may be composed entities (Guppy and Hawkes, 1925).

6 150 2.3 The Hökulvík and Hellufjall localities

151 The composite dike at site II outcrops in a secluded gully at Færivellir in the mountain

152 ridge on the north side of Breiðdalsvík. Detailed bathymetric maps reveal a possible

153 continuation of the dike on the sea ﬂoor to about 1.1 km south of Hökulvík (pers. comm.

154 Á. Vésteinsson). The enclaves visible at site II, ca. 300 m a.s.l., often have a rust red

155 alteration halo and are markedly more angular than in Streitishvarf. The dolerite margins

156 diminish in thickness upwards and disappears at ca. 400–500 m altitude. Above this point

157 the quartz-porphyry core expands markedly in thickness upwards (Fig. 1c). On the slopes

158 of Hellufjall three outcrops of the dike can be found. One at sea level (sampled as site III),

159 and two further up at ca. 200 and 400 m altitude respectively. The upper outcrops are

160 somewhat obscured by scree and soil. In the lower one of them a fold indicate horizontal

161 shearing, and thus ﬂow. The fold appear in the eastern margin of the quartz-porphyry ca. 3

162 m west of the contact towards the dolerite (Fig. 4d). In the upper-most outcrop the felsic

163 core lacks dolerite margins, as in site II. A pitchstone marks the contact towards the

164 country rock.

165 3Theory

166 The magnetic susceptibility can mathematically be described by a symmetric tensor of the

167 second order. The susceptibility is nearly constant for inducing ﬁeld strengths up to 23.9

168 kA/m (Tarling and Hrouda, 1993). It thus linearly relates the induced magnetization M,to

169 the inducing magnetic ﬁeld H:

Mi = κi, jHj (1)

7 170 The susceptibility tensor can be visualized with a magnitude ellipsoid (Nye, 1985). The

171 ellipsoid is a three-dimensional representation of the tensor elements where the principal

172 axes in the ellipsoid (κa ≥ κb ≥ κc) are determined in relative magnitude and direction by

173 the susceptibility tensor. The direction of the principal axes of the magnitude ellipsoid

174 have been plotted in a lower hemisphere stereographic projection to ease interpretation.

175 We further characterise the ellipsoid with the scalar shape parameter T and the anisotropy

176 degree PJ by Jelínek (1981). For a discussion on alternative parameters see Cañón-Tapia

177 (1994). Parameter T describes the shape of the ellipsoid and is given by:

2η − η − η T = b a c − 1(2) ηa − ηc

178 where ηi = ln(κi), i = a,b,c. Values of T where −1 ≤ T < 0 correspond to prolate

179 ellipsoids, T ≈ 0 corresponds to sphericals and 0 > T ≤ 1reﬂects oblate ellipsoids. The

180 corrected anisotropy degree PJ describes the degree of anisotropy the shape ellipsoid

181 inhibits and is given by:

2 2 2 Pj = exp 2((ηa − ηm) +(ηb − ηm) +(ηc − ηm) ) (3)

√ 3 182 where ηm = η1 · η2 · η3. PJ ranges from 1 and upwards but generally does not exceed

183 1.10 (10%) for pristine igneous rocks (Tarling and Hrouda, 1993). The bulk susceptibility

184 parameter Km is expressed as an arithmetic average:

κ + κ + κ K = a b c (4) m 3

185 3.1 Magma ﬂow in dikes

186 The seminal contributions of anisotropy of magnetic susceptibility studies on dikes were

187 made by Khan (1962), Symons (1975) and Ellwood (1978). After the introduction of the

8 188 imbrication model by Knight and Walker (1988) anisotropy of magnetic susceptibility has

189 been widely used to infer magma ﬂow (e.g. Aubourg et al., 2008; Chadima et al., 2009).

190 Geoffroy et al. (2002, 2007) suggested that the use of the major axis should be replaced

191 with the minor, after having observed a discrepancy between the silicate mineral lineation

192 and the major axis. The suggestion to use the minor axis as a shear plane indicator was

193 originally made by Halvorsen (1974). The model is based on the idea that magma ﬂow in a

194 dike will experience shear at the margins (Blanchard et al., 1979; Merle, 2000; Kratinová

195 et al., 2006). The model is analogous to laminar ﬂow trough a pipe (e.g. Fig. 2 by Merle,

196 2000). The minor susceptibility axis is expected to reﬂect the pole of these

197 shear/ﬂow-planes developed during magma movement. Since magma ﬂow is most likely

198 laminar in dike conduits (Delaney and Pollard, 1982), and the solidiﬁcation time at the

199 outer edges of a dike is relatively short, the imposed shear would be preserved at the

200 margins given that the magma is viscous enough to record the imposed shear at the time of

201 intrusion.

202 3.2 Flow determination

203 The absolute ﬂow direction is determined by comparing and averaging the orientation of

204 the magnetic foliation plane from each margin (Geoffroy et al., 2002, 2007). Thus local

205 geometric deviations in the dike walls and anomalous, i.e. inverse fabrics, which are

206 characterised by a parallel relation between the dike attitude and the minor susceptibility

207 axis, at one of the two margins may be accounted for. In the case of the quartz-porphyry

208 core of the Streitishvarf dike, ﬁeld relations and the symmetry of the magnetic foliation

209 planes in all three outcrops enable us to determine the ﬂow using both margins from each

9 210 outcrop calculating the line in which the two foliation planes bisect (Fig. 5). The magma

211 ﬂow is then perpendicular to this line. One advantage using this technique is that no

212 absolute comparison of the dike margin strike is needed. Since the strike is measured with

213 a magnetic compass its accuracy may vary. The ﬁeld relations that merits such treatment is

214 the congenial intrusion of the maﬁc and felsic magma. The contact between the

215 quartz-porphyry and the dolerite is thus planar and smooth. Variations in strike, as in site

216 III, between the margins do not need to be problematic for the interpretation if one

217 considers magma movement at the margins to have been simultaneous, i.e. part of the

218 same velocity proﬁle. In order to calculate the intersection line and quantify its accuracy

219 we utilize the procedure developed by Henry (1997a,b), here modiﬁed to calculate not the

220 ’zone axis’, but the vector product between the samples on the west and east margin

221 respectively, i.e. the vector (Vf = κc,E × κc,W ) that draws out the intersection line in ﬁgure

222 5. Conﬁdence limits and the mean direction is produced by bootstrapping (Constable and

223 Tauxe, 1990; Tauxe, 1998).

224

225 For comparison we also calculate the the ﬂow direction obtained by using the original

226 imbrication model, i.e. inferring ﬂow by using the major susceptibility axis (Knight and

227 Walker, 1988; Soriano et al., 2008; Varga et al., 2008). The ﬂow direction in the original

228 model may be inferred from the resultant vector, calculated as κR = κa,E + κa,W ,giventhe

229 same prerequisites as when calculating the intersection line.

10 230 4 Sampling & Methodology

231 A total number of 65 samples have been collected, from site I (41 samples), site II (10

232 samples) and site III (14 samples, Fig. 1 and Table 1). Between 5–9 samples were

233 collected from each margin, as well as along a section across the width of the quartz

234 porphyry at site I. Six samples were collected from the margin of the east dolerite

235 juxtaposed to the eastern margin of the quartz-porphyry at site I. The margin samples were

236 used for ﬂow determination, while the interior samples were used for assessing interior

237 fabric. The samples were collected using a portable core drill and oriented using sun and

238 magnetic compasses. Measurements of AMS were made using the KLY-3S Kappabridge

−8 239 instrument (AGICO), which detects variation down to 2 × 10 SI.

240 Temperature-susceptibility dependency was measured with the CS3 furnace apparatus

241 (AGICO) using powder samples heated/cooled in air. In addition to the AMS natural and

242 characteristic remanence directions were determined using a cryogenic magnetometer (2G

243 DC SQUID). The samples were demagnetized using alternating ﬁeld (AF)

244 demagnetization in steps of 5 mT for the range 0–25 mT and thereafter in steps of 10 mT

245 until the magnetization intensity had decreased by more than 90%. This was generally

246 reached in demagnetization ﬁelds of 70 mT. The measurements were performed at the

247 Geophysics Laboratory at Luleå University of Technology. In addition hysteresis curves

248 were obtained from 5 samples, three of which were from the margin of the felsic dike, and

249 one from the maﬁc (site I) and another from the central part of of the felsic dike in site III.

250 These measurements were done in order to estimate the magnetic granulometry (Day et al.,

251 1977; Dunlop, 2002). The measurements were performed at the Department of Earth and

252 Ecosystem Sciences, Lund University, Sweden.

11 253 5 Experimental results

254 In addition to the AMS measurements the natural magnetic remanence (NRM) directions

255 including characteristic remanence (ChRM), median destructive ﬁelds (MDF, Dunlop and

256 Özdemir, 1997), Königsberger ratio for natural magnetization (Qn, Königsberger, 1938),

257 bulk susceptibilities (Km), hysteresis curves on grains and Curie temperatures (Tc) from

258 susceptibility/temperature evaluations have been determined. On average 70% of the

259 samples subjected to AF-treatment yield stable remanence directions and ca. 90% of the

260 samples have been used for calculating AMS characteristics.

261 5.1 Natural magnetic remanence

262 Stable characteristic magnetic remanence vectors were obtained from all three sampled

263 sites (I,II,III). The natural remanent magnetization (NRM) has two components of

264 magnetization, one erased during demagnetization in low ﬁeld strengths (<20 mT), and a

265 second with high coercivity (Fig. 6). The direction of the low coercivity magnetization

◦ ◦ 266 (Decl. ∼350 ,Incl.∼80 ) is very close to that of the present Earth ﬁeld (PEF from IGRF,

◦ ◦ ◦ ◦ 267 Decl. = 348.2 and Incl. = 75.6 ,at64.8 N and 13.9 W) and it is therefore interpreted to

268 be of viscous origin. The high coercivity component has a direction which is not

269 signiﬁcantly different between the three sites and forms a rather well deﬁned mean at

◦ ◦ ◦ 270 Decl. = 209 , Incl. = −46 (α95 = 10.7 ; Table 2). Subsequent to emplacement it is

271 assumed that the dike was tilted with the lava pile according to the Pálmason model (cf.

272 lava tilt in Fig. 2; Pálmason, 1986). Tectonic corrections therefore need to be made on the

273 characteristic remanence. Two corrections are plausible, either a correction based on

274 present average lava dip at the site or to assume vertical dike intrusion and correct to a

12 275 paleovertical position of the dike. No exact determinations of lava tilt has been made by

276 us, whereas Walker (1974) examined the lava tilt of east Iceland in detail. Correction of the

277 characteristic remanence to a paleo-horizontal of the lava using lava dip measurements by

◦ ◦ ◦ 278 Walker (1974) yield a mean direction of Decl. = 198 and Incl. = −48 , with α95 = 11.3

279 (Fig. 6c and Table 2). Thus with a minor decrease of the precision of the mean. A

◦ ◦ 280 paleovertical correction yields a remanence direction of Decl. = 199 and Incl. = −49 ,

◦ 281 with α95 = 14.4 (Table 2). The virtual geomagnetic pole (VGP) calculated for the

282 paleo-horizontally tilt corrected high coercivity remanence, plots in the southern

◦ ◦ 283 hemisphere (Plat. = 53 S, Plong. = 140 E; Table 2). Since the precision of the mean dike

284 tilt corrected is lower decrease by 3.1° this scenario is disregarded.

285 5.2 Rock magnetic properties

286 The magnetic properties of the different rock types of the dike, quartz-porphyry, hybrid

287 rock and dolerite differ slightly (Table 2). The unstable remanence in the quartz-porphyry

288 of Streitishvarf was explained by Gunn and Watkins (1969) as being caused by large

289 magnetic grain sizes. Our petrographic investigation shows the presence of small- to

290 medium-sized cubic magnetites (see section on Streitishvarf outcrop). The small grains

291 are in the pseudo-single-domain range while the larger are slightly within and over the

292 pseudo-single-domain range, but, well below multi-domain grain sizes determined from

293 (Tarling and Hrouda, 1993). In site I there is no fundamental difference in MDF (∼14 mT)

294 between the dolerite and the quartz-porphyry (Table 2), which could indicate similar grain

295 sizes of magnetite. However the Königsberger ratio is low for the quartz-porphyry in this

296 site (Qn = 0.22) in contrast to the dolerite (Qn = 1.60), which indicates predominantly

13 297 larger grain sizes in the felsic part and thus unstable remanences. For the other outcrops

298 (sites II and III) the Königsberger ratio is low for the quartz-porphyry, while slightly higher

299 in the hybrid rocks, on average 0.25 and 0.70 respectively, indicating the presence of

300 single-domain grains in the latter hybrid rock (Stacey, 1974). The hysteresis results

301 obtained from grains indicate a magnetic granulometry obtained in the

302 pseudo-single-domain range ﬁeld, with the exception of the dolerite sample which fall in

303 the single-domain ﬁeld (Fig. 7; Day et al., 1977; Dunlop, 2002). The felsic samples fall

304 around the theoretical curve for multi-domain behaviour. The granulometry, as indicated

305 by the Day plot, is therefore likely to constitute a mixture between single- and

306 multi-domain grains. The single-domain afﬁnity of the doleritic sample is supported by the

307 high Königsberger ratio.

308

309 The MDFs for all collected samples vary around 10 ± 2.5 mT. Based on distribution

310 density and not average values (cf. Table 2), which indicate (based on MDF only)

311 primarily pseudo-single to multi-domain remanence carriers (Dunlop and Özdemir, 1997).

312 The quartz-porphyry from site III (Hellufjall) yields far higher MDFs (ca. 45 mT) and

313 accompanying sigmoidal demagnetization curves, a hallmark for single-domain behaviour

−3 314 (Fig. 6, Table 2). The bulk susceptibility ranges between 6.0–21.5×10 SI, suggesting

315 that magnetite determines the magnetic properties (Tarling and Hrouda, 1993). Since no

316 alteration is observed in site I and II and the alteration in site III is accompanied by a 50%

317 drop in bulk susceptibility (Table 2) the magnetite that account for the rock magnetic

318 properties is suggested to be pristine and of magmatic origin. The Curie temperatures

319 average between 540–570°C (obtained from heating curves, Fig. 8) indicating

14 320 titanomagnetite of low Titanium content, consistent with the high bulk susceptibility and

321 the petrographic investigations. In total, 10 samples distributed over all three outcrops

322 were investigated for their thermal properties. They revealed similar

323 susceptibility/temperature dependency with cooling curves showing reduced

324 susceptibilities (Fig. 8), which indicates mineral alteration during the heating procedure.

325 5.3 Anisotropy of magnetic susceptibility

326 5.3.1 Evaluation of AMS results from dike margins

327 For each sampled outcrop of the dike, a susceptibility ellipsoid has been determined

328 statistically from measurements on samples from the margins. At site I samples from the

329 interior transect and samples collected in the dolerite juxtaposed to the quartz-porphyry

330 have also been evaluated. As introduced in the theory, section 3.2, the absolute ﬂow

331 direction has been determined by use of the intersection line (Vf ) and the resultant vector

332 (κR). The intersection line is treated ﬁrst, where after the results from the two methods is

333 compared. The orientation of the minor susceptibility axis and the ellipse of 95%

334 conﬁdence around the mean is given in Table 3 and ﬁgure 9 (geographical coordinates).

335 The conﬁdence limits for the minor axis are small, with an average angular length of 11.1°

336 and 5.8° for the long and short axis respectively. The corrected anisotropy degree is low,

337 averaging ca. 3%, which is to be expected from pristine igneous rocks (Tarling and

338 Hrouda, 1993). The shape of the susceptibility ellipsoid for the margins varies between

339 oblate to prolate shapes, with a tendency towards more prolate shapes. The susceptibility

340 ellipsoids from all three localities in this study show a tri-axial behavior, in the sense that

341 the major, intermediate and minor axes form relatively distinct groups and do generally not

15 342 intermingle (Fig. 9). In site I and II the minor axes are tightly grouped while in site III they

343 are more scattered. The calculated intersection lines thus form distinct groups for site I and

344 II while they scatter in site III (Table 4). The intersection line predicts that the ﬂow regime

345 were directed from north to south in all three outcrops, and inclined upwards from the

◦ ◦ ◦ 346 horizon with 43 for site I, 64 for site II and 30 for site III (Table 4). For the dolerite

347 samples no meaningful intersection line can be obtained due to the prolate nature of their

348 magnetic fabric.

349

350 The resultant vector gives for the quartz-porphyry a ﬂow regime from north-to-south,

◦ 351 inclined upward from the horizon by 32 for site I and downward sub-vertical ﬂow regimes

352 in site I and II. A resultant vector has also been calculated for the dolerite from an

353 synthetic margin pair obtained trough mirroring the fabric against the dike attitude, which

◦ 354 indicate a downward ﬂow of 59 from north-to-south. The uncertainty limits on both the

355 intersection line and the resultant vector are smaller than the angular difference between

356 the calculated site mean directions, making them in statistical terms signiﬁcantly different.

357 5.3.2 Evaluation of AMS results from dike transect

358 The samples collected along a section across the quartz-porphyry in site I were separated

359 by a distance of ∼1 m between the cores. The analyses are made from the position of the

360 minor axis, which is taken as a pole to the magnetic foliation plane, indicating plane of

361 shear or compression. The bulk susceptibility for the section (Fig. 10c) is similar to that of

362 the marginal samples, while there is a trend of increasing susceptibility from the margins

363 towards the center of the dike, indicating larger grain sizes in the inner parts. From both

16 364 the west and east margin the susceptibility slightly decreases, towards the parabolic zone

365 (Figs. 10c-d), but increases again in the middle of the parabolic zone. The corrected

366 anisotropy degree shows an inverse relation to the susceptibility with higher anisotropy

367 degree at the margins and towards the parabolic zone and lower within the inner parts.

368

369 The mean minor axis of the susceptibility ellipsoid from the marginal samples of site I

370 (Streitishvarf) yield a steep foliation plane sub-parallel to dike strike (Fig 10aα,and

371 corresponding stereograph, Fig. 10bα). The interior samples can be divided into two

372 groups, side series (β) and central series (γ). The side series span ca. 3 m into the

373 quartz-porphyry and reveal a shallower plane, sub-parallel to dike strike (Fig 10aβ and bβ).

374 The central series (γ) sampled at the very center yield a horizontal foliation plane (Fig.

375 10aγ and bγ). No interior variations in the parabolic zone are detected. Compared to the

376 95% conﬁdence cone of the marginal samples, the interior samples show many times

377 larger conﬁdence estimates (Fig. 10b). The mean dike tilt corrected direction of the minor

◦ ◦ ◦ ◦ 378 susceptibility axis is for the side series D = 111 , I = 39 and D = 289 , I = 28 for the

379 west and east side, respectively (Fig. 10a). If an intersection line is estimated from these

◦ ◦ 380 directions it yields a line with an inclination signiﬁcantly different (D = 200 , I = 2 ) from

◦ ◦ 381 the intersection line deﬁned from the marginal samples (D = 188 , I = 47 in tilt corrected

382 coordinates).

383 6 Discussion

384 The discussion of results will focus on interpretations of the fossilized magma ﬂow regime

385 obtained from anisotropy of magnetic susceptibility. The discussion will ﬁrst treat the rock

17 386 magnetic properties, then the natural remanent magnetization (NRM) and ﬁnally the AMS.

387 6.1 Rock magnetic properties

388 The rock magnetic properties of all three sites (I, II and III, Fig. 1b) are interpreted from

389 Curie temperatures, bulk susceptibility, hysteresis data and MDFs to be carried by Ti-poor

390 titanomagnetite. At site I the occurrence of magnetite(s) is supported by petrographic

391 investigations by both Gunn and Watkins (1969) and us, and from site II by Guppy and

392 Hawkes (1925). Note that petrographic investigations alone are unable to discriminate

393 between different compositions of titanomagnetite. Curie temperature determinations

394 agree with Ti-poor titanomagnetite for all sites, except for one out of three samples from

◦ 395 site III (Fig. 8b), where maghemite (Tc = 610 C) in the quartz porphyry was revealed as

396 the dominating magnetic mineral and Ti-poor titanomagnetite of secondary importance.

397 The surface of this outcrop is weathered and the bulk susceptibility is ca. 50% lower than

398 in the other sites (Table 2). The demagnetization behavior revealed sigmoidal AF-curves in

399 this outcrop (Fig. 6e) and very high MDFs (∼45 mT; Table 2, site III). Thus indicating a

400 remanence carried by high coercivity minuscule grains which probably had their origin in

401 low temperature oxidation of magnetite to maghemite. The mean bulk susceptibility from

402 site III is still so high that magnetite is required to explain a substantial part of the observed

403 magnetic properties (Tarling and Hrouda, 1993). A late stage magmatic Ti-poor

404 titanomagnetite is therefore suggested as the primary magnetic mineral in all three

405 outcrops.

406

407 Regarding the sizes of the magnetite(s) in the dike the evidences are ambiguous and no

18 408 decisive answer can be offered. Our petrographic investigations from site I showed cubic

409 magnetite in the pseudo-single domain range. The magnetic granulometry as indicated by

410 the Day plot showed grain sizes which fell along the theoretical multi-domain magnetite

411 line in the pseudo-single-domain ﬁeld for the felsic samples. Since the magnetization has

412 proved unstable in the quartz-porphyry of site I, already explained by Gunn and Watkins

413 (1969) as a consequence of large magnetite grains (but never proved), the grain distribution

414 may be a mixture of single- and multi-domain grains with predominantly multi-domain

415 grains present. Additionally, both the low Königsberger ratio and the low MDF (Table 2)

416 in the quartz-porphyry of site I allow for multi- to pseudo-single domain range grains,

417 albeit no large magnetite grains have been observed in site I. It may also be noted that the

418 magnetization of site II is stable whereas it shares the low MDF and Königsberger ratio

419 with site I.

420 6.2 Natural remanent magnetization (NRM)

421 Albeit the domain state distributions of the magnetic grains remains unclear all three sites

422 reveal a similar characteristic reversed magnetic remanence (ChRM) from which a mid

423 latitude VGP located in the southern hemisphere was calculated. The lava tilt corrected

424 ChRM was chosen as it is a more probable scenario, and for its lower scatter in respect to

425 assuming a strictly vertical dike tilt. The southern hemisphere pole is most certainly of

426 transitional nature and does not reﬂect continental drift. This kind of VGPs have been

427 obtained in a large number of Icelandic rocks (Watkins and Walker, 1977; Kristjánsson,

428 1999, 2009)), especially in dikes (Piper et al., 1977).

429

19 430 The recently obtained ages on the Streitishvarf composite dike (10.1 ± 0.2Ma,Ar/Arand

431 10.7 ± 0.2 Ma, U/Pb, Martin, et al. (in prep.)) enables us to attempt to correlate the

432 remanence with the present geomagnetic polarity time scale (Ogg and Smith, 2004). The

433 dike falls under the prominent C5N2n polarity interval, which stretches between 9.99 and

434 11.04 Ma. From magneto-stratigraphic studies on ﬂood basalts in Iceland it is evident that

435 this period is intercepted by at least two short reversals, found in both east (Blakely, 1974;

436 Watkins and Walker, 1977), north (Saemundsson et al., 1980) and the north-west

437 (McDougall et al., 1984). If the ages of these reversals from McDougall et al. (1984) are

438 recalculated with the present geomagnetic time scale, (Ogg and Smith, 2004), two of the

439 reversals in C5N2n fall at the time between 10.11–10.12 and 10.73–10.76 Ma. Thus it

440 seems that the ages obtained from the dike both fall within or close to these short lived

441 reversals or excursions, and the dike could have been emplaced during one of them. It is

442 difﬁcult to envisage that a shallow crustal dike intrusion cooled from ca. 900°C through

443 300–400°C in as long as 600 ky ± 200 y (from 10.7 to 10.1 Ma). We postulate that the

444 zircon is inherited from an earlier crystallization stage. The time of emplacement of the

40 39 445 dike should therefore be closer to the Ar/ Ar age (10.1 Ma).

446 6.3 Anisotropy of magnetic susceptibility

447 6.3.1 Choice of ﬂow proxy ( Vf or κR)

448 The magnetic fabrics determined on the samples from the margins at all three sites are

449 consistent with the imbrication model, both using the intersection line and the resultant

450 vector to infer flow, but the flow implications given are not unanimous. The available field

451 evidence in form of the parabolic zone at site I, the vertical widening at site II, the fold at

20 452 site III and the overall widening of the dike from south-to-north are all in accordance with

453 the interpretation offered by the intersection line, an upward ﬂow from north-to-south. If

454 one instead interprets ﬂow using the resultant vector, the AMS data from site I would

455 indicate a shallow ﬂow from north-to-south, in accordance with the ﬂow pattern in the

456 parabolic zone. For site II and III the ﬂow would be interpreted as downward sub-vertical

457 which is not supported by the fold at site III (Fig. 4d). In addition the vertical widening of

458 the dike observed at Hökulvík (site II) indicate, albeit not unambiguously, vertical

459 propagation. It was expressed in Guppy and Hawkes (1925) that there was some evidence

460 that the direction of ﬂow of the dike magmas had a horizontal component, and it was

461 suggested that the movement was from north to south.

462

463 Regarding the parabolic zone at site I, one could argue that the ﬁeld evidence offered by

464 the aligned enclaves in fact could constitute a later pulse of magma, i.e. by another dike

465 enclosed in the main quartz-porphyry. Endogenous growth, interpreted from AMS or

466 susceptibility, but unfortunately not backed up by absolute ﬁeld evidence, has been

467 reported elsewhere (Aïfa and Lefort, 2000; de Wall et al., 2004; Cañón-Tapia, 2004).

468 There are no visible contacts between the parabolic zone and the rest of the rock indicating

469 internal dike margins, but the lowered susceptibility encountered when approaching the

470 parabolic zone, similar to the lowered susceptibility at the edges towards the dolerite

471 margins (Fig. 10c), may be interpreted as interior margins. It can be noted that the

472 anisotropy degree also rises at these positions, as it does towards the margins to the

473 dolerite. If it would be the case that the ﬁeld relations, both in site I and III supporting

474 lateral ﬂow were individual “inner dikes” their strong support to the interpretation offered

21 475 by the intersection line deﬁned from the margins samples would lessen somewhat. Only,

476 and only if these potential inner dikes had perpendicular or adverse growth/ﬂow directions

477 in relation to the main quartz-porphyry, which seems somewhat implausible from a

478 mechanical view, would these ﬁeld evidences be misleading. Rather, the directional ﬂow

479 banding could indicate several pulses all directed from north to south.

480

481 The discrepancy between ﬂow directions given by the resultant vector in the three

482 outcrops, together with the discrepancy between these ﬂow indications and ﬁeld evidence,

483 together with the warnings by Geoffroy et al. (2002) on using the major axis, enables us to

484 favor the interpretation were the intersection line is used.

485 6.3.2 Dike transect

486 The samples collected as a section across the quartz-porphyry at site I reveal a quite

487 different fabric than that from the marginal parts. A horizontal ﬂow component in the

488 interior part is indicated from ﬁeld observations (Fig. 3b). The AMS data from the inner

489 section in site I show an untilted parabola (Fig. 10a), i.e. lacking a horizontal component.

490 The lack of the horizontal component in the interior is interpreted as overprinting by

491 compaction of the crystal mush due to gravitational forces (Hrouda et al., 2002; Philpotts

492 and Philpotts, 2007; Raposo et al., 2007). Thus the AMS tensor are not correlated to ﬂow

493 markers in the center of the dike. Why the enclaves does not reﬂect this downward

494 movement whereas the rock fabric does, can potentially be explained with differences in

495 the scale of stress. The enclaves can only be orientated by large strain rates, such as is

496 prevalent during ﬂow, while the rock fabric is determined when the rock has completely

22 497 solidiﬁed. At the time when ﬂow has ceased, there would still be interstitial melt,

498 susceptible to deformation, thus determining the ﬁnal rock texture without visible

499 reorientation of the enclaves. To conclude, if primary ﬂow is to be assessed samples must

500 be taken close (10 − 15 cm) to the margin.

501 6.4 Geological model

502 6.4.1 Origin of the felsic magma

503 The origin of the Streitishvarf composite dike was discussed by Guppy and Hawkes (1925)

504 and Gudmundsson (1985). Guppy and Hawkes (1925) did not discuss the origin of the

505 dike in any wider context since they were possibly unacquainted with other outcrops than

506 Hökulvík. They interpreted the intrusion sequence of the dike as an intrusion of maﬁcand

507 felsic magma from the same source, with incremental growth. They favored a

508 predominantly vertical ﬂow model but argued for a horizontal component of ﬂow from the

509 north. Such models where both the felsic and maﬁcmagmaﬂowed in the same direction

510 from the same source has been challenged, and seems to be inconsistent with ﬁeld

511 evidence (Snyder et al., 1997). Gudmundsson (1985) favored a lateral intrusion of a

512 basaltic dike into the top of an unspeciﬁed, stratiﬁed magma chamber. Since the felsic

513 magma, situated at the top of the magma chamber, it is both substantially cooler and far

514 more viscous than the maﬁc magma, it does generally not form dikes, but domes. Felsic

515 dikes are hindered in their propagation both by being rapidly chilled and solidiﬁed against

516 the host rock and by the inner resistance caused by the high viscosity (Blake et al., 1965).

517 If however, a maﬁc dike cut through a reservoir of felsic magma the felsic magma close to

518 the maﬁc dike could become super-heated and mobilized. Subsequently, the not yet

23 519 solidiﬁed maﬁc dike may act as a conduit for the felsic magma, which intrude at the center

520 of the mafic dike and will then readily flow, protected from chilling by the mafic margins.

521 The difference in density would force the maﬁc magma to pond at the bottom of the

522 magma chamber and the felsic magma to rise and escape sub-laterally through the dike

523 conduit. Naturally the rate of which this occur will be dependant on initial crystal content

524 of the magmas (Snyder et al., 1997; Wiebe and Ulrich, 1997). Such a model is presented in

525 Figure 11 and might explain the formation of the Streitishvarf composite dike.

526

527 The model implies different sources for the magmas, for the felsic magma our ﬂow

528 interpretations indicate a source north of site III. The Sandfell laccolith, close to site III has

529 traditionally been referred to the Reyðarfjörður volcanic system (Gibson et al., 1966). The

530 felsic rocks from Reyðarfjörður and Streitishvarf share geochemical characteristics like

531 high Th/Zr and Th/La–ratio, low Th/U-ratio, LREE depletion, HREE enrichment,

87 86 532 fractionation of zircons and similar Sr/ Sr values that indicate fractionation of zircon

533 and a LREE sink and a similar magma source (Martin and Sigmarsson, 2010). The

534 Sandfell laccolith does not share these characteristics. These observations should be

535 regarded with caution since the results by Martin and Sigmarsson (2010) are based on very

536 few samples. If the quartz-porphyry belong to the Reyðarfjörður system it would have

537 been active at either 10.1 or 10.7 Ma. The Reyðarfjörður volcano has not been dated, but

538 an upper age limit may be obtained from the base of the Hólmar olivine basalt group

539 immediately overlying felsic volcanic products from the central volcano. The olivine

39 40 540 group has been dated to 11.23 ± 0.15 Ma (Duncan and Helgason, 1998, Ar/ Ar age

541 recalculated to the FCs monitor age of 28.02 Ma from Renne et al. (1998). A lower age

24 542 limit of 12.2 Ma can be estimated from magnetostratigraphy and the location of the

543 Vindháls porphyritic group about 400 m below the basal felsic volcanics belonging the the

544 Reyðarfjörður central volcano (Watkins and Walker, 1977; Kristjansson et al., 1995; Ogg

545 and Smith, 2004). The time constraints places the Reyðarfjörður volcano quite far back in

546 time in comparison with the age of the dike. Another origin for the felsic magma must

547 therefore be sought, unless this volcanic system was very long lived (>1.5 m.y.).

548 6.4.2 Origin of the maﬁc magma

549 The dolerite margins have according to the model of Blake et al. (1965) and Gudmundsson

550 (1985) a different source than the felsic magma. We speculate that geochemical indication

87 86 551 in the form of widely different Sr/ Sr values of the maﬁc enclaves (0.7033) and the

552 quartz-porphyry (0.7054 Martin and Sigmarsson, 2010) is indicative of this. Unfortunately,

553 we have only obtained AMS results from one side of the dolerite margin at site I. Another

554 separate study should be conducted on the dolerite, but, our results enable us to speculate

◦ 555 on possible origins. The resultant vector (κR) indicate a downward ﬂow of 59 from

556 north-to-south. There are two possible central volcanoes north for site III, Reyðarfjörður

557 and a submerged center east of Gerpir. Both of these centers are however too old

558 (Moorbath et al., 1968; Duncan and Helgason, 1998). No intersection line was calculated

559 for the dolerite, but if one should be estimated from the mean direction of the minor axes,

560 it would indicate a downward ﬂow from south-to-north, similar to Figure 11. Admittedly,

561 the reason for doing this is very weak, the fabric is clearly unsuitable for inferring ﬂow

562 from the minor axis. Nevertheless, the central volcano south of site I is the Álftafjörður

563 central volcano, has been suggested as the origin of both magmas for the Streitishvarf dike

25 564 by Martin and Sigmarsson (2010), but no argument has been presented to support this. The

565 Álftafjörður volcano is offset far south-west of the dike. As indicated in Figure 1 the dike

566 dilatation maxima from the Reyðarfjörður central volcano passes west of the dike, the

567 dilatation maxima for the Álftafjörður dike swarm is located even further to the west and is

568 about parallel to the dike (this dilatation maxima is outside the ﬁgure frame, see also

569 Walker (1974)). If the dolerite had its origin in Álftafjörður central volcano, this volcano

570 should have to have been active around 10.1 or 10.7 Ma, but from magneto-stratigraphic

571 work it may be estimated that the Álftafjörður central volcano were emplaced in bedrock

572 between 9.5–10 Ma old, and seems thus to be even younger (Blake, 1970; Watkins and

573 Walker, 1977). We ﬁnd it highly unlikely that any part of the Streitishvarf composite dike

574 originated in the Álftafjörður central volcano.

575

576 Another origin may be a volcanic system out at sea south of site I. No such volcanic

577 system is known, but aeromagnetic anomaly maps indicate a small positive magnetic

578 anomaly just southwest of site I (Kristjánsson, 2008). This anomaly is not as strong as the

579 ones indicating the Álftafjörður or Austurhorn volcanic centers, but neither is the anomaly

580 of the Reyðarfjörður volcanic system (Walker, 1958; Kristjánsson, 2008). So the

581 possibility for another volcanic center in the sea cannot be ruled out. A third option is that

582 the dike intruded vertically and that the observed magnetic fabric in the dolerite came

583 about from stress exercised by the felsic magma as it ﬂowed.

26 584 6.4.3 Geological scenario

585 Disregarding the unknown origin of the melts, a geological scenario of development can be

586 envisioned in which a shallow felsic magma reservoir, north of site III is pierced by either

587 a laterally south-to-north or vertically intruding dike (similar to Fig. 11), allowing the

588 felsic magma to escape through the conduit formed by the dolerite dike (Fig. 12) similar to

589 the models by Blake et al. (1965) and Wiebe and Ulrich (1997). At the time of the Sandfell

590 intrusion (11.7 Ma) the paleosurface was 540 m a.s.l., while the base of the laccolith have

591 been estimated to be at ca. 140 m a.s.l. (Hawkes and Hawkes, 1933). Rates of buildup of

592 the lava pile have been estimated to between 690–1000 m/m.y. (McDougall et al., 1976;

593 Watkins and Walker, 1977; Kristjansson et al., 1995; Duncan and Helgason, 1998) which

594 would have produced a surface of 1400–1900 m a.s.l. at the time of the Streitishvarf dike

595 intrusion (10.1–10.7 Ma). The average estimate of a paleosurface of 1600–1700 m ﬁts

596 quite well with estimations based on zeolite minerals (Walker, 1974; Neuhoff et al., 1999).

597 The dolerite margins disappears at ca 400 m altitude, both at Hökulvík and Hellufjall,

598 leaving only the felsic core at higher altitudes (Fig. 1c), now displaying a pitchstone

599 margins towards the country rock. The loss of the dolerite margins will, expose the felsic

600 magma to the cold bedrock thereby cooling it in a much higher degree thus vastly increase

601 the viscosity of the magma. This will prevent further ﬂow and the felsic core will begin to

602 form a dome instead. We envisage the level of 400 m a.s.l. to be at the level of neutral

603 buoyancy for the dolerite, where-after the quartz-porphyry will arch up and begin to form

604 an elongated dome. Since the dike widens both with altitude and to the north the body thus

605 produced would ideally have the shape of an keel on an ﬁshing boat. Slightly below the

606 level of neutral buoyancy the ﬂow regime would probably have changed from horizontal to

27 607 vertical, feeding the dome, since the lack of the dolerite margins would also effectively

608 prevent lateral migration. The horizontal thickening of the felsic core to the north

609 mentioned earlier may reﬂect closer proximity to the source.

610

611 The inclination of ﬂow in the dike in the three sites is somewhat inconsistent with a central

612 magma chamber north of site III, since shallower inclinations would be expected further

613 away from the source, whereas the inclinations are irregularly distributed. It is however

614 uncertain whether diking follows simple intrusion trajectories at all. The high inclination

◦ 615 angle at site II (64 ) could possibly be explained by its relatively higher crustal level (ca.

616 300 m). This level could represent the start of the breaking point at which a sub-horizontal

617 dike intrusion would change direction and traverse the quickest way to the surface. The

618 ﬂow trajectories in Figure 12 are adapted to this scenario and a potential surface eruption is

619 indicated above site II. The present outcrop on the ridge at ca. 720 m would only be 800 m

620 below the paleosurface. Some caution should be observed when generalising ﬂow

621 trajectories from the data presented. Direct evidence from diking episodes of the vertical

622 ﬂow trajectory is lacking, neither this kind of staged intrusion mode nor any other

623 trajectory has been well constrained.

624 7 Summary & conclusions

625 An AMS study has been conducted on samples from three different outcrops of the felsic

626 part on the Streitishvarf composite dike. The outcrops were separated by 12 km. The AMS

627 results were consistent and is interpretable as magma ﬂow using the imbrication model

628 with the minor axis as fabric proxy. The ﬂow directions have been quantiﬁed using vector

28 629 algebra and bootstrapping. The calculations show in all three outcrops magma ﬂow from

630 north to south, with an additional upward ﬂow component. The inclination of the magma

◦ ◦ 631 ﬂow direction ranges from 30 − 64 , with 95% conﬁdence ellipses between 3 − 9 .The

632 AMS results are in agreement with ﬁeld evidence at the outcrops in form of ﬂow banding

633 and ﬂow aligned maﬁc enclaves. A geological model of the intrusion history has been

634 suggested in which the felsic part of the dike originated in a magma chamber that was

635 punctuated by a maﬁc dike. The dike reached at least up to a depth of 1 km below an

636 inferred paleosurface (1400 − 1900 m a.s.l.) at the time of intrusion. The study

637 demonstrates the value of the AMS technique in deriving emplacement modes for igneous

638 dikes in Iceland, and thus its value in connection to petrological studies on eroded central

639 volcanoes and shallow crustal magma plumbing systems.

640 8 Acknowledgments

641 Birgir V. Óskarsson at Háskólí Íslands, is acknowledged for aiding in ﬁeld work. Sigurður

642 Steinþórsson at Háskóli Íslands is gratiﬁed for petrographic observations. Erwan Martin at

643 Institut de Physique du Globe de Paris is acknowledged for kindly making radiometric

644 ages of the Sandfell laccolith and the Streitishvarf composite dike available to us. We

645 thank Árni Vésteinsson at Landhelgisgæsla Íslands, Sjómælingasvið, for making detailed

646 bathymetric maps available to the authors. Thongchai Suteerasak is thanked for

647 performing hysteresis measurements. We also wish to thank Laurent Geoffroy and

648 Edgardo Cañón-Tapia for constructive reviews on an earlier version of the manuscript.

649 This work was carried out as a part of P. I. Eriksson’s Licentiate studies and was to a large

650 extent funded through a fellowship with the Nordic Volcanological Center.

29 651 References

652 Aubourg, C., Giordano, G., Mattei, M., Speranza, F., 2002. Magma ﬂow in sub-aqueous rhyolitic 653 dikes inferred from magnetic fabric analysis (Ponza Island, W. Italy). Physics and Chemistry of 654 the Earth, Parts A/B/C 27, 1263–1272.

655 Aubourg, C., Tshoso, G., Le Gall, B., Bertrand, H., Tiercelin, J.J., Kampunzu, A., Dyment, J., 656 Modisi, M., 2008. Magma ﬂow revealed by magnetic fabric in the Okavango giant dyke swarm, 657 Karoo igneous province, northern Botswana. Journal of Volcanology and Geothermal Research 658 170, 247–261.

659 Aïfa, T., Lefort, J.P., 2000. Fossilisation des contraintes régionales miocènes sous climat aride en 660 bordure d’un ﬁlon doléritique carbonifère en bretagne. apport de l’anisotropie de susceptibilité 661 magnétique et du paléomagnétisme. Comptes Rendus de l’Académie des Sciences – Series IIA, 662 Earth and Planetary Science 330, 15–22.

663 Blake, D.H., 1970. Geology of the Álftafjörður volcano, a Tertiary volcanic centre in South-Eastern 664 Iceland. Science in Iceland 2, 43–63.

665 Blake, D.H., Elwell, R.W.D., Gibson, I.L., Skelhorn, R.R., Walker, G.P.L., 1965. Some 666 relationships resulting from the intimate association of acid and basic magmas. Quarterly 667 Journal of the Geological Society of London 121, 31–49.

668 Blakely, R.J., 1974. Geomagnetic reversals and crustal spreading rates during the Miocene. Journal 669 of Geophysical Research 79, 2979–2985.

670 Blanchard, J.P., Boyer, P., Gagny, C., 1979. Un nouveau critere de sens de mise en place dans une 671 caisse ﬁlonienne: Le "pincement" des mineraux aux epontes: Orientation des minéraux dans un 672 magma en écoulement. Tectonophysics 53, 1–25.

673 Bodvarsson, G., Walker, G.P.L., 1964. Crustal drift in Iceland. Geophysical Journal of the Royal 674 Astronomical Society 8, 285–300.

675 Brooks, C.K., Nielsen, T.F.D., 1978. Early stages in the differentiation of the Skaergaard magma as 676 revealed by a closely related suite of dike rocks. Lithos 11, 1–14.

677 Buck, R.W., Einarsson, P., Brandsdóttir, B., 2006. Tectonic stress and magma chamber size as 678 controls on dike propagation: Constraints from the 1975-1984 Kraﬂa rifting episode. Journal of 679 Geophysical Research, Solid Earth 111, B12404.

680 Callot, J.P., Geoffroy, L., 2004. Magma ﬂow in the East Greenland dyke swarm inferred from study 681 of anisotropy of magnetic susceptibility: Magmatic growth of a volcanic margin. Geophysical 682 Journal International 159, 816–830.

683 Carmichael, I.S.E., 1964. The petrology of Þingmúli, a Tertiary volcano in eastern Iceland. Journal 684 of Petrology 5, 435–460.

685 Carmichael, I.S.E., 1967. The mineralogy of Þingmúli, a tertiary volcano in eastern iceland. The 686 American Mineralogist 52, 1815–1841.

687 Cañón-Tapia, E., 1994. Anisotropy of magnetic susceptibility parameters: Guidelines for their 688 rational selection. PAGEOPH 142, 365–382.

689 Cañón-Tapia, E., 2004. Flow direction and magnetic mineralogy of lava ﬂows from the central 690 parts of the Peninsula of Baja California, Mexico. Bulletin of Volcanology 66, 431–442.

691 Chadima, M., Cajz, V., Týcová, P., 2009. On the interpretation of normal and inverse magnetic 692 fabric in dikes: Examples from the Eger Graben, NW Bohemian massif. Tectonophysics 466, 693 47–63.

694 Chadima, M., Hrouda, F., 2006. Remasoft 3.0 a user-friendly paleomagnetic data browser and 695 analyzer. Travaux Géophysiques XXVII, 20–21.

30 696 Constable, C., Tauxe, L., 1990. The bootstrap for magnetic susceptibility tensor. Journal of 697 Geophysical Research 95, 8383–8395.

698 Coward, M.P., 1980. The analysis of ﬂow proﬁles in a basaltic dyke using strained vesicles. Journal 699 of the Geological Society of London 137, 605–615.

700 Craddock, J.P., Kennedy, B.C., Cook, A.L., Pawlisch, M.S., Johnston, S.T., Jackson, M., 2008. 701 Anisotropy of magnetic susceptibility studies in Tertiary ridge-parallel dykes (Iceland), Tertiary 702 margin-normal Aishihik dykes (Yukon), and Proterozoic Kenora-Kabetogama composite dykes 703 (Minnesota and Ontario). Tectonophysics 448, 115–124.

704 Day, R., Fuller, M., Schmidt, V.A., 1977. Hysteresis properties of titanomagnetites: Grain-size and 705 compositional dependence. Physics of the Earth and Planetary Interiors 13, 260–267.

706 de Wall, H., Kontny, A., Vahle, C., 2004. Magnetic susceptibility zonation of the melilititic 707 Riedheim dyke (Hegau volcanic ﬁeld, Germany): evidence for multiple magma pulses? Journal 708 of Volcanology and Geothermal Research 131, 143–163.

709 Delaney, P.T., Pollard, D.D., 1982. Solidiﬁcation of basaltic magma during ﬂow in a dike. 710 American Journal of Science 282, 856–885.

711 Duncan, R.A., Helgason, J., 1998. Precise dating of the Holmatindur cooling event in eastern 712 Iceland: Evidence for mid-Miocene bipolar glaciation. Journal of Geophysical Research, Solid 713 Earth 103, 12397–12404.

714 Dunlop, D.J., 2002. Theory and application of the Day plot (mrs/ms versus hcr/hc) 1. theoretical 715 curves and tests using titanomagnetite data. Journal of Geophysical Research 107, 2056–2077.

716 Dunlop, D.J., Özdemir, Ö., 1997. Rock Magnetism. Cambridge University Press.

717 Ellwood, B.B., 1978. Flow and emplacement direction determined for selected basaltic bodies 718 using magnetic susceptibility anisotropy measurements. Earth and Planetary Science Letters 41, 719 254–264.

720 Ellwood, B.B., 1979. Anisotropy of magnetic susceptibility variations in Icelandic columnar 721 basalts. Earth and Planetary Science Letters 42, 209–212.

722 Geoffroy, L., Aubourg, C., Callot, J.P., Barrat, J.A., 2007. Mechanisms of crustal growth in large 723 igneous provinces: The north Atlantic province as a case study. Geological Society of America, 724 Special Paper 430, 747–774.

725 Geoffroy, L., Callot, J.P., Aubourg, C., Moreira, M., 2002. Magnetic and plagioclase linear fabric 726 discrepancy in dykes: A new way to deﬁne the ﬂow vector using magnetic foliation. Terra Nova 727 14, 183–190.

728 Gibson, I.L., Kinsman, D.J.J., Walker, G.P.L., 1966. Geology of the Fáskrúðsfjörður area, Eastern 729 Iceland. Societas Scientarium Islandica, Greinar IV, 1–52.

730 Gibson, I.L., Walker, G.P.L., 1963. Some composite rhyolite/basalt lavas and related composite 731 dykes in eastern Iceland. Proceedings of the Geologists’ Association 74, 301–318.

732 Gudmundsson, A., 1985. Samsetti gangurinn á Streitishvarﬁ við Breiðdalsvík. 733 Náttúrufræðingurinn 54, 135–148.

734 Gunn, B.M., Watkins, N.D., 1969. The petrochemical effect of the simultaneous cooling of 735 adjoining basaltic and rhyolitic magmas. Geochimica et Cosmochimica Acta 33, 341–356.

736 Guppy, E.M., Hawkes, L., 1925. A composite dyke from Eastern Iceland. Quarterly Journal of the 737 Geological Society of London 81, 325–341.

738 Halvorsen, E., 1974. The magnetic fabric of some dolerite intrusions, northeast Spitsbergen; 739 implications for their mode of emplacement. Earth and Planetary Science Letters 21, 127–133.

31 740 Hardarson, B.S., Fitton, G.J., 1997. Mechanisms of crustal accretion in Iceland. Geology 25, 741 1043–1046.

742 Hawkes, L., Hawkes, H.K., 1933. The Sandfell laccolith and ’Dome of elevation’. Quarterly 743 Journal of the Geological Society of London 89, 379–400.

744 Henry, B., 1997a. Complementary directional data in magnetic fabric studies: The intersection of 745 magnetic foliation. Physics and Chemistry of the Earth 22, 175–177.

746 Henry, B., 1997b. The magnetic zone axis: a new element of magnetic fabric for the interpretation 747 of the magnetic lineation. Tectonophysics 271, 325–331.

748 Herrero-Bervera, E., Walker, G.P.L., Cañon-Tapia, E., Garcia, M.O., 2001. Magnetic fabric and 749 inferred ﬂow direction of dikes, conesheets and sill swarms, Isle of Skye, Scotland. Journal of 750 Volcanology and Geothermal Research 106, 195–210.

751 Hrouda, F., Chlupacova, M., Novak, J.K., 2002. Variations in magnetic anisotropy and opaque 752 mineralogy along a kilometer deep proﬁle within a vertical dyke of the syenogranite porphyry at 753 Cinovec (Czech Republic). Journal of Volcanology and Geothermal Research 113, 37–47.

754 Jelínek, V., 1981. Characterization of the magnetic fabric of rocks. Tectonophysics 79, T63–T67.

755 Jóhannesson, H., Sæmundsson, K., 1998. Geological map of Iceland, 1:500 000, bedrock geology. 756 Icelandic Institute of Natural History, Reykjavík 2nd ed.

757 Khan, M.A., 1962. The anisotropy of magnetic susceptibility of some igneous and metamorphic 758 rocks. Journal of Geophysical Research 67, 2873–2885.

759 Kissel, C., Laj, C., Sigurdsson, H., Guillou, H., 2010. Emplacement of magma in Eastern Iceland 760 dikes: Insights from magnetic fabric and rock magnetic analyses. Journal of Volcanology and 761 Geothermal Research 191, 79–92.

762 Knight, M.D., Walker, G.P.L., 1988. Magma ﬂow directions in dikes of the Koolau complex, Oahu, 763 determined from magnetic fabric studies. Journal of Geophysical Research, Solid Earth 93, 764 4301–4319.

765 Königsberger, J.G., 1938. Natural residual magnetism of eruptive rocks. Terrestrial Magnetism and 766 Atmospheric Electricity 43, 119–130, 299–320.

767 Kratinová, Z., Závada, P., Hrouda, F., Schulmann, K., 2006. Non-scaled analogue modelling of 768 AMS development during viscous ﬂow: A simulation on diapir-like structures. Tectonophysics 769 418, 51–61.

770 Kristjánsson, L., 1999. On low-latitude virtual geomagnetic poles in Icelandic basalt lava 771 sequences. Physics of the Earth and Planetary Interiors 115, 137–145.

772 Kristjánsson, L., 2008. Paleomagnetic research on Icelandic lava ﬂows. Jökull 58, 101–116.

773 Kristjánsson, L., 2009. A new study of paleomagnetic directions in the Miocene lava pile between 774 Arnarfjörður and Breiðafjörður in the Vestﬁrðir peninsula, Northwest Iceland. Jökull 59, 33–50.

775 Kristjansson, L., Gudmundsson, A., Haraldsson, H., 1995. Stratigraphy and paleomagnetism of a 776 3-km-thick Miocene lava pile in the Mjoifjördur area, eastern Iceland. Geologische Rundschau 777 84, 813–830.

778 Martin, E., Sigmarsson, O., 2010. Thirteen million years of silicic magma production in Iceland: 779 Links between petrogenesis and tectonic settings. Lithos 116, 129–144.

780 McDougall, I., Kristjansson, L., K., S., 1984. Magnetostratigraphy and geochronology of Nortwest 781 Iceland. Journal of Geophysical Research 89, 7029–7060.

32 782 McDougall, I., Watkins, N.D., Walker, G.P.L., Kristjansson, L., 1976. Potassium-argon and 783 paleomagnetic analysis of Icelandic lava ﬂows: Limits on the age of Anomaly 5. Journal of 784 Geophysical Research, Solid Earth 81, 1505–1511.

785 Merle, O., 2000. Numerical modelling of strain in lava tubes. Bulletin of Volcanology 62, 53–58.

786 Moorbath, S., Sigurdsson, H., Goodwin, R., 1968. K-Ar ages of the oldest exposed rocks in 787 Iceland. Earth and Planetary Science Letters 4, 197–205.

40 39 788 Mussett, A.E., Ross, J.G., Gibson, I.L., 1980. Ar/ Ar dates of eastern Iceland lavas. 789 Geophysical Journal of the Royal Astronomical Society 60, 37–52.

790 Neuhoff, P.S., Fridriksson, T., Arnorsson, S., Bird, D.K., 1999. Porosity evolution and mineral 791 paragenesis during low-grade metamorphism of basaltic lavas at Teigarhorn, Eastern Iceland. 792 American Journal of Science 299, 467–501.

793 Nicolas, A., 1992. Kinematics in magmatic rocks with special reference to gabbros. Journal of 794 Petrology 33, 891–915.

795 Nye, J.F., 1985. Physical properties of crystals: Their representation by tensors and matrices. 796 Oxford University Press.

797 Ogg, J.G., Smith, A.G., 2004. The geomagnetic polarity time scale, in: Gradstein, F.M., Ogg, J.G., 798 Smith, A.G. (Eds.), A geologic time scale. Cambridge University Press, pp. 63–86.

799 Pálmason, G., 1986. Model of crustal formation in Iceland, and application to submarine 800 mid-ocean ridges, in: Vogt, P.R., Tucholke, B.E. (Eds.), The Geology of North America, Volume 801 M. Geological Society of America, pp. 87–97.

802 Paquet, F., Dauteuil, O., Hallot, E., Moreau, F., 2007. Tectonics and magma dynamics coupling in a 803 dyke swarm of Iceland. Journal of Structural Geology 29, 1477–1493.

804 Philpotts, A.R., Philpotts, D.E., 2007. Upward and downward ﬂow in a camptonite dike as 805 recorded by deformed vesicles and the anisotropy of magnetic susceptibility (AMS). Journal of 806 Volcanology and Geothermal Research 161, 81–94.

807 Piper, J.D.A., Fowler, M.G., Gibson, I.L., 1977. Dyke magnetization, magnetostratigraphy and 808 upper-crustal structure in the Reyðarfjörður area of eastern Iceland. Tectonophysics 40, 227–244.

809 Poland, M.P., Fink, J.H., Tauxe, L., 2004. Patterns of magma ﬂow in segmented silicic dikes at 810 Summer Coon volcano, Colorado: AMS and thin section analysis. Earth and Planetary Science 811 Letters 219, 155–169.

812 Raposo, M.I.B., D’Agrella-Filho, M.S., Pinese, J.P.P., 2007. Magnetic fabrics and rock magnetism 813 of Archaean and Proterozoic dike swarms in the southern São Francisco craton, Brazil. 814 Tectonophysics 443, 53–71.

815 Renne, P.R., Swisher, C.C., Deino, A.L., Karner, D.B., Owens, T.L., DePaolo, D.J., 1998. 40 39 816 Intercalibration of standards, absolute ages and uncertainties in ar/ ar dating. Chemical 817 Geology 145, 117–152.

818 Saemundsson, K., 1979. Outline of the geology of Iceland. Jökull 29, 7–28.

819 Saemundsson, K., Kristjansson, L., McDougall, I., Watkins, N.D., 1980. K-Ar dating, geological 820 and paleomagnetic study of a 5-km lava succession in Northern Iceland. Journal of Geophysical 821 Research 85, 3628–3646.

822 Sigmundsson, F., 2006. Iceland Geodynamics, Crustal Deformation and Divergent Plate Tectonics. 823 Springer Verlag.

824 Snyder, D., Crambes, C., Tait, S., Wiebe, R.A., 1997. Magma mingling in dikes and sills. The 825 Journal of Geology 105, 75–86.

33 826 Soriano, C., Beamud, E., Garcés, M., 2008. Magma ﬂow in dikes from rift zones of the basaltic 827 shield of Tenerife, Canary Islands: Implications for the emplacement of buoyant magma. Journal 828 of Volcanology and Geothermal Research 173, 55–68.

829 Stacey, F.D., 1974. The physical principles of rock magnetism. Elsevier.

830 Symons, D.T.A., 1975. Age and ﬂow direction from magnetic measurements on the historic 831 Aiyansh ﬂow, British Columbia. Journal of Geophysical Research, Solid Earth 80, 2622–2626.

832 Tarling, D.H., Hrouda, F., 1993. The Magnetic Anisotropy of Rocks. Chapman & Hall, London.

833 Tauxe, L., 1998. Paleomagnetic Principles and Practice. Kluwer Academic Publishers.

834 Varga, R.J., Horst, A.J., Gee, J.S., Karson, J.A., 2008. Direct evidence from anisotropy of magnetic 835 susceptibility for lateral melt migration at superfast spreading centers. Geochemistry, 3 836 Geophysics, Geosystems (G ) 9, Q08008.

837 Walderhaug, H., 1993. Rock magnetic and magnetic fabric variations across three thin alkaline 838 dykes from Sunnhordland, Western Norway; inﬂuence of initial mineralogy and secondary 839 chemical alterations. Geophysical Journal International 115, 97–108.

840 Walker, G.P.L., 1958. Geology of the Reyðarfjörður area, Eastern Iceland. Quarterly Journal of the 841 Geological Society of London 114, 367–391.

842 Walker, G.P.L., 1960. Zeolite zones and dike distribution in relation to the structure of the basalts of 843 Eastern Iceland. Journal of Geology 68, 515–528.

844 Walker, G.P.L., 1963. The Breiðdalur central volcano, Eastern Iceland. Quarterly Journal of the 845 Geological Society of London 119, 29–63.

846 Walker, G.P.L., 1966. Acid volcanic rocks in Iceland. Bulletin of Volcanology 29, 375–402.

847 Walker, G.P.L., 1974. The structure of Eastern Iceland, in: Kristjansson, L. (Ed.), Geodynamics of 848 Iceland and the North Atlantic Area, NATO Advanced Study Institutes Series, Volume C11. 849 Reidel Publishing Company, Holland, Dordrecht, pp. 177–188.

850 Watkins, N.D., Haggerty, S.E., 1968. Oxidation and magnetic polarity in single Icelandic lavas and 851 dikes. Geophysical Journal of the Royal Astronomical Society 15, 305–315.

852 Watkins, N.D., Walker, G.P.L., 1977. Magnetostratigraphy of Eastern Iceland. American Journal of 853 Science 277, 513–584.

854 Wiebe, R.A., Ulrich, R., 1997. Origin of composite dikes in the Gouldsboro granite, coastal Maine. 855 Lithos 40, 157–178.

34 Table 1: Dike characteristics.

No. Locality Width Strike/Dip Altitude Long. Lat. Marginal Interior (m) (°/°) (m a.s.l.) N W samples samples I Streitishvarf 9 ∼20/80 s.l. 64°44’ 13°59’ 18+6b 17 II Hökulvík 12 ∼4/85 ∼300m 64°47’ 13°55’ 10 - III Hellufjall 28 ∼ 10a/80 s.l. 64°50’ 13°53’ 7 - Width in m is given for the sampled quartz-porphyry unit. Direction of mean strike/dip given in geographical coordinates corrected for magnetic declination (12.4°W), (a) denote large differences in strike between the west and east margin. Altitude above sea level in m for each sample site is given. Long./Lat.: geographical coordinates for sample site. Marginal/Interior samples: numbers of samples collected. (b) denotes samples collected from dolerite margin.

35 Table 2: Rock density and properties pertaining to rock magnetism and characteristic remanent magnetization (ChRM).

Rock density and rock magnetic properties Magnetic remanence Tectonic correction Dike tilt correction No. n Type Density Km M50 Qn Tc D/I α95 k Lava Tilt Corr. dir. Dike tilt Corr. dir. − --(g/cm3)(103SI) (mT) - °C (°/°) (°) - (Strike°/Dip°) (D°/I°) (Strike°/Dip°) (D°/I°) I 3 Q 2.08 12.5 15.6 0.22 ◦ ∼ 560 207.8a/-38.7 3.4 236 191/9 200.4a/-40.7 200/13 197.2a/-39.3 I 6 D - 21.5 12.9 1.60 a a a II 7 Q 2.18 12.5 7.8 0.31 ◦ 209.0 /-46.9 5.5 119 200.5 /-49.2 203.9 /-48.8 ∼ 560 187/8 184/5 II 4 H 2.22 10.5 19.5 0.73 348.9/78.0 3.7 611 321.6/73.7 329.3/78.9 III 4 Q 2.16 6.0 45.9 0.21 ◦ ∼ 570 209.1a/-53.4 3.7 334 197/12 192.6a/-54.2 180/10 195.7a/-57.2 III 2 H 2.57 8.5 44.6 0.24

36 ∑ 26 - 2.24 11.9 24.4 0.56 Mean dir.: 208.6/-46.7 10.7 133 198.1/-48.1 199.0/-48.5 - - (k:119, α:11.3°) (k:75, α:14.4°) Virtual Geomagnetic Pole (VGP) for 64.8°N, 13.9°W: 49.0°S, 306°E, Dp:8.9, Dm:13.8 52.6°S, 319.6°E, Dp:9.7, Dm:14.8 52.7°S, 318.2°E, Dp:12.4, Dm:18.9 Rock magnetic properties are given for n samples from each rock type (Q–quartz porphyry, D–dolerite and H–hybrid rock) at each sampled site I (Streitishvarf), II (Hökulvík) and III (Hellufjall). Density given for bulk rock mass. Km: Bulk magnetic susceptibility. M50: Field strength where 50% of the magnetization have been eliminated by AF-treatment (MDF). Qn: Königsberger ratio for natural magnetization. Tc: Curie temperature (°C). Characteristic remanence direction (ChRM) is given for each site, except for site II where the two rock types gave different magnetic remanences. Remanences are given as declination (D°) and inclination (I°) with the radius of the 95% conﬁdence circle (α95) and Fisher’s precision parameter k.(a) denotes which directions have been used for average. Lava Tilt: Average lava tilt for each outcrop given in geographical coordinates as strike and dip. Dike tilt: Average tilt plane for each dike given as strike and dip. Corrected directions of remanence for lava/dike tilt given as declination and inclination. Virtual Geomagnetic pole: Pole position for calculated and corrected mean remanences respectively, given as latitude/longitude with Dp/Dm: Angular lengths of the conﬁdence ellipse of the calculated VGP. Table 3: Characteristics for the anisotropy of magnetic susceptibility ellipsoid and axis directions with statistical parameters.

Site Side n κa εa κb εb κc εc PJ s T s I W 6/9 35/33 5.3/4.3 199/56 9.3/3.6 300/8 9.1/3.8 1.020 .001 -0.184 .270 I E 7/9 64/33 20.8/5.4 202/50 19.7/5.6 320/21 9.3/5.4 1.022 .003 0.081 .233 I D 6/6 226/64 12.4/5.6 24/24 35.4/3.9 118/9 34.7/6.7 1.031 .014 -0.329 .312 II W 5/5 286/86 5.7/3.7 17/0 8.5/3.7 107/4 6.8/3.7 1.032 .003 -0.334 .149 II E 5/5 156/63 26.9/9.9 36/14 26.2/6.4 300/23 11.3/2.8 1.053 .008 0.482 .309 37 III W 7/7 278/74 14.3/7.7 141/12 14.6/10.3 48/11 14.6/12.6 1.030 .008 -0.266 .259 III E 7/7 116/72 8.6/5.3 25/0 16.5/3.9 295/18 15.2/6.4 1.039 .007 -0.375 .220 ∑ 44/48 Ø 1.032 Ø .006 - Ø .250 Directions of axes of the AMS ellipsoid from each outcrop and each side of the dike (W,E) and the dolerite (D) samples from the east margin in site I, together with statistical parameters PJ and T given with their standard deviations, s. Key to table. n: Number of samples used for statistics and sampled. Directions (κ) given as strike and dip in geographical coordinates together with the angular length of axes of the 95% conﬁdence ellipse (ε) given as major and minor value. T: shape parameter, (T>0 → oblate, T<0 → prolate shape). Pj: Corrected anisotropy degree (Jelínek, 1981). Ø: Arithmetic mean. Table 4: Directions of the intersection line and the resultant vector.

Intersection line Resultant vector Site Dike DI ε D’ I’ ∠ DI ε D’ I’ C IQ199 48 8.9/2.2 188 47 -43 50 37 3.8/1.2 236 -32 N ID------179 64 2.4/1.9 163 59 -

38 II Q 199 25 7.1/2.0 197 26 -64 167 79 7.8/2.2 146 77 N III Q 160 66 5.7/3.1 145 60 -30 155 88 2.8/1.7 108 79 N Table 5: Intersection line and resultant vector given in geographical coordinates (D,I) and rotated, tilt adjusted coordinates (D’,I’), together with angular axis length of bootstrapped confidence ellipse (ε). Q denotes quartz-porphyry and D denotes dolerite margin. ∠, angle of flow above the horizon cf. fig. 5. C, qualitative comparison between the flow direction indicated by the intersection line and the resultant vector, given as agreeing (Y) or not agreeing (N). Note that the flow direction is possible to discern from the pair D’/∠ for the intersection line and D’,I’ for the resultant vector. The declination indicate direction (north-to-south D’>90, from south-to-north D’<90), negative ∠ and I’ denote upwards flow. Figure 1: Geological map over Iceland and sections at dike outcrops.

(a) Geological map of Iceland showing the age succession of the bedrock. The enclosed area is shown in (b). Miocene (∼16 − 3.1 Ma) rocks are found along the northwest and east coast. These are overlaid by volcanics of Plio-Pleistocene age (3.1−0.7 Ma), and of volcanics in the neovolcanic zone (< 0.7 Ma). Holocene sandur deposits occur prominently along the south coast. Map simpliﬁed from Jóhannesson and Sæmundsson (1998). (b) Schematic geological map over the study area, showing felsic and composite dikes, larger felsic intrusives and extrusives. Visible outcrops are denoted by black lines, their assumed continuation is denoted with dotted lines. The thin dashed lines indicate the zone of maximum dilatation within the dike swarm belonging to the Reyðarfjörður volcanic system. The dike dilatation maxima of the Álftafjörður volcanic system lie further down to the south-west outside the ﬁgure frame. The cross section marked A–B is shown in Figure 12.

The dots represent selected mountain peaks, with height above sea level included. The strike/dip directions for the composite dike and the regional lavas are marked by ⊥ and given for selected areas. The easternmost part of the lava pile should not exceed ∼13 Ma (Gerpir porphyritic group) while the westernmost should not exceed 11 Ma (McDougall et al., 1976; Watkins and Walker, 1977;

Duncan and Helgason, 1998). (c) Schematic vertical sections of site I, II and III. The section at site

III is poorly constrained since the outcrops are partly obscured by debris, but ﬁeld evidence supports the loss of the dolerite margins at ca. 400 m a.s.l.. Figure (c) constructed from own ﬁeld evidence and observations by Guppy and Hawkes (1925) and Gudmundsson (1985).

39 Figure 2: Field photography of the Streitishvarf composite dike.

View at site I where the dike has dolerite margins, several meters thick and a 8 − 9 m wide inner core of quartz-porphyry. The dike continues in the distant mountain range to the north. Both the dolerite and the quartz-porphyry show columnar jointing, the dolerite in half-meter scale and the felsic in decimetre-scale. The columnar jointing in the dolerite margins is near horizontal while the quartz-porphyry is sectioned. The contact to the dolerite (see 1 in ﬁgure) is sub-vertical while the inner columnar jointing (2) is markedly tilted towards the west at the west margin while sub-horizontal at the eastern margin (3).

Figure 3: Photographs of lineation features of maﬁc enclaves occurring in the felsic part of site I.

Both (a) and (b) show horizontal cuts of the dike. (a) Hybrid zone followed by quartz-porphyry to the right on the eastern side in site I. In ﬁgure: 1. Sharp contact between the hybrid zone showing

ﬂow banding features and the more homogeneous quartz-porphyry. 2. Enclaves embedded, ﬂow lineated and partly mixed into the hybrid rock. 3. Elongated enclaves lineated parallel to dike trend.

4. Micro-fault system perpendicular to dike trend. (b) Parabolic shape outlined by maficenclaves and flow banding (shown by the arrows) indicating a horizontal flow regime. Also note the varying tone of the quartz-porphyry in the interior of the parabola. The hammer shaft is parallel to dike trend and the handle points to the north.

40 Figure 4: Photographs on features of the maﬁc enclaves in the quartz-porphyry at site I.

(a) Different mixing characteristics of the enclaves. 1. Flow banding shown by hybrid rock. 2.

Flow banding connecting to possibly disbanding enclaves. 3. Crenulated edges. 4. Back-veining of enclaves. Pen aligned perpendicular to dike trend. Note the lineation of the ﬂow banding and the enclaves. (b) Three-dimensional cut showing enclaves, 1, that have a tabular shape with their

flat surface foliated parallel to dike strike. (c) Fracture systems in the dike showing faults, 1, perpendicular to dike trend filled with quartz/heulandite and 2, unfilled faults parallel to dike trend.

3. Globular enclave cut by fault, observe the displacement of ca. 5 mm. 4. Enclave possibly showing shearing and disbandment in the rhyolitic magma. 5. Lineated enclave cut by fault. Pen perpendicular to dike trend. (d) Micro-folds and signs of horizontal shearing (stippled line) in a ﬂow banded hybrid rock zone at Hellufjall middle outcrop. North-arrow roughly parallel to dike trend.

Pen as scale.

Figure 5: Line drawing of the imbrication model and the deﬁnition of the intersection line.

Magma flow yields a flow profile (bottom right) in a tabular body such as a dike. Observe that the

ﬂow is slightly inclined. Due to rheological properties a shear plane will form at the dike walls, imposing a magmatic and magnetic foliation plane, P1,2 for margin 1 and 2 respectively. The minor

κ susceptibility axis ( c,1/2) is perpendicular to this plane (not shown). Note that the imbrication in the horizontal plane is slightly uneven (βw > βe), while the imbrication in the vertical plane is equal

(αw = αe). The imbrication planes cut each other in a line, the intersection line (Vf ). Magma ﬂow

(indicated by the large white arrow) is perpendicular to this line given the prior requisites are met

(see theory section). The flow line (Vf ) can be divided into horizontal (Vh) and vertical (Vv) vector components to determine their relative effect. The inclination of flow above (or below) the horizon is indicated by ∠ while the direction of flow must lie close to the dike plane if the imbrication angles are sound.

41 Figure 6: Magnetic remanence characteristics.

(a) Remanence vector plot from site I (dolerite) indicating a single remanence direction apart from a small component held by low coercivity grains. (b) Remanence vector plot from site

III (quartz-porphyry) for the demagnetization steps 0 − 90 mT, note the two component system where an alternate direction is held by low coercivity grains. (c) Stereograph of characteristic remanences for all outcrops with 95% confidence ellipse and mean direction of the reversely magnetized directions. The present earth’s field (PEF) is given without confidence ellipse (calculated for 64.8◦ N13.9◦ W). The reverse magnetizations are corrected for lava tilt while the normal magnetization are not. (d) Accompanying normalized demagnetization graph for vector plot a, showing a pseudo-exponential shape indicating middle sized multi-domain grains as remanence carriers. (e) Normalized demagnetization curve for plot b, showing the demagnetization of a reversed component at 0 − 20 mT and thereafter a sigmoidal shape indicating single domain held remanence.

Figure 7: Granulometry plot.

Granulometric estimation plot after Day et al. (1977). Open circles samples from the quartz-porphyry. Closed circle sample from dolerite margin. Solid line denotes the theoretical curve for multi-domain behaviour in pure magnetite according to Dunlop (2002). Samples which fall left of this curve indicate single- or pseudo-single domain behaviour. Sample 1 from site III, central part.

Sample 2 from site II margin, hybrid rock. Sample 3 from site III margin, hybrid rock. Sample 4 from site I margin.

42 Figure 8: Thermomagnetic graphs.

Normalized susceptibility/temperature graphs for two samples. (a) Representative sample from site

II (quartz-porphyry) indicating two phases of magnetite with low titanium content, one minor phase which loses its magnetization from 400°C and one major phase with a distinct Curie temperature of ca. 550°C. (b) Anomalous sample from site III (quartz-porphyry) showing a clear Curie temperature point at ca. 625°C that probably indicates maghemite.

Figure 9: Anisotropy of magnetic susceptibility graphs.

Stereographic lower hemisphere projections of the AMS ellipsoid together with calculated intersections lines. (a) site I (b) site II and (c) site III. The AMS stereographs are accompanied by a

T/PJ graph. The stereographic projections is given in geographic coordinates corrected for westward declination of the magnetic ﬁeld. The great circle represents the margin attitude. denotes major susceptibility axis, intermediate and the minor susceptibility axis, small ellipses 95% conﬁdence cone. indicate calculated intersection lines. Note the proximity between the mean intersection line direction and the margin attitude.

43 Figure 10: Idealized geological section from site I including bulk susceptibility, anisotropy degree,

AMS data and interpretation of magnetic fabric.

(a) Model representation of magnetic foliation planes in vertical section. The orientation of the foliation plane is indicated and given in paleovertical coordinates. The margin samples (α)are imbricated in both the vertical and horizontal plane while the inner samples (β) are only imbricated in the vertical plane. The Greek letters (α,β,γ) correspond to the AMS data in the stereographs

(b) shown in paleovertical coordinates. The great circle represents dike strike. α corresponds to the west and east marginal samples, β and γ correspond to interior samples. The samples from the dolerite are shown under ω. The specimen ranges shown in the stereographs are indicated by the braces over the bulk susceptibility curve, and with dashed lines. (c) Bulk susceptibility curve and corrected anisotropy degree. Interior samples are numbered from 1 to 17 while the marginal and dolerite samples are not numbered, the spatial distribution of the samples is indicated in the geological section (d) a horizontal section showing rock type zones, and their width. Samples are represented by the dotted circles. Zone I: Interface between the hybrid and quartz-porphyry, enclaves cross cut the interface and show foliation parallel to dike plane (cf. Fig. 4a). Zone II: The foliated appearance of the enclaves is retained some distance into the dike. Zone III: In the middle of the dike a more irregular enclave fabric occur while some parallel foliation is retained. Zone IV: horizontal

flow parabola (cf. Fig. 4b) with flow banding and aligned enclaves which distinctly mark a prior horizontal flow component from north to south.

44 Figure 11: Conceptual model showing behaviour of felsic magma when a stratiﬁed magma chamber is pierced by a maﬁcdike.

(a) A maﬁc dike (1) propagates laterally (2) eventually reaching a shallow magma chamber (3). (b)

The mafic dike conduit is split by the buoyant felsic magma (4) and thus allows upwards directed movement of the felsic magma within the mafic dike (5). (c) If the magma pressure is high enough thefelsicmagmamayriseabovethepriormafic dike conduit (6) where it rapidly chills and expands, eventually into a dome. In the magma chamber (7) the denser mafic magma will sink to the bottom of the chamber. (c) Section seen from the side. Chilling and expansion of the tip of the felsic dike (8) will occur as a consequence of the loss of the mafic margins (9) which insulates the felsic magma.

In the magma chamber the maﬁc magma will sink in pods in the buoyant felsic magma.

45 Figure 12: Geological model inferred from ﬁeld evidence and AMS results.

The cross section A–B is outlined in figure 1. The small solid arrows at the sites indicate flow regime in the quartz-porphyry obtained from AMS (43°, 64° and 30° for site I, II and III). Heavy lines mark known outcrops, cf. figure 1. The paleosurfaces are estimated from crustal accretion rates (690 − 1000 m/m.y) and field evidence from the Sandfell intrusion (Hawkes and Hawkes,

1933) supporting a paleosurface of 540 m a.s.l. just prior to the intrusion event of the laccolith.

Sandfell has an age of 11.7 Ma while the composite dike has an age of 10.2 or 10.7 Ma (Martin et al. (in prep.)). Potential ﬂow trajectories are shown by dashed lines. Potential outer limits shown by dash-dotted line, indicating a surface eruption above site II. The mean standard deviation of the ﬂow directions is maximum 9°, error limits are not shown. The lateral position of the magma chamber, placed under Fáskrúðsfjörður is speculative, its depth under the paleosurface have been inferred from known present chambers (Sigmundsson, 2006). According to Martin and Sigmarsson (2010), the evolved roof zone with felsic magma in the magma chamber were generated by partial melting of hydrated meta-basalts followed by fractional crystallization. Vertical versus horizontal scale is retained. The large arrows in the lower left corner indicate a speculative intrusion direction for the dolerite surrounding the quartz-porphyry, see section 6.4.2.

46 figure01.ai 2010-11-09 08.32.19

N (a) (b) B REYÐARFJÖRÐUR Reyðarfjörður felsic extrusives 586m Múli Gerpir ~13 Ma Kerlingarfjall sill 194/9°

157/14°

FÁSKRÚÐSFJÖRÐUR

Legend 172/10° Neogene (> 3.1 Ma) N Plio-Pleistocene (3.1 - 0.7 Ma) Sandfell Neovolcanic Zone (< 0.7 Ma) laccolith Kumlafell Holocene sandur deposits and lavas 884m 769m Miðfell 859m Hellufjall Site (c) 164/12° Site III N 170/8° ~400m a.s.l. III 0/80° Margins obscured STÖÐVARFJÖRÐUR

? Snæhvammstindur 857m Sandhöfʔadalur 808m Lambafell s.l. ~700m Heyklif 28m 172/8° Hökulvík Site II Dike dilatation 4/85° of 4-8% 25-35m Possible continuation (~1.1 km) ~700m II from bathymetry Quartz BREIÐDALSVÍK Sanidine type porphyry composite and

~400m a.s.l. felsic dikes 164/9° 12m

8km 5km 20/80° Mafic extrusives s.l. Site I 8 m Streitishvarf Felsic extrusives Felsic intrusives

10 m A 9 km s.l. I figure02.ai 2010-11-09 09.10.48

Merkitindur Snæhvammstindur (857m)

Lambafell Súlur (~644m) (~700m) Mosfell

Lava tilt Hökulvík outcrop

1122 3

Dolerite margin

Streitishvarf outcrop N Quartz porphyry figure03.ai 2010-11-16 12.20.0

(a) (b)

Hybrid rock Quartz porphyry 4. N

3. 1.

N figure04.ai 2010-11-09 09.11.19

(a) (b) 1.

3. 1. 4. 3.

2. (c) 2.

4. (d) 5. 3.

1. 1.

N figure05.ai 2010-11-09 09.11.56

Dike strike Vh

Vv Vf e

Flow velocity profile in P2 _2 horizontal cut

_1 `2 Flow velocity profile in 3D

Dike wall

Dike section figure06.ai 2010-11-09 09.12.16

(a) Site I (b) Site III N Up N Up

W E W E W E W E

Horizontal Vertical Horizontal Vertical

S Down S Down N (c)

PEF PEF Present earth field Normal polarity Reverse polarity

III II I

Lower hemisphere projection (d) (e) Site I Site III 1 1 0.9 0.9 0.8 0.8 0.7 0.7 0.6 0.6 max 0.5 0.5

M / 0.4 0.4 0.3 0.3 0.2 0.2 0.1 0.1 0 0 0 1020304050607080 0 102030405060708090100 Peak demagnetizing field (mT) Peak demagnetizing field (mT) figure07.ai 2010-11-09 09.12.47

Mrs/Mr

Single- domain

Pseudo- single- domain 1

2 3

Multi-domain

Hcr/Hr 0.005 0.02 0.5 1.0 1525010 20 30 40 Susceptibility (K/K0) 0.2 0.4 0.6 0.8 1.0 0 (a) figure08.ai 2010-11-0908.34.34 0 0 0 0 0 600 500 400 300 200 100 Temperature (°C) ieI SiteIII Site II Heating Cooling 700 0 (b) 0 0 0 0 0 600 500 400 300 200 100 Temperature (°C) 700 figure09.ai 2010-11-09 08.34.54

Western margin Eastern margin Intersection line

N N N (a) Site I T T 1 1 P Pj j 1.025 1.027

-1 -1

(b) Site II T T 1 1 Pj

Pj 1.037 1.067

-1 -1

Pj Pj 1.046 1.053

-1 -1

Major axis Intermediate axis Minor axis T > 0: Oblate T < 0: Prolate Direction of intersection line figure10.ai 2010-11-09 08.37.23

Idealized vertical section with the magnetic foliation planes represented 120/5° 111/39° 65/80° 289/28° 318/10° (a) WE_ ` a ` _

Stereographic plots of AMS axes _`a `_ N N N N N

(b) 270 90

K1 K2 K3 { { {

K × 10-2 SI t Bulk magnetic susceptibility variation among samples m N

1 (c) 0.5 0 N 1. 2. 3.4. 5. 6. 7. 8. 9.10.11.12.13. 14. 15. 16. 17. PJ 1.017 1.025 1.027 1.013 1.031 1.031

PJ 1.022 1.024 1.019 1.012 1.021 1.026 1.031 1.013 1.013 1.018 1.022 Dolerite Hybr. Quartz-porphyryParabolic zone Quartz-porphyry Hybr. Dolerite Drill hole IV Dolerite samples (d) IIIII III I Bedrock

Marginal samples Marginal samples Columnar jointing ~6-7m 0.1 4.8 1.2 2.7 0.2 ~6-7m (m) figure_11.ai 2010-11-16 12.18.40 a) b) c) d)

2 6 8 1 5 9 3 7 4 10 figure12.ai 2010-11-16 12.21.12

Length of section ~29.2 km 11.3 - 12 Ma Depth below ? Reyðarfjörður C.V. paleosurface 10.1 or 10.7 Ma ? ? 11.7 Ma (km) Site I Site II Site III Sandfell laccolith Paleosurface 1500m 0 Surface at the time of the dike intrusion 1200m Younger lavas banking up Up-heaved lavas -0.5 against the dome Present surface 600m Surface at the time of the Sandfell intrusion -1.0 Present sea level Hellufjall A B -1.5 Streitishvarf Breiðdalsvík Hökulvík Stöðvarfjörður Fáskrúðsfjörður Reyðarfjörður 7 km 5.1 km -2.0 ? Mafic extrusives -2.5 Roof zone melting Potential trajectory of flow -3.0 Felsic volcanics Mantle-derived basaltic -3.5 magma Granophyre -4.0 Outer limits of dike conduit Speculative intrusion direction of dolerite dike from unrecognized central volcano south or south-west of site I Part II Appendix – Paper 2

Eriksson, P.I., Riishuus, M.S., Sigmundsson, F., Elming, S.Å. (to be submitted) ’Preferred sub-horizontal dike propagation deduced from magnetic fabric analyses on regional dikes in east Iceland: Implications for shallow crustal magma transport in Icelandic volcanic systems’ Journal of Structural Geology

1 Preferred sub-horizontal dike propagation deduced from magnetic 2 fabric analyses on regional dikes in east Iceland: Implications for 3 shallow crustal magma transport in Icelandic volcanic systems

1. Per I. Eriksson a,b,∗ 2. Morten S. Riishuus a 4 3. Freysteinn Sigmundsson a 4. Sten-Åke Elming b

a 5 Afﬁliations: Nordic Volcanological Center, Institute of Earth Science, University of Iceland. Askja, Sturlugata 7, b 6 IS-101 Reykjavík, Iceland. Division of Applied Geophysics, Department of Chemical Engineering and Geosciences,

7 Luleå University of Technology, Sweden. ∗ 8 Corresponding author, e-mail: [email protected], telephone +46 ??? ??? ???.

9 November 18, 2010

10 Abstract

11 Regional maﬁc dikes extending north of the Álftafjörður central volcano in the Neogene

12 bedrock of east Iceland have been studied using anisotropy of magnetic susceptibility (AMS)

13 to deﬁne fossilized magma ﬂow regimes. Imbrication of the plane perpendicular to the minor

14 susceptibility axis has been used as ﬂow plane indicator. The dikes are parts of an elongated

15 dike swarm, 3–5 km in width and up to 40 km in length. Dike swarms are generally

16 considered to be the sub-surface continuation of ﬁssure swarms extending from central

17 volcanoes in active volcanic systems. Flow directions could be calculated in 15 of the 29

18 dikes that were sampled. The remaining dikes were discarded due to features such as parallel

19 imbrications and parallel relations between the minor axis and the dike attitude. Samples

20 were collected in dikes at varying lateral distance from the central volcano and they show

21 predominantly sub-horizontal ﬂow regimes with varying inclinations. The absolute majority

22 of the utilized dikes, 10 of 15, show a ﬂow away from the Álftafjörður central volcano. The

23 presented ﬂow directions have all been inferred to a geo-tectonic model favoring

24 predominantly lateral diking from a shallow magma chamber in order to explain the origins

25 of regional dike swarms.

27 Keywords: AMS; Iceland; dike swarm; rock magnetism; dike propagation

28 1 Introduction

29 The Mid-Atlantic-Ridge which cut across Iceland in a branched manner is revealed by the layout

30 of the presently active volcanic systems (Fig. 1). The rift segmentation is complicated by the

1 31 increased melting centered under central east Iceland. This increased melting has caused the

32 build-up of the Iceland marine plateau and the land mass. Magma movement and emplacement is

33 discontinuous and the melt is channeled into discrete volcanic systems where it may pond in deep

34 axial reservoirs near the mantle/crust-boundary, in hypabyssal sills, dikes or pipe conduits or in

35 shallow magma chambers (Sigurdsson, 1987; Lin et al., 1990; Gudmundsson, 1995; Rubin and

36 Sinton, 2007). Various models have been suggested to account speciﬁcally for crustal dilatation

37 and the role of diking. The models either favor vertical dike intrusion from axial reservoirs (e.g.

38 Walker, 1975; Gudmundsson, 1990; Tentler and Temperley, 2007), lateral intrusions from

39 shallow magma chambers (e.g. Buck et al., 2006; Paquet et al., 2007) or a combination of the two

40 (Walker, 1992).

42 In this study we present an attempt to determine ﬂow directions in Neogene regional maﬁcdikes

43 belonging to the Álftafjörður dike swarm in east Iceland. This is accomplished through the

44 interpretation of anisotropy of magnetic susceptibility (AMS) using the imbrication of the plane

45 perpendicular to the minor susceptibility axis as a proxy for the bulk mineral fabric (e.g. Knight

46 and Walker, 1988; Herrero-Bervera et al., 2001; Geoffroy et al., 2002; Aubourg et al., 2008). We

47 have sampled margins from 29 regional dikes belonging to the dike swarm northeast of

48 Álftafjörður central volcano in east Iceland. We demonstrate that the magnetic fabrics can in

49 some cases be interpreted as fossilized ﬂow directions, and present a diking model favoring

50 lateral diking from shallow magma chambers to account for the origin of regional dikes and by

51 extension ﬁssure swarms in present volcanic systems.

2 52 2 Geological background

53 Iceland is a part of the large elevated area of oceanic lithosphere situated at the junction of the

54 Mid-Atlantic-Ridge and the Greenland-Iceland-Faroe ridge (Sandwell and Smith, 2009). The

55 Icelandic Neogene bedrock is stratiﬁed and consist mainly of monotonous sequences of tholeiitic

56 or olivine-tholeiitic lava layers which dip towards the current rift zone (Saemundsson, 1979;

57 Hardarson and Fitton, 1997). The rift zones on land are parts of the Mid-Atlantic-Ridge, and the

58 rift segments can be divided into discrete volcanic systems on basis of seismic activity

59 (Einarsson, 1991). Each of these typically consists of a central volcano complex, representing the

60 maximum of volcanic production, with high-temperature geothermal ﬁelds and often a shallow

61 magma chamber and associated felsic rocks (Walker, 1964, 1966; Saemundsson, 1986). An

62 elongated ﬁssure swarm with open fractures, normal faults and linear eruptive ﬁssures generally

63 extends from the central volcano complex. It often trends obliquely to the rift segment, locally

64 the ﬁssure swarms are arranged in directions of least tensile strength of the bedrock

65 (Sigmundsson, 2006). Some volcanic systems may consist only of a central volcano complex or a

66 ﬁssure swarm. The ﬁssure swarms can overlap and are generally en echelon distributed.

68 The ﬁssure swarms are generally believed to be the upward continuation of dike swarms visible

69 with remnants of exhumed volcanic centers in the Neogene areas of east Iceland (Walker, 1974;

70 Gudmundsson, 1983; Sigurdsson, 1987; Gudmundsson, 1983; Helgason and Zentilli, 1985;

71 Tentler, 2005). Yet, dikes exposed in east Iceland are seldom seen to emanate into eruptive units

72 (Walker, 1958; Gudmundsson, 1983). The dikes and intrusions have been uncovered by glacial

73 erosion and raised by subsequent isostatic rebound of the bedrock (Geirsdóttir et al., 2007).

74 Estimations from the distribution of zeolite minerals and vertical dike frequency suggests that in

75 east Iceland the original surface was situated 1000–1500 m above present sea level (Walker,

3 76 1960, 1974; Neuhoff et al., 1999).

78 Regional dikes are numerous throughout the ﬂood basalt pile, contracted into narrow swarms

79 extending from exhumed central volcanoes. The dikes in these swarms can locally dilate the

80 bedrock with 10–20%, but an average between 2–8% is more common (Fig. 2a; Walker, 1964;

81 Paquet et al., 2007). The strike of these swarms are generally to the north-north-east (Walker,

82 1974; Gudmundsson, 1995). Geological mapping across the Álftafjörður dike swarm has shown

83 periodic peaks in the frequency of dikes, occurring with a distance of 2.5 km (Paquet et al.,

84 2007). The same periodic pattern was shown across the active Kraﬂa ﬁssure swarm, but then

85 occurring every 1.2–1.3 km (Paquet et al., 2007, and references therein). In a volcanic system

86 there is generally three types of tabular intrusives present: inclined sheets, radial dikes and

87 regional dikes (Gudmundsson, 1995; Klausen, 2006). The inclined sheets are thin, less than 10 m

88 wide, but generally much thinner. They are conﬁned around the central volcano complex from

89 which they emanate, as are the radial dikes which are sub-vertical and radiate around the magma

90 chamber. The regional dikes are often thicker (4 m on average) than the locally conﬁned dikes

91 and sheet, and are generally sub-vertical and sub-parallel (Gudmundsson, 1983).

92 2.1 Álftafjörður central volcano

93 The Álftafjörður volcano is one of several exhumed volcanic centers in east and southeast

94 Iceland. It is visible in ﬁeld as assemblages of maﬁc, intermediate and felsic lavas, pyroclastic

95 rocks minor sediments and numerous intrusions, mainly consisting of irregular pod like basaltic

96 intrusion and larger felsic bodies (Walker, 1963; Blake, 1969). The dikes extend in an orderly

97 manner north of the immediate vicinity of the central volcano, they strike NNE and have most

98 likely originated within that volcanic system while it was still active. One can however not be

4 99 absolutely certain that each dike in this swarm belong to Álftafjörður volcanic system. The

100 reasons are that no indisputable characteristic neither geophysical nor geochemical have been

101 found that enable us to discern dikes from each other, and that the ﬁssure swarms of the active

102 volcanic systems have been shown to overlap, which should by inference also include the dike

103 swarms (Einarsson, 1991). However, the locations of the nearby exhumed volcanoes in the area

104 (Fig. 2) indicate however that Álftafjörður dike swarm may overlap with only regional dikes from

105 the Reyðarfjörður central volcano, and the two exhumed centers are separated by 73 km, making

106 interference unlikely. The Breiðdalur and Þingmúli centers are offset north-west of Álftafjörður

107 and these volcanic systems are thus most unlikely to have overlapped with Álftafjörður. The

108 Álftafjörður volcanic units have not been dated, but it should be younger than the Hólmatindur

109 clastic bed horizon east of Álftafjörður which have been dated to 10.69 ± 0.14 Ma (recalculated

40 39 110 relative to the FCs monitor age of 28.02 Ma from Renne et al., 1998), using Ar/ Ar dating on

111 plagioclase from a tuff layer in the sediment horizon (Duncan and Helgason, 1998). Time

112 estimates from magneto-stratigraphic work indicate that the Álftafjörður central volcano is

113 emplaced into lavas about 9.5 Ma old (Dagley et al., 1967; Watkins and Walker, 1977; Gradstein

114 et al., 2004).

115 2.2 Field relations

116 Two major trends in the strike of the dikes can be discerned, 8 out of 29 dikes strike between

117 20–30°E, 9 out of 29 strike between 30–50°E. Four dikes strike perpendicular to this trend at

118 150–170°E, and 5 dikes strike between 0–20°E. This distribution of strikes with the two major

119 directions of ca. 25°E and 40°E is comparable to the results by Paquet et al. (2007), even if based

120 on a few number of dikes. The dikes sampled are overall micro-crystalline, but generally

121 porphyritic, albeit with low phenocrysts content (< 15%). Paquet et al. (2007) noted that some

5 122 dikes have substantially higher phenocryst content (30%). In addition to columnar jointing and

123 chilled outer margins these features indicate a shallow emplacement into a cold host rock. The

124 erosional level, as obtained by Neuhoff et al. (1999), suggests a level of maximum 1500 m below

125 the paleosurface at Þeigarhorn, in the proximity of our sampling area. The sampling sites south

126 of Berufjörður are at sea level while the sites in Breiðdalur valley are located at ca. 100 m

127 altitude. The dikes are sampled with a distance of 10 km across the dike swarm and 30 km along

128 strike. Since the lava pile has been tilted westward about 8° the westernmost dike is inferred to be

129 sampled at a crustal depth 800 m above the easternmost dike.

130 3 Theory of methods

131 3.1 Anisotropy of magnetic susceptibility

132 The magnetic susceptibility determines the degree of magnetization a rock acquires in response

133 to an applied magnetic ﬁeld. The magnetic susceptibility is mathematically described as a

134 symmetric tensor of second order. The susceptibility is nearly constant for low inducing ﬁeld

3 135 strengths (< 23.9 × 10 A/m, Tarling and Hrouda, 1993). Thus the susceptibility linearly relates

136 the induced magnetization (M), to the inducing magnetic ﬁeld (H) in a given material. M and H

137 are three dimensional vector ﬁelds and κi, j, the magnetic susceptibility tensors, in matrix entry

138 denotation i, j is deﬁned by:

Mi = κi, jHj (1)

139 The susceptibility tensor can be visualized with a magnitude ellipsoid (Nye, 1985). The

140 Nye–ellipsoid is a three-dimensional representation of the tensor elements where the principal

141 axes in the ellipsoid (κa ≥ κb ≥ κc) are determined in relative magnitude and direction by the

142 susceptibility tensor. The main axes of the magnitude ellipsoid can be plotted in a stereographic

6 143 projection. The convention in paleomagnetic and AMS research is to use lower hemisphere

144 projections (Tarling and Hrouda, 1993). In addition to the stereographic plots of the magnitude

145 ellipsoid, two scalar parameters are used to characterize the ellipsoid, the shape parameter T and

146 the corrected anisotropy degree PJ by Jelínek (1981). For a discussion on alternate parameters

147 see Cañón-Tapia (1994). The ﬁrst parameter is the shape parameter T describing the shape of the

148 ellipsoid as a scalar unit. 2(η − η ) T = b c − 1(2) ηa − ηc

149 where ηa = ln(κa), ηb = ln(κb) and ηc = ln(κc).For−1 ≤ T < 0 the magnitude ellipsoid is

150 prolate, T ≈ 0 corresponds to a spherical shape and 0 > T ≤ 1reﬂects an oblate shapes. The

151 second parameter is the corrected anisotropy degree PJ given by:

2 2 2 Pj = exp 2((ηa − ηm) +(ηb − ηm) +(ηc − ηm) ) (3)

η +η +η η = a b c 152 where m 3 . It describes the magnitude of anisotropy of the shape ellipsoid. PJ ranges

153 from 1 and upwards but do generally not exceed 1.10 (10%) for pristine rocks (Tarling and

154 Hrouda, 1993). The absolute value of magnetic susceptibility is expressed with the bulk

155 susceptibility parameter Km, which is an average of the three main susceptibilities.

κ + κ + κ K = a a c (4) m 3

156 3.2 Magma ﬂow in dikes

157 The mineral fabric in the dike is imposed by the ﬂow of magma during dike formation. Magma is

158 unlikely to cause turbulence in conduits less than 10 m wide, and is therefore expected to be

159 laminar in most dikes (Petcovic and Dufek, 2005). The laminar ﬂow regime align early forming

160 mineral grains due to mechanical interactions even at low (8%) concentrations (Komar, 1972;

161 Shelley, 1985). Regardless whether ﬂow is Newtonian, Pseudo-plastic or Binghamian, similar

7 162 shear-controlled zones of mineral alignment develop near the edges of the dike (Dragoni et al.,

163 1997; Blanchard et al., 1979). The imbricated, mineral fabric near the edges thus enables us to

164 infer the absolute direction of flow. Magma solidification preserves this initial flow-imposed

165 silicate mineral fabric if there is no if later tectonic stresses or deformations (cf. Philpotts and

166 Philpotts, 2007). The late stage growth of iron oxides and sulﬁdes, which account for the

167 ferrimagnetic properties of the rock, will spatially be controlled by the silicate fabric thus

168 reminiscing of ﬂow (Hargraves et al., 1991). Using the magnetic foliation, or the plane

169 perpendicular to the minor susceptibility axis, as a proxy of mineral foliation from both margins

170 the absolute ﬂow direction can be inferred with the line of intersection between the two

171 imbricated planes from each margin (Henry, 1997; Eriksson et al., In revision, see also Geoffroy

172 et al., 2002, 2007 for the general method).

173 4 Sampling & laboratory procedures

174 Samples from dikes belonging to the Álftafjörður central volcano have been collected in

175 Breiðdalur, Berufjörður and Hamarsfjörður in east Iceland (Fig. 2). A total of 29 dikes were

176 sampled, with an average number of 8 samples per margin from each dike (Table 1). Samples

177 were taken 8–30 cm from the chilled margin of each dike. The average thickness of the dikes is

178 5.3 m. The samples were collected as cores, obtained using a hand-held drill, and orientated

179 using sun and magnetic compasses. Laboratory analyses include measurements of the AMS, bulk

180 susceptibility and temperature-susceptibility variations using powder samples in air. The

181 measurements were done with a KLY-3S Kappabridge equipment and a CS3 furnace apparatus

182 from Advanced Geoscience Instrument Company. Natural remanence magnetization was

183 measured with a 2G-Enterprise cryogenic magnetometer. De-magnetizations were carried out

184 with alternating ﬁeld (AF) treatment. The samples were demagnetized to less than 10% of its

8 185 initial remanence, using in general maximum ﬁeld strengths of 70 mT. These analyses were

186 conducted at the Geophysical Laboratory at Luleå University of Technology, Sweden. Hysteresis

187 measurements of grains were conducted at the Department of Earth and Ecosystem Sciences,

188 Lund University, Sweden. In total hysteresis measurements were performed on 18 samples from

189 the margins of 18 separate dikes. Natural remanent magnetization strength (M0), Königsberger

190 natural ratio (Qn, Königsberger, 1938) and median destructive ﬁeld (M50, Dunlop and Özdemir,

191 1997) have been calculated. Magnetic remanence vectors have been determined by principal

192 component analysis and Fisher statistics (Fisher, 1953; Kirschvink, 1980). Granulometry of

193 magnetic grains have been estimated with the Day plot (Day et al., 1977; Dunlop, 2002)

194 5 Experimental results

195 5.1 Paleomagnetic results

196 The dikes carry two components of magnetization, one which is carried by low-coercivity

197 magnetic grains which are demagnetized at low ﬁeld strengths (<20 mT). The second, high

198 coercive remanence is interpreted as the characteristic remanent magnetization (ChRM) and has

199 been isolated in 27 of 29 sampled dikes in total (Table 2). Since the dikes most probably formed

200 when the Álftafjörður central volcano was active and thus close to the previous rift axis, it is

201 expected that tilting of the lava pile occurred mainly during emplacement (Pálmason, 1986). The

202 remanence directions will thus need to be partly or totally tilt adjusted. Two types of corrections

203 have been tested. Corrections for lava tilt to simulate horizontal emplacement of lavas using

204 average lava tilt measured by Walker (1974) and correction simulating vertical dike emplacement

205 using measured dike dip. The bootstrapped mean direction of the characteristic remanence for the

206 untilted normal polarities are 19/79, with η = 3.2° and ζ = 7.7°, and for the reverse polarity

9 207 227/-82 with η = 4.5° and ζ = 9.9°. For the lava tilt corrected, normal polarity the mean is

208 337/79, with η = 7.7° and ζ = 3.2°, and for the reverse 153/-84 with η = 9.6° and ζ = 4.3°. For

209 the dike tilt corrected, normal remanences the mean direction is 358/78 with η = 8.5° and

210 ζ = 3.6°, and for the reverse polarity 174/-81 with η = 9.6° and ζ = 5.0° (Fig. 4, for details on

211 bootstrapping see Efron and Tibshirani, 1986). Virtual geomagnetic poles (VGP) have been

212 calculated for the lava tilt corrected remanences (Table 2). The calculated of poles are generally

213 located at latitudes higher than 60°, in only 5 of 27 dikes the calculated pole latitudes fall below

214 60°, conﬁrming observations by Kristjánsson and Jonsson (2007). The latitudinal position of the

215 VGP shows a weak logarithmic relation to the intensity of magnetization subsequent to 15 mT

216 demagnetization (Fig. 5; cf. Kristjánsson, 2008)

217 5.2 Rock magnetic properties

−2 218 The maﬁc dikes are characterized by a high bulk magnetic susceptibility, in average 6.9 × 10

−2 219 SI, ranging from 1.7 − 14.7 × 10 SI, indicating that the magnetic properties of even the least

220 susceptible dike is governed by magnetite (Tarling and Hrouda, 1993). The amplitude of the

221 mean natural remanent magnetization is 6.2 A/m and the median destructive ﬁeld is in average

222 13.4 mT (ranging 3.0–28.3 mT), which indicate a dike speciﬁc grain distributions with very low

223 to intermediate coercivity. The behaviour of remanence during demagnetization show trends of

224 sigmoidal to linear to exponential shapes, indicating multi-domain grains for the latter two shapes

225 (Fig. 3). A Day plot has been produced to further delineate magnetic granulometry and it

226 indicates a magnetic grain distribution falling within the single- to pseudo-single domain range

227 for all the 18 samples analysed (Fig. 6a). In this range the magnetic granulometry consists of a

228 mixture of single- and multi-domain grains (Dunlop, 2002). This is partly in agreement with the

229 predominantly low medium destructive ﬁelds (M50; Table 2), and with the Königsberger ratios,

10 230 which for Qn > 0.5 indicate a signiﬁcant contribution to the magnetization by single-domain

231 grains (Stacey, 1974).

232

233 Curie temperatures obtained from susceptibility temperature dependency measurements reveal a

234 range of Curie points. There are two main types of heating/cooling curves observed. The ﬁrst is

235 characterized by one to three phases with clear Curie points between 500–580 °C, interpreted as

236 magnetite (Fig. 7a). The second type shows a more or less distinct loss of susceptibility

237 (20–50%) at ca. 350, 400 or 500 °C as well as additional phases near 580 °C (Fig. 7b). A fraction

238 of the magnetization remains at temperatures higher than 580 °C, with Curie point at ca. 620 °C.

239 There are also a few cases with very low Curie points where the mineral(s) thereby represented

240 yield(s) most of the susceptibility (Fig. 7c). The cooling curves are all irreversible yielding

241 substantially lower susceptibilities, indicating mineral alteration during heating. The Curie

242 temperatures indicate that titanomagnetite with varying composition (0% < Ti < 10%) is the

243 main magnetic mineral, maghemite (Tc = 350 and 620 °C) is also common. Titanomagnetite with

244 higher titanium content (10% < Ti < 30%) seems to be preserved in some cases

245 (400 < Tc < 500°C). Regarding which mineral(s) are reﬂected by the low Curie temperatures, no

246 decisive answer can be given.

247 5.3 Anisotropy of magnetic susceptibility

248 The susceptibility tensor for each margin of the 29 dikes is characterized by a mean corrected

249 anisotropy degree of 1.05, ranging between 1.00–1.50 (Table 3). Such anisotropy degrees indicate

250 everything from predominantly low fabric strengths, i.e. a spherical susceptibility ellipsoid shape,

251 to fabric strengths comparable to high-grade metamorphosed rocks, i.e. acutely shaped ellipsoids

252 (Tarling and Hrouda, 1993). High PJ values are here anomalous in only 5 of 58 sampled margins,

11 253 with a degree of anisotropy higher than 1.10 (Fig. 8). The shapes of the susceptibility ellipsoid

254 range from being strongly prolate (T = −0.68) to strongly oblate (T = 0.94). The majority of

255 sampled dike margins (37 of 58) are oblate with a low (PJ<1.10) anisotropy degree.

256

257 The ﬂow directions have been obtained by calculating and bootstrapping the line of intersection

258 between the magnetic foliation planes deﬁned as the planes whose poles are the minor axes of the

259 east and west margins respectively (Constable and Tauxe, 1990; Henry, 1997; Eriksson et al., In

260 revision). Each margin has been treated separately, the intersection line has been calculated from

261 a margin pair created through mirroring one of the sides against the dike plane. If two natural

262 margins are present the ﬂow direction results from both margins are compared and averaged. In

263 order for the calculations to be sound the fabric of each margin must fulﬁl some criteria. (i) The

264 margin fabric should preferably be oblate, or have a well deﬁned grouping of the minor axes. (ii)

265 The imbrication angles to the dike plane should be sound, i.e deviate 45° from the dike attitude

266 (Tauxe et al., 1998). (iii) The foliation planes must if both margins pass the prior requirements

267 (i–ii) be symmetric against the dike plane, i.e. be imbricated towards each other and not be

268 sub-parallel. If these requirements are not met, no ﬂow determination can be made from the data.

269 A graphical guide to the selection process is given in Figure 9. Examples of obtained magnetic

270 fabrics are presented in Figure 10.

271

272 The magnetic fabrics presented in Table 3 (and Fig. 10) show that in 14 of 29 dikes both margins

273 fulﬁll requirements (i) and (ii). In another 8 dikes one of the margins fulﬁl requirements (i) and

274 (ii). For the 14 dikes where both margins fulﬁlled requirements (i) and (ii), requirement (iii) also

275 apply. Closer examination shows however that only 7 of these 14 dikes have sub-symmetric

276 magnetic fabrics and are eligible for ﬂow determination. Therefore interpretation of ﬂow is

12 277 possible in only 15 out of 29 dikes in total, 7 where both margins are used and 8 where only one

278 margin is used for determination. Parallel magnetic fabrics were found in 7 dikes, the remaining

279 had various types of inverse fabrics and were likewise discarded. The results from the

280 intersection line calculation on the 15 eligible dikes are presented in Table 4. The ﬂow directions

281 in the 15 dikes analysed using the intersection line show predominantly shallow ﬂows, 12 of 15

282 dikes have a inclination of ﬂow, above or below the horizon of less than 36°. Of these horizontal

283 ﬂows 10 ﬂow from south to north, the remaining two have adverse directions. The three

284 high-inclination flows show one upwards directed vertical flow and two with flows from north to

285 south with inclinations above 66°over the horizon.

286 6 Discussion

287 The discussion will ﬁrst treat the rock magnetic mineralogy and the remanent magnetization, then

288 the magnetic granulometry, the magnetic fabrics and their interpretation as ﬂow, then ﬁeld

289 relations and ﬁnally discuss diking model implications given by the ﬂow interpretation.

290 6.1 Rock magnetism and magnetization

291 The magnetic mineralogy has been inferred from Curie temperatures. In addition to the high

292 values of susceptibility it seems plausible that the higher Curie temperatures (∼580°C) deﬁned in

293 the dikes should reﬂect titanomagnetite grains with very low Ti–content. The somewhat lower

294 Curie temperatures (400 < Tc < 520°C) may be attributed to cooling rates of the dikes in

295 question. In a relatively slow cooling body such as a thick dike (>10 m) the titanomagnetite

296 should exsolve to the respective end-members, magnetite and ilmenite. In the thin dikes (<1.8 m)

297 the original composition should be preserved (60% Ti) according to Petersen (1976). It is

298 therefore likely that the margin samples from our dikes preserve partially exsolved

13 299 titanomagnetite. Curie temperatures around 350°C could indicate maghemite, or Ti–rich

300 titanomagnetite. Maghemite is a common mineral in Icelandic basalt and formed due to low

301 temperature oxidation of primary titanomagnetite (Steinthorsson et al., 1992). The occurrence of

302 magnetite(s) and maghemite ensures that the anisotropy of magnetic susceptibility is governed by

303 shape anisotropy and not crystallographic properties (Tarling and Hrouda, 1993; Borradaile and

304 Jackson, In press, corrected proof).

305

306 The characteristic remanent magnetization (ChRM) were tilt-adjusted using two techniques. The

307 lava tilt correction are favored since it yields normal magnetization which strike northwest and

308 reverse magnetization which strike southeast (Fig. 4). Since Iceland has remained fairly

309 stationary in the north Atlantic (Lawver and Müller, 1994), and given that the axis of the

310 geomagnetic dipole has remained fairly stable since the Neogene it is expected the magnetic

311 remanences from the rocks should line up with the westward magnetic declination. The majority

312 of the acquired remanences are normally magnetized (19N and 8R). If the emplacement age of

313 Álftafjörður central volcano is correctly estimated to be slightly younger than 9.5 Ma, the

314 majority of dikes could belong to the C4An polarity interval (8.8–9.15 Ma, Gradstein et al.,

315 2004).

316

317 The magnetic granulometry and thus stability of the remanent magnetization is not trivial to infer.

318 The Day plot and the hysteresis curves all indicated single-domain type granulometry (Fig. 6 and

319 7). The high Königsberger ratios support this but not the demagnetization curves of the dikes

320 which yielded exponential to pseudo-exponential decrease in magnetization. In addition only a

321 few dikes, 4 of 29, have medium destructive ﬁelds above 20 mT, implying that the bulk of the

322 magnetization is carried by large low-coercivity grains for those dikes (Dunlop and Özdemir,

14 323 1997). Two problems arise from this. If the magnetic properties are governed by single-domain

324 grains the magnetic fabrics will likely be inverse, (Potter and Stephenson, 1988; Rochette et al.,

325 1992), and thus not reﬂect the petrofabric correctly. If large multi-domain grains govern the

326 magnetic properties the remanent magnetization will be susceptible to change over short

327 geological times. Regarding the latter problem the vector analysis has revealed two components

328 of remanence in 27 of 29 dikes, with semi-independent coercivity spectra where a high coercivity

329 component is isolated in ﬁelds ≥20 mT. It is not likely that dikes have been reheated at

330 temperatures above or close to the Curie temperatures, thus erasing the previous magnetization,

331 and the samples show no conspicuous signs of high temperature alteration. Detailed petrographic

332 analyses are required to ﬁrmly establish this. However, since a two component magnetization

333 was found, the original magnetization should be preserved in the high coercivity range, even if no

334 pseudo- or single-domain are present.

335 6.2 AMS and fabric interpretations

336 In only 7 of 29 dikes the requirements for calculation of ﬂow direction were satisﬁed in both

337 margins, and in several of these dikes the directions obtained differed in inclination (Table 4).

338 The angular differences could be the result of faulty strike measurements of the dikes, which are

339 sometimes difﬁcult to perform accurately, or naturally occurring irregularities. The large number

340 of margins not satisfying the requirements of oblate-type fabrics and small imbrication angles is

341 troublesome. Inverse fabrics are common and were observed by Kissel et al. (2010) who did a

342 similar study further north in Reyðarfjörður. Kissel et al. (2010) noted that the inverse type

343 fabrics were transformed into normal fabric when heated and concluded that the inverse fabrics

344 were held by large magnetite grains whereas the normal fabrics were held by small grains in the

345 single- to pseudo-single domain range (Rochette et al., 1992; Kissel et al., 2010). Observe that

15 346 this is the adverse behaviour as would be expected if single-domain grains governed the magnetic

347 fabric (Potter and Stephenson, 1988). The results from the hysteresis measurements, which

348 indicated that the grains were likely in single-domain size, can be compared with the occurrence

349 of inverse fabrics. The comparison shows that in 8 of the 19 margins were hysteresis analyses

350 were carried out the fabric were inverse, the remaining were normal (cf. Table 2 and Table 3).

351 Therefore single-domain grains cannot be coupled to the troublesome inverse types fabric in this

352 dike suite. The explanation model proposed by Kissel et al. (2010) needs to be fully tested but

353 may explain our inverse type fabrics, whereas it can not explain the parallel type fabrics. It was

354 noted in a study on Brazilian dikes that a likely cause of parallel imbrication may be due to

355 trans-tensional dike openings (Lefort et al., 2006). Shear induced fabrics in dikes have been

356 investigated and found elsewhere (Féménias et al., 2004; Yamamoto, 2006; Nagaraju et al., 2008).

357 The ﬂow fabric are themselves shear fabrics, so it is not impossible that different generations of

358 tectonic stress may have been imposed on the dike prior to solidiﬁcation. Gudmundsson (1983)

359 has proposed that dikes are preceded by en echelon distributed fractures that combine and form

360 the dike body once magma is intruded. This would imply a trans-tensional stress regime at the

361 dike end. Contrary Paquet et al. (2007), who studied dikes around Álftafjörður and Berufjörður,

362 found that there were no major offset in the lava pile from one side to the other of the dike. They

363 proposed that the dike opening should have been orthogonal and not transtensive.

364

365 We propose that the parallel disposition of the magnetic fabrics in some of our dikes indicate a

366 trans-tensional dike opening, albeit small. We have not studied possible offset of the host rock

367 across the dike, but even if such offset is not visible AMS should still reﬂect small changes in the

368 stress ﬁeld. Notably, all but one of the dikes with trans-tensional fabrics fall along a straight line

369 spanning between dike C-2 to C-28 (Fig. 11). This line may have represented the trend of a

16 370 regional shear zone imposing the parallel type fabrics on the dikes.

371 6.3 Field relations

372 The success ratio in determining ﬂow direction can be related to the strike of the dikes in question

373 (Fig. 12). Dikes which did not pass the requirements for ﬂow calculation (requirement i and ii for

374 at least one margin) can be found amongst those dikes striking between 0–20°E (4 of 5 of these

375 dikes failed), at ca. 40°E (5 of 9 dikes failed) and between 150–170°E (3 of 4 dikes failed).

376 Paquet et al. (2007) interpreted the strike of the regional dikes at 40°E to be a cause of local

377 perturbation of the regional stress ﬁeld by the central volcano at Álftafjörður. They also

378 interpreted the strike direction at 25°E to relate to the regional extensive stress ﬁeld, i.e. that of

379 the overall crustal extension. (Paquet et al., 2007) interprets the deviation from the trend at 25°E

380 as consistent with a genesis of the dike swarm through lateral diking. They support the statement

381 with the occurrence of phenocrysts in the dikes, which could indicate that the magma has been

382 allowed to cool prior to eruption which is more consistent with an origin in a shallow magma

383 chamber than in a mantle reservoir. It is noteworthy that the majority of dikes which did not yield

384 any ﬂow in this study, strike at other directions than at 25°E. This may indicate that complicated

385 tectonic stress are recorded in these dikes due to them being in an oblique position to the regional

386 trend of least tensile strength.

387

388 Since the lava pile tilt, which is noted in the geology section, the westernmost dikes should be

389 sampled at ca. 800 m above the easternmost dikes. It can be speculated that these dikes should

390 reveal steeper ﬂow directions, i.e. that the magma at the upper part of the dikes would have

391 travelled to the (near) surface since these sampling site are closer to it. But the western-most

392 dikes, C-1,10 and C-29 all have very low ﬂow inclinations (Fig 11).

17 393 6.4 Comparison with other studies and implications of ﬂow

394 The ﬂow directions obtained in this study can be compared to those of Kissel et al. (2010), who

395 studied dikes in the proximity of the Reyðarfjörður central volcano. Kissel et al. (2010) used the

396 major susceptibility axis as a direct proxy to ﬂow direction in the dikes, and concluded that the

397 ﬂow directions all were vertical. Kissel et al. (2010) speculates in that if lateral propagation of

398 dikes took place as shown by e.g. Einarsson and Brandsdottir (1978); Sigurdsson and Sparks

399 (1978); Brandsdóttir and Einarsson (1979) and in this article, it must have been active at greater

400 depths in the lava pile. Another explanation might be considered. At the proximity of a central

401 volcano the propagation direction could be sub-vertical above the volcano, ﬂattening out as the

402 dike propagates further away from it. This mode of dike propagation is not in conﬂict with the

403 models which explain regional diking as a magma chamber driven process (Buck et al., 2006;

404 Paquet et al., 2007). Craddock et al. (2008) who sampled 13 maﬁc dikes spread across the west

405 and east fjords also concluded, using the major susceptibility axis to infer ﬂow, vertical dike

406 propagation. Kissel et al. (2010) did not discuss the origin of the dikes in respect to the two

407 models presented in the introduction whereas Craddock et al. (2008) seems to support the

408 reservoir model in their discussion. There is another fundamental difference between this study

409 and that of Kissel et al. (2010) and Craddock et al. (2008), the way to infer ﬂow. If we would use

410 the major axis in this study we would likewise ﬁnd a number of fabrics interpretable as vertical

411 ﬂow, but also horizontal (using the major axis, Table 3). The ﬂow regime obtained is thus not

412 completely dependent on which method is used to infer it.

413

414 If the flow directions indicated by the intersection lines reflect ancient magma flow regimes they

415 have tectonic implications. In total, absolute ﬂow direction were obtained from 15 dikes, most of

416 which were directed sub-horizontally (Table 4). It is noteworthy that of the obtained ﬂow

18 417 directions is that only one single dike of the 15 dikes where ﬂow determinations was possible to

418 obtain, show a sub-vertical propagation direction. The other can be classiﬁed as either inclined or

419 shallow. The magma propagation directions in the regional dikes sampled thus strongly indicate a

420 possible origin in a shallow magma chamber at the Álftafjörður central volcano as the majority

421 (10 out of 15) move away from the volcano. The downward inclined ﬂows can possibly be

422 explained if dikes are allowed crenulated upper parts or complicated ﬂow patterns within the dike

423 body as suggested by Gudmundsson (1984). A smooth large scale crenellation would force

424 magma ﬂow up and down as the dike propagates (Fig. 13a). Steep wedges at the upper margin

425 would not cause this behavior, but form stagnant areas with no ﬂow. The high inclination ﬂows

426 are particularly interesting, since two of them ﬂow from north to south. If a ﬁssure eruption

427 should occur, as envisioned by Paquet et al. (2007), magma would ﬂow towards the ﬁssure from

428 both sides in the lobe-like dike body, potentially with high inclinations (Fig. 13). The dike with

429 the vertical ﬂow is either a dike intruding vertically from below or just below a ﬁssure eruption.

430 Another explanation for the ﬂows from north to south, including both shallow and steep

431 directions, 4 in total, may be that they belong to the Reyðarfjörður volcanic system. This is

432 however unlikely due to the distance between the systems (73 km). The majority of ﬂows are

433 shallow and seems possible to infer to the shallow magma chamber diking model. This model

434 attribute the regional dikes sampled in the area to the Álftafjörður volcanic system, which is in

435 agreement with results from Sigurdsson (1987); Gudmundsson (1984); Buck et al. (2006) and

436 Paquet et al. (2007).

437 7 Conclusions

438 1. The magnetic mineralogy of the maﬁc dikes are governed by titanomagnetite ranging from

439 pure magnetite to 20-30% Ti–substituted magnetite. There is some ambiguity in the

19 440 presence of maghemite or Ti–rich titanomagnetite, but at lest one of these minerals are

441 common in the sampled dikes.

442 2. The 15 dikes whose magnetic fabric(s) passed the criteria for determination of absolute

443 ﬂow direction, inferred from the intersection line, indicate that the majority, 10 out of 15

444 dikes, were intruded with shallow inclinations from the Álftafjörður central volcano.

445 3. The major trends in strike of the collected dikes is similar to those presented by Paquet

446 et al. (2007). Notably the dikes which failed to give ﬂow direction had strikes which were

447 interpreted by Paquet et al. (2007) as either being caused by local perturbation of the

448 regional stress ﬁeld by the Álftafjörður magma chamber, or which were oblique to the

449 regional stress ﬁeld. Dikes in the Álftafjörður volcanic system which are likely to retain

450 ﬂow imposed fabrics can thus possibly be found amongst those who strike at

451 approximately 25°N.

452 4. An explanation for the common inverse type fabric were not found and for the two prior

453 conclusions to be established further study is required to examine whether the minor

454 susceptibility axis is reliably correlated to silicate mineral foliation.

455 8 Acknowledgements

456 Birgir V. Óskarsson and Þorsteinn Jónsson (Háskóla Íslands) is acknowledged for assistance in

457 ﬁeld and Leó Kristjánsson (Háskóla Íslands) for instrumental aid. Rósa Ólafsdóttir (Háskóla

458 Íslands) is acknowledged for preparing maps to the authors. Thongchai Suteerasak (Luleå

459 University of Technology) is thanked for performing hysteresis measurements on grains for the

460 authors.

20 461 References

462 Aubourg, C., Tshoso, G., Le, Gall, B., Bertrand, H., Tiercelin, J.J., Kampunzu, A., Dyment, J., Modisi, M., 2008.

463 Magma ﬂow revealed by magnetic fabric in the Okavango giant dyke swarm, Karoo igneous province, northern

464 Botswana. Journal of Volcanology and Geothermal Research 170, 247–261.

465 Blake, D.H., 1969. Welded tuffs and the Mælifell caldera, Älftafjörður volcano, south-eastern Iceland. Geological

466 Magazine 106, 531–541.

467 Blanchard, J.P., Boyer, P., Gagny, C., 1979. Un nouveau critere de sens de mise en place dans une caisse ﬁlonienne:

468 Le "pincement" des mineraux aux epontes: Orientation des minéraux dans un magma en écoulement.

469 Tectonophysics 53, 1–25.

470 Borradaile, G.J., Jackson, M., In press, corrected proof. Structural geology, petrofabrics and magnetic fabrics (AMS,

471 AARM, AIRM). Journal of Structural Geology .

472 Brandsdóttir, B., Einarsson, P., 1979. Seismic activity associated with the September 1977 deﬂation of the Kraﬂa

473 central volcano in northeastern Iceland. Journal of Volcanology and Geothermal Research 6, 197–212.

474 Buck, R.W., Einarsson, P., Brandsdóttir, B., 2006. Tectonic stress and magma chamber size as controls on dike

475 propagation: Constraints from the 1975–1984 Kraﬂa rifting episode. Journal of Geophysical Research 111,

476 B12404.

477 Cañón-Tapia, E., 1994. Anisotropy of magnetic susceptibility parameters: Guidelines for their rational selection. Pure

478 and Applied Geophysics 142, 365–382.

479 Chadima, M., Hrouda, F., 2006. Remasoft 3.0 a user-friendly paleomagnetic data browser and analyzer. Travaux

480 Géophysiques XXVII, 20–21.

481 Constable, C., Tauxe, L., 1990. The bootstrap for magnetic susceptibility tensor. Journal of Geophysical Research 95,

482 8383–8395.

483 Cox, A., Doell, R.R., 1960. Review of paleomagnetism. Geological Society of America Bulletin 71, 645–768.

484 Craddock, J.P., Kennedy, B.C., Cook, A.L., Pawlisch, M.S., Johnston, S.T., Jackson, M., 2008. Anisotropy of magnetic

485 susceptibility studies in Tertiary ridge-parallel dykes (Iceland), Tertiary margin-normal Aishihik dykes (Yukon),

486 and Proterozoic Kenora-Kabetogama composite dykes (Minnesota and Ontario). Tectonophysics 448, 115–124.

487 Dagley, P., Wilson, R.L., Ade-Hall, J.M., Walker, G.P.L., Haggerty, S.E., Sigurgeirsson, T., Watkins, N.D., Smith, P.J.,

488 Edwards, J., Grasty, R.L., 1967. Geomagnetic polarity zones for Icelandic lavas. Nature 216, 25–29.

489 Day, R., Fuller, M., Schmidt, V.A., 1977. Hysteresis properties of titanomagnetites: Grain-size and compositional

490 dependence. Physics of the Earth and Planetary Interiors 13, 260–267.

491 Dragoni, M., Lanza, R., Tallarico, A., 1997. Magnetic anisotropy produced by magma ﬂow: Theoretical model and

492 experimental data from Ferrar dolerite sills (Antarctica). Geophysical Journal International 128, 230–240.

493 Duncan, R.A., Helgason, J., 1998. Precise dating of the Holmatindur cooling event in eastern Iceland: Evidence for

494 mid–Miocene bipolar glaciation. Journal of Geophysical Research 103, 12397–12404.

495 Dunlop, D.J., 2002. Theory and application of the Day plot (mrs/ms versus hcr/hc) 1. theoretical curves and tests 496 using titanomagnetite data. Journal of Geophysical Research 107, 2056–2077.

497 Dunlop, D.J., Özdemir, Ö., 1997. Rock Magnetism. Cambridge University Press.

498 Efron, B., Tibshirani, R., 1986. Bootstrap methods for standard errors, conﬁdence intervals, and other measures of

499 statistical accuracy. Statistical Science 1, 54–75.

21 500 Einarsson, P., 1991. Earthquakes and present-day tectonism in Iceland. Tectonophysics 189, 261–279.

501 Einarsson, P., Brandsdottir, B., 1978. Seismological evidence for Lateral magma intrusion during the July 1978

502 deﬂation of the Kraﬂa volcano in NE-Iceland. University of Iceland, Reykjavik.

503 Eriksson, P., Riishuus, M.S., Sigmundsson, F., Elming, S.Å., In revision. Magma ﬂow directions inferred from ﬁeld

504 evidence and magnetic fabric studies of the Streitishvarf composite dike, East Iceland. Journal of Volcanology and

505 Geothermal Research .

506 Féménias, O., Diot, H., Berza, T., Gauffriau, A., Demaiffe, D., 2004. Asymmetrical to symmetrical magnetic fabric of

507 dikes: Paleo-ﬂow orientations and paleo-stresses recorded on feeder-bodies from the Motru dike swarm (Romania).

508 Journal of Structural Geology 26, 1401–1418.

509 Fisher, R., 1953. Dispersion on a sphere. Proceedings of the Royal Society of London, Series A 217, 295–305.

510 Geirsdóttir, Ä., Miller, G.H., Andrews, J.T., 2007. Glaciation, erosion, and landscape evolution of Iceland. Journal of

511 Geodynamics 43, 170–186.

512 Geoffroy, L., Aubourg, C., Callot, J.P., Barrat, J.A., 2007. Mechanisms of crustal growth in large igneous provinces:

513 The north Atlantic province as a case study. Geological Society of America, Special Papers 430, 747–774.

514 Geoffroy, L., Callot, J.P., Aubourg, C., Moreira, M., 2002. Magnetic and plagioclase linear fabric discrepancy in

515 dykes: A new way to deﬁne the ﬂow vector using magnetic foliation. Terra Nova 14, 183–190.

516 Gradstein, F.M., Ogg, J.G., Smith, A.G., Bleeker, W., Lourens, L.J., 2004. A new Geologic Time Scale, with special

517 reference to Precambrian and Neogene. volume 27(2).

518 Gudmundsson, A., 1983. Form and dimensions of dykes in eastern Iceland. Tectonophysics 95, 295–307.

519 Gudmundsson, A., 1984. Formation of dykes, feeder-dykes, and the intrusion of dykes from magma chambers.

520 Bulletin of Volcanology 47, 537–550.

521 Gudmundsson, A., 1990. Emplacement of dikes, sills and crustal magma chambers at divergent plate boundaries.

522 Tectonophysics 176, 257–275.

523 Gudmundsson, A., 1995. Infrastructure and mechanics of volcanic systems in Iceland. Journal of Volcanology and

524 Geothermal Research 64, 1–22.

525 Hardarson, B.S., Fitton, G.J., 1997. Mechanisms of crustal accretion in Iceland. Geology 25, 1043–1046.

526 Hargraves, R.B., Johnson, D., Chan, C.Y., 1991. Distribution anisotropy: The cause of AMS in igneous rocks ?

527 Geophysical Research Letters 18, 2193–2196.

528 Helgason, J., Zentilli, M., 1985. Field characteristics of laterally emplaced dikes: Anatomy of an exhumed Miocene

529 dike swarm in Reydarfjördur, Eastern Iceland. Tectonophysics 115, 247–274.

530 Henry, B., 1997. The magnetic zone axis: A new element of magnetic fabric for the interpretation of the magnetic

531 lineation. Tectonophysics 271, 325–331.

532 Herrero-Bervera, E., Walker, G.P.L., Cañón-Tapia, E., Garcia, M.O., 2001. Magnetic fabric and inferred ﬂow direction

533 of dikes, conesheets and sill swarms, Isle of Skye, Scotland. Journal of Volcanology and Geothermal Research 106,

534 195–210.

535 Jelínek, V., 1981. Characterization of the magnetic fabric of rocks. Tectonophysics 79, T63–T67.

536 Jóhannesson, H., Sæmundsson, K., 1998. Geological map of Iceland, 1:50 000, bedrock geology. Icelandic Institute of

537 Natural History, Reykjavík 2nd ed.

22 538 Kirschvink, J., 1980. The least-squares line and plane and the analysis of paleomagnetic data. The Geophysical

539 Journal of the Royal Astronomical Society 62, 699–718.

540 Kissel, C., Laj, C., Sigurdsson, H., Guillou, H., 2010. Emplacement of magma in Eastern Iceland dikes: Insights from

541 magnetic fabric and rock magnetic analyses. Journal of Volcanology and Geothermal Research 191, 79–92.

542 Klausen, M.B., 2006. Geometry and mode of emplacement of dike swarms around the Birnudalstindur igneous centre,

543 SE Iceland. Journal of Volcanology and Geothermal Research 151, 340–356.

544 Knight, M.D., Walker, G.P.L., 1988. Magma ﬂow directions in dikes of the Koolau complex, Oahu, determined from

545 magnetic fabric studies. Journal of Geophysical Research 93, 4301–4319.

546 Komar, P.D., 1972. Mechanical interactions of phenocrysts and ﬂow differentiation of igneous dikes and sills.

547 Geological Society of America Bulletin 83, 973–988.

548 Königsberger, J.G., 1938. Natural residual magnetism of eruptive rocks. Terrestrial Magnetism and Atmosspheric

549 Electricity 43, 119–130, 299–320.

550 Kristjánsson, L., 2008. Paleomagnetic research on Icelandic lava ﬂows. Jökull 58, 101–116.

551 Kristjánsson, L., Jonsson, G., 2007. Paleomagnetism and magnetic anomalies in Iceland. Journal of Geodynamics 43,

552 30–54.

553 Lawver, L.A., Müller, R.D., 1994. Iceland hotspot track. Geology 22, 311–314.

554 Lefort, J.P., Aïfa, T., Hervé, F., 2006. Structural and AMS study of a Miocene dyke swarm located above the

555 Patagonian subduction, in: Hanski, Mertanen, Rämö, Vuollo (Eds.), Dyke swarms: time markers of crustal

556 evolution. Taylor & Francis, pp. 225–241.

557 Lin, J., Purdy, G.M., Schouten, H., Sempere, J.C., Zervas, C., 1990. Evidence from gravity data for focused magmatic

558 accretion along the Mid-Atlantic Ridge. Nature 344, 627–632.

559 Nagaraju, J., Chetty, T., Prasad, G.V., Patil, S., 2008. Transpressional tectonics during the emplacement of

560 Pasupugallu gabbro pluton, western margin of eastern Ghats mobile belt, India: Evidence from AMS fabrics.

561 Precambrian Research 162, 86–101.

562 Neuhoff, P.S., Fridriksson, T., Arnorsson, S., Bird, D.K., 1999. Porosity evolution and mineral paragenesis during

563 low-grade metamorphism of basaltic lavas at Teigarhorn, Eastern Iceland. American Journal of Science 299(6),

564 467–501.

565 Nye, J.F., 1985. Physical properties of crystals: Their representation by tensors and matrices. Oxford University Press.

566 Pálmason, G., 1986. Model of crustal formation in Iceland, and application to submarine mid-ocean ridges, in: Vogt,

567 P.R., Tucholke, B.E. (Eds.), The geology of North America, Volume M. Geological Society of America, pp. 87–97.

568 Paquet, F., Dauteuil, O., Hallot, E., Moreau, F., 2007. Tectonics and magma dynamics coupling in a dyke swarm of

569 Iceland. Journal of Structural Geology 29, 1477–1493.

570 Petcovic, H.L., Dufek, J.D., 2005. Modeling magma ﬂow and cooling in dikes: Implications for emplacement of

571 Columbia river ﬂood basalts. Journal of Geophysical Research 110, ARTN B10201.

572 Petersen, N., 1976. Notes on the variation of magnetization within basalt lava ﬂows and dikes. Pure and Applied

573 Geophysics 114, 177–193.

574 Philpotts, A.R., Philpotts, D.E., 2007. Upward and downward ﬂow in a camptonite dike as recorded by deformed

575 vesicles and the anisotropy of magnetic susceptibility (AMS). Journal of Volcanology and Geothermal Research

576 161, 81–94.

23 577 Potter, D.K., Stephenson, A., 1988. Single-domain particles in rocks and magnetic fabric analysis. Geophysical

578 Research Letters 15, 1097–1100.

579 Renne, P.R., Swisher, C.C., Deino, A.L., Karner, D.B., Owens, T.L., DePaolo, D.J., 1998. Intercalibration of 40 39 580 standards, absolute ages and uncertainties in ar/ ar dating. Chemical Geology 145, 117–152.

581 Rochette, P., Jackson, M., Aubourg, C., 1992. Rock magnetism and the interpretation of anisotropy of magnetic

582 susceptibility. Reviews of Geophysics 30, 209–226.

583 Rubin, K.H., Sinton, J.M., 2007. Inferences on mid–ocean ridge thermal and magmatic structure from MORB

584 compositions. Earth and Planetary Science Letters 260, 257–276.

585 Saemundsson, K., 1979. Outline of the geology of Iceland. Jökull 29, 7–28.

586 Saemundsson, K., 1986. Subaerial volcanism in the western north atlantic, in: Vogt, P.R., Tucholke, B.E. (Eds.), The

587 Geology of North America, Volume M, The Western North Atlantic Region. Geological Society of America, pp.

588 69–86.

589 Sandwell, D.T., Smith, W.H.F., 2009. Global marine gravity from retracked Geosat and ERS-1 altimetry: Ridge

590 segmentation versus spreading rate. Journal of Geophysical Research 114, B01411.

591 Shelley, D., 1985. Determining paleo-ﬂow directions from groundmass fabrics in the Lyttelton radial dykes, New

592 Zealand. Journal of Volcanology and Geothermal Research 25, 69–79.

593 Sigmundsson, F., 2006. Iceland Geodynamics – Crustal Deformation and Divergent Plate Tectonics. Springer Verlag.

594 Sigurdsson, H., 1987. Dyke injection in Iceland: A review, in: Halls, H.C., Fahrig, W.F. (Eds.), Maﬁc dyke swarms,

595 Geological Association of Canada Special Paper 34, pp. 55–64.

596 Sigurdsson, H., Sparks, S.R.J., 1978. Lateral magma ﬂow within rifted Icelandic crust. Nature 274, 126–130.

597 Stacey, F.D., 1974. The physical principles of rock magnetism. Elsevier.

598 Steinthorsson, S., Helgason, Ö., Madsen, M.B., Bdener, K.C., Bentzon, M.D., Mørup, S., 1992. Maghemite in

599 Icelandic basalts. Mineralogical Magazine 56, 185–199.

600 Tarling, D.H., Hrouda, F., 1993. The magnetic anisotropy of rocks. Chapman & Hall, London.

601 Tauxe, L., 2010. PMAGPY 2.41 Software package. Scripps Institution of Oceanography, San Diego, U.S.A.

602 Tauxe, L., Gee, J.S., Staudigel, H., 1998. Flow directions in dikes from anisotropy of magnetic susceptibility data: The

603 bootstrap way. Journal of Geophysical Research 103, 17775–17790.

604 Tentler, T., 2005. Propagation of brittle failure triggered by magma in Iceland. Tectonophysics 406, 17–38.

605 Tentler, T., Temperley, S., 2007. Magmatic ﬁssures and their systems in Iceland: A tectonomagmatic model. Tectonics

606 26, ARTN TC5019.

607 Walker, G.P.L., 1958. Geology of the Reyðarfjörður area, Eastern Iceland. Quarterly Journal of the Geological Society

608 of London 114, 367–391.

609 Walker, G.P.L., 1960. Zeolite zones and dike distributions in relation to the structure of the basalts of Eastern Iceland.

610 Journal of Geology 68, 515–528.

611 Walker, G.P.L., 1963. The Breidðalur central volcano, Eastern Iceland. Quarterly Journal of the Geological Society of

612 London 119, 29–63.

613 Walker, G.P.L., 1964. Geological investigations in Eastern Iceland. Bulletin of Volcanology 27, 351–363.

24 614 Walker, G.P.L., 1966. Acid volcanic rocks in Iceland. Bulletin of Volcanology 29, 375–402.

615 Walker, G.P.L., 1974. The structure of Eastern Iceland, in: Krístjansson, L. (Ed.), Geodynamics of Iceland and the

616 North Atlantic Area, NATO Advanced Study Institutes Series, Volume C11. Reidel Publishing Company, Holland,

617 Dordrecht, pp. 177–188.

618 Walker, G.P.L., 1975. Intrusive sheet swarms and the identity of crustal layer 3 in Iceland. Journal of the Geological

619 Society 131, 143–161.

620 Walker, G.P.L., 1992. "coherent intrusion complexes" in large basaltic volcanoes – a new structural model. Journal of

621 Volcanology and Geothermal Research 50, 41–54.

622 Watkins, N.D., Walker, G.P.L., 1977. Magnetostratigraphy of Eastern Iceland. American Journal of Science 277,

623 513–584.

624 Yamamoto, Y., 2006. Systematic variation of shear-induced physical properties and fabrics in the Miura-Boso

625 accretionary prism: The earliest processes during off-scraping. Earth and Planetary Science Letters 244, 270–284.

25 Name n Width (m) Extent Strike/Dip Lava tilt Latitude Longitude ◦ ◦ ◦ ◦ ◦ ◦ C-I 17 15.6 >100m 45 a/90 186 /11 64 48’58” -15 39’18” ◦ ◦ ◦ ◦ ◦ ◦ C-II 14 4.7 <20m 15 /80 184 /8 64 47’49” -15 46’55” ◦ ◦ ◦ ◦ ◦ ◦ C-III 14 6.8 ∼50m 35 /85 184 /8 64 47’38” -15 47’17” ◦ ◦ ◦ ◦ ◦ ◦ C-IV 14 4 <20m 350 /85 184 /8 64 47’38” -15 47’17” ◦ ◦ ◦ ◦ ◦ ◦ C-V 14 6 <20m 350 /85 184 /8 64 46’12” -15 53’10” ◦ ◦ ◦ ◦ ◦ ◦ C-VI 17 4 ∼50m 205 /90 184 /8 64 46’12” -15 53’10” ◦ ◦ ◦ ◦ ◦ ◦ C-VII 14 2.2 <20m 45 /70 184 /8 64 45’0” -15 32’53” ◦ ◦ ◦ ◦ ◦ ◦ C-VIII 16 3.9 <20m 45 /85 174 /8 64 44’6” -14 0’50” ◦ ◦ ◦ ◦ ◦ ◦ C-IX 13 18.5 >100m 20 a/85 184 /8 64 43’55” -14 0’54” ◦ ◦ ◦ ◦ ◦ ◦ C-X 14 7.2 <20m 255 /90 174 /8 64 43’19” -15 35’56” ◦ ◦ ◦ ◦ ◦ ◦ C-XI 14 6.4 <20m 10 /80 175 /8 64 42’36” -15 40’1” ◦ ◦ ◦ ◦ ◦ ◦ C-XII 14 4 <20m 217 /90 175 /8 64 42’14” -15 40’34” ◦ ◦ ◦ ◦ ◦ ◦ C-XIII 18 5.6 >100m 25 /80 175 /8 64 42’7” -15 42’47” ◦ ◦ ◦ ◦ ◦ ◦ C-XIV 19 4.5 >100m 10 /90 175 /8 64 42’4” -15 46’37” ◦ ◦ ◦ ◦ ◦ ◦ C-XV 15 2.5 >100m 25 /90 175 /8 64 42’4” -15 45’36” ◦ ◦ ◦ ◦ ◦ ◦ C-XVI 18 5.4 ∼50m 60 /85 175 /8 64 41’35” -15 48’36” ◦ ◦ ◦ ◦ ◦ ◦ C-XVII 14 1.4 <20m 45 /90 175 /8 64 41’28” -15 46’1” ◦ ◦ ◦ ◦ ◦ ◦ C-XVIII 14 3.5 <20m 55 /80 175 /8 64 41’28” -15 46’1” ◦ ◦ ◦ ◦ ◦ ◦ C-XIX 16 3.7 ∼50m 20 /85 175 /8 64 41’20” -15 46’16” ◦ ◦ ◦ ◦ ◦ ◦ C-XX 18 4.9 ∼50m 50 /75 175 /8 64 41’17” -15 46’19” ◦ ◦ ◦ ◦ ◦ ◦ C-XXI 16 1.8 <20m 5 /80 190 /8 64 39’43” -15 42’36” ◦ ◦ ◦ ◦ ◦ ◦ C-XXII 14 3.2 <20m 60 /90 190 /8 64 39’43” -15 37’26” ◦ ◦ ◦ ◦ ◦ ◦ C-XXIII 16 4.4 <20m 20 /80 190 /8 64 39’43” -15 37’26” ◦ ◦ ◦ ◦ ◦ ◦ C-XXIV 14 2.2 <20m 35 /80 190 /8 64 38’56” -15 38’49” ◦ ◦ ◦ ◦ ◦ ◦ C-XXV 14 4.3 <20m 45 /80 190 /8 64 37’52” -15 34’12” ◦ ◦ ◦ ◦ ◦ ◦ C-XXVI 14 3.1 <20m 50 /80 168 /9 64 37’30” -15 34’23” ◦ ◦ ◦ ◦ ◦ ◦ C-XXVII 14 2 <20m 355 /90 168 /9 64 35’53” -15 31’41” ◦ ◦ ◦ ◦ ◦ ◦ C-XXVIII 15 2.8 <20m 0 /75 168 /9 64 35’53” -15 31’34” ◦ ◦ ◦ ◦ ◦ ◦ C-XXIX 15 4.2 ∼50m 50 /80 168 /9 64 35’53” -15 25’41” ∑29 ∑439 ∅4.9

Table 1: Dike characteristics in the ﬁeld. n: number of samples, width of dike (m), extent of outcrop (m), strike and dip ◦ ◦ uncorrected for westward magnetic declination ( / ), where a denote dikes with large (>45°) difference in strike ◦ ◦ between margins. Tilt direction is showed of the surrounding lava pile at sea level ( / ) according to Walker (1974). ◦ ◦ The location of the dikes sampled ( N/ E).

26 Magnetic scalars Curie classes ChRM Lava corr. Dike corr. VGP σ ◦ ◦ α◦ ◦ ◦ ◦ ◦ δ◦ δ◦ Name Km M0 M50% Qn Tc nD I 95 k D I D I °E °N p m P ◦ ◦ C-I* 3.7 0.50 11.7 25.5 7.95 350 , 580 4 33.1 68.8 10.2 83 37133 69 155 81 15.6 17.8 N ◦ ◦ ◦ C-II* 12.5 2.13 2.0 6.1 0.40 290 , 475 , 580 4 1.0 70.2 8.7 113 340 68 336 68 213 73 12.3 14.7 N ◦ C-III* 11.0 2.22 7.5 7.0 1.71 550 4 334.6 69.3 20.1 22 320 64 327 65 235 61 25.8 32.2 N ◦ ◦ C-IV 7.9 1.60 3.1 10.4 0.99 520 , 580 2 333.3 46.6 15.2 28 327 42 328 46 210 44 11.5 18.7 N ◦ ◦ ◦ C-V 5.6 1.40 6.0 13.4 2.69 475 , 520 , 580 4 339.5 64.8 5.8 248 326 61 334 65 222 60 6.7 8.8 N ◦ ◦ C-VI* 14.7 1.30 3.1 4.6 0.53 425 , 580 4 78.0 78.3 12.3 57 49 85 78 78 6 70 24.1 24.4 N ◦ C-VII* 8.1 0.67 5.0 7.4 1.55 130 4 343.1 75.9 4.6 399 320 72 320 58 251 69 7.1 8.1 N ◦ ◦ ◦ C-VIII* 3.8 0.49 11.6 11.1 7.67 350 , 520 , 620 4 338.4 86.4 6.4 206 285 80 329 84 303 63 11.8 12.3 N ◦ ◦ C-IX* 4.4 0.34 14.6 19.5 8.34 350 , 580 4 9.6 73.8 6.3 217 343 73 354 72 225 80 10.0 11.2 N ◦ ◦ ◦ C-X* 4.9 0.58 10.2 23.4 5.23 350 , 550 , 580 4 145.4 -87.0 4.5 426 100 -80 145 -87 123 -61 8.3 8.6 R ◦ ◦ ◦ C-XI* 11.5 1.13 5.0 9.5 1.09 350 , 475 , 550 4 160.9 -77.4 4.0 541 133 -74 131 -72 84 -68 6.4 7.2 R ◦ ◦ C-XII* 10.7 1.82 1.4 3.0 0.33 520 , 580 ◦ C-XIII 6.4 1.35 7.7 12.5 3.02 520 10 38.9 79.9 4.4 124 348 83 348 78 330 78 8.4 8.6 N ◦ C-XIV 2.4 0.31 4.9 11.7 5.13 520 11 15.7 83.4 3.9 135 313 82 16 83 304 72 7.3 7.6 N ◦ C-XV* 10.6 1.88 2.9 7.2 0.69 550 7 196.9 -69.5 11.9 27 175 -71 197 -70 4 -80 18.1 20.7 R ◦ ◦ C-XVI 4.3 2.02 2.8 17.4 1.64 475 , 620 4 298.1 -83.2 17.4 29 27 -86 298 -83 159 -57 34.2 34.5 R ◦ C-XVII 6.2 1.84 23.4 28.3 9.48 520 4 51.5 84.5 17.5 29 307 85 52 85 325 69 34.3 34.7 N

27 ◦ ◦ ◦ C-XVIII* 3.4 1.17 4.8 18.0 3.55 520 , 580 , 620 10 65.6 72.2 1.8 752 51 79 66 72 39 70 3.3 3.4 N ◦ ◦ C-XIX* 9.2 1.09 5.9 13.5 1.61 520 , 580 4 55.7 70.6 4.3 454 39 77 56 71 56 74 7.5 8.0 N ◦ ◦ C-XX 6.9 1.55 10.1 17.8 3.68 350 , 580 4 239.0 -77.3 4.4 439 207 -84 177 -68 189 -75 8.5 8.6 R ◦ ◦ ◦ C-XXI 1.7 0.30 1.9 26.8 2.81 425 , 520 , 550 4 315.7 -65.5 17.0 30 330 -71 7-80185 -33 26.0 29.8 R ◦ ◦ C-XXII* 12.5 2.13 4.9 7.6 0.98 520 , 580 4 35.1 86.5 6.8 182 306 83 35 87 311 70 13.0 13.3 N ◦ ◦ ◦ C-XXIII 5.4 1.25 2.6 14.1 1.21 350 , 425 , 520 10 17.3 70.8 4.3 127 355 70 352 68 183 79 6.4 7.4 N ◦ ◦ C-XXIV 2.1 0.15 1.4 10.6 1.68 475 , 580 ◦ C-XXV* 6.8 1.04 3.4 8.0 1.26 520 4 201.5 -82.3 7.8 141 150 -80 172 -80 117 -77 14.3 15.0 R ◦ ◦ C-XXVI* 5.4 0.52 6.5 15.2 3.02 425 , 580 4 51.9 77.5 5.9 245 10 84 976354 76 11.4 11.6 N ◦ C-XXVII 8.9 0.77 3.6 10.7 1.02 520 4 66.2 86.6 6.8 184 265 84 66 87 321 62 13.2 13.4 N ◦ ◦ ◦ C-XXVIII* 5.2 0.39 0.8 13.2 0.39 425 , 580 , 620 3 136.0 64.3 13.3 88 155 68 157 68 3 27 18.6 22.3 N ◦ ◦ ◦ C-XXIX* 3.2 0.40 9.7 14.4 7.62 520 , 550 , 580 4 207.0 -73.8 8.0 132 174 -77 179 -70 106 -87 14.0 15.0 R ∑29 ∅6.9 ∅1.1 ∅6.2 ∅13.4 ∅3.0 ∑133 ∅8.7 ∅202 ∅14.0 ∅15.5

Table 2: Characteristics of remanent magnetization and calculated virtual geomagnetic pole (VGP) for each dike. Dike names with * denote dikes which also has been evaluated on for −2 −2 magnetic hysteresis. Values for scalars properties given for bulk susceptibility (Km × 10 SI, with standard deviation σ × 10 SI), strength of natural remanent magnetization (M0, A/m), median destructive field (M , mT) and Königsberger ratio (Q = M0 ,whereH = 38.9 A/m). Curie temperatures given as Curie classes ( °C) and not as exact Curie temperature(s). 50% n H×Km Characteristic remanent magnetization (ChRM) properties including vector orientation (D/I), angular confidence radii (α95) and mean precision parameter (k) (Fisher, 1953). Directions of ChRM corrected for lava tilt and dike tilt respectively. VGP calculated from lava tilt corrected directions and given as paleo-longitude and paleo-latitude with the angular 95% confidence length of the parallel and the meridian respectively (Cox and Doell, 1960). Mean pole direction for each polarity and tilt case see text. P polarity. Name n PJ σ T σ κa εa κc εc C-I E 8 1.01 .004 0.53 .341 212/8 25.6/4.5 121/2 5.1/4.0 W 9 1.02 .003 0.23 .384 137/75 12.5/2.8 323/15 7.6/4.8 C-II E 7 1.07 .008 0.17 .264 26/18 7.4/5.2 164/66 8.0/4.5 W 7 1.04 .020 0.49 .338 136/30 34.1/2.1 299/59 14.0/6.1 C-III E 7 1.02 .013 0.78 .236 359/35 60.8/5.2 258/15 17.4/7.2 W 7 1.04 .018 0.02 .489 37/63 18.5/6.7 210/27 16.6/8.7 C-IV E 7 1.03 .007 0.14 .079 1/74 5.1/2.9 98/2 4.6/2.5 W 7 1.02 .007 0.03 .200 328/71 3.2/2.5 91/11 11.1/2.6 C-V E 7 1.04 .042 0.14 .551 294/0 12.4/8.7 204/70 10.3/4.6 W 7 1.02 .003 0.21 .374 77/76 11.0/3.2 282/13 7.2/4.4 C-VI E 9 1.09 .065 0.49 .180 112/8 14.1/6.2 219/64 16.1/2.2 W 8 1.09 .045 0.12 .395 283/6 10.2/5.3 186/52 12.9/8.4 C-VII E 7 1.50 .086 0.58 .363 311/59 23.9/2.7 213/5 5.1/2.5 W 7 1.24 .031 0.41 .280 126/15 6.4/3.1 32/14 4.1/3.0 C-VIII E 8 1.06 .039 -0.58 .301 38/31 17.7/2.8 131/5 16.0/3.3 W 8 1.09 .029 -0.57 .308 54/9 14.5/6.2 148/23 38.8/7.1 C-IX E 7 1.00 .003 -0.38 .355 65/64 20.5/7.4 281/21 48.0/15.9 W 6 1.01 .001 0.00 .128 309/20 5.3/3.5 204/36 11.3/4.2 C-X E 7 1.01 .008 0.02 .387 172/54 33.6/7.1 316/31 26.0/3.8 W 7 1.02 .009 0.91 .072 225/88 26.6/3.8 348/1 5.8/1.8 C-XI E 7 1.04 .014 0.83 .168 56/15 52.4/5.7 197/71 10.3/8.7 W 7 1.05 .024 -0.11 .461 343/1 22.3/10.0 252/56 15.6/10.9 C-XII E 7 1.09 .062 0.54 .171 309/19 2.8/1.3 134/71 5.4/0.8 W 7 1.01 .022 -0.18 .376 6/52 47.6/10.5 102/5 24.7/5.7 C-XIII E 9 1.01 .002 0.18 .305 209/81 22.6/11.1 91/4 26.3/7.0 W 9 1.01 .012 0.01 .457 137/16 28.1/6.8 43/16 18.9/6.8 C-XIV E 8 1.01 .005 -0.17 .340 252/54 17.7/7.5 130/21 14.5/5.8 W 11 1.01 .007 0.29 .263 145/58 41.6/15.1 284/25 52.9/39.1 C-XV E 8 1.03 .017 0.37 .373 213/12 28.3/14.5 324/59 34.1/14.9 W 7 1.14 .048 0.84 .082 339/1 39.8/4.6 72/79 7.2/6.7 C-XVI E 9 1.01 .012 0.12 .411 14/10 37.9/11.8 157/78 14.3/10.0 W 9 1.01 .010 -0.68 .380 277/86 6.9/3.2 173/1 11.1/2.4 C-XVII E 7 1.01 .008 -0.56 .580 166/84 15.3/10.8 66/1 72.2/14.2 W 7 1.01 .002 0.69 .344 312/16 76.7/22.4 218/14 22.9/22.4 C-XVIII E 7 1.01 .005 -0.17 .264 54/78 22.5/13.8 156/3 23.3/7.7 W 7 1.04 .021 0.64 .070 60/85 5.9/2.0 152/0 4.9/2.0 C-XIX E 8 1.06 .025 -0.64 .225 312/13 4.8/3.5 82/70 27.7/4.8 W 8 1.06 .013 -0.36 .184 302/14 6.0/3.3 74/69 18.1/3.6 C-XX E 10 1.04 .100 0.57 .194 341/78 14.4/2.3 119/9 8.4/2.4 W 8 1.03 .007 -0.17 .312 309/83 5.7/3.8 132/7 5.3/3.1 C-XXI E 9 1.04 .034 -0.55 .443 37/52 20.8/10.9 270/25 44.9/9.6 W 7 1.06 .048 0.46 .382 205/41 21.1/5.8 108/7 7.7/3.7 C-XXII E 7 1.08 .038 0.52 .255 340/8 15.1/3.8 138/81 7.0/3.4 W 7 1.08 .020 0.45 .363 357/15 15.1/3.4 197/74 9.0/3.2 C-XXIII E 8 1.02 .011 -0.16 .262 201/22 26.8/18.0 98/28 46.1/10.6 W 8 1.07 .089 0.31 .456 236/4 20.3/11.8 337/70 24.8/7.9 C-XXIV E 7 1.06 .041 0.31 .406 1/17 13.1/7.1 268/10 13.5/6.4 W 7 1.06 .021 0.63 .240 41/20 29.0/2.1 306/12 10.7/4.8 C-XXV E 7 1.05 .036 0.86 .191 22/37 29.4/4.8 124/16 8.8/6.5 W 7 1.03 .010 0.13 .471 160/1 19.2/6.1 258/81 7.1/5.0 C-XXVI E 7 1.06 .039 -0.42 .280 146/65 19.7/5.6 272/15 10.3/5.1 W 7 1.09 .036 0.07 .318 46/84 15.2/3.6 294/2 14.5/1.6 C-XXVII E 7 1.13 .073 0.77 .194 263/6 24.7/2.8 13/72 6.9/2.8 W 7 1.10 .071 0.94 .318 148/9 61.7/2.6 258/65 4.4/2.5 C-XXVIII E 7 1.02 .017 0.41 .214 183/27 33.4/7.9 90/5 23.3/6.7 W 8 1.03 .012 0.07 .351 130/74 7.5/5.2 276/14 7.1/5.1 C-XXIX E 8 1.02 .013 0.08 .326 34/22 15.2/5.6 129/13 9.5/5.8 W 7 1.02 .004 0.40 .264 240/45 24.3/9.3 147/4 11.4/5.6 ∑439 ∅1.04 ∅.030 −0.36/0.40 ∅.299

Table 3: AMS characteristics for each dike margin. Name and number of each dike in roman numerals with margin speciﬁed (East/West). n: number of samples. PJ: corrected anisotropy degree and T: shape parameter, both with their σ κ standard deviations ( ). a/c: orientation in degrees of the major and minor axis respectively in paleovertical ε coordinates given as declination/inclination. The long/short angular length of the 95% conﬁdence ellipse ( a/c)tothe respective orientation of the susceptibility axis is also given.

28 Dike Margin Strike * Int. line Flow ∠ ηζ* Flow ∠ C-I E 70/90 M 180/88 S→N2 2.2 1.8 S→N-10 W 15/90 M 180/67 S→N -23 1.5 1.3 -- C-II E Inv -- WInv -- C-III E 20/85 M 0/55 S→N354.7 2.6 S→N35 WInv -- C-IV E 340/85 M 0/87 N→S3 2.3 1.2 -- W 340/85 M 0/61 S→N293.4 1.3 -- C-V E Inv -- W 340/90 M 180/66 S→N -24 3.4 2.2 S→N-24 C-VI E Inv -- WInv -- C-VII E Inv -- WInv -- C-VIII E 30/90 M 0/84 N→S -6 17.4 6 P -- W 30/85 M 0/34 S→N565.9 6.6P -- C-IX E 230/90 M 180/54 S→N -36 14.6 7.6 S→N-36 WInv -- C-X E Inv -- W 80/90 M 0/84 N→S -6 17.2 0.8 N→S-6 C-XI E Inv -- WInv -- C-XII E 40/90 M 0/79 S→N11 - - F -- W 40/90 M 180/69 N→S 21 14.3 7 F -- C-XIII E 25/80 M 180/82 S→N-85.6 2.4 S→N-8 WInv -- C-XIV E 10/90 M 0/55 N→S -35 4.1 2.2 N→S-19 W 20/90 M 180/86 N→S -4 14.2 3.8 F -- C-XV E 25/90 M 180/24 N→S 66 10.1 8.1 F N→S66 WInv -- C-XVI E 50/90 M 0/82 N→S -8 24.8 17.8 F S→N10 W 75/90 M 0/80 S→N107.5 0.9 -- C-XVII E 45/90 M 360/78 S→N2 1.9 0.7FS→N2 WInv -- C-XVIII E 45/90 M 180/84 N→S 6 11.2 4.1 -- W 45/90 M 360/90 S→N0 2.7 0.5 -- C-XIX E Inv -- WInv -- C-XX E 50/70 M 180/67 S→N -23 2.5 1 -- W 50/70 M 180/53 N→S375.2 1 -- C-XXI E 15/70 M 180/57 N→S 33 23.9 8.7 F N→S68 W 15/70 M 0/19 ; 180/25 Up 68 7.1 ; 12.9 1.6 ; 2.7 T -- C-XXII E Inv -- WInv -- C-XXIII E 20/80 M 180/43 S→N -47 16.4 9.8 F S→N-30 W 20/80 M 180/78 S→N -12 4.9 2 F -- C-XXIV E 25/80 M 0/75 S→N15 8 4.2 S→N-14 W 25/75 M 180/47 S→N -43 6.6 2.3 -- C-XXV E 35/85 M 0/25 ; 180/19 Up 90 8.5 ; 6.5 5.0 ; 4.5 T Up 90 WInv -- C-XXVI E 40/80 M 0/69 S→N213.9 2.9 -- W 40/80 M 0/87 N→S-3 4 0.8 -- C-XXVII E Inv -- WInv -- C-XXVIII E 350/80 M 0/73 N→S -17 26.1 7 -- W 350/80 M 180/32 S→N -58 5.6 2.7 T -- C-XXIX E 35/80 M 0/27 ; 180/34 Down -60 3.0 ; 9.4 0.9 ; 5.8 T S→N11 W 45/80 M 0/79 S→N116.8 1.4 --

Table 4: Calculation of intersection line and interpreted flow directions. Dike name with margin indicated and margin strike. Strike only given for margins were calculations are performed as indicated in *: M=Imbricated fabric to be mirrored. Inv=Inverse fabric. P=Prolate fabric. F=Fabric with fever samples then 5. T=Fabric with two major intersection lines, indicating vertical flow. Direction of intersection line in lower hemisphere stereograph given followed by flow sense and inclination (∠) above horizon (positive values are above). Bootstrapping statistics η and ζ are given (see Constable and Tauxe, 1990). In the last two columns the interpretation of flow is given.

29 Figure 1: Geological map over Iceland showing regional geology with now active volcanic systems including both the outline of the ﬁssure swarms and the central volcano complexes, with occasional caldera structures. The

Mid-Atlantic-Ridge passes onto land from the Reykjanes ridge extending into the Reykjanes peninsula and is reconnected to the Kolbinsey ridge via the Tjörnes fracture zone in the north. Figure simpliﬁed from Jóhannesson and

Sæmundsson (1998).

Figure 2: (a) Map showing percentage of dilatation of the bedrock caused by dikes. The letters A, B, R and T indicate locations of exhumed central volcanoes Álftafjörður, Breiðdalur, Reyðarfjörður and Þingmúli respectively. Figure redrawn and modified from original by Walker (1974). (b) Map showing sampled dikes in the Álftafjörður dike swarm. Note the difference in scale and projection from figure (a). The sampled dikes are given with numbers omitting group letter (Table 1). Letters A, B and E denote exhumed central volcanoes as in figure (a) with the names written out in capitals. The dashed contour line indicates the zone of maximum dike dilatation in the Álftafjörður volcanic system according to Walker (1974).

Figure 3: Examples of remanence behavior during alternating ﬁeld (AF) demagnetization. (a) Two components of magnetization as shown by the change in direction after step 2 or 3. Sigmoidal decrease of magnetization strength with intermediate (∼ 25 mT) MDF, indicating primarily single-domain held remanence. (b) Near single remanence component carried by two distinct populations of grains shown by the kink in the magnetization strength graph. (c)

Two component remanence held in rock dominated by large low coercivity grains evident by the exponential decrease of total magnetization strength.

Figure 4: Stereographic equal area lower hemisphere plot over characteristic remanent magnetization (ChRM) directions for the dikes. Before (a), and after using lava tilt correction (b), and dike tilt correction (c).The symbols denotes positive and negative inclination respectively. Large ellipses 95% conﬁdence estimate (Fisher, 1953).

Figure 5: Logarithmic values of dike magnetization subsequent to 15 mT demagnetization plotted against the absolute value of the respective dikes calculated paleo-latitude. Solid and dashed line are linear and quantile regression ﬁts respectively. Inset ﬁgure, histogram over absolute values of paleo-latitude.

30 Figure 6: Granulometric estimation of magnetic grains. (a) Day plot with sketched theoretical curve for multi-domain component of single- to multi-domain grain distribution (Day et al., 1977; Dunlop, 2002). (b) Hysteresis graph showing typical single-domain grain behaviour with a very steep increase in magnetization indicating that the magnetization is carried by very few domains. (c) Hysteresis graph with steep increase in magnetization, still indicating single-domain type behaviour. The hysteresis graphs shown in (b) and (c) are equally common.

Figure 7: Examples of susceptibility temperature dependency, with solid line showing heating curve, and dashed line cooling curve. (a) Magnetite type curve with clear curie point near 580°C. (b) Maghemite curve with a drop in susceptibility around 350°C, either caused by inversion of maghemite to hematite or by exolution of Ti–rich titanomagnetite. The susceptibility drop around 610°C and 630°C indicate the presence of maghemite, as shown by the high susceptibility. (c) Anomalous type with low curie point around 200°C.

Figure 8: Shape parameter T plotted against corrected anisotropy degree PJ for each margin of the dikes. Margins with

Pj ≥ 1.150 are not shown here (5 of 58 margins).

Figure 9: Selection procedure of AMS data when inferring flow with use of the intersection line. The examples are given in two dimensions only, but the cases applies in three dimensions as well. The thick short lines represent the plane perpendicular to the minor susceptibility axis. (a) Parallel type fabric, no flow can be inferred since the flow directions will become anti-parallel. Note that requirement i and ii is still met. (b) Parallel type fabric, no flow can be inferred since the planes never cross-cut. In nature this type seldom occurs since the planes must be absolutely parallel. (c) Symmetric fabric, flow can be inferred, requirements i, ii and iii is fulfilled. (d) Sub-symmetric fabric,

ﬂow can be inferred as in the prior example. (e) Non-symmetric example, ﬂow can be inferred through mirroring of the left fabric against the dike plane, thus creating a synthetic symmetric margin pair. The right fabric is disregarded since requirement ii is not met. (f) Non-symmetric example, same procedure as in the prior example.

31 Figure 10: Examples of stereographic projections of the AMS ellipsoid in four dikes. Symbol denotes major axis, intermediate axis and minor axis in stereographs. Small ellipses are 95% of conﬁdence cone. denotes sample in

T − PJ plot, T > 0 denote oblate fabrics and P < 0 prolate fabrics. Magnetic fabrics in stereographs rotated to dike coordinates, dike attitude, solid line. (a) Dike with inverse fabric in western margin and normal in eastern margin, imbricated only against the vertical, thus indicating vertical upwards ﬂow. (b) Dike with parallel fabrics. (c) Dike with normal fabric in western margin and inverse in eastern margin. (d) Dike with normal fabrics in both margins with large imbrication angles, indicating a ﬂow from the north.

Figure 11: Geological map over east Iceland with the sampled dikes and the inferred ﬂow directions shown. The letter

A,B denotes the exhumed central volcanoes Álftafjörður and Breiðdalur respectively. C indicates the positive magnetic anomaly south of Streitishvarf which may indicate a central volcano (see Eriksson et al., In revision, cf. Kristjánsson,

2008). The dashed contour indicate the zone of maximum dike dilatation in the Álftafjörður volcanic system according to Walker (1974). The flow direction in the sampled dikes are given with one arrow and an inclination, where positive numbers denote flows up from the horizon. If the flow is sub-vertical the symbol (·\·) is given. Dikes which did not yield either flow directions or had possible transtensional fabrics are not shown (dike numbers retained from Fig. 2). The small arrows on the outcrops of the Streitishvarf dike denote the propagation direction of the felsic part in that dike according to Eriksson et al. (In revision)

Figure 12: Rose diagram over tilt adjusted strike for the sampled dikes. The trends of 25°E and 40°E from Paquet et al. (2007) have been added.

32 Figure 13: (a) Conceptual model for lateral dike intrusion from shallow magma chambers compiled from

Gudmundsson (1984) and Paquet et al. (2007). From the magma chamber situated at A under the central volcano, lateral diking is expected. One such dike is shown where the upper part of the dike body is crenelated (B) forcing magma flow upwards and downwards. The tectonic stress regime is overcome at a distance of 12-15 km from the magma chamber allowing a fissure eruption (C). Note that the flow regime in the same dike at C may yield contradicting results if sampled at the present level of erosion. The flow regimes at fissures should also be near vertical. At the propagating tip of the dike (D) the flow would be difficult to asses due to conflicting flow regimes. (b)

Obtained flow directions from the dikes transposed onto a longitudinal line. The vertical level difference between the arrows do not correspond to the sampling locations altitude above sea level but have been introduced to reduce clutter in the figure. Scales in figure (a) and (b) differ.

33 figure_01.ai 2010-11-17 12.09.33

24° 22° 20° 18° 16° 14° Kolbinsey ridge

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66° 66°

65° Snaefellsnes 65°

Legend Volcanic system including central volcano complex and fissure swarm N Caldera

64° 64° Glacier 0 50 km

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Demagnetization behaviours during AF-treatment

N Up N Up N Up a) b) c)

W E W E W E W E W E W E 10 mT 40 mT 5 mT 40 mT

Horizontal component 20 mT Vertical component 20 mT 0 mT 0 mT 0 mT S Down S Down S Down M/Mmax M/Mmax M/Mmax 1 1 1 0.8 0.8 0.8 0.6 0.6 0.6 0.4 0.4 0.4 0.2 0.2 0.2 0 0 0 0 10203040506070mT 0 20 40 60 80 100mT 01020304050607080mT figure_04.ai 2010-11-17 12.07.22

Characteristic remanent magnetization (ChRM) with tilt corrections

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Fáskrúðsfjörður

Sandfell

BREIÐDALUR B 64°50'N

Stöðvarfjörður -10° Streitishvarf composite dike 1 35° 2 3 -24° 4 5 Breiðdalsvík 6

-36° 7 8 Streitishvarf 9 10 -8° -19° -6° 66° 14 11 13 10° 15 2°16 12 18 19 17 64°40'N 20 -30° 23 21 Berufjörður N -14° 22 C 68° Hamarsfjörður 24

25 26 Legend 11° 28 Papey 10° 29 27 Lateral flow with an inclination of +10° and a vertical flow respectively Álftafjörður

Parallel imbrications Sand dunes

Mafic dike 64°30'N Felsic or composite dike A ÁLFTAFJÖRÐUR Þeigarhorn

Neoge lava pile

Felsic extrusives

Felsic intrusions

AUSTURHORN Mafic intrusions Lón 10 km

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N 25° 40° +

S figure_13.ai 2010-11-16 16.42.34 a)

Central volcano C Surface fissure Paleosurface B A Present level of erosion 1.5 km

3 km Shallow Laterally intruding dike magma chamber D

10 km b) C-XV S N

C-XXI C-XVI C-XVII C-X

C-XXIX C-XXV C-XXIV C-XIV C-XIII C-V C-III C-I C-XXIII C-IX Part III Appendix – Tables

Series of samples named as a letter, sample number and year in two digits, example A001.09, indicating sample series A, sample number 1 collected year 2009. Sample series S01–S18.08 and series S from 2009 collected from composite dikes, in general the felsic part. The remaining series collected from maﬁc dikes. Additional data other than presented here, such as detailed values of grain hysteresis measurements and temperature-susceptibility variations have been omitted due to the large volume of data.

Appendix A. Anisotropy of magnetic susceptibility characteristics for all samples collected. Samples enclosed by box are samples whose AMS has been determined subsequent to AF-demagnetization. Key to table: Km bulk susceptibility in SI. L lineation parameter by Balsley and Buddington (1960). F foliation parameter by Stacey et al. (1960) Pjcorrected anisotropy degree and T shape parameter and U difference shape factor by Jelínek (1981). K1d, K1i, etc. declination and inclination of the major, intermediate and minor axis respectively, given in geographic coordinates in lower hemisphere projection.

Appendix B. Location and sample ranges for the dikes in east Iceland. Locations given in decimal degrees as °N and °E.

Appendix C. AF-demagnetization data for all samples demagnetized. Key to table: First row denotes for each sample name, azimuth, plunge and P1–P4 parameters adopted for software by Chadima and Hrouda (2006). The columns contain demagnetization step in mT, magnetization strength in A/m, declination and inclination of the measured remanence in specimen and geographic coordinates respectively.

Appendix D. Hysteresis characteristics. Key to table: Ms saturation magnetisation. Mr residual magnetization. Hc coercivity. Hcr retentivity.

Appendix A Name Km L F Pj T U K1d K1i K2d K2i K3d K3i D01.08 1.14E+4 1.021 1.014 1.036 -0.200 -0.208 177.3 52.6 25.3 34.0 285.8 13.7 D02.08 1.52E+4 1.044 1.055 1.102 0.115 0.091 186.7 51.6 22.0 37.4 286.3 7.5 D03.08 2.01E+4 1.018 1.038 1.058 0.348 0.335 160.1 64.7 20.3 19.9 284.8 15.1 D04.08 2.19E+4 1.012 1.062 1.080 0.664 0.654 185.2 14.2 55.3 68.5 279.2 15.8 D05.08 1.82E+4 1.035 1.108 1.153 0.498 0.472 197.4 27.5 48.1 58.8 294.6 13.6 D06.08 1.44E+4 1.014 1.016 1.030 0.076 0.068 199.7 8.8 52.8 79.5 290.6 5.7 D07.08 1.54E+4 1.012 1.005 1.017 -0.416 -0.420 17.9 1.3 283.5 73.9 108.3 16.0 D08.08 1.94E+4 1.002 1.009 1.012 0.606 0.605 117.8 37.1 339.0 44.9 225.4 21.8 D09.08 1.48E+4 1.036 1.015 1.053 -0.396 -0.407 21.0 37.4 144.9 36.1 262.2 32.1 D10.08 1.64E+4 1.047 1.020 1.070 -0.398 -0.412 28.0 39.7 290.6 8.9 190.3 48.9 D11.08 1.69E+4 1.004 1.009 1.013 0.394 0.392 203.5 40.1 86.1 28.6 332.3 36.6 D12.08 1.59E+4 1.059 1.021 1.085 -0.462 -0.477 69.6 43.4 329.2 10.7 228.5 44.6 D13.08 2.17E+4 1.060 1.031 1.094 -0.310 -0.330 61.0 30.0 182.2 42.0 308.6 33.4 D14.08 1.71E+4 1.065 1.019 1.089 -0.543 -0.558 55.7 39.8 322.6 3.7 228.2 50.0 D15.08 1.20E+4 1.005 1.010 1.015 0.356 0.353 42.4 57.6 177.1 24.1 276.6 20.3 D16.08 1.68E+4 1.028 1.013 1.043 -0.370 -0.379 164.4 47.3 271.6 15.2 14.1 38.7 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i D17.08 3.85E+4 1.050 1.034 1.086 -0.192 -0.212 54.8 13.0 277.0 72.7 147.4 11.2 D18.08 3.87E+4 1.090 1.021 1.119 -0.618 -0.634 49.1 20.6 285.6 55.8 149.7 26.1 D19.08 2.75E+4 1.073 1.010 1.091 -0.749 -0.758 58.2 4.5 325.2 34.6 154.6 55.1 D20.08 3.49E+4 1.068 1.028 1.101 -0.405 -0.425 229.9 25.1 18.5 61.3 133.6 13.1 D21.08 3.61E+4 1.031 1.029 1.061 -0.028 -0.043 57.4 52.5 205.4 33.0 305.9 15.7 D22.08 3.69E+4 1.117 1.010 1.143 -0.834 -0.843 62.6 5.3 306.0 78.4 153.5 10.3 D23.08 3.81E+4 1.042 1.038 1.082 -0.050 -0.070 51.8 21.6 308.3 30.5 171.4 51.2 D24.08 3.13E+4 1.091 1.043 1.141 -0.343 -0.371 53.0 4.8 320.7 24.8 153.2 64.7 D25.08 3.58E+4 1.018 1.035 1.055 0.305 0.294 234.1 45.6 41.7 43.7 137.7 6.2 D26.08 3.42E+4 1.020 1.017 1.037 -0.078 -0.087 227.2 4.7 328.9 68.0 135.4 21.4 D27.08 4.53E+4 1.055 1.016 1.075 -0.552 -0.564 15.7 38.7 142.2 36.6 257.8 30.3 D28.08 4.56E+4 1.046 1.018 1.066 -0.441 -0.453 39.5 20.2 176.0 63.1 303.0 17.0 D29.08 3.85E+4 1.094 1.036 1.138 -0.434 -0.460 45.9 42.5 201.9 44.9 304.4 12.2 D30.08 4.50E+4 1.030 1.016 1.047 -0.302 -0.312 36.4 33.5 237.3 54.7 133.0 9.9 D31.08 3.59E+4 1.093 1.036 1.137 -0.430 -0.455 33.1 29.4 301.9 2.1 208.1 60.5 D32.08 4.13E+4 1.046 1.011 1.061 -0.621 -0.629 36.8 30.6 202.1 58.6 302.9 6.6 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i D33.08 6.30E+4 1.013 1.016 1.029 0.130 0.123 226.4 47.2 353.4 29.1 100.8 28.3 D34.08 7.19E+4 1.013 1.020 1.034 0.213 0.205 195.4 23.8 321.9 53.4 93.0 26.0 D35.08 3.65E+4 1.008 1.027 1.037 0.549 0.543 243.3 25.5 344.1 21.4 109.0 55.6 D36.08 4.80E+4 1.014 1.024 1.040 0.253 0.244 214.1 7.4 311.9 46.1 117.1 43.0 D37.08 3.00E+4 1.017 1.015 1.032 -0.076 -0.084 156.8 51.9 56.0 8.4 319.6 36.8 D38.08 5.36E+4 1.020 1.037 1.058 0.288 0.275 166.6 35.7 11.4 51.6 265.5 12.2 D39.08 3.68E+4 1.016 1.008 1.024 -0.338 -0.343 240.6 10.0 332.5 10.5 108.1 75.4 D40.08 6.04E+4 1.021 1.028 1.050 0.136 0.124 185.8 22.3 14.3 67.5 277.0 3.0 D41.08 6.55E+4 1.025 1.197 1.251 0.758 0.735 245.5 17.3 154.6 2.9 55.4 72.5 D42.08 6.11E+4 1.011 1.220 1.267 0.898 0.888 131.3 3.3 222.0 11.7 26.0 77.8 D43.08 6.03E+4 1.028 1.059 1.090 0.352 0.333 269.9 1.0 179.6 19.6 2.9 70.4 D44.08 5.99E+4 1.027 1.039 1.068 0.174 0.158 90.9 2.1 181.5 15.6 353.5 74.2 D45.08 5.03E+4 1.044 1.013 1.060 -0.532 -0.542 230.8 0.6 136.0 82.8 320.9 7.2 D46.08 7.03E+4 1.035 1.040 1.076 0.066 0.048 225.7 31.6 79.1 53.6 326.0 16.2 D47.08 4.26E+4 1.048 1.041 1.091 -0.083 -0.105 60.6 57.6 207.6 28.0 305.7 14.9 D48.08 5.76E+4 1.016 1.022 1.039 0.150 0.141 41.1 25.6 184.8 59.3 303.3 15.8 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i F095.08 3.43E+4 1.004 1.010 1.015 0.403 0.399 24.4 24.8 208.4 65.1 115.2 1.5 F096.08 2.92E+4 1.005 1.008 1.013 0.171 0.168 90.2 39.8 307.9 43.5 197.8 20.0 F097.08 2.97E+4 1.008 1.010 1.018 0.100 0.095 52.9 74.1 259.7 14.3 168.0 6.9 F098.08 2.99E+4 1.008 1.006 1.015 -0.122 -0.126 42.9 53.3 286.3 18.5 184.9 30.4 F099.08 3.30E+4 1.007 1.009 1.016 0.076 0.072 211.4 19.9 19.7 69.7 120.0 3.8 F100.08 3.53E+4 1.001 1.014 1.017 0.920 0.919 28.3 16.2 213.7 73.7 118.8 1.5 F101.08 3.97E+4 1.004 1.013 1.018 0.537 0.534 209.6 33.1 43.2 56.2 303.7 6.3 F102.08 4.16E+4 1.005 1.020 1.027 0.596 0.592 35.7 1.9 287.1 84.2 125.9 5.5 F103.08 3.35E+4 1.007 1.011 1.018 0.237 0.233 117.0 76.1 217.5 2.6 308.1 13.6 F104.08 4.03E+4 1.003 1.013 1.017 0.609 0.606 161.1 69.8 53.9 6.2 321.8 19.2 F105.08 3.93E+4 1.012 1.006 1.018 -0.341 -0.345 137.8 70.5 45.7 0.7 315.4 19.5 F106.08 4.68E+4 1.009 1.009 1.018 0.030 0.025 114.6 66.6 238.7 13.6 333.4 18.6 F107.08 3.87E+4 1.013 1.005 1.019 -0.481 -0.484 120.1 70.8 248.9 12.3 342.1 14.5 F108.08 3.35E+4 1.005 1.018 1.024 0.528 0.524 200.0 69.1 58.0 16.7 324.3 12.1 F109.08 3.87E+4 1.005 1.015 1.022 0.474 0.470 227.3 43.9 58.0 45.6 322.5 5.4 F110.08 4.33E+4 1.009 1.010 1.019 0.090 0.085 110.1 71.2 222.3 7.4 314.6 17.2 F111.08 3.72E+4 1.004 1.008 1.012 0.399 0.396 122.0 75.2 236.6 6.3 328.1 13.4 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i K01.08 1.02E+5 1.018 1.038 1.058 0.359 0.347 34.2 10.7 146.3 63.4 299.3 24.0 K02.08 1.13E+5 1.009 1.054 1.069 0.707 0.699 125.5 43.8 217.3 1.8 309.2 46.2 K03.08 1.07E+5 1.005 1.033 1.042 0.724 0.719 99.2 38.3 220.0 33.0 336.4 34.4 K04.08 1.09E+5 1.013 1.034 1.049 0.431 0.421 198.0 24.0 106.8 2.8 10.5 65.8 K05.08 1.14E+5 1.010 1.029 1.041 0.465 0.457 202.4 28.4 110.8 2.9 15.4 61.4 Appendix A, page 1 of 9 Appendix A K06.08 7.56E+4 1.011 1.030 1.042 0.474 0.466 13.3 4.0 282.9 6.7 134.3 82.2 K07.08 6.99E+4 1.001 1.016 1.019 0.919 0.919 205.8 8.7 298.7 18.1 91.1 69.8 K08.08 8.39E+4 1.013 1.007 1.020 -0.328 -0.332 67.4 6.0 336.5 8.4 192.5 79.6 K10.08 1.34E+5 1.011 1.096 1.119 0.784 0.774 182.9 4.0 274.3 19.1 81.6 70.5 K11.08 9.88E+4 1.022 1.103 1.136 0.639 0.621 142.5 5.7 234.6 20.8 37.8 68.4 K12.08 1.02E+5 1.008 1.050 1.064 0.709 0.702 187.7 10.6 282.4 23.6 75.4 63.9 K13.08 1.12E+5 1.011 1.175 1.213 0.873 0.862 302.7 0.3 212.7 6.9 34.9 83.1 K14.08 1.34E+5 1.025 1.144 1.187 0.693 0.672 305.0 3.0 214.9 2.2 88.9 86.3 K15.08 1.26E+5 1.017 1.124 1.157 0.755 0.740 2.5 0.8 272.3 9.1 97.5 80.8 K16.08 1.16E+5 1.021 1.104 1.136 0.650 0.633 9.9 3.5 279.0 14.2 113.5 75.3 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i K17.08 3.26E+4 1.010 1.036 1.049 0.567 0.560 59.1 84.7 239.9 5.3 149.9 0.1 K18.08 2.24E+4 1.006 1.032 1.041 0.700 0.695 14.2 85.8 241.0 2.9 150.9 3.0 K19.08 3.04E+4 1.010 1.051 1.066 0.676 0.668 176.0 87.6 66.8 0.8 336.8 2.3 K20.08 3.91E+4 1.009 1.049 1.064 0.677 0.669 54.8 82.9 244.7 7.0 154.6 1.2 K21.08 2.42E+4 1.003 1.019 1.024 0.711 0.708 65.4 67.5 242.3 22.4 332.7 1.1 K22.08 1.53E+4 1.003 1.011 1.015 0.557 0.554 45.6 79.7 236.9 10.1 146.6 2.0 K23.08 1.71E+4 1.004 1.014 1.019 0.562 0.559 59.4 83.2 226.4 6.6 316.6 1.5 K24.08 3.97E+4 1.014 1.007 1.022 -0.318 -0.323 324.2 64.7 66.7 5.9 159.4 24.6 K25.08 4.80E+4 1.007 1.002 1.010 -0.495 -0.497 70.9 59.1 213.0 25.3 311.1 16.5 K26.08 5.16E+4 1.007 1.006 1.013 -0.008 -0.012 58.4 66.6 247.5 23.2 156.1 3.3 K27.08 5.14E+4 1.008 1.003 1.011 -0.409 -0.412 74.4 55.7 262.0 34.1 169.6 3.5 K28.08 3.77E+4 1.006 1.001 1.008 -0.650 -0.651 79.0 81.4 246.1 8.3 336.4 1.9 K29.08 3.04E+4 1.005 1.003 1.008 -0.232 -0.234 170.7 74.5 66.3 4.0 335.2 15.0 K30.08 2.95E+4 1.007 1.008 1.015 0.095 0.091 194.7 79.2 58.0 7.9 327.0 7.3 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i K31.08 1.02E+5 1.037 1.014 1.053 -0.441 -0.451 305.9 16.5 215.2 2.5 116.9 73.4 K32.08 9.04E+4 1.041 1.011 1.055 -0.588 -0.596 294.2 23.1 186.7 35.1 50.3 45.9 K33.08 8.47E+4 1.045 1.026 1.073 -0.271 -0.287 301.9 15.3 204.8 24.4 61.1 60.6 K34.08 9.34E+4 1.036 1.019 1.057 -0.311 -0.324 312.3 11.6 218.1 19.6 71.2 67.0 K35.08 9.09E+4 1.024 1.019 1.044 -0.118 -0.128 302.6 6.2 207.7 38.0 40.4 51.3 K36.08 9.14E+4 1.025 1.010 1.036 -0.423 -0.430 300.9 8.7 208.1 17.5 56.3 70.4 K37.08 1.04E+5 1.033 1.032 1.067 -0.014 -0.031 302.5 12.6 32.8 1.3 128.8 77.3 K38.08 1.03E+5 1.043 1.026 1.070 -0.243 -0.259 297.5 13.9 207.1 1.7 110.5 76.0 K39.08 9.12E+4 1.057 1.028 1.088 -0.333 -0.352 308.3 10.3 215.0 17.7 67.2 69.3 K40.08 1.08E+5 1.060 1.027 1.090 -0.374 -0.392 307.5 12.2 216.4 4.7 105.5 76.9 K41.08 8.40E+4 1.052 1.007 1.065 -0.752 -0.758 313.4 6.5 211.9 60.1 47.1 29.0 K42.08 7.26E+4 1.018 1.009 1.028 -0.319 -0.325 312.9 21.6 205.6 36.9 66.5 45.2 K43.08 9.10E+4 1.038 1.003 1.047 -0.834 -0.837 312.5 12.2 42.9 1.7 140.8 77.7 K44.08 7.53E+4 1.021 1.011 1.033 -0.321 -0.328 312.0 27.1 204.3 30.7 75.1 46.8 K45.08 1.11E+5 1.057 1.022 1.083 -0.434 -0.450 313.0 16.1 48.3 17.9 183.5 65.5 K46.08 8.64E+4 1.038 1.005 1.048 -0.759 -0.763 318.0 10.1 212.8 55.8 54.4 32.3 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i K47.08 5.82E+4 1.016 1.011 1.027 -0.170 -0.176 100.4 73.4 221.4 8.7 313.6 14.0 K48.08 4.70E+4 1.023 1.008 1.032 -0.481 -0.487 130.9 73.4 40.7 0.1 310.6 16.6 K49.08 4.11E+4 1.021 1.005 1.028 -0.619 -0.623 140.6 69.9 44.6 2.2 313.8 20.0 K50.08 4.90E+4 1.020 1.009 1.030 -0.376 -0.382 142.5 72.2 38.2 4.6 306.7 17.2 K51.08 7.23E+4 1.014 1.016 1.031 0.069 0.061 163.9 75.0 37.6 9.0 305.7 11.9 K52.08 4.88E+4 1.031 1.017 1.049 -0.298 -0.309 163.7 76.4 42.2 7.2 310.8 11.5 K53.08 5.09E+4 1.018 1.021 1.039 0.086 0.076 178.1 81.1 45.9 6.0 315.2 6.5 K54.08 8.25E+4 1.011 1.020 1.032 0.284 0.277 170.6 81.2 44.4 5.2 313.8 7.0 K55.08 8.51E+4 1.014 1.033 1.048 0.411 0.402 158.6 75.6 28.9 9.3 297.1 10.9 K56.08 7.44E+4 1.012 1.025 1.039 0.344 0.336 157.9 74.0 24.1 11.2 291.9 11.3 K57.08 8.77E+4 1.006 1.022 1.029 0.570 0.565 183.0 65.9 27.9 22.1 294.1 9.2 K58.08 7.81E+4 1.004 1.025 1.032 0.709 0.705 142.4 70.8 30.6 7.4 298.2 17.7 K59.08 7.91E+4 1.004 1.032 1.040 0.783 0.779 57.2 70.5 207.0 17.0 299.9 9.2 K60.08 7.53E+4 1.015 1.038 1.055 0.444 0.434 152.2 79.1 33.7 5.3 302.8 9.6 K61.08 7.91E+4 1.003 1.023 1.029 0.802 0.800 37.9 37.0 199.8 51.6 301.1 8.8 K62.08 7.53E+4 1.018 1.034 1.054 0.305 0.294 100.3 81.4 214.0 3.5 304.5 7.8 K63.08 8.56E+4 1.004 1.035 1.042 0.809 0.806 51.0 59.6 219.0 29.9 312.0 5.2 K64.08 7.80E+4 1.009 1.034 1.046 0.561 0.553 35.9 64.8 189.3 22.8 283.6 10.1 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i K65.08 4.80E+4 1.005 1.003 1.008 -0.229 -0.231 125.7 73.3 347.9 12.5 255.4 10.8 K66.08 5.64E+4 1.004 1.013 1.018 0.568 0.565 275.3 86.9 58.4 2.5 148.5 1.8 K67.08 3.93E+4 1.006 1.002 1.008 -0.533 -0.535 216.1 80.2 38.0 9.7 308.0 0.3 K68.08 5.45E+4 1.002 1.014 1.018 0.721 0.719 137.4 82.6 15.7 3.9 285.3 6.3 K69.08 4.51E+4 1.001 1.007 1.009 0.707 0.706 178.7 46.5 13.5 42.5 276.6 7.5 K70.08 5.89E+4 1.000 1.026 1.030 0.971 0.971 313.3 31.9 156.9 55.8 50.3 11.0 K71.08 3.22E+4 1.008 1.006 1.015 -0.120 -0.123 98.1 7.2 344.9 72.4 190.2 16.0 K72.08 8.28E+4 1.013 1.004 1.017 -0.524 -0.527 131.6 16.7 34.3 23.0 254.4 61.0 K73.08 8.91E+4 1.005 1.008 1.014 0.230 0.227 103.7 21.4 350.0 45.8 210.6 36.5 K74.08 8.60E+4 1.010 1.001 1.012 -0.785 -0.786 311.3 36.3 49.2 10.7 153.0 51.7 K75.08 7.75E+4 1.008 1.005 1.013 -0.238 -0.241 279.6 44.4 24.9 15.1 128.9 41.7 K76.08 8.20E+4 1.009 1.009 1.018 -0.034 -0.038 348.3 52.0 136.6 33.7 237.3 15.6 K77.08 5.91E+4 1.008 1.006 1.014 -0.146 -0.149 111.3 52.6 270.7 35.5 7.9 10.0 Appendix A, page 2 of 9 Appendix A K78.08 5.77E+4 1.006 1.006 1.013 0.021 0.017 145.5 67.2 328.1 22.7 237.7 0.9 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i K79.08 6.96E+4 1.011 1.005 1.016 -0.356 -0.359 335.5 3.9 244.7 12.0 83.1 77.4 K80.08 6.33E+4 1.013 1.016 1.029 0.132 0.125 16.4 1.3 286.3 4.2 124.0 85.6 K81.08 6.73E+4 1.021 1.016 1.037 -0.116 -0.125 353.4 6.5 262.9 4.3 139.2 82.2 K82.08 6.06E+4 1.007 1.005 1.013 -0.169 -0.172 356.3 31.3 232.6 42.4 108.3 31.7 K83.08 6.59E+4 1.015 1.016 1.031 0.040 0.032 42.9 10.1 310.4 13.4 168.7 73.1 K84.08 6.30E+4 1.018 1.017 1.036 -0.021 -0.030 41.4 2.0 311.1 9.7 142.8 80.1 K85.08 2.38E+4 1.009 1.001 1.012 -0.781 -0.782 1.7 75.7 248.6 5.7 157.3 13.1 K86.08 4.71E+4 1.001 1.003 1.005 0.544 0.543 50.6 79.3 305.3 2.8 214.8 10.3 K87.08 3.50E+4 1.007 1.001 1.009 -0.697 -0.698 88.3 61.5 267.5 28.5 357.6 0.3 K88.08 4.92E+4 1.006 1.011 1.017 0.244 0.240 256.0 81.1 72.4 8.9 162.5 0.6 K89.08 3.44E+4 1.003 1.016 1.020 0.688 0.686 252.0 60.4 74.9 29.6 344.2 1.2 K90.08 3.44E+4 1.018 1.022 1.040 0.095 0.086 301.0 84.9 89.6 4.3 179.8 2.6 K91.08 5.52E+4 1.007 1.006 1.013 -0.120 -0.124 359.3 4.3 114.2 79.8 268.6 9.2 K92.08 5.27E+3 1.005 1.008 1.013 0.201 0.198 104.8 78.5 273.3 11.2 3.7 2.2 K93.08 1.57E+4 1.015 1.010 1.026 -0.215 -0.221 360.0 8.8 157.9 80.5 269.4 3.5 K94.08 1.51E+4 1.008 1.002 1.011 -0.629 -0.631 6.4 75.8 197.4 14.0 106.7 2.6 K95.08 2.80E+4 1.006 1.008 1.014 0.089 0.086 356.2 54.9 169.3 34.9 261.6 3.2 K96.08 4.76E+4 1.004 1.002 1.006 -0.330 -0.332 24.5 82.7 270.4 3.0 180.1 6.6 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i K098.08 2.24E+4 1.004 1.010 1.014 0.462 0.460 128.7 32.1 32.2 10.3 286.6 55.9 K099.08 2.36E+4 1.005 1.009 1.015 0.320 0.317 121.8 36.0 14.7 21.9 260.2 45.9 K100.08 3.30E+4 1.011 1.015 1.026 0.147 0.140 163.4 75.8 12.6 12.5 281.1 6.7 K101.08 2.50E+4 1.005 1.011 1.017 0.400 0.397 155.8 72.0 250.8 1.6 341.4 17.9 K102.08 2.60E+4 1.009 1.004 1.013 -0.381 -0.384 128.6 0.7 38.4 15.3 221.2 74.7 K103.08 2.40E+4 1.005 1.009 1.015 0.284 0.281 132.4 21.4 35.2 17.7 268.9 61.7 K104.08 2.50E+4 1.015 1.012 1.027 -0.134 -0.140 118.9 29.6 24.8 7.3 282.2 59.4 K105.08 2.42E+4 1.011 1.015 1.026 0.161 0.155 187.1 55.3 66.0 19.7 325.3 27.3 K106.08 2.36E+4 1.018 1.015 1.034 -0.087 -0.095 287.8 83.3 21.8 0.5 111.8 6.6 K107.08 2.59E+4 1.007 1.011 1.018 0.234 0.230 272.4 83.6 160.2 2.4 70.0 5.9 K108.08 2.32E+4 1.007 1.006 1.013 -0.115 -0.119 191.2 65.7 343.9 21.9 78.0 10.1 K109.08 2.24E+4 1.005 1.007 1.013 0.142 0.139 263.3 48.2 45.4 35.2 150.0 19.6 K110.08 1.98E+4 1.012 1.005 1.017 -0.375 -0.379 256.8 67.9 29.8 15.5 124.2 15.4 K111.08 2.00E+4 1.005 1.006 1.011 0.095 0.092 249.6 38.3 22.9 41.0 137.5 25.6 K113.08 2.67E+4 1.011 1.010 1.022 -0.047 -0.052 192.5 70.8 23.3 18.9 292.2 3.3 K114.08 1.97E+4 1.002 1.006 1.009 0.547 0.545 218.7 30.7 352.7 49.5 113.6 23.7 K115.08 2.55E+4 1.013 1.006 1.019 -0.358 -0.362 264.3 48.0 127.5 33.2 21.8 22.5 K116.08 2.13E+4 1.003 1.006 1.009 0.409 0.407 228.4 35.5 9.8 47.6 123.4 20.0 K117.08 1.81E+4 1.003 1.006 1.009 0.340 0.338 225.7 37.8 12.6 47.2 121.9 17.0 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i K118.08 7.76E+4 1.006 1.030 1.039 0.674 0.670 194.4 26.7 300.1 28.3 68.7 49.2 K119.08 8.05E+4 1.002 1.006 1.008 0.579 0.578 340.8 86.0 199.5 3.1 109.3 2.5 K120.08 6.60E+4 1.006 1.003 1.009 -0.273 -0.275 147.9 79.6 23.3 5.9 292.4 8.5 K121.08 8.09E+4 1.007 1.006 1.013 -0.087 -0.090 211.6 41.6 18.8 47.7 115.9 6.4 K122.08 5.56E+4 1.003 1.006 1.010 0.323 0.320 142.5 72.1 342.0 16.9 250.2 5.6 K123.08 5.45E+4 1.003 1.004 1.007 0.237 0.235 169.7 86.6 335.9 3.3 66.0 0.8 K124.08 5.59E+4 1.002 1.005 1.008 0.415 0.414 157.0 60.6 7.2 25.9 270.8 12.8 K125.08 6.74E+4 1.001 1.005 1.006 0.552 0.551 13.9 54.8 160.3 30.4 259.9 16.0 K126.08 5.80E+4 1.004 1.004 1.008 -0.010 -0.012 154.0 52.7 357.1 35.1 259.1 11.2 K127.08 6.85E+4 1.003 1.003 1.006 -0.061 -0.062 53.6 77.6 156.4 2.8 247.0 12.1 K128.08 7.41E+4 1.028 1.007 1.037 -0.584 -0.590 311.3 7.7 60.8 68.1 218.4 20.4 K129.08 4.46E+4 1.000 1.007 1.009 0.927 0.927 149.3 36.3 293.3 47.7 45.0 18.6 K130.08 7.90E+4 1.002 1.002 1.004 0.156 0.155 212.2 4.7 113.3 62.0 304.6 27.5 K131.08 7.29E+4 1.013 1.011 1.024 -0.097 -0.103 314.5 0.6 219.0 83.5 44.5 6.4 K132.08 8.43E+4 1.008 1.021 1.030 0.457 0.452 319.6 2.3 181.9 86.9 49.7 2.1 K133.08 4.79E+4 1.003 1.003 1.007 0.055 0.053 200.4 47.5 99.6 9.8 1.0 40.8 K134.08 3.87E+4 1.004 1.005 1.009 0.156 0.153 162.7 45.6 278.7 23.2 26.4 35.3 K135.08 5.78E+4 1.010 1.005 1.015 -0.300 -0.303 143.9 47.7 288.6 36.5 32.7 18.2 K136.08 5.27E+4 1.008 1.004 1.011 -0.363 -0.365 161.9 11.6 259.8 33.9 55.7 53.6 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i S01.08 1.30E+4 1.011 1.014 1.026 0.126 0.120 60.9 48.9 197.9 32.5 303.0 22.2 S02.08 1.31E+4 1.011 1.015 1.027 0.151 0.144 65.3 52.8 207.4 30.9 309.0 18.6 S03.08 1.43E+4 1.009 1.011 1.020 0.116 0.111 78.7 60.4 223.6 25.0 320.7 14.9 S04.08 1.19E+4 1.020 1.006 1.027 -0.525 -0.530 65.3 18.6 183.7 54.7 324.7 28.8 S05.08 1.18E+4 1.015 1.003 1.019 -0.654 -0.657 35.9 11.8 136.8 42.1 293.6 45.5 S06.08 1.17E+4 1.009 1.009 1.019 0.007 0.002 54.0 8.5 174.4 73.5 321.9 14.0 S07.08 1.14E+4 1.013 1.011 1.025 -0.072 -0.078 67.1 16.0 180.6 54.3 327.2 31.0 S08.08 1.23E+4 1.012 1.011 1.023 -0.048 -0.054 70.9 31.9 202.9 47.1 323.7 25.4 S09.08 9.80E+3 1.015 1.002 1.018 -0.758 -0.760 3.6 45.3 235.0 31.6 125.9 27.9 S10.08 9.93E+3 1.013 1.004 1.018 -0.554 -0.557 356.3 42.6 207.7 42.8 101.9 16.3 S11.08 8.25E+3 1.015 1.003 1.020 -0.674 -0.676 357.0 45.7 264.1 2.8 171.3 44.2 S12.08 7.95E+3 1.018 1.006 1.025 -0.509 -0.514 352.9 52.2 123.6 26.8 227.0 24.5 S13.08 1.25E+4 1.009 1.010 1.020 0.049 0.044 33.3 39.5 200.7 49.9 298.1 6.2 S14.08 1.16E+4 1.013 1.007 1.020 -0.271 -0.275 35.6 30.3 185.5 55.9 297.2 14.0 Appendix A, page 3 of 9 Appendix A S15.08 1.18E+4 1.016 1.005 1.021 -0.545 -0.548 24.1 32.1 178.3 55.1 286.3 12.2 S16.08 1.24E+4 1.012 1.010 1.023 -0.090 -0.096 39.2 33.8 222.7 56.1 130.3 1.6 S17.08 1.19E+4 1.013 1.006 1.020 -0.387 -0.391 41.4 36.4 208.1 52.8 306.6 6.4 S18.08 1.36E+4 1.009 1.013 1.023 0.168 0.162 33.8 23.4 183.9 63.4 298.6 11.8 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i S19.08 3.92E+4 1.000 1.002 1.002 0.738 0.738 68.7 45.2 190.8 27.8 300.0 31.9 S20.08 3.76E+4 1.006 1.003 1.009 -0.230 -0.232 81.7 84.2 196.1 2.4 286.4 5.3 S21.08 3.89E+4 1.003 1.002 1.005 -0.097 -0.098 29.1 63.9 132.4 6.5 225.5 25.2 S22.08 4.40E+4 1.003 1.005 1.008 0.311 0.309 63.4 70.4 214.4 17.3 307.2 9.0 S23.08 4.66E+4 1.002 1.001 1.003 -0.219 -0.220 105.8 27.3 351.3 38.9 220.5 39.0 S24.08 4.15E+4 1.001 1.002 1.002 0.291 0.291 73.9 48.8 341.6 2.0 249.8 41.1 S25.08 4.50E+4 1.002 1.002 1.005 -0.041 -0.042 73.5 48.2 341.2 2.1 249.3 41.7 S26.08 4.40E+4 1.005 1.003 1.008 -0.327 -0.329 15.0 19.6 113.7 23.1 248.8 59.0 S27.08 4.73E+4 1.004 1.004 1.008 0.055 0.053 310.2 7.0 54.8 64.0 217.0 24.9 S28.08 4.69E+4 1.004 1.003 1.007 -0.161 -0.162 305.0 16.5 77.6 66.4 210.0 16.4 S29.08 4.72E+4 1.004 1.003 1.007 -0.060 -0.062 303.2 14.2 51.9 51.7 203.0 34.7 S30.08 4.57E+4 1.003 1.003 1.006 -0.149 -0.150 303.0 3.7 37.5 50.2 209.9 39.6 S31.08 4.46E+4 1.004 1.003 1.008 -0.189 -0.191 311.1 16.2 56.5 42.2 205.2 43.3 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i D33.08 6.21E+4 1.019 1.012 1.031 -0.223 -0.230 205.0 46.8 347.4 36.6 92.7 19.6 D35.08 4.05E+4 1.012 1.033 1.047 0.456 0.447 238.2 26.1 337.3 17.9 97.9 57.6 D38.08 5.33E+4 1.023 1.025 1.049 0.044 0.032 178.2 18.5 11.5 71.0 269.6 4.1 D39.08 3.86E+4 1.022 1.012 1.035 -0.318 -0.326 243.9 9.6 338.3 24.6 134.2 63.4 D40.08 6.02E+4 1.026 1.029 1.055 0.047 0.034 186.9 30.0 11.6 59.9 278.1 2.1 D41.08 6.26E+4 1.021 1.180 1.227 0.776 0.757 282.7 7.6 190.7 15.1 38.7 73.0 D42.08 5.95E+4 1.023 1.207 1.260 0.784 0.763 289.7 3.3 198.9 13.8 32.8 75.8 D44.08 5.74E+4 1.048 1.023 1.074 -0.335 -0.351 278.2 5.1 187.5 7.6 42.1 80.8 D46.08 7.18E+4 1.050 1.017 1.071 -0.480 -0.493 239.3 33.4 117.6 38.6 355.4 33.7 D48.08 5.90E+4 1.006 1.029 1.038 0.641 0.635 38.3 4.8 211.0 85.2 308.2 0.6 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i K2.08 1.12E+5 1.018 1.064 1.087 0.550 0.536 154.4 37.3 50.8 17.2 301.0 47.6 K3.08 1.08E+5 1.014 1.039 1.055 0.474 0.464 183.7 43.4 76.2 17.6 330.1 41.4 K4.08 1.10E+5 1.035 1.041 1.078 0.080 0.061 205.4 19.8 295.5 0.2 26.2 70.2 K5.08 1.16E+5 1.024 1.039 1.065 0.228 0.213 220.7 18.9 126.6 11.7 6.6 67.5 K7.08 6.31E+4 1.012 1.015 1.028 0.111 0.104 191.2 11.3 284.6 16.8 68.9 69.5 K10.08 1.20E+5 1.009 1.117 1.143 0.844 0.835 192.1 7.6 284.4 16.9 78.8 71.3 K11.08 1.08E+5 1.004 1.091 1.109 0.910 0.906 242.1 6.8 150.9 10.4 4.7 77.5 K14.08 9.96E+4 1.006 1.065 1.079 0.819 0.813 9.9 12.3 279.2 3.0 175.7 77.3 K12.08 5.18E+4 1.004 1.066 1.079 0.894 0.891 193.5 12.8 288.0 19.1 71.6 66.7 K16.08 1.14E+5 1.015 1.132 1.165 0.782 0.768 20.8 1.1 290.6 11.9 116.2 78.1 K13.08 1.26E+5 1.020 1.204 1.254 0.807 0.789 283.8 2.8 193.5 6.3 37.5 83.1 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i K17.08 2.91E+4 1.003 1.046 1.055 0.871 0.869 69.3 75.5 242.3 14.4 332.7 1.7 K19.08 2.67E+4 1.003 1.065 1.077 0.902 0.899 169.0 87.3 68.7 0.5 338.7 2.7 K20.08 3.26E+4 1.005 1.059 1.072 0.839 0.834 70.3 69.0 246.2 21.0 336.7 1.4 K22.08 1.38E+4 1.001 1.013 1.016 0.838 0.837 67.7 3.2 288.5 85.8 157.9 2.7 K23.08 1.54E+4 1.001 1.015 1.018 0.875 0.874 54.6 16.6 241.2 73.2 145.2 1.8 K24.08 3.63E+4 1.007 1.008 1.015 0.061 0.057 320.6 72.0 65.1 4.7 156.5 17.4 K26.08 4.76E+4 1.004 1.003 1.007 -0.078 -0.080 60.0 53.2 217.1 34.6 314.8 11.0 K27.08 4.70E+4 1.004 1.005 1.008 0.081 0.079 86.2 42.6 250.5 46.3 348.9 7.9 K28.08 3.44E+4 1.003 1.002 1.005 -0.135 -0.136 86.4 33.8 256.1 55.7 353.2 4.8 K30.08 2.84E+4 1.003 1.009 1.013 0.500 0.498 242.2 56.0 71.8 33.6 338.8 4.5 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i K102.08 2.84E+4 1.016 1.008 1.025 -0.361 -0.366 327.3 33.0 82.7 33.5 205.4 39.1 K104.08 2.58E+4 1.014 1.009 1.023 -0.234 -0.240 308.1 4.7 45.0 55.8 215.0 33.8 K105.08 2.55E+4 1.022 1.009 1.032 -0.430 -0.437 232.8 51.8 99.8 28.2 356.4 23.5 K106.08 2.56E+4 1.035 1.013 1.050 -0.442 -0.452 268.7 74.3 16.6 4.9 107.9 14.9 K107.08 2.58E+4 1.014 1.009 1.023 -0.221 -0.227 308.1 31.4 168.8 51.2 51.3 20.4 K108.08 2.41E+4 1.007 1.008 1.015 0.072 0.068 296.9 16.6 189.1 45.7 41.2 39.6 K109.08 2.41E+4 1.016 1.006 1.023 -0.436 -0.440 244.6 41.6 27.5 41.9 136.1 19.6 K111.08 2.13E+4 1.017 1.006 1.024 -0.473 -0.477 251.4 45.6 25.8 34.4 133.9 24.4 K113.08 2.89E+4 1.031 1.009 1.042 -0.554 -0.561 216.9 62.4 16.9 26.2 111.0 8.2 K115.08 2.62E+4 1.021 1.013 1.035 -0.246 -0.254 219.5 43.9 125.1 4.6 30.4 45.7 K116.08 2.27E+4 1.012 1.006 1.018 -0.333 -0.337 224.8 35.8 1.3 45.1 116.7 23.2 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i K118.08 1.04E+5 1.013 1.008 1.021 -0.263 -0.268 251.3 32.7 350.9 14.5 101.3 53.4 K120.08 6.25E+4 1.014 1.001 1.017 -0.803 -0.804 238.7 4.9 60.4 85.1 328.7 0.1 K122.08 5.13E+4 1.010 1.003 1.014 -0.573 -0.575 38.2 21.4 138.3 24.2 271.5 56.7 K123.08 5.27E+4 1.011 1.002 1.014 -0.706 -0.708 46.3 22.7 312.1 9.9 200.1 65.0 K125.08 6.63E+4 1.012 1.003 1.016 -0.585 -0.587 38.8 33.9 137.9 13.3 246.1 52.8 K128.08 7.18E+4 1.020 1.028 1.048 0.175 0.164 122.1 2.8 29.9 38.9 215.5 50.9 K129.08 4.12E+4 1.004 1.009 1.013 0.415 0.413 76.2 39.7 323.8 24.7 210.9 40.3 K130.08 7.18E+4 1.005 1.004 1.009 -0.058 -0.060 100.7 35.1 10.2 0.7 279.2 54.9 K132.08 7.65E+4 1.008 1.029 1.039 0.545 0.538 343.7 25.6 90.3 30.8 221.6 47.9

Appendix A, page 4 of 9 Appendix A K136.08 4.64E+4 1.010 1.004 1.015 -0.376 -0.379 31.6 26.1 124.2 5.3 224.9 63.3 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i A0109 5.75E+4 1.010 1.021 1.031 0.372 0.366 258.6 34.7 50.7 52.0 158.9 13.7 A0209 1.47E+5 1.024 1.075 1.105 0.498 0.480 31.4 28.0 212.6 61.9 121.7 0.5 A0309 6.64E+4 1.008 1.039 1.050 0.644 0.637 25.1 42.5 233.5 43.8 129.0 14.6 A0409 6.50E+4 1.004 1.031 1.039 0.751 0.747 326.6 75.0 213.6 6.0 122.1 13.7 A0509 7.35E+4 1.002 1.035 1.042 0.892 0.890 228.8 3.4 328.2 70.3 137.6 19.4 A0609 9.45E+4 1.007 1.030 1.040 0.619 0.613 274.2 63.7 9.5 2.6 100.8 26.2 A0709 1.01E+5 1.006 1.099 1.120 0.872 0.865 29.8 36.8 229.0 51.6 126.9 9.4 A0809 6.61E+4 1.014 1.013 1.028 -0.024 -0.031 22.4 12.1 290.1 10.7 159.6 73.7 A0909 5.42E+4 1.011 1.020 1.031 0.308 0.301 127.8 12.1 218.4 2.9 321.8 77.5 A1009 6.01E+4 1.003 1.036 1.044 0.828 0.825 339.3 6.3 70.1 6.7 206.8 80.8 A1109 7.65E+4 1.013 1.011 1.024 -0.050 -0.055 352.6 3.6 82.8 3.9 220.4 84.7 A1209 6.69E+4 1.031 1.019 1.052 -0.228 -0.240 327.2 4.2 58.6 18.5 225.0 71.0 A1309 6.86E+4 1.016 1.015 1.032 -0.024 -0.032 158.8 2.7 68.7 0.9 321.0 87.2 A1409 6.47E+4 1.033 1.006 1.043 -0.703 -0.708 343.4 3.4 252.4 17.0 84.4 72.6 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i A1509 5.80E+4 1.023 1.015 1.039 -0.215 -0.224 119.7 57.8 8.0 13.1 270.6 28.9 A1609 4.24E+4 1.106 1.032 1.148 -0.528 -0.551 146.5 42.2 15.3 36.0 263.7 26.8 A1709 5.83E+4 1.051 1.007 1.064 -0.745 -0.752 160.9 55.1 349.6 34.6 256.8 4.1 A1809 5.60E+4 1.033 1.001 1.039 -0.927 -0.928 121.2 60.0 14.9 9.2 279.9 28.2 A1909 6.19E+4 1.034 1.019 1.054 -0.282 -0.294 158.8 60.6 11.0 25.5 274.4 13.7 A2009 5.27E+4 1.041 1.018 1.061 -0.380 -0.393 97.8 76.6 195.0 1.7 285.4 13.3 A2109 5.99E+4 1.023 1.016 1.040 -0.193 -0.203 152.5 46.0 24.2 30.9 275.7 27.9 A2209 5.17E+4 1.076 1.039 1.121 -0.315 -0.340 82.2 76.4 209.7 8.3 301.2 10.6 A2309 5.47E+4 1.063 1.065 1.132 0.017 -0.013 110.1 77.0 15.3 1.1 285.1 13.0 A2409 5.13E+4 1.051 1.068 1.123 0.135 0.107 104.6 72.1 4.3 3.3 273.3 17.5 A2509 4.85E+4 1.013 1.026 1.040 0.333 0.325 26.7 27.6 191.4 61.5 293.4 6.4 A2609 5.60E+4 1.070 1.052 1.127 -0.147 -0.176 190.7 70.2 39.5 17.5 306.7 8.9 A2709 4.81E+4 1.010 1.046 1.061 0.652 0.644 69.5 69.5 204.4 14.8 298.1 13.9 A2809 5.42E+4 1.044 1.047 1.093 0.024 0.002 56.8 69.9 211.9 18.4 304.5 7.9 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i A2909 9.50E+4 1.025 1.087 1.120 0.539 0.519 154.9 1.7 64.3 18.9 250.0 71.0 A3009 8.23E+4 1.007 1.087 1.105 0.841 0.835 150.5 5.5 58.0 24.8 252.2 64.5 A3109 9.11E+4 1.025 1.108 1.144 0.608 0.588 114.1 25.2 16.5 15.8 257.6 59.6 A3209 9.37E+4 1.017 1.194 1.240 0.822 0.806 95.4 23.2 3.4 4.6 262.8 66.3 A3309 9.54E+4 1.014 1.035 1.051 0.412 0.402 13.5 12.6 107.3 16.4 247.8 69.1 A3409 9.58E+4 1.019 1.029 1.049 0.222 0.211 17.5 9.7 112.2 25.5 268.4 62.5 A3509 9.30E+4 1.021 1.020 1.041 -0.038 -0.048 214.2 7.2 119.4 33.4 314.7 55.6 A3609 7.89E+4 1.017 1.027 1.045 0.209 0.199 183.3 36.0 281.2 10.7 25.1 52.0 A3709 7.51E+4 1.012 1.034 1.049 0.463 0.454 130.4 23.3 228.1 17.3 351.4 60.3 A3809 8.66E+4 1.016 1.111 1.141 0.734 0.720 274.2 0.8 184.0 15.7 7.1 74.3 A3909 7.57E+4 1.013 1.086 1.109 0.722 0.710 117.5 3.9 208.8 19.0 16.4 70.6 A4009 9.40E+4 1.040 1.151 1.208 0.563 0.532 251.8 8.4 159.3 16.5 7.9 71.4 A4109 9.59E+4 1.031 1.163 1.215 0.660 0.634 266.6 3.8 176.1 7.6 22.7 81.5 A4209 8.61E+4 1.022 1.154 1.197 0.734 0.714 241.3 14.9 148.2 11.8 21.2 70.8 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i A4309 2.63E+4 1.004 1.008 1.012 0.356 0.354 240.7 14.0 56.7 76.0 150.4 0.9 A4409 3.00E+4 1.003 1.019 1.024 0.723 0.720 68.5 73.2 216.8 14.4 309.0 8.4 A4509 2.87E+4 1.005 1.011 1.016 0.342 0.339 226.6 51.0 68.7 36.9 330.4 10.9 A4609 2.65E+4 1.011 1.013 1.023 0.094 0.089 248.9 64.6 71.6 25.4 341.1 1.1 A4709 2.80E+4 1.007 1.012 1.019 0.307 0.303 232.4 30.6 80.7 56.1 330.4 13.1 A4809 2.85E+4 1.009 1.010 1.019 0.026 0.021 232.3 30.2 60.8 59.5 324.5 3.7 A4909 3.18E+4 1.008 1.007 1.015 -0.063 -0.067 224.3 47.9 68.9 39.4 328.5 12.4 A5009 3.83E+4 1.017 1.026 1.044 0.217 0.207 297.5 22.1 40.0 28.0 174.8 53.0 A5109 3.47E+4 1.010 1.012 1.022 0.097 0.092 39.3 24.0 241.0 64.5 133.1 8.4 A5109 3.76E+4 1.007 1.011 1.019 0.230 0.226 39.1 2.2 288.7 83.8 129.3 5.8 A5209 3.57E+4 1.019 1.008 1.028 -0.394 -0.400 197.1 5.6 292.5 44.0 101.3 45.5 A5209 3.46E+4 1.010 1.012 1.022 0.108 0.103 43.7 25.6 226.5 64.4 134.2 1.1 A5309 3.55E+4 1.018 1.009 1.028 -0.341 -0.347 37.8 15.8 273.4 63.4 134.0 20.8 A5409 3.71E+4 1.004 1.007 1.012 0.241 0.238 21.4 17.8 178.2 70.7 289.1 7.1 A5409 3.70E+4 1.005 1.007 1.012 0.226 0.223 20.5 16.0 179.3 72.9 288.8 5.9 A5509 3.24E+4 1.006 1.015 1.022 0.401 0.397 42.5 54.3 222.7 35.7 132.6 0.1 A5509 3.23E+4 1.007 1.015 1.023 0.351 0.346 42.7 54.2 220.0 35.8 310.9 1.3 A5609 3.25E+4 1.014 1.034 1.050 0.403 0.393 351.7 17.8 256.2 16.6 125.9 65.3 A5609 3.24E+4 1.015 1.034 1.050 0.382 0.372 350.7 18.5 255.2 16.1 126.8 65.1 A5609-2 3.04E+4 1.026 1.016 1.044 -0.235 -0.245 349.7 21.6 243.7 35.0 104.8 47.1 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i A5709 5.29E+4 1.028 1.016 1.045 -0.275 -0.285 105.5 43.3 2.4 13.5 259.2 43.6 A5709 5.26E+4 1.028 1.016 1.045 -0.252 -0.262 105.5 43.3 2.3 13.6 259.1 43.5 A5809 4.86E+4 1.005 1.013 1.018 0.449 0.445 122.5 50.7 357.7 25.0 253.3 28.1 A5909 4.94E+4 1.012 1.022 1.034 0.301 0.293 96.7 67.0 189.2 1.1 279.6 23.0 A6009 4.97E+4 1.007 1.012 1.020 0.256 0.251 112.6 53.2 10.0 9.2 273.4 35.2 A6109 5.29E+4 1.009 1.009 1.018 -0.010 -0.014 122.4 58.1 10.8 12.9 273.6 28.6 A6209 5.31E+4 1.008 1.013 1.021 0.243 0.238 118.8 71.4 15.1 4.6 283.6 18.0 Appendix A, page 5 of 9 Appendix A A6309 4.67E+4 1.002 1.017 1.021 0.761 0.759 143.4 68.0 14.5 14.2 280.2 16.4 A6309-2 4.93E+4 1.006 1.016 1.023 0.455 0.450 102.7 69.1 359.0 5.2 267.1 20.2 A6409 4.23E+4 1.006 1.015 1.021 0.447 0.443 300.6 70.8 179.1 10.3 86.1 16.0 A6509 5.39E+4 1.005 1.011 1.017 0.343 0.339 176.7 27.9 358.1 62.1 267.0 0.6 A6609 5.92E+4 1.001 1.013 1.016 0.822 0.821 153.7 46.8 8.5 37.6 264.0 18.0 A6709 5.40E+4 1.003 1.040 1.049 0.846 0.843 100.8 28.3 191.6 1.5 284.5 61.6 A6809 5.43E+4 1.002 1.010 1.013 0.630 0.628 12.6 82.8 181.2 7.0 271.4 1.4 A6909 5.36E+4 1.002 1.046 1.054 0.903 0.901 91.7 25.1 184.9 6.8 288.9 63.9 A7009 5.38E+4 1.003 1.013 1.017 0.587 0.585 194.5 1.6 102.1 55.8 285.5 34.1 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i B0109 1.18E+5 1.077 1.018 1.102 -0.615 -0.629 178.2 1.1 87.7 22.9 270.8 67.1 B0209 1.11E+5 1.007 1.048 1.061 0.736 0.730 107.8 18.7 12.2 16.1 244.1 65.0 B0409 9.86E+4 1.040 1.019 1.061 -0.342 -0.355 4.2 7.0 273.1 9.5 130.1 78.1 B0409 1.14E+5 1.022 1.016 1.039 -0.166 -0.175 357.1 31.5 112.5 34.9 237.2 39.2 B0509 9.49E+4 1.016 1.008 1.024 -0.341 -0.346 338.9 2.3 70.9 40.7 246.1 49.2 B0609 1.14E+5 1.040 1.013 1.056 -0.505 -0.514 139.6 4.8 44.8 45.0 234.3 44.6 B0709 1.12E+5 1.029 1.037 1.067 0.120 0.104 339.0 11.7 71.3 10.6 202.4 74.1 B0809 1.30E+5 1.012 1.018 1.030 0.175 0.168 47.3 8.4 138.1 5.6 261.7 79.9 B0909 1.21E+5 1.009 1.023 1.034 0.430 0.423 105.3 7.2 13.0 17.6 216.7 70.9 B1009 1.25E+5 1.016 1.047 1.066 0.489 0.478 63.0 0.9 332.6 24.3 155.0 65.6 B1109 1.34E+5 1.007 1.037 1.048 0.661 0.655 42.2 11.8 308.4 17.7 164.2 68.6 B1209 1.22E+5 1.020 1.037 1.059 0.296 0.283 312.1 16.9 48.6 20.5 185.6 62.9 B1309 1.13E+5 1.014 1.029 1.044 0.350 0.340 201.6 1.7 292.1 19.3 106.8 70.6 B1409 1.02E+5 1.016 1.003 1.020 -0.680 -0.682 35.9 56.2 217.8 33.8 127.2 0.9 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i B1509 8.00E+4 1.014 1.030 1.045 0.353 0.344 27.3 65.9 193.2 23.4 285.5 5.2 B1609 8.75E+4 1.000 1.006 1.007 0.865 0.864 243.5 41.3 338.0 5.1 73.7 48.3 B1709 8.69E+4 1.009 1.010 1.019 0.048 0.043 25.4 72.0 193.2 17.6 284.3 3.6 B1809 1.17E+5 1.019 1.043 1.064 0.393 0.380 300.2 12.5 31.6 6.1 147.0 76.1 B1909 1.04E+5 1.004 1.005 1.008 0.125 0.123 0.4 46.3 225.0 34.2 117.7 23.6 B2009 1.06E+5 1.004 1.002 1.006 -0.318 -0.320 7.1 19.3 235.5 62.2 104.1 19.2 B2109 1.07E+5 1.003 1.010 1.014 0.507 0.505 314.3 10.0 218.9 28.1 62.0 59.8 B2209 9.53E+4 1.009 1.023 1.034 0.429 0.422 175.1 79.2 28.0 9.1 297.1 5.8 B2309 9.15E+4 1.003 1.011 1.015 0.517 0.515 203.4 59.4 22.8 30.6 113.0 0.3 B2409 1.24E+5 1.030 1.074 1.109 0.420 0.399 309.3 19.9 219.3 0.2 128.7 70.1 B2509 1.35E+5 1.019 1.123 1.157 0.727 0.710 300.7 17.6 33.3 8.3 147.6 70.4 B2609 1.35E+5 1.040 1.078 1.123 0.318 0.292 309.8 20.5 216.6 8.4 105.4 67.7 B2709 1.28E+5 1.056 1.121 1.188 0.355 0.318 308.8 18.0 39.8 3.0 138.8 71.8 B2809 1.02E+5 1.013 1.088 1.111 0.743 0.732 315.3 17.4 45.8 1.6 140.8 72.5 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i D0109 3.95E+4 1.058 1.084 1.147 0.177 0.144 3.9 68.8 189.6 21.1 98.9 1.9 D0209 4.36E+4 1.012 1.048 1.064 0.607 0.597 2.1 38.2 159.0 49.4 262.8 11.6 D0309 2.48E+4 1.043 1.046 1.090 0.032 0.010 14.5 19.0 133.5 54.6 273.7 28.6 D0409 2.01E+4 1.018 1.037 1.057 0.355 0.343 18.7 27.9 152.1 52.3 275.7 23.1 D0509 2.07E+4 1.014 1.031 1.046 0.374 0.365 356.9 16.6 164.1 73.0 265.9 3.6 D0609 2.10E+4 1.030 1.008 1.041 -0.574 -0.581 359.3 22.6 120.4 51.1 255.5 29.8 D0709 1.90E+4 1.015 1.009 1.023 -0.259 -0.265 329.7 4.0 197.8 84.0 60.0 4.4 D0809 2.18E+4 1.031 1.083 1.121 0.448 0.426 149.4 23.6 243.9 10.1 355.3 64.1 D0909 2.16E+4 1.018 1.052 1.074 0.479 0.465 38.2 8.1 137.9 49.6 301.5 39.2 D1009 2.03E+4 1.034 1.031 1.067 -0.042 -0.059 217.1 15.2 104.2 55.1 316.3 30.6 D1109 2.14E+4 1.017 1.044 1.064 0.429 0.416 49.0 15.3 160.3 53.1 308.9 32.7 D1209 2.26E+4 1.007 1.047 1.059 0.732 0.726 151.1 59.3 59.2 1.1 328.6 30.7 D1309 1.99E+4 1.025 1.041 1.068 0.244 0.229 52.0 36.5 194.8 47.1 307.0 19.3 D1409 2.17E+4 1.025 1.044 1.071 0.282 0.266 51.4 39.9 199.2 45.3 306.9 16.7 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i D1509 4.75E+4 1.002 1.001 1.003 -0.194 -0.195 25.2 7.9 119.3 27.7 280.7 61.1 D1609 4.88E+4 1.008 1.001 1.011 -0.718 -0.719 181.1 39.8 22.1 48.3 280.0 10.6 D1709 4.64E+4 1.010 1.003 1.014 -0.550 -0.552 173.7 25.4 58.9 41.5 285.4 37.9 D1809 5.29E+4 1.008 1.007 1.015 -0.106 -0.109 149.3 61.7 52.0 3.9 319.9 28.0 D1909 5.25E+4 1.007 1.019 1.027 0.424 0.419 96.6 61.2 238.0 23.3 335.1 16.0 D2009 3.84E+4 1.004 1.002 1.006 -0.394 -0.395 178.4 51.7 53.4 24.4 309.7 27.6 D2109 4.68E+4 1.007 1.002 1.010 -0.578 -0.580 188.4 41.0 81.6 18.4 333.4 43.3 D2209 5.34E+4 1.003 1.020 1.025 0.763 0.760 121.0 78.5 250.1 7.3 341.3 8.9 D2309 4.51E+4 1.000 1.010 1.011 0.962 0.962 254.3 51.3 78.5 38.7 346.8 2.0 D2409 4.65E+4 1.000 1.005 1.006 0.848 0.847 72.5 14.6 265.5 75.0 163.3 3.2 D2509 4.38E+4 1.002 1.024 1.029 0.848 0.846 261.0 78.1 79.0 11.9 169.1 0.4 D2609 4.77E+4 1.002 1.013 1.016 0.778 0.777 263.0 85.9 79.4 4.0 169.4 0.2 D2709 5.94E+4 1.001 1.025 1.030 0.899 0.898 258.9 17.6 86.6 72.3 349.6 2.2 D2809 5.90E+4 1.001 1.021 1.025 0.909 0.908 326.7 85.8 79.1 1.6 169.3 3.9 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i D2909 1.12E+5 1.026 1.055 1.084 0.345 0.328 324.4 8.1 233.9 3.8 119.0 81.1 D3009 1.25E+5 1.019 1.073 1.098 0.585 0.571 334.0 9.5 243.8 1.2 146.8 80.4 D3109 1.27E+5 1.035 1.057 1.095 0.230 0.209 347.6 3.3 256.7 15.8 89.0 73.9 D3209 1.42E+5 1.026 1.091 1.125 0.548 0.528 347.0 4.4 256.9 1.5 148.6 85.4 D3309 9.86E+4 1.019 1.023 1.043 0.087 0.076 326.4 17.2 56.5 0.2 147.2 72.8 Appendix A, page 6 of 9 Appendix A D3409 1.30E+5 1.013 1.075 1.096 0.690 0.678 42.6 7.8 311.3 9.0 172.9 78.0 D3509 8.26E+4 1.007 1.007 1.014 0.040 0.037 340.2 6.6 70.7 4.1 192.7 82.2 D3609 1.53E+5 1.057 1.044 1.104 -0.134 -0.159 0.9 10.7 92.7 9.4 223.1 75.7 D3709 1.52E+5 1.026 1.088 1.122 0.540 0.520 349.0 12.4 82.1 14.1 219.0 71.0 D3809 1.28E+5 1.039 1.046 1.087 0.083 0.062 10.3 19.0 279.5 2.3 182.9 70.8 D3909 1.37E+5 1.011 1.063 1.081 0.698 0.689 8.1 19.4 98.4 0.7 190.3 70.6 D4009 1.20E+5 1.013 1.064 1.084 0.661 0.651 327.8 7.1 60.5 20.7 219.7 68.0 D4109 9.50E+4 1.003 1.048 1.057 0.887 0.885 3.8 17.3 269.3 14.1 142.1 67.4 D4209 1.43E+5 1.017 1.062 1.085 0.554 0.541 326.1 12.5 57.6 6.6 174.8 75.9 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i E0109 6.60E+4 1.015 1.018 1.034 0.082 0.074 3.5 71.5 184.9 18.5 94.8 0.4 E0209 6.00E+4 1.016 1.021 1.038 0.124 0.115 359.9 72.6 185.9 17.3 95.3 1.7 E0309 6.08E+4 1.017 1.024 1.041 0.167 0.157 5.3 68.0 189.5 21.9 99.0 1.5 E0409 6.63E+4 1.011 1.015 1.026 0.163 0.157 16.8 69.1 188.9 20.8 279.9 2.6 E0509 6.46E+4 1.010 1.013 1.023 0.136 0.131 63.9 76.7 185.7 7.1 277.1 11.2 E0609 6.05E+4 1.016 1.016 1.032 0.006 -0.002 23.7 69.3 188.8 20.1 280.6 4.9 E0709 6.79E+4 1.010 1.018 1.029 0.260 0.254 28.7 71.3 190.4 17.8 282.2 5.5 E0809 9.47E+4 1.013 1.017 1.030 0.136 0.128 348.7 74.6 192.6 14.2 101.1 6.0 E0909 9.14E+4 1.011 1.016 1.027 0.180 0.174 355.3 67.6 188.2 21.8 96.4 4.5 E1009 8.77E+4 1.009 1.015 1.024 0.233 0.228 333.7 71.4 188.6 15.4 95.8 10.1 E1109 9.25E+4 1.016 1.010 1.027 -0.225 -0.231 329.7 69.4 173.4 19.0 80.8 7.7 E1409 1.03E+5 1.016 1.024 1.041 0.194 0.185 340.4 68.8 169.0 21.0 77.9 2.9 E1209 9.37E+4 1.009 1.014 1.023 0.239 0.234 348.6 74.2 183.7 15.3 92.6 3.9 E1309 9.36E+4 1.011 1.028 1.040 0.441 0.433 254.9 25.3 3.4 33.8 136.3 45.5 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i E1509 7.31E+4 1.005 1.017 1.023 0.558 0.554 188.6 75.9 8.9 14.1 278.9 0.1 E1609 6.84E+4 1.003 1.010 1.014 0.563 0.561 77.9 69.4 180.5 4.7 272.2 20.0 E1709 7.12E+4 1.008 1.014 1.022 0.274 0.269 90.7 75.2 191.5 2.8 282.2 14.5 E1809 6.86E+4 1.008 1.011 1.019 0.196 0.192 66.1 70.4 195.0 12.6 288.3 14.8 E1909 6.71E+4 1.009 1.011 1.021 0.113 0.108 79.4 74.2 190.4 5.8 281.9 14.6 E2009 6.85E+4 1.004 1.011 1.016 0.409 0.406 49.5 66.8 188.3 17.9 283.0 14.3 E2109 7.49E+4 1.014 1.004 1.019 -0.527 -0.530 87.3 66.2 221.8 17.2 316.9 16.0 E2209 4.29E+4 1.016 1.004 1.022 -0.609 -0.612 304.9 12.0 38.5 16.3 180.2 69.6 E2309 4.14E+4 1.010 1.001 1.012 -0.869 -0.870 348.4 33.5 99.5 28.6 220.1 43.1 E2409 4.88E+4 1.013 1.037 1.052 0.483 0.474 110.0 16.5 13.7 20.3 236.3 63.4 E2409 3.93E+4 1.011 1.002 1.014 -0.638 -0.640 341.5 26.5 81.2 18.8 202.3 56.6 E2509 4.88E+4 1.014 1.036 1.052 0.452 0.442 109.4 3.2 18.2 20.8 207.8 68.9 E2609 4.92E+4 1.066 1.049 1.119 -0.150 -0.178 288.5 5.3 19.9 14.1 178.4 74.8 E2709 4.47E+4 1.059 1.041 1.102 -0.178 -0.201 107.7 5.2 16.1 17.1 214.1 72.1 E2809 3.80E+4 1.014 1.001 1.017 -0.912 -0.912 1.0 29.8 193.5 59.6 94.1 5.5 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i E2909 7.60E+4 1.009 1.017 1.027 0.295 0.289 127.2 14.9 31.1 21.6 249.1 63.3 E3009 6.87E+4 1.006 1.025 1.033 0.631 0.626 121.2 17.0 212.1 3.0 311.8 72.7 E3109 6.68E+4 1.002 1.031 1.038 0.867 0.865 138.4 25.2 45.4 6.4 302.2 63.9 E3209 7.26E+4 1.006 1.021 1.028 0.577 0.572 131.5 23.6 226.3 10.9 339.2 63.8 E3309 8.12E+4 1.002 1.047 1.056 0.902 0.900 137.7 19.6 44.8 8.0 293.8 68.7 E3409 5.75E+4 1.031 1.033 1.065 0.032 0.017 157.8 27.3 51.2 28.9 283.1 48.2 E3509 6.53E+4 1.029 1.045 1.076 0.216 0.198 108.4 11.0 201.5 15.6 344.6 70.8 E3609 7.70E+4 1.013 1.038 1.053 0.494 0.485 58.5 2.7 327.9 12.2 160.6 77.5 E3709 7.94E+4 1.022 1.046 1.071 0.339 0.325 25.9 15.3 289.2 23.0 146.7 61.9 E3809 9.12E+4 1.034 1.039 1.075 0.061 0.043 27.0 9.5 293.1 21.9 139.1 65.9 E3909 9.03E+4 1.034 1.042 1.078 0.093 0.074 25.6 13.5 288.6 27.1 139.4 59.2 E4009 8.74E+4 1.029 1.041 1.072 0.177 0.160 33.5 13.2 295.4 31.1 143.5 55.6 E4109 8.74E+4 1.042 1.021 1.065 -0.317 -0.331 21.5 11.7 285.0 28.8 131.3 58.4 E4209 7.73E+4 1.021 1.042 1.065 0.339 0.325 28.1 26.0 284.8 25.3 157.1 52.3 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i E4309 1.31E+5 1.011 1.026 1.038 0.411 0.404 137.9 13.7 42.0 22.8 256.4 63.0 E4409 1.37E+5 1.015 1.033 1.050 0.367 0.356 180.1 0.9 89.1 49.3 270.9 40.6 E4509 1.49E+5 1.011 1.060 1.077 0.690 0.681 117.2 26.9 21.6 10.8 271.7 60.7 E4609 1.53E+5 1.017 1.056 1.077 0.526 0.513 101.2 17.6 8.9 7.1 257.8 71.0 E4709 1.61E+5 1.063 1.127 1.202 0.320 0.279 110.3 2.4 18.9 31.1 204.3 58.8 E4809 1.55E+5 1.067 1.097 1.172 0.174 0.135 297.5 3.6 29.9 33.8 202.2 56.0 E4909 1.31E+5 1.014 1.036 1.052 0.418 0.407 173.4 0.3 83.3 22.6 264.2 67.4 E4909-2 1.55E+5 1.010 1.054 1.069 0.680 0.672 356.1 6.2 89.3 27.2 254.2 62.0 E4909-3 1.57E+5 1.067 1.111 1.188 0.239 0.198 293.5 4.1 26.0 31.3 196.9 58.4 E5009 1.33E+5 1.060 1.080 1.145 0.136 0.103 99.4 0.8 8.6 46.4 190.2 43.6 E5109 1.17E+5 1.010 1.039 1.052 0.597 0.589 295.3 19.5 44.7 43.2 187.8 40.4 E5209 1.44E+5 1.049 1.051 1.103 0.018 -0.007 107.0 0.0 17.0 27.0 197.0 63.0 E5309 1.41E+5 1.059 1.078 1.141 0.135 0.103 289.9 4.6 22.2 26.0 190.6 63.5 E5409 1.49E+5 1.085 1.058 1.149 -0.179 -0.213 102.1 2.1 10.5 37.4 194.8 52.5 E5509 1.63E+5 1.040 1.046 1.088 0.075 0.053 285.0 17.1 37.9 51.5 183.4 33.2 E5609 1.60E+5 1.007 1.043 1.055 0.705 0.699 266.5 29.6 17.4 32.2 144.0 43.4 E5609-2 1.54E+5 1.001 1.034 1.040 0.952 0.952 243.1 9.9 339.6 32.7 138.4 55.5 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i E5709 8.16E+4 1.209 1.137 1.378 -0.192 -0.268 297.2 62.3 105.8 27.2 198.2 4.7 Appendix A, page 7 of 9 Appendix A E5809 9.07E+4 1.033 1.395 1.498 0.823 0.793 302.0 43.3 110.1 46.1 206.3 5.9 E5909 8.03E+4 1.179 1.241 1.465 0.133 0.039 54.3 81.6 311.6 1.9 221.3 8.1 E6009 9.15E+4 1.084 1.378 1.529 0.599 0.532 309.5 49.2 119.3 40.4 213.6 5.1 E6109 8.39E+4 1.063 1.450 1.597 0.717 0.661 310.1 75.9 121.5 13.9 212.0 2.0 E6209 8.03E+4 1.077 1.448 1.610 0.667 0.602 99.9 80.9 302.3 8.4 211.8 3.4 E6309 7.79E+4 1.126 1.398 1.602 0.476 0.385 117.1 79.9 306.3 10.0 216.0 1.6 E6409 7.82E+4 1.052 1.154 1.223 0.479 0.441 304.9 8.0 192.4 69.8 37.6 18.4 E6509 8.59E+4 1.055 1.174 1.249 0.500 0.460 126.9 0.6 219.8 78.4 36.8 11.6 E6609 7.92E+4 1.104 1.155 1.277 0.187 0.128 129.4 2.1 230.8 79.7 39.1 10.1 E6709 6.84E+4 1.110 1.112 1.234 0.008 -0.045 299.6 3.0 191.4 80.3 30.0 9.2 E6809 9.08E+4 1.013 1.179 1.218 0.857 0.844 285.0 46.3 139.0 38.4 34.4 17.6 E6909 8.50E+4 1.025 1.160 1.207 0.711 0.689 300.1 26.8 146.2 60.6 35.8 11.1 E7009 7.38E+4 1.092 1.170 1.282 0.282 0.224 310.1 5.5 202.4 72.2 41.8 16.8 E7009 7.41E+4 1.093 1.171 1.284 0.280 0.222 306.0 4.6 201.7 71.8 37.5 17.6 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i E7109 1.17E+5 1.003 1.033 1.041 0.830 0.827 74.1 73.5 327.1 4.9 235.8 15.7 E7209 9.34E+4 1.002 1.016 1.019 0.803 0.802 160.6 5.5 57.1 67.7 252.8 21.5 E7309 9.95E+4 1.005 1.033 1.041 0.723 0.718 1.2 8.1 109.3 65.5 267.8 23.0 E7409 9.33E+4 1.004 1.005 1.010 0.161 0.159 12.4 7.0 124.5 72.0 280.3 16.5 E7509 9.41E+4 1.004 1.020 1.026 0.629 0.625 122.5 11.5 27.8 21.8 238.4 65.0 E7609 8.86E+4 1.001 1.007 1.009 0.653 0.652 350.6 11.1 96.0 53.5 253.0 34.3 E7709 1.01E+5 1.002 1.026 1.031 0.836 0.834 9.7 55.9 170.0 32.5 265.9 9.2 E7809 1.10E+5 1.014 1.065 1.085 0.645 0.634 81.6 56.7 301.0 26.9 201.4 18.1 E7909 1.00E+5 1.015 1.022 1.037 0.201 0.193 77.3 72.0 300.1 13.4 207.2 11.8 E8009 9.71E+4 1.014 1.043 1.060 0.519 0.508 51.3 54.1 298.3 15.9 198.3 31.3 E8109 1.51E+5 1.012 1.048 1.064 0.603 0.594 26.4 54.4 134.6 12.6 232.8 32.7 E8209 1.51E+5 1.031 1.008 1.041 -0.597 -0.603 17.0 58.8 252.4 19.0 153.7 23.8 E8309 1.45E+5 1.019 1.014 1.033 -0.148 -0.156 9.7 54.6 272.5 5.0 179.0 34.9 E8409 1.02E+5 1.030 1.016 1.047 -0.303 -0.313 233.5 84.8 19.0 4.3 109.2 2.9 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i S00109 1.33E+4 1.008 1.009 1.017 0.055 0.050 55.1 38.3 163.3 21.5 275.6 43.9 S00209 1.23E+4 1.008 1.016 1.025 0.318 0.312 31.0 2.6 124.7 54.4 299.1 35.5 S00309 1.23E+4 1.006 1.020 1.027 0.566 0.562 238.2 7.9 144.9 22.2 346.7 66.3 S00409 1.30E+4 1.006 1.007 1.013 0.086 0.083 246.0 3.5 336.7 11.3 139.0 78.1 S00509 1.24E+4 1.002 1.026 1.031 0.879 0.877 199.6 16.7 297.6 24.8 79.0 59.4 S00609 1.17E+4 1.002 1.025 1.031 0.819 0.817 331.0 21.4 225.8 33.8 87.1 48.3 S00709 7.72E+3 1.015 1.006 1.022 -0.418 -0.422 50.7 27.9 157.7 28.8 285.0 47.8 S00809 1.47E+4 1.012 1.011 1.024 -0.040 -0.046 70.6 79.6 216.6 8.7 307.5 5.7 S00909 1.39E+4 1.007 1.012 1.019 0.266 0.262 46.3 35.2 156.4 26.0 274.0 43.6 S01009 1.14E+4 1.009 1.002 1.012 -0.715 -0.716 57.3 78.8 189.2 7.6 280.3 8.3 S01109 1.00E+4 1.016 1.004 1.021 -0.629 -0.632 353.5 46.1 235.3 24.4 127.6 33.8 S01209 1.21E+4 1.020 1.004 1.026 -0.682 -0.686 322.6 46.0 195.9 30.0 87.3 28.9 S01309 1.35E+4 1.015 1.016 1.031 0.026 0.019 2.5 23.3 230.0 57.5 102.2 21.3 S01409 1.39E+4 1.008 1.013 1.022 0.221 0.216 347.3 69.0 206.7 16.5 112.9 12.6 S01509 1.41E+4 1.004 1.013 1.018 0.477 0.474 320.7 75.6 64.1 3.4 155.0 14.0 S01609 1.18E+4 1.010 1.002 1.013 -0.666 -0.668 21.4 32.8 272.4 26.8 151.8 45.2 S01709 9.91E+3 1.003 1.009 1.013 0.532 0.530 310.0 40.0 42.4 2.9 135.8 49.9 S01809 1.63E+4 1.016 1.028 1.044 0.276 0.266 232.7 75.6 350.9 6.9 82.5 12.6 S01909 2.07E+4 1.019 1.005 1.026 -0.572 -0.576 237.7 72.1 3.1 10.6 95.9 14.2 S02009 2.01E+4 1.016 1.007 1.024 -0.375 -0.380 203.9 67.0 25.2 23.0 295.0 0.5 S02109 2.21E+4 1.012 1.005 1.017 -0.396 -0.399 216.1 65.0 63.0 22.6 328.7 10.2 S021-09-2 2.74E+4 1.025 1.025 1.051 0.008 -0.004 236.1 53.6 27.4 32.9 126.5 13.8 S021-09-3 2.38E+4 1.025 1.020 1.046 -0.106 -0.117 226.0 50.7 54.3 39.0 321.0 4.1 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i S02209 1.03E+4 1.023 1.011 1.035 -0.352 -0.360 187.0 87.0 12.1 3.0 282.1 0.3 S02309 9.93E+3 1.026 1.010 1.037 -0.419 -0.426 352.9 80.9 209.3 7.4 118.6 5.4 S02409 9.69E+3 1.021 1.007 1.029 -0.508 -0.513 250.2 85.1 17.7 3.0 107.9 3.9 S02509 1.10E+4 1.018 1.014 1.032 -0.116 -0.123 280.2 80.2 13.3 0.5 103.4 9.8 S02609 1.06E+4 1.019 1.011 1.031 -0.276 -0.283 246.9 84.6 17.1 3.5 107.4 4.1 S02709 1.06E+4 1.021 1.015 1.037 -0.171 -0.180 21.7 57.7 199.1 32.3 289.8 1.2 S02809 1.18E+4 1.019 1.019 1.038 -0.008 -0.017 257.4 70.9 21.0 10.8 114.0 15.5 S02909 1.20E+4 1.025 1.026 1.052 0.003 -0.009 283.3 35.2 174.1 25.0 56.9 44.4 S03009 1.36E+4 1.051 1.024 1.078 -0.351 -0.367 258.4 76.0 14.6 6.3 106.0 12.5 S03109 1.22E+4 1.021 1.020 1.042 -0.006 -0.016 219.2 51.7 15.6 35.9 114.2 11.6 S03209 1.17E+4 1.031 1.023 1.055 -0.155 -0.168 345.9 75.9 188.9 13.0 97.7 5.3 S03309 1.19E+4 1.016 1.026 1.042 0.235 0.226 314.1 63.8 222.6 0.7 132.3 26.2 S03409 1.21E+4 1.031 1.017 1.049 -0.289 -0.300 227.0 79.1 3.7 8.0 94.7 7.4 S03509 1.21E+4 1.034 1.025 1.060 -0.148 -0.163 225.2 58.7 357.0 22.0 95.9 21.0 S03609 1.13E+4 1.012 1.039 1.054 0.519 0.509 258.1 58.1 1.3 8.1 96.1 30.7 S03709 1.15E+4 1.037 1.017 1.055 -0.372 -0.384 199.8 81.4 27.4 8.5 297.2 1.1 S03809 1.10E+4 1.035 1.021 1.058 -0.250 -0.263 178.5 17.4 339.9 71.7 86.8 5.5 S03909 1.11E+4 1.020 1.040 1.061 0.327 0.314 198.1 21.9 76.1 52.7 300.7 28.4 S04009 1.06E+4 1.019 1.027 1.047 0.180 0.169 189.6 65.7 33.2 22.5 299.6 8.8 S04109 1.05E+4 1.010 1.052 1.067 0.661 0.652 67.8 52.6 195.4 25.1 298.5 25.9 S04209 1.05E+4 1.034 1.022 1.057 -0.202 -0.215 146.4 75.2 22.5 8.4 290.7 12.1 Appendix A, page 8 of 9 Appendix A S04309 1.00E+4 1.024 1.039 1.064 0.236 0.221 129.4 55.9 37.7 1.1 307.0 34.1 S04409 1.04E+4 1.018 1.033 1.053 0.289 0.277 144.9 69.6 257.2 8.0 349.9 18.6 Name Km L F Pj T U K1d K1i K2d K2i K3d K3i S4509 3.63E+3 1.030 1.012 1.044 -0.429 -0.438 83.5 76.4 202.0 6.6 293.3 11.8 S4609 1.61E+3 1.023 1.008 1.032 -0.476 -0.482 104.1 83.5 211.5 2.0 301.7 6.2 S4709 5.94E+3 1.018 1.018 1.036 -0.005 -0.014 118.2 74.0 209.1 0.2 299.1 16.0 S4809 9.23E+3 1.020 1.019 1.039 -0.011 -0.021 92.5 69.4 186.3 1.4 276.9 20.5 S4909 5.08E+3 1.030 1.010 1.041 -0.509 -0.516 132.3 69.0 222.7 0.2 312.8 21.0 S5009 4.41E+3 1.027 1.014 1.042 -0.308 -0.317 106.9 64.6 11.6 2.5 280.4 25.2 S5109 5.50E+3 1.038 1.013 1.053 -0.477 -0.487 137.0 66.0 228.8 0.8 319.2 24.0 S5209 7.55E+3 1.021 1.008 1.029 -0.456 -0.461 127.8 74.2 23.1 4.1 292.0 15.2 S5309 7.43E+3 1.028 1.007 1.037 -0.599 -0.605 145.1 65.1 50.7 2.0 319.7 24.8 S5409 7.80E+3 1.020 1.007 1.028 -0.501 -0.506 94.7 72.4 217.1 9.6 309.6 14.6 S5509 6.75E+3 1.016 1.007 1.023 -0.384 -0.389 125.6 67.7 15.9 7.9 282.9 20.8 S5609 3.49E+3 1.014 1.002 1.017 -0.705 -0.707 104.0 64.6 209.6 7.3 302.9 24.2 S5709 1.68E+3 1.009 1.006 1.016 -0.216 -0.220 53.9 33.4 248.1 55.8 148.3 6.6 S5809 4.67E+3 1.012 1.015 1.027 0.119 0.112 274.9 77.1 103.2 12.7 12.8 1.8 S5909 2.43E+3 1.014 1.001 1.017 -0.852 -0.853 139.7 82.3 340.8 7.2 250.4 2.7 S6009 8.60E+2 1.021 1.007 1.030 -0.507 -0.513 84.2 75.8 322.9 7.5 231.3 12.0 S6109 8.01E+2 1.007 1.010 1.017 0.204 0.200 90.2 73.4 230.3 12.8 322.6 10.3 S6209 4.26E+2 1.006 1.002 1.008 -0.534 -0.535 39.1 49.6 171.6 29.9 276.8 24.5 S6309 9.70E+2 1.013 1.003 1.017 -0.680 -0.682 25.9 68.0 168.9 17.9 262.9 12.4 S6409 4.35E+2 1.009 1.004 1.013 -0.430 -0.433 102.4 86.3 270.4 3.7 0.4 0.8 S6509 9.39E+3 1.017 1.016 1.033 -0.037 -0.045 6.1 49.0 181.2 40.9 273.3 2.4 S6609 1.01E+4 1.030 1.019 1.050 -0.223 -0.234 290.3 18.5 27.9 21.7 163.5 60.9 S6709 1.44E+4 1.029 1.010 1.041 -0.480 -0.487 324.8 42.7 233.8 1.0 142.7 47.3 S6809 8.03E+3 1.022 1.019 1.041 -0.077 -0.087 41.2 63.2 244.1 25.0 149.8 9.2 S6909 1.26E+4 1.022 1.025 1.047 0.057 0.046 336.3 46.0 187.0 39.7 83.4 15.8 S7009 9.75E+3 1.022 1.003 1.027 -0.754 -0.756 249.8 30.9 142.8 26.0 20.6 47.5 S7109 9.16E+3 1.011 1.002 1.014 -0.696 -0.698 261.2 41.1 149.6 22.9 38.7 40.2 S7209 4.51E+3 1.001 1.004 1.005 0.582 0.581 184.9 54.8 334.7 31.4 73.6 14.3 S7309 7.98E+3 1.010 1.005 1.016 -0.317 -0.320 240.9 48.5 142.4 7.4 46.0 40.6 S7409 9.45E+3 1.016 1.005 1.022 -0.485 -0.489 279.3 55.6 114.3 33.5 19.6 7.0 S7509 3.60E+3 1.002 1.004 1.006 0.424 0.422 252.6 45.3 139.5 21.3 32.3 37.1 S7609 1.29E+4 1.019 1.008 1.028 -0.412 -0.417 237.1 70.6 130.9 5.6 39.0 18.5 S7709 8.20E+3 1.014 1.026 1.042 0.293 0.284 265.8 65.2 142.1 14.4 46.8 19.8 S7809 8.12E+3 1.023 1.010 1.034 -0.399 -0.406 52.7 79.0 155.6 2.5 246.0 10.7 S7909 7.93E+3 1.019 1.015 1.035 -0.118 -0.126 275.6 59.4 131.9 25.5 34.2 15.8 S8009 8.57E+3 1.032 1.012 1.046 -0.455 -0.464 275.0 73.7 166.3 5.4 74.9 15.4 S8109 1.05E+4 1.023 1.015 1.039 -0.189 -0.198 292.8 62.8 152.5 21.6 56.1 15.7 S8209 1.08E+4 1.013 1.007 1.020 -0.273 -0.278 19.5 74.4 117.8 2.3 208.4 15.4

Appendix A, page 9 of 9

Appendix B

Series Lat. DD Long. DD Year Name F 95-111 64.910 -13.712 2008 C-I E 29-42 64.816 -14.345 2009 C-II E 71-84 64.797 -14.218 2009 C-III E 1-14 64.794 -14.212 2009 C-IV E 15-28 64.794 -14.212 2009 C-V E 43-56 64.770 -14.114 2009 C-VI E 57-70 64.770 -14.114 2009 C-VII D 17-32 64.750 -14.452 2008 C-VIII S 1-18 64.735 -13.986 2008 Streitishvarf (I) S 1-21 64.735 -13.986 2009 Streitishvarf (I) S 22-44 64.798 -13.925 2009 Hökulvík (II) S 44-82 64.837 -13.899 2009 Hellufjall (III) S 19-31 64.732 -13.985 2008 C-IX D 15-28 64.722 -14.401 2009 C-X B 1-14 64.710 -14.333 2009 C-XI B 15-28 64.704 -14.324 2009 C-XII K 117-136 64.702 -14.287 2008 C-XIII K 1-16 64.701 -14.223 2008 C-XIV K 97-117 64.701 -14.240 2008 C-XV K 79-96 64.693 -14.190 2008 C-XVI K 17-30 64.691 -14.233 2008 C-XVII K 65-78 64.691 -14.233 2008 C-XVIII K 31-46 64.689 -14.229 2008 C-XIX K 47-64 64.688 -14.228 2008 C-XX D 1-16 64.662 -14.376 2008 C-XXI D 29-42 64.662 -14.290 2009 C-XXII D 33-48 64.662 -14.376 2008 C-XXIII D 1-14 64.649 -14.353 2009 C-XXIV A 1-14 64.631 -14.430 2009 C-XXV A 15-28 64.625 -14.427 2009 C-XXVI A 29-42 64.598 -14.474 2009 C-XXVII A 43-56 64.598 -14.472 2009 C-XXVIII A 57-70 64.598 -14.572 2009 C-XXIX

Appendix B, page 1 of 1

Appendix C a00209 -61 34.00000000 12 90 12 90 A 20 0.00145800 186.1 11.8 82.5 76.5 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00126900 186.4 11.4 82.9 76 A 0 0.00149200 0.8 74.3 299.2 18.3 A 30 0.00113700 185.6 11.4 79.9 76.3 A 5 0.00034160 5.2 8.6 306.6 -47.1 A 40 0.00095990 185.7 11.6 80.6 76.5 A 10 0.00021620 3.2 -22.4 313.5 -78.1 A 50 0.00085740 185.4 10.7 78.1 75.7 A 15 0.00016880 359.3 -32.1 281.6 -88 A 60 0.00076370 185.2 12.1 79.4 77.1 A 20 0.00016160 355.4 -29.9 254.2 -84.3 A 70 0.00071000 185.9 10.6 79.7 75.5 A 25 0.00012770 352.8 -35.3 194.6 -83.9 A 80 0.00065410 185.2 10.7 77.3 75.8 A 30 0.00013050 355.8 -30.7 250.8 -85.2 A 90 0.00060030 185.3 10.3 77.1 75.4 A 40 0.00009422 347.7 -37.8 184.6 -79.3 A 100 0.00054950 186.4 10.4 81.2 75.1 A 50 0.00007450 1.8 -26.6 311.3 -82.4 A 110 0.00050840 186.8 11.2 84 75.7 A 60 0.00006238 0.1 -30.2 300.3 -86.2 a02409 90 53.00000000 12 90 12 90 A 70 0.00004951 355 -25.3 271.2 -80.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige a00509 -69 30.00000000 12 90 12 90 A 0 0.00463400 183.1 61.7 80.4 81.1 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 5 0.00404400 189.4 63.7 69.2 78.2 A 0 0.00030040 248.2 67.9 265.5 35.8 A 10 0.00354100 194.6 63.2 58.9 77.3 A 5 0.00010740 340.1 54.8 279.7 -3.5 A 15 0.00256300 193.8 62.5 57.9 78 A 10 0.00007184 0.3 -12.6 292 -72.6 A 20 0.00186700 192 63.2 63.1 78 A 15 0.00008970 0.6 -29.4 332.1 -89.2 A 25 0.00127700 189.7 63 66.8 78.8 A 20 0.00009652 3.4 -29.6 14.1 -87 A 30 0.00089650 189.2 63.7 69.6 78.3 A 25 0.00009751 1.2 -28.8 332.4 -88.4 A 40 0.00051190 190.3 63.8 67.8 78 A 30 0.00008880 1 -31.4 79.7 -88.4 A 50 0.00028960 199 62.7 51.6 76.1 A 40 0.00007724 358.7 -26.7 271.6 -86.5 A 60 0.00017610 216.1 60.9 36.5 69.1 A 50 0.00006018 359 -29.9 207.3 -89.1 A 70 0.00012140 244.1 48 19.6 50.3 A 60 0.00004599 9.1 -26.8 1.4 -81.4 A 80 0.00008604 254.8 37.1 14.3 37.4 A 70 0.00003366 10.3 -36.1 59 -79.4 a02709 146 52.00000000 12 90 12 90 A 80 0.00002875 355.6 -21.7 264.5 -80.8 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 90 0.00002436 12.5 -37.6 60.6 -77.1 A 0 0.00680600 200.3 48.5 48.9 76.6 A 100 0.00002049 24.7 -17.2 357 -64.1 A 5 0.00586800 201.6 47.5 46.6 75.4 A 110 0.00001108 17.5 -23.9 3.8 -73.3 A 10 0.00379600 200.9 47.4 45.4 75.8 a00809 222 39.00000000 12 90 12 90 A 15 0.00230600 200 47.2 43.5 76.2 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 20 0.00147800 199.8 49.7 53.4 77.3 A 0 0.00180900 356.2 -19.7 211.3 -70.4 A 25 0.00091840 200 50.3 56.2 77.4 A 5 0.00187300 356.3 -23.6 209.4 -74.3 A 30 0.00059580 202 51.5 62.6 76.4 A 10 0.00118200 353.7 -24.3 200.2 -74.4 A 40 0.00030920 205.8 54.1 74 74.4 A 15 0.00068730 352.8 -23.9 197.9 -73.7 A 50 0.00016260 212.3 54.5 76.2 70.7 A 20 0.00043080 352.4 -23.3 197.4 -73 A 60 0.00009038 226.7 52.6 76 61.9 A 25 0.00030110 352.3 -23.1 197.4 -72.8 A 70 0.00005610 238.1 39.7 62.4 48.9 A 30 0.00023530 353.9 -24 201.2 -74.1 a03309 31 34.00000000 12 90 12 90 A 40 0.00015690 353.9 -24.5 200.6 -74.6 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 50 0.00011800 355.5 -24.4 206.1 -74.9 A 0 0.00373800 186.7 46.8 11.4 76.2 A 60 0.00008359 356.3 -26.5 207 -77.1 A 5 0.00249800 178.7 35.4 68 88.2 A 70 0.00006842 358.1 -25.7 214.6 -76.6 A 10 0.00151900 175.8 34.4 113.3 86.5 a01009 225 35.00000000 12 90 12 90 A 15 0.00088480 174.7 31.8 145.8 85 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 20 0.00052100 174.2 29.6 161.2 83.4 A 0 0.00981200 3.8 -28.3 251.8 -82.6 A 25 0.00032720 173.9 31.3 147.1 84.2 A 5 0.00864800 1.3 -29 235.8 -83.9 A 30 0.00023010 175 31.7 148.3 85.2 A 10 0.00563600 359.4 -29 220 -84 A 40 0.00013820 173.6 32.6 133.9 84.5 A 15 0.00383800 359.2 -27.6 219.5 -82.6 A 50 0.00007945 176.2 31.5 158 85.9 A 20 0.00265400 358.6 -27.9 215.1 -82.8 A 60 0.00006195 167 37.3 99.9 78.9 A 25 0.00183200 358.2 -27.6 212.8 -82.4 A 70 0.00003726 175 37.5 78.8 84.6 A 70 0.00019350 358.4 -32.3 198.3 -87 a03509 12 38.00000000 12 90 12 90 A 75 0.00016100 358.6 -30.8 209 -85.6 IDStep[mT] M[A/m] Dsp Isp Dge Ige a01609 -55 18.00000000 12 90 12 90 A 0 0.00482500 184.5 53.3 2 74.4 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 5 0.00365400 183.9 44.4 348.6 83 A 0 0.01146000 165.9 19.1 28.1 76.6 A 10 0.00218700 181 43.8 4.9 84.2 A 5 0.01068000 165.2 18.4 31.1 75.9 A 15 0.00120600 180.2 41.4 9.5 86.6 A 10 0.00790300 164 19.1 28.3 74.8 A 20 0.00062630 179.6 40.5 18.9 87.5 A 15 0.00580900 164.3 18.7 29.8 75.1 A 25 0.00034650 179.2 37.6 134.1 89.3 A 20 0.00453600 164.1 18.8 29.5 74.9 A 30 0.00020750 180.7 37.1 223.9 88.9 A 25 0.00343100 164.1 18.3 31.4 74.9 A 40 0.00011010 181 34.7 206 86.6 A 30 0.00262400 163.4 18.1 32.1 74.2 A 50 0.00006592 180.9 44.9 6.7 83.1 A 40 0.00174700 163.6 17.4 34.7 74.4 A 60 0.00004185 185.2 40.5 315.5 85.3 A 50 0.00114800 162.5 16.6 37.1 73.2 A 70 0.00003261 176 30.5 167.1 81.8 A 60 0.00078870 161.6 15.9 39 72.3 a03809 -29 52.00000000 12 90 12 90 A 70 0.00056990 160.2 15.3 40.2 70.8 IDStep[mT] M[A/m] Dsp Isp Dge Ige a02109 236 24.00000000 12 90 12 90 A 0 0.00423400 166.5 50.1 68.3 81.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 5 0.00380900 165.7 54.8 37.2 81 A 0 0.00319300 200.7 27.3 160.4 71.1 A 10 0.00276000 165.7 55.7 31.6 80.8 A 5 0.00254300 194.1 13 109 72.7 A 15 0.00162000 165.6 55.1 35.4 80.9 A 10 0.00208700 189.5 11.5 93.5 74.6 A 20 0.00096210 165.1 54.1 41.9 80.8 A 15 0.00173600 187 11 84.3 75.4 A 25 0.00056140 164.7 54.4 40.3 80.5 Appendix C, page 1 of 18 Appendix C

A 30 0.00034000 164.9 51.6 57.5 80.7 A 0 0.00118100 218.2 57.7 336.4 61.4 A 40 0.00015730 166.2 50.8 63.5 81.3 A 5 0.00087030 210.3 55.6 335.2 66.2 A 50 0.00008213 168.6 48.3 83.4 81.8 A 10 0.00050340 203.4 54.7 337.6 70.1 A 60 0.00005562 165.1 52.4 52.6 80.9 A 15 0.00033440 202 54.4 338.1 70.9 A 70 0.00003841 163.7 40.3 100.8 73.8 A 20 0.00022930 204.9 56.1 339.8 68.6 a04109 -26 33.00000000 12 90 12 90 A 25 0.00015640 207.2 55.7 337.2 67.7 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00011970 208.6 56.9 339.1 66.5 A 0 0.00184400 185 -11.9 160.9 44.8 A 40 0.00007463 205 56 339.5 68.6 A 5 0.00150200 183.3 30.4 202.1 86.2 A 50 0.00004212 202.9 53.2 334.1 71.1 A 10 0.00108000 176.2 35.4 25.6 86 A 60 0.00002196 189.8 39.4 274 82.1 A 15 0.00075070 173.6 36.4 29.3 83.7 A 70 0.00001037 190 24.5 228.5 70.6 A 20 0.00054990 172.8 36 35.2 83.4 a06209 18 55.00000000 12 90 12 90 A 25 0.00041140 173.5 35.3 39 84.2 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00032070 169.7 35.4 45.4 81.2 A 0 0.00070440 158.9 7.6 170.4 39.7 A 40 0.00020750 168 36.3 42.2 79.6 A 5 0.00066760 157.2 33.9 151.7 63.6 A 50 0.00014890 173.4 35.2 40.2 84.1 A 10 0.00049480 154.6 38.6 141.3 66.3 A 60 0.00009454 185.5 37.5 290.6 83.6 A 15 0.00032550 153.6 38.5 140 65.8 A 70 0.00006342 178 42.6 342.7 80.3 A 20 0.00020770 152.6 39.7 136.6 66.2 a04609 126 23.00000000 12 90 12 90 A 25 0.00013510 152.8 41.1 134.5 67.4 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00009036 152.6 40.5 135.3 66.8 A 0 0.01561000 18.9 -21.8 215.7 -72.5 A 40 0.00004877 151.1 43.4 127.9 68.1 A 5 0.01474000 17.5 -22.2 216.6 -73.8 A 50 0.00002566 159.7 35.8 153.6 66.3 A 10 0.01133000 16.2 -21.8 214.6 -75 A 60 0.00001195 164.5 27.5 169.4 60.3 A 15 0.00698100 13.8 -22.8 217.8 -77.3 A 70 0.00000977 145.3 9.6 153.4 37 A 20 0.00398600 11.7 -23.5 221 -79.2 a06509 42 52.00000000 12 90 12 90 A 25 0.00217700 9.9 -22.7 216 -80.9 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00111500 8.5 -24.1 225.7 -82.1 A 0 0.00084100 30.8 67 55.5 31.2 A 40 0.00045480 8.3 -26.8 244.5 -81.6 A 5 0.00024960 87.4 62 81.9 43.1 A 50 0.00020890 11.8 -27.3 240.4 -78.5 A 10 0.00015630 123.4 43.9 121.2 52.2 A 60 0.00013160 10.4 -29.4 252.7 -78.7 A 15 0.00010790 131.5 38 135.1 53.8 A 70 0.00009544 9 -29.3 255.9 -79.8 A 20 0.00007456 132.2 37.5 136.4 53.9 a04909 92 66.00000000 12 90 12 90 A 25 0.00004692 133.5 35 140.7 53 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00003035 140.4 38.5 142.4 59.5 A 0 0.01574000 45.7 -71.1 219.5 -73 A 40 0.00001600 135.2 37.9 138.5 56 A 5 0.01501000 42.6 -70.7 217.8 -74 A 50 0.00000761 128 16.6 152.9 36 A 10 0.01145000 42.2 -70.9 218.5 -74.1 A 60 0.00000421 128.6 15.9 154 35.8 A 15 0.00747300 40.2 -71.1 219.2 -74.8 A 70 0.00000192 112 5.7 146.1 17.9 A 20 0.00465900 41 -72.4 224.1 -74.5 a06909 40 61.00000000 12 90 12 90 A 25 0.00273900 40 -72.5 224.6 -74.8 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00160800 40.3 -73.2 227.2 -74.6 A 0 0.00010690 284.3 37.5 341.3 25.9 A 40 0.00075910 42.1 -73.3 227.3 -74.1 A 5 0.00024010 173.8 73.1 48.5 77.7 A 50 0.00042360 43.6 -73.7 228.6 -73.6 A 10 0.00017110 150.5 59.7 122.1 75.5 A 60 0.00026330 40.8 -73.3 227.5 -74.5 A 15 0.00011670 143.8 52.5 137.1 68.8 A 70 0.00019100 37.2 -72.4 224.5 -75.6 A 20 0.00008531 141.2 50.9 137.7 66.5 a05309 -12 48.00000000 12 90 12 90 A 25 0.00005827 138.5 46.6 142.1 62.2 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00003951 135.3 43.7 142.7 58.6 A 0 0.00539000 329.1 -67.8 195.1 -64.8 A 40 0.00002099 128.8 28.9 149.8 43.5 A 5 0.00493200 330.5 -67.3 195.3 -65.6 A 50 0.00001356 121.3 23.5 145.9 35.4 A 10 0.00295300 330.3 -65.9 198.2 -66.3 A 60 0.00001120 126.6 11.9 157.6 27.6 A 15 0.00148300 330.5 -64.7 200.6 -67 A 70 0.00000957 99.8 -13 144.8 -6.7 A 20 0.00088610 330.5 -65.4 199.1 -66.7 b00509 -21 74.00000000 12 90 12 90 A 25 0.00052900 329.3 -64.7 201.3 -66.6 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00036640 328 -64.2 203.1 -66.4 A 0 0.00756100 258.6 -69.5 205.6 -61.8 A 40 0.00024890 332.1 -65.1 198.8 -67.4 A 5 0.00594900 254.6 -88.5 164.1 -73.5 A 50 0.00018000 327.9 -65 201.4 -65.9 A 10 0.00346400 79.3 -89 155.4 -74.2 A 60 0.00014470 330.9 -65.5 198.7 -66.7 A 15 0.00198900 69.9 -88.2 152.7 -74.5 A 70 0.00010940 321.7 -66.3 201.4 -63.1 A 20 0.00126800 47.5 -88.2 153.8 -75.2 a05609 -42 4.00000000 12 90 12 90 A 25 0.00081600 70.5 -87.7 150.8 -74.6 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00061950 41.3 -88.2 154.3 -75.3 A 0 0.00199400 341 -11.9 204.1 -69.6 A 40 0.00043480 53.7 -88.1 153.1 -75 A 5 0.00247400 344 -18.9 183.1 -68.4 A 50 0.00032600 113.4 -87.4 150.9 -72.8 A 10 0.00186400 344 -16.9 187.4 -69.7 A 60 0.00023480 335.8 -88.8 160.9 -75.1 A 15 0.00125300 344.8 -15.1 190.4 -71.4 A 70 0.00017340 43.3 -87.3 151.4 -75.8 A 20 0.00083440 343.9 -14.6 193.2 -70.9 b00609 -28 63.00000000 12 90 12 90 A 25 0.00054070 343.5 -14 195.4 -70.9 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00037870 344.8 -15.5 189.4 -71.1 A 0 0.00839900 3.9 -45.3 341 -72.2 A 40 0.00023040 344.4 -17 186.5 -69.9 A 5 0.00561200 357 -72.6 157.3 -80.3 A 50 0.00015080 341.8 -17.6 189.3 -67.6 A 10 0.00333800 357.4 -76.5 154.6 -76.5 A 60 0.00011840 344.8 -17.5 184.7 -69.9 A 15 0.00190100 358 -76.8 153.9 -76.2 A 70 0.00008306 348.5 -21.5 169.6 -69.2 A 20 0.00125000 356.6 -78 154.7 -75 a05909 20 42.00000000 12 90 12 90 A 25 0.00080800 358.8 -77.1 153.1 -75.9 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00059450 5.3 -78.8 148.2 -74.1 Appendix C, page 1 of 18 Appendix C

A 40 0.00040890 358.7 -78.2 153 -74.8 A 5 0.00008370 187.9 70.9 334.4 86.1 A 50 0.00029230 7.8 -79.2 146.8 -73.6 A 10 0.00003285 100.8 48.9 195.1 49.3 A 60 0.00020770 355.2 -78.3 155.7 -74.6 A 15 0.00002718 92.5 13.8 201.5 13.9 A 70 0.00015490 20.9 -75.6 131.1 -75.6 A 20 0.00002142 90.9 0.7 203.7 0.9 b01009 104 74.00000000 12 90 12 90 A 25 0.00001878 123.5 1 235.2 9.7 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00002548 111.9 0.5 224 6.4 A 0 0.00166000 7.8 -24.5 113.3 -40.3 A 40 0.00001798 53.6 30.8 160.6 20.6 A 5 0.00138100 19 -60.4 141.5 -74.7 A 50 0.00001525 106.6 -12.7 222.4 -7.7 A 10 0.00056960 21.5 -67 160.2 -80.1 A 60 0.00001628 78.9 -15.6 196.7 -18 A 15 0.00025890 24.4 -66.4 163.4 -78.9 A 70 0.00001287 94.4 7.5 205.2 8.4 A 20 0.00014280 32 -70.7 191 -79.9 d00109 -63 40.00000000 12 90 12 90 A 25 0.00009996 33.4 -59.4 162.6 -70.8 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00008950 31.8 -61.6 163.8 -73.1 A 0 0.00089210 310.9 37.4 260.1 -0.5 A 40 0.00006976 31.3 -70.6 189.7 -80 A 5 0.00049580 320.7 -5.2 241 -40.4 A 50 0.00005703 61.9 -55.5 190.6 -60 A 10 0.00029790 315 -4.5 236.1 -36.2 A 60 0.00004405 33.2 -54.5 156.6 -66.4 A 15 0.00020010 315 -1 239 -33.6 A 70 0.00004120 27.2 -64.8 163.5 -76.9 A 20 0.00012730 328.2 -5.5 248.9 -45.2 b01309 97 70.00000000 12 90 12 90 A 25 0.00011160 344 -14.9 263.3 -61.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00009938 352.2 -14.1 280 -63.2 A 0 0.00242800 86.8 6.6 181.7 5.1 A 40 0.00006873 1.1 -19.7 300 -69.7 A 5 0.00271300 46.4 -61.4 185.4 -69.7 A 50 0.00004966 13.7 -18.7 330 -65.7 A 10 0.00147000 30.6 -65.2 179.3 -77.6 A 60 0.00002905 356 -17.9 287 -67.6 A 15 0.00084440 28.2 -65.9 179.3 -78.8 A 70 0.00003115 8.4 -9.5 313.1 -58.6 A 20 0.00048490 26.2 -65.7 176 -79.3 d00309 244 54.00000000 12 90 12 90 A 25 0.00031320 27.7 -64.4 172.7 -78 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00021910 27.6 -64.1 171.5 -77.9 A 0 0.00095280 334.1 68.9 233 34.4 A 40 0.00014850 28.4 -64.5 174 -77.9 A 5 0.00091150 326.3 59.1 225.5 26.3 A 50 0.00009519 34.1 -68.2 194.8 -77.9 A 10 0.00073440 301.3 65.1 217.1 37.2 A 60 0.00007830 45.3 -67.9 201.3 -74 A 15 0.00051800 302.8 64.9 217.6 36.7 A 70 0.00006060 16 -78.2 256.4 -80.8 A 20 0.00032690 311 62.9 219.8 33 b01809 166 71.00000000 12 90 12 90 A 25 0.00017310 324.7 58.5 224.4 26 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00012860 337.6 48.7 228.9 14.4 A 0 0.00125600 88.4 81.6 190.1 69.1 A 40 0.00006239 340.2 47.3 230.4 12.7 A 5 0.00034550 43.6 2.2 210.7 -11.5 A 50 0.00003502 347.6 38.6 234.3 3.2 A 10 0.00017600 43.9 -4.3 212.6 -17.7 A 60 0.00002736 355.7 54.1 241.3 18.2 A 15 0.00008716 50.9 -2.8 219.2 -14.6 A 70 0.00001924 6.2 30.1 249.4 -5.7 A 20 0.00004870 53.7 -0.9 221.5 -12 d4088 58 54.00000000 12 90 12 90 A 25 0.00003076 47.3 7.4 213.1 -5.6 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00001607 48.5 9.1 213.8 -3.6 A 0 0.00178500 282.3 -4.3 335.5 -10.7 A 40 0.00001547 55 3.9 221.4 -7 A 5 0.00160400 292.3 -31.9 324.4 -38.1 A 50 0.00000864 50.1 -25.4 225.5 -36.5 A 10 0.00136100 299.7 -36.3 326 -45.5 A 60 0.00000775 34.6 13.7 199.5 -2.1 A 15 0.00097200 303.7 -37.1 328.3 -48.4 A 70 0.00000796 17.5 2.8 184.1 -15.3 A 20 0.00075760 306.7 -39.9 327.4 -52 b02009 157 75.00000000 12 90 12 90 A 25 0.00060660 310 -42.8 326.2 -55.8 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00048170 311.9 -44.9 324.5 -58.1 A 0 0.00185400 137.5 72.5 237.9 78.1 A 40 0.00033440 313 -47.4 321.2 -60.1 A 5 0.00042480 102.7 44.6 244.5 46 A 50 0.00022420 313.6 -47 322.3 -60.2 A 10 0.00018280 83.2 23 234.3 20.4 A 60 0.00014080 311.7 -50.1 315.6 -60.6 A 15 0.00010960 74.7 14.7 228.5 10.3 A 70 0.00010390 305.8 -44.4 320.8 -54.3 A 20 0.00007070 72.3 13.6 226.5 8.7 d5088 53 60.00000000 12 90 12 90 A 25 0.00003978 70.8 12.6 225.3 7.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00002608 64.7 9.4 220.3 2.8 A 0 0.00316000 294.2 32.3 359.3 16.8 A 40 0.00000711 42.2 24.6 195.8 13.2 A 5 0.00191500 291.9 -19 332.2 -27.3 A 50 0.00000610 27.4 -30.3 190.1 -43.3 A 10 0.00171500 298.6 -33.3 328.6 -42.5 A 60 0.00000582 57.6 -19.2 220.1 -26.7 A 15 0.00134600 303.9 -38.3 329.1 -49.1 A 70 0.00000580 20.8 -45 185.9 -58.7 A 20 0.00104300 305.9 -41 328.2 -52.1 b02509 130 73.00000000 12 90 12 90 A 25 0.00080660 308.7 -43.6 327.8 -55.4 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00064360 309.4 -43.6 328.4 -55.8 A 0 0.00096530 184.2 48.2 316.7 65.1 A 40 0.00044890 310.9 -44.2 329.1 -57 A 5 0.00011110 91.3 25.1 213.4 24.3 A 50 0.00030310 308.6 -44 327.2 -55.7 A 10 0.00006214 79.9 14.4 206.1 10.8 A 60 0.00020190 307.8 -38.1 333 -50.9 A 15 0.00004628 78.5 7.4 206.9 3.7 d01109 148 69.00000000 12 90 12 90 A 20 0.00003774 66.5 4.9 196.1 -2 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00003554 79.4 8.6 207.4 5.2 A 0 0.00197600 29.5 71.9 162.5 52.2 A 30 0.00002118 77.5 -16.2 212.9 -19.1 A 5 0.00124000 23.3 59.1 163.2 39.2 A 40 0.00001042 84.8 7.6 212.8 5.8 A 10 0.00077350 22.1 61.5 161.9 41.5 A 50 0.00001460 56.5 25.1 181.4 15 A 15 0.00045200 17.6 62.7 158.8 42.3 A 60 0.00000888 58.6 39.3 179.2 29.2 A 20 0.00026700 24.1 61.9 163 42 A 70 0.00001271 52.4 -10.1 186.1 -20.1 A 25 0.00015810 17.3 61.8 158.8 41.4 b02809 113 74.00000000 12 90 12 90 A 30 0.00009894 21.3 49.1 163.8 29.1 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 40 0.00005183 54.3 57.5 184.3 42.5 A 0 0.00124400 235.5 72.2 43.9 74.4 A 50 0.00003663 40.5 41.6 180.3 24.6 Appendix C, page 1 of 18 Appendix C

A 60 0.00002112 39.1 63.8 171.5 45.6 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 70 0.00001733 34.7 6.3 183.2 -11 A 0 0.02129000 2.5 -58.6 91.6 -88.6 d1308 -50 36.00000000 12 90 12 90 A 5 0.02117000 1.1 -58.6 112.5 -89.2 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 10 0.02075000 0.3 -60 151.7 -88 A 0 0.00138200 348 32 299.1 -21.1 A 15 0.01964000 359.3 -62.6 160 -85.4 A 5 0.00161700 342.5 0 281.8 -50.5 A 20 0.01525000 357.3 -63.7 167.8 -84.2 A 10 0.00203800 347.9 -17.5 276.7 -68.6 A 25 0.01063000 355.6 -64.4 172.4 -83.3 A 15 0.00194200 348.9 -23.3 269.9 -74.1 A 30 0.00735900 354.9 -64.3 175.1 -83.2 A 20 0.00156800 348.7 -24.3 267.1 -74.8 A 40 0.00350000 354.1 -64.7 176.3 -82.7 A 25 0.00123500 348.6 -24.3 266.9 -74.7 A 50 0.00158800 354.9 -66.5 169.4 -81.2 A 30 0.00094180 348.6 -24.4 266.6 -74.8 A 60 0.00080500 359.5 -68.5 157 -79.5 A 40 0.00059780 347.9 -23.1 267.6 -73.4 A 70 0.00041950 13.2 -70.2 136.5 -76.6 A 50 0.00039280 348.9 -22.7 271.1 -73.6 d2108 252 46.00000000 12 90 12 90 A 60 0.00027660 350.1 -23.5 272.9 -74.9 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 70 0.00020650 349.8 -21.2 276.2 -72.7 A 0 0.01237000 174.3 49.3 299.2 84.9 A 80 0.00016360 341 -24.3 250.3 -69.9 A 5 0.00971300 173.2 49.1 305.5 84.5 A 90 0.00012330 341.9 -26.5 246.6 -71.9 A 10 0.00536200 171.7 48.9 311.7 83.7 d01309 96 50.00000000 12 90 12 90 A 15 0.00332800 171.6 48.9 311.9 83.6 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 20 0.00230800 171.5 48.5 315.5 83.7 A 0 0.00157500 109.6 -9.4 207.1 5 A 25 0.00160000 172.5 48.9 309.5 84.2 A 5 0.00147600 91.2 -28 205.7 -20.3 A 30 0.00118900 171.8 48.3 316.6 84 A 10 0.00095560 99.2 -15.2 202.8 -5.8 A 40 0.00075410 173.4 48.6 309.5 84.8 A 15 0.00060410 101.4 -14 203.6 -3.6 A 50 0.00050390 170.8 49.7 307.7 82.8 A 20 0.00037560 99.2 -18.7 205 -8.5 d02409 152 58.00000000 12 90 12 90 A 25 0.00023780 94.5 -25.6 206.3 -16.6 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00016970 95.7 -31.5 211.3 -20.2 A 0 0.00281800 352.6 -61.6 14.8 -84.8 A 40 0.00010120 86.7 -51.3 223.2 -38.4 A 5 0.00325100 358.8 -60 348.7 -87.9 A 50 0.00005806 90.8 -51.5 225.3 -36.4 A 10 0.00255500 358.5 -57.8 75.4 -89.2 A 60 0.00004060 66.4 -45.7 207 -46.7 A 15 0.00162800 357.6 -57.8 69.9 -88.7 A 70 0.00003463 84.5 -55.4 226.8 -41.7 A 20 0.00114900 358.3 -58.5 32.1 -89 A 80 0.00002563 164.1 -87.3 274.9 -47.4 A 25 0.00079610 359.3 -57.7 100.5 -89.5 d1608 34 45.00000000 12 90 12 90 A 30 0.00062270 359.8 -57.9 105.2 -89.9 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 40 0.00040180 1.7 -58.2 255.3 -89.1 A 0 0.00136100 280.8 58.5 356.6 32.3 A 50 0.00024540 0.5 -58.3 290.9 -89.6 A 5 0.00137500 304.7 10.1 336.7 -15.8 A 60 0.00014820 0.5 -57.1 168.8 -89.1 A 10 0.00152200 321.3 -19.7 329.5 -49.3 A 70 0.00008373 5.5 -56.1 211.9 -86.5 A 15 0.00161100 330.5 -34.1 319.5 -65 d2808 229 62.00000000 12 90 12 90 A 20 0.00146600 333.5 -38.1 314 -69.1 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00124700 335.7 -40.3 310.2 -71.6 A 0 0.01215000 227.6 80.5 210.5 67.4 A 30 0.00099750 335.6 -40.5 309.5 -71.6 A 5 0.00966600 192.1 65.4 176.7 83.7 A 40 0.00070710 335.5 -40.2 310.3 -71.4 A 10 0.00682900 186.9 60.6 119.1 86.4 A 50 0.00048130 335.6 -40 311 -71.4 A 15 0.00509000 185.3 60.4 109.3 87 A 60 0.00035290 336.4 -41 308.8 -72.4 A 20 0.00397700 184.5 61.2 120.5 87.7 A 70 0.00024890 336.5 -40.8 309.5 -72.3 A 25 0.00296500 184.1 60.5 103.6 87.5 A 80 0.00019720 337.8 -42 306.7 -73.7 A 30 0.00231600 183.6 60.9 108 88 A 90 0.00016130 341.2 -41.9 310.2 -76 A 40 0.00157300 184.3 61 114.9 87.7 A 100 0.00012300 337.6 -41.1 309.5 -73.2 A 50 0.00103100 183.8 60.9 109.5 87.9 d01809 -53 66.00000000 12 90 12 90 A 60 0.00073070 183.6 62.3 150.7 88.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige d02809 189 40.00000000 12 90 12 90 A 0 0.01382000 4.9 -71.8 112.4 -83.9 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 5 0.01410000 5.8 -72.2 111.2 -83.5 A 0 0.00279500 357.8 -34.5 170.7 -84.2 A 10 0.01367000 4.9 -71.6 111.7 -84.1 A 5 0.00320800 358.4 -38.5 148.9 -88.1 A 15 0.01254000 3.3 -71.4 116 -84.5 A 10 0.00299700 358.6 -37.6 164.1 -87.4 A 20 0.01081000 1.9 -71.8 121.2 -84.2 A 15 0.00242100 358.1 -37.3 159.6 -86.9 A 25 0.00796200 0.3 -70.8 125.8 -85.2 A 20 0.00179800 357.1 -37.4 147 -86.6 A 30 0.00588500 358.2 -71.6 132.8 -84.4 A 25 0.00128500 356.5 -38.3 129.9 -86.8 A 40 0.00312600 355.3 -72.5 139.2 -83.3 A 30 0.00092240 355.9 -38.3 125.8 -86.4 A 50 0.00135800 351.8 -73.3 144.5 -82.2 A 40 0.00051300 355.7 -40.2 94.1 -86.7 A 60 0.00065440 350.4 -75 142.1 -80.5 A 50 0.00024500 358.8 -40.3 80.5 -89 A 70 0.00034020 353.1 -77.3 134.6 -78.5 A 60 0.00012330 7.5 -38.3 265.1 -83.9 d1908 215 45.00000000 12 90 12 90 A 70 0.00005604 28.7 -29.2 263.2 -64.2 IDStep[mT] M[A/m] Dsp Isp Dge Ige d3008 112 79.00000000 12 90 12 90 A 0 0.01364000 175.3 39.8 359.7 83.8 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 5 0.01050000 170.8 42.6 321.6 82.9 A 0 0.00794600 188.4 82.6 95.7 86.2 A 10 0.00655600 168.7 41.8 322.3 81.2 A 5 0.00678600 186.7 80.9 83.7 87.8 A 15 0.00392800 168.9 40.2 331.6 80.5 A 10 0.00496900 189.2 80.2 62.3 88 A 20 0.00260800 168 40.4 328.4 80.1 A 15 0.00355100 189.8 79.9 53.4 88 A 25 0.00173000 168.5 39.3 334.8 79.8 A 20 0.00275100 190.5 80.1 57.1 87.8 A 30 0.00123200 167.7 40.6 326.7 80 A 25 0.00200300 189.8 79.7 47.9 88.1 A 40 0.00076400 167.8 41 324.9 80.2 A 30 0.00150700 189.6 80.4 65.9 87.8 A 50 0.00049890 165.5 39.8 325.9 78.1 A 40 0.00099740 188.1 80.3 67.7 88.1 d02009 -24 58.00000000 12 90 12 90 A 50 0.00063160 186.6 79.6 51.3 88.6 Appendix C, page 1 of 18 Appendix C

A 60 0.00043150 190.1 80.8 72.4 87.5 A 90 0.00003093 127.6 31.6 54 46.6 d03109 -50 54.00000000 12 90 12 90 D3908 -19 31.00000000 12 90 12 90 IDStep[mT] M[A/m] Dsp Isp Dge Ige IDStep[mT] M[A/m] Dsp Isp Dge Ige A 0 0.00382600 204.7 69.7 283.9 70.7 A 0 0.00207300 170.5 51.8 356.9 68.1 A 5 0.00159500 183.4 62.3 299.2 81.5 A 5 0.00160300 166.8 47 9.7 71.1 A 10 0.00085980 177.7 57.3 330.5 86.5 A 10 0.00100900 166.1 45.9 13 71.6 A 15 0.00047130 174 54.6 27.8 86.4 A 15 0.00061670 165.1 45.4 15.7 71.5 A 20 0.00030670 173.9 52.8 55.8 86.2 A 20 0.00036260 164.8 44.9 17.3 71.7 A 25 0.00021210 172.4 49.8 78.8 83.7 A 25 0.00021760 165.8 44.1 17.5 72.8 A 30 0.00015900 174.9 49.5 92.9 84.5 A 30 0.00013480 163.1 39.9 33.4 73.7 A 40 0.00010400 172.6 45.2 98.5 80 A 40 0.00006708 159.3 40.6 35.4 70.7 A 50 0.00006237 177 44.7 117 80.5 A 50 0.00003035 163.9 31.4 65.2 76.2 A 60 0.00004340 170.9 43.3 97.1 77.7 D4008 -41 29.00000000 12 90 12 90 A 70 0.00002838 178.7 47.4 122.4 83.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige D3308 -58 42.00000000 12 90 12 90 A 0 0.00194800 178.6 65.7 320 53.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 5 0.00122100 170.5 43.9 343.4 73.3 A 0 0.00375800 164.7 59.4 325.4 70.2 A 10 0.00083100 166.9 38.5 4.4 75.6 A 5 0.00277700 164.7 46.3 5.4 78.2 A 15 0.00057020 165.3 37.3 11.1 75.2 A 10 0.00198000 162.6 42.2 25.3 77.1 A 20 0.00037590 161.4 37.2 16.3 72.4 A 15 0.00143600 162.4 41 30.4 76.8 A 25 0.00027730 164.7 33.9 24.5 76.1 A 20 0.00101000 161.4 40 33.9 75.8 A 30 0.00018820 160.7 33.9 27.5 72.9 A 25 0.00069820 161.1 39 37.5 75.4 A 40 0.00011550 164.2 34.2 23.8 75.6 A 30 0.00046430 161.5 37.4 43.8 75.1 A 50 0.00006789 161 20.6 70.7 70.9 A 40 0.00022170 161.9 31.9 61.2 72.4 d04009 144 57.00000000 12 90 12 90 A 50 0.00009363 164.5 12.2 93.1 57.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige d03309 -69 50.00000000 12 90 12 90 A 0 0.00227500 201.7 55.8 57.4 78 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 5 0.00098620 197.2 51.9 34.2 78.8 A 0 0.01152000 175.7 59.9 303.3 79.8 A 10 0.00043720 194.6 51.9 29.1 80.1 A 5 0.00978000 170.1 56.2 330.9 81.4 A 15 0.00026350 189.7 53.2 23.7 83.3 A 10 0.00804200 168.3 54.6 343.7 81.5 A 20 0.00017430 187 52.6 9.4 84 A 15 0.00631700 168 54 347.9 81.6 A 25 0.00013950 185.7 50.2 352.8 82.4 A 20 0.00474500 167.2 53.8 350.4 81.3 A 30 0.00011390 185.5 54.3 15.3 85.9 A 25 0.00334000 167.6 53.8 349.8 81.5 A 40 0.00008361 197.3 53.7 42.7 79.7 A 30 0.00219400 167.4 51 9 81.9 A 50 0.00005867 190.8 55.1 41 83.7 A 40 0.00104400 168.1 48.9 24.5 82.2 A 60 0.00005100 209.1 67.4 103.8 73.2 A 50 0.00042770 170.9 46 50.9 82.7 A 70 0.00003807 215.5 60.8 80.7 71.5 A 60 0.00018640 176.3 44.2 86.2 83.7 D4108 111 78.00000000 12 90 12 90 A 70 0.00008447 194.9 39.3 161.2 75 IDStep[mT] M[A/m] Dsp Isp Dge Ige D3408 -50 28.00000000 12 90 12 90 A 0 0.00462700 269.4 78.7 66.9 73.7 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 5 0.00150200 240.8 73 34.1 74.8 A 0 0.00349800 182.1 51.5 306.7 66.4 A 10 0.00097950 244.9 71 32.8 72.5 A 5 0.00223500 170.1 34.7 359.1 79.2 A 15 0.00073050 246.5 71.1 34.3 72.2 A 10 0.00164600 166.8 30.8 23.1 78.2 A 20 0.00058770 246.1 69.7 31.3 71.2 A 15 0.00114700 166 29 32 77.7 A 25 0.00048480 248 70.1 33.6 71.1 A 20 0.00081720 164.2 29.1 31.7 76.1 A 30 0.00044590 253.7 71.5 40.9 71.1 A 25 0.00056450 163.3 27.3 38.8 75.2 A 40 0.00033370 247.3 67.6 28.8 69.2 A 30 0.00037390 162.3 26 43.1 74.1 A 50 0.00027050 248.4 68.9 31.9 70.1 A 40 0.00019720 160.7 22.2 54.1 71.6 D4208 87 66.00000000 12 90 12 90 A 50 0.00009511 159 10.1 78.1 63.4 IDStep[mT] M[A/m] Dsp Isp Dge Ige D3508 -41 40.00000000 12 90 12 90 A 5 0.00033750 217 47.8 332 63.5 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 10 0.00032830 215.3 52.2 336.1 67.7 A 0 0.00221700 147.8 60.9 351.6 61.3 A 15 0.00031770 220.2 51.7 341.2 65.4 A 5 0.00158700 145.8 52 10.4 63.7 A 20 0.00029190 214.9 53.2 337.2 68.6 A 10 0.00096670 143.8 49.2 17 62.9 A 25 0.00029680 215.1 53.8 338.6 69 A 15 0.00055170 143 48.4 18.9 62.5 A 30 0.00025700 222.7 55.6 350.5 67.3 A 20 0.00035900 142.2 48.2 19.4 62 A 40 0.00024210 212.3 58.2 344.7 73.3 A 25 0.00023970 140.2 47.7 20.5 60.6 A 50 0.00023270 212.1 58.1 344.2 73.3 A 30 0.00016500 141.7 46.2 23.6 61.6 A 60 0.00020150 213.4 61.4 355.3 74.7 A 40 0.00010150 141.3 47.6 20.7 61.4 A 70 0.00016030 222.7 62.7 6.8 71.6 D3808 -25 35.00000000 12 90 12 90 A 80 0.00015030 210.4 61.3 351.9 75.9 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 90 0.00013410 220.5 62.9 5.8 72.6 A 5 0.00003024 176.8 9.9 147.6 64.7 A 100 0.00012150 218.6 61.4 359.9 72.6 A 10 0.00002829 158.9 17 103.3 64 d04209 145 56.00000000 12 90 12 90 A 15 0.00002993 166.9 17.9 117.4 69.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 20 0.00002676 151.6 30.3 68.1 65.7 A 0 0.00222600 185.2 43.2 341.8 76.8 A 25 0.00002579 160.3 16.8 106 64.7 A 5 0.00109000 180.2 42.9 325.6 76.9 A 30 0.00002504 154.9 19.8 92.9 63.2 A 10 0.00042620 173.6 42.2 305.6 75.6 A 40 0.00002437 148 23.1 79.5 59.8 A 15 0.00017790 164.7 42.7 282.1 73.5 A 50 0.00002667 130.7 32.3 54.3 49.3 A 20 0.00009725 160.7 46.1 266.4 74.4 A 60 0.00002575 147.6 32.4 61.2 63 A 25 0.00007243 167.4 59.6 201.6 82.4 A 70 0.00002648 128.3 34 50.9 47.9 A 30 0.00006216 185.3 61 118.3 84.3 A 80 0.00001980 128.2 47.5 30.5 49.9 A 40 0.00007576 174.6 54 265.6 86.3 Appendix C, page 1 of 18 Appendix C

A 50 0.00005880 174.9 58.6 189.5 86.2 A 40 0.00007322 63.5 -63.8 269.4 -62.7 A 60 0.00004969 166.8 59 206.6 82.3 A 50 0.00008972 60.7 -56 254.2 -59.6 A 70 0.00003915 171.1 63.6 171.7 81.2 A 60 0.00006319 57.2 -74 291.6 -67.6 D4408 98 64.00000000 12 90 12 90 A 70 0.00005260 30.9 -47.9 212 -67.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige e01209 179 4.00000000 12 90 12 90 A 0 0.00470700 144.3 75.5 129.2 73.6 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 5 0.00289400 213.6 65.2 27.9 75.7 A 0 0.00273400 198.3 23.2 138 63.9 A 10 0.00223500 220.8 62.6 22.2 71.9 A 5 0.00075880 166.6 -20.2 330.9 62.5 A 15 0.00168900 221.7 61.4 19.3 71.1 A 10 0.00025620 153 -25.8 319.2 50.3 A 20 0.00134400 221.5 61.6 19.7 71.2 A 15 0.00010340 115.5 -28.3 301.1 20.2 A 25 0.00104600 221.2 62.6 22.4 71.8 A 20 0.00007923 62.2 -24.2 294.2 -26.9 A 30 0.00084470 222.9 61.4 20.1 70.5 A 25 0.00008770 40.1 -14.4 286.5 -49.2 A 40 0.00060260 219.3 61.6 18.3 72.2 A 30 0.00009497 27.8 -8.9 280.5 -62 A 50 0.00045300 220.6 61.5 18.9 71.6 A 40 0.00009936 19 -4.3 270.6 -71 D4608 97 63.00000000 12 90 12 90 A 50 0.00008645 30.3 -11 283.8 -59.2 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 60 0.00006938 12.2 -3.6 267.5 -77.8 A 0 0.00305900 225.7 72.6 56.1 70.9 A 70 0.00005793 20.4 -3.5 268.3 -69.6 A 5 0.00139400 220.8 67.9 41.2 72.7 e01609 125 30.00000000 12 90 12 90 A 10 0.00086690 219.5 63.6 26.6 72.5 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 15 0.00060340 221.1 62.6 24.3 71.5 A 0 0.00380400 199.2 20.9 11.7 70.5 A 20 0.00043380 221 62.4 23.6 71.5 A 5 0.00269500 195.1 13.5 348.5 68.4 A 25 0.00031810 222 60.3 18.3 70.2 A 10 0.00179700 194.3 11.6 343.8 67.3 A 30 0.00024030 221.4 60.6 18.7 70.6 A 15 0.00117700 193.3 10.7 340.5 67.1 A 40 0.00016430 217.7 61.5 19.1 72.6 A 20 0.00076850 192.8 9.8 338.2 66.5 A 50 0.00011210 216.5 56.4 3.8 70.8 A 25 0.00048850 190.6 9.1 332.5 66.9 A 60 0.00008595 232.6 63.9 32.9 67.1 A 30 0.00028630 189.2 8.7 328.9 67 A 70 0.00007171 207.2 66.3 34.9 78 A 40 0.00011060 187.8 6.4 323.8 65.3 A 80 0.00006073 216.5 70.3 49.8 74.1 A 50 0.00004636 187.3 7.4 323.3 66.4 D4808 54 35.00000000 12 90 12 90 A 60 0.00003054 189.3 7.2 327.8 65.6 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 70 0.00002341 193.4 0.1 330.5 57.5 A 0 0.00344400 209.2 65.2 33 55.1 e02009 106 26.00000000 12 90 12 90 A 5 0.00238400 205.2 57.6 25.1 61.8 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 10 0.00157600 207.2 54.8 18.9 62.7 A 0 0.00454000 208.5 18.6 6.2 62.7 A 15 0.00104900 206.8 54.6 18.9 63 A 5 0.00351400 204.9 14.6 354.8 64.1 A 20 0.00069320 206.7 55.5 20.5 62.5 A 10 0.00253600 204 13.7 352 64.4 A 25 0.00039740 205.6 54.4 19.4 63.7 A 15 0.00179300 202.3 12.9 348.2 65.3 A 30 0.00024520 205.5 54.8 20.2 63.5 A 20 0.00116600 199.9 13.1 345.2 67.3 e00509 -85 7.00000000 12 90 12 90 A 25 0.00069320 196 12.7 337.6 69.9 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00033640 190.7 14.5 329.1 74.8 A 0 0.00283000 158.4 23.8 323.6 63.3 A 40 0.00006324 161.1 18.5 215.4 71 A 5 0.00259500 156.4 21.3 330.5 63.1 A 50 0.00002269 72.6 16 173.8 -7.9 A 10 0.00208100 154.5 14.1 347.1 64 A 60 0.00001348 30.2 10.8 148.4 -42.9 A 15 0.00158500 153.5 12.4 351.3 63.3 A 70 0.00000753 131 59.3 137.6 42.7 A 20 0.00117300 150.6 13.4 350.1 60.4 e02209 -70 16.00000000 12 90 12 90 A 25 0.00081340 149.6 14.7 347.9 59.2 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00058310 145.1 17.9 343.9 54.3 A 0 0.00812400 158.4 27.6 346.2 66.9 A 40 0.00036720 141.6 22.5 338.1 49.9 A 5 0.00669000 156 26.9 349.9 65.2 A 50 0.00026580 139.6 24.7 335.7 47.5 A 10 0.00559400 155.6 27.8 348.2 64.5 A 60 0.00022240 138.6 24 337.1 46.9 A 15 0.00452200 155.8 28 347.6 64.6 A 70 0.00019420 140.8 23 337.7 49.1 A 20 0.00355000 155 28.3 347.6 63.9 e00709 265 34.00000000 12 90 12 90 A 25 0.00279800 154.8 27.8 348.8 63.9 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00222500 154.5 28 348.6 63.6 A 0 0.00167200 159.6 33.5 351 73.1 A 40 0.00153500 155.1 27.9 348.4 64.1 A 5 0.00144400 153.4 30 357.7 67.2 A 50 0.00099480 155.4 27 350.1 64.7 A 10 0.00116600 146.5 24 5 59.2 A 60 0.00064770 156.2 27.8 347.7 65 A 15 0.00094640 145.8 25.8 1.3 59.4 A 70 0.00041620 154.4 29.7 345.3 62.8 A 20 0.00074960 143.7 29.1 354 58.8 e02509 -71 34.00000000 12 90 12 90 A 25 0.00055090 141.5 31.4 348.7 57.7 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00040240 136.2 33.6 343 53.9 A 0 0.00761700 144.9 54.1 328.9 58.3 A 40 0.00024490 128 37 335.4 48.1 A 5 0.00615700 146.6 49.8 336 60.9 A 50 0.00014930 121.4 40.3 329.2 43.7 A 10 0.00502800 146.6 49.4 336.7 61 A 60 0.00010400 126.2 37.5 334.2 46.8 A 15 0.00381000 147.3 49.2 336.8 61.5 A 70 0.00007512 130.4 41 329.8 50.6 A 20 0.00300500 147.4 49.4 336.4 61.5 e01009 149 63.00000000 12 90 12 90 A 25 0.00232800 147.9 49 336.9 62 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00183900 147.4 49 337.1 61.7 A 0 0.00515500 200.1 59.7 49.1 79.9 A 40 0.00128200 148.7 48.5 337.5 62.6 A 5 0.00079410 180.8 42.1 330.7 69.1 A 50 0.00085820 148.4 47.6 339.5 62.8 A 10 0.00026540 172.8 24.9 318.5 51.6 A 60 0.00057970 148.6 48.4 337.8 62.6 A 15 0.00011230 164.5 4.2 311.1 30.1 A 70 0.00039890 150.9 48.2 337 64.1 A 20 0.00007348 132.8 -37.1 291.3 -16.9 e03409 74 30.00000000 12 90 12 90 A 25 0.00007780 108.8 -57.7 285.7 -42.5 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00009037 94.6 -64.8 285.1 -52.3 A 0 0.00176700 220.6 61.2 45.4 49 Appendix C, page 1 of 18 Appendix C

A 5 0.00037930 206.1 56.7 47.2 57.7 A 50 0.00002531 148.5 33.3 280.6 64 A 10 0.00019540 196.8 49 44.8 67.1 A 60 0.00001754 182.8 30 42 84.5 A 15 0.00013700 196.4 41.9 30.5 72.2 A 70 0.00002310 180 42.8 196 82.2 A 20 0.00010220 199.9 43.6 30.2 69.1 e05009 178 25.00000000 12 90 12 90 A 25 0.00007916 192.9 41.5 35.3 74.5 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00007001 191.4 35.3 15.9 79 A 0 0.00359300 187.6 45.1 162.9 69 A 40 0.00004628 191.8 34.5 11.3 79.1 A 5 0.00196000 181.6 15.3 7.1 80.2 A 50 0.00003226 179.3 28.7 228.7 88.6 A 10 0.00106000 180 12.2 358 77.2 A 60 0.00002544 218.7 25.6 346.3 55.6 A 15 0.00057730 178.4 13.2 350.4 78.1 A 70 0.00001551 195 20.8 313.2 73.6 A 20 0.00031240 178.2 14.5 348.5 79.4 e03509 96 7.00000000 12 90 12 90 A 25 0.00016770 179.5 13.7 355.5 78.7 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00009997 179.1 13.9 353.5 78.9 A 0 0.00191000 215.5 48.9 66.8 38.5 A 40 0.00005538 165.8 15.7 300.3 73.8 A 5 0.00069060 203.5 7.3 8.2 66.7 A 50 0.00003117 171.2 2.9 335.6 66.3 A 10 0.00046830 199.5 4.7 0.3 70.5 A 60 0.00001246 179.9 -4.5 357.8 60.5 A 15 0.00029120 199.6 4.4 359.5 70.3 A 70 0.00001427 190.4 -49 5.1 15.4 A 20 0.00020700 200.6 4.6 0.4 69.4 e05409 180 23.00000000 12 90 12 90 A 25 0.00014400 193.2 5.5 0.2 76.8 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00009857 204 -1 348.4 64.8 A 0 0.00442200 208.7 52.2 150.4 53.5 A 40 0.00006542 202.3 -1.1 346.8 66.3 A 5 0.00128900 184.2 18.9 44.5 84.3 A 50 0.00003116 190.5 -12.9 303.7 67.5 A 10 0.00056980 181 12.8 5.5 79.8 A 60 0.00002735 180.8 -3 280.6 80 A 15 0.00025380 177.1 13.5 343.4 80.1 A 70 0.00002490 206.1 7.5 8.8 64.1 A 20 0.00014130 182.6 21.2 53.7 87 e03709 260 21.00000000 12 90 12 90 A 25 0.00009652 184.2 24.6 113.4 85.8 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00004549 185.9 19 55.1 83.2 A 0 0.00130000 152.5 35.9 312.2 61.8 A 40 0.00004439 170.2 -7.2 341.2 58.3 A 5 0.00097100 145.7 12.4 359.2 56.1 A 50 0.00003624 198.4 12.8 62.9 69.8 A 10 0.00065150 149.4 11.3 3.5 59.1 A 60 0.00001705 171.1 47.1 194.4 64.9 A 15 0.00038920 150.2 11 4.6 59.7 A 70 0.00001991 191.2 23 92.2 79.7 A 20 0.00027130 151.8 12.1 3.8 61.6 e05709 204 35.00000000 12 90 12 90 A 25 0.00020620 151.3 11.7 4.1 61 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00017530 154.3 12.7 4.5 64.1 A 0 0.00518500 185.1 43.9 181.7 80.3 A 40 0.00011850 152.6 14.1 0.3 63 A 5 0.00176800 165.7 24.9 329.4 74 A 50 0.00008613 153.4 13.3 2.6 63.5 A 10 0.00110900 163.4 23.1 329 71.3 A 60 0.00005958 150.2 3.2 17.5 56 A 15 0.00080330 163.9 22.6 331.1 71.3 A 70 0.00005408 143.6 14.4 354.7 54.8 A 20 0.00061160 164 23.6 329.1 72 e04009 -73 26.00000000 12 90 12 90 A 25 0.00047240 165.1 22 335 71.6 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00039810 165.1 25.3 327 73.9 A 0 0.00324100 166.4 58.3 299.9 56.3 A 40 0.00030210 163.4 22.2 331 70.7 A 5 0.00192100 152.7 43 332.6 62 A 50 0.00022430 168 23.6 338.3 74.6 A 10 0.00125300 155.4 37.2 342.7 66.3 A 60 0.00018380 170.5 25.8 339.8 77.7 A 15 0.00078850 156.7 35 347.2 68.1 A 70 0.00014850 164.7 23.3 331.2 72.3 A 20 0.00056340 156.2 35.6 346 67.5 e06109 193 28.00000000 12 90 12 90 A 25 0.00041590 157.5 34 349.3 69 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00032460 157.6 31.5 356.1 69.6 A 0 0.00775200 181.1 21 21.4 82.9 A 40 0.00024090 155.7 34.5 349.1 67.4 A 5 0.00595900 174.3 14.6 350.3 75.6 A 50 0.00017250 155 30.1 0.7 67.6 A 10 0.00413300 173.3 13.8 347.9 74.5 A 60 0.00017550 173.7 27.7 358.8 84.1 A 15 0.00289400 173 13.2 347.8 73.8 A 70 0.00000653 60.4 58.8 314.1 8.3 A 20 0.00209500 172.5 13.4 345.9 73.8 e04409 -76 23.00000000 12 90 12 90 A 25 0.00151600 172.1 13.8 344 74 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00116000 172.3 13.8 344.7 74.1 A 0 0.00235400 181.3 32.8 277.6 80.1 A 40 0.00076650 172.7 15 344 75.3 A 5 0.00120600 157.7 15.3 30.1 67.6 A 50 0.00050580 176.6 17.6 355.5 79.1 A 10 0.00055990 155.8 16.2 26.2 66.2 A 60 0.00035660 181 19.9 19.6 81.8 A 15 0.00024310 159.1 14.2 34.3 68.4 A 70 0.00026050 187.2 26.9 94.9 83.5 A 20 0.00012110 155.8 16.4 25.8 66.3 e06609 129 15.00000000 12 90 12 90 A 25 0.00005339 169.3 19.8 29.8 79.5 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00003191 168.9 17.4 40.3 78.2 A 0 0.00396400 192.2 20.9 67.7 77 A 40 0.00002366 164 -25.1 85.1 39.5 A 5 0.00297300 188.9 5.4 352.3 77 A 50 0.00001203 173.9 29.3 323.7 81.7 A 10 0.00175100 187.3 5.5 346.8 78.1 A 60 0.00001518 149 22 9.9 61.4 A 15 0.00105000 186.7 6.1 346.2 78.9 A 70 0.00001521 107.2 37.9 341.8 27.1 A 20 0.00070610 187 5.3 345.1 78.1 e04809 196 35.00000000 12 90 12 90 A 25 0.00051960 187.3 5.2 346 77.9 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00042500 186.8 6.1 346.6 78.9 A 0 0.00206300 192.2 65.4 186.2 58.7 A 40 0.00029320 185.3 5.7 338.8 79.3 A 5 0.00073610 168.9 18.5 342.3 70.8 A 50 0.00021270 187.6 7 352.8 79.1 A 10 0.00039570 173.4 18.1 355.2 72.1 A 60 0.00016520 184.7 5.8 336.1 79.7 A 15 0.00019470 172.2 18.9 350.8 72.5 A 70 0.00011880 187.9 5.6 349.4 77.8 A 20 0.00009520 171.5 12.4 355.1 66.1 e06809 124 18.00000000 12 90 12 90 A 25 0.00006878 180.4 24.7 18 79.7 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00005549 177.8 12.7 10.4 67.6 A 0 0.00315100 192 43 104.4 63 A 40 0.00004216 155 50.5 237.7 66.2 A 5 0.00169900 190.8 11.3 2.8 77.6 Appendix C, page 1 of 18 Appendix C

A 10 0.00093220 189.3 10.7 356.2 78.4 f10008 17 65.00000000 12 90 12 90 A 15 0.00058650 189.8 9.9 354.9 77.5 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 20 0.00041730 188.6 11.2 355.9 79.3 A 0 0.00881300 241.7 84.6 4.7 67.1 A 25 0.00032330 188.2 10.1 350.3 78.8 A 5 0.00866500 246.5 84.3 3.7 66.7 A 30 0.00026590 188.4 9.7 349.6 78.4 A 10 0.00840300 252.6 84 2.7 66.1 A 40 0.00019830 193.6 8.9 1.2 74 A 15 0.00799400 256 83.8 2.2 65.8 A 50 0.00013890 191.2 10 359.1 76.5 A 20 0.00747900 258.7 83.8 2.2 65.5 A 60 0.00010430 188.1 10.8 352.5 79.4 A 25 0.00646900 260.9 83.6 1.8 65.2 A 70 0.00008871 186.9 6 334.2 76.2 A 30 0.00546100 263.4 83.5 1.6 65 e07109 225 23.00000000 12 90 12 90 A 40 0.00360900 267 83.7 2.2 64.6 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 50 0.00188200 271.3 83.5 2 64.1 A 0 0.01115000 177.8 22.6 325.7 87.9 A 60 0.00089620 275.2 83.2 1.6 63.6 A 5 0.00946200 175.7 13.4 21.2 79.6 A 70 0.00040230 278.1 82.6 0.7 63 A 10 0.00650200 174.2 11.5 18.4 77.2 A 80 0.00016780 281.6 81.4 358.8 62.1 A 15 0.00397800 172.7 10.6 14.5 75.8 f10708 87 48.00000000 12 90 12 90 A 20 0.00213100 170.6 9.7 9.4 73.9 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00107600 168.8 10.2 3.3 73.3 A 0 0.01565000 215.9 57 33.2 66.7 A 30 0.00060050 167.9 9 3.4 71.8 A 5 0.01506000 215 56.7 32.6 67.2 A 40 0.00025960 168.6 8.8 5.6 72.1 A 10 0.01308000 214.7 56.5 32.1 67.4 A 50 0.00012450 173.9 7.9 22.8 73.8 A 15 0.01013000 213.3 56.6 32.6 68.2 A 60 0.00008594 175.6 12.8 22 79 A 20 0.00721100 212.1 58.8 38.8 68.3 A 70 0.00004953 181.3 14.7 53.6 81.6 A 25 0.00444200 209.5 57.2 35.5 70.1 e07209 263 35.00000000 12 90 12 90 A 30 0.00254600 209.2 59.1 40.9 69.7 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 40 0.00094260 206.9 60 44.6 70.4 A 0 0.00884000 153.2 63.5 284.7 57.1 A 50 0.00029530 209.2 59.8 42.8 69.4 A 5 0.00594000 142.4 65.8 287 52.1 f11108 131 50.00000000 12 90 12 90 A 10 0.00363700 140.8 64.4 289.5 52.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 15 0.00223700 139.7 65.1 289 51.6 A 0 0.01250000 207.6 41.7 28.1 69.2 A 20 0.00119100 138.5 63.4 291.8 52 A 5 0.01227000 212.1 42.8 35.2 66.9 A 25 0.00063270 138.4 62.6 293 52.3 A 10 0.01127000 212 43 35.6 67.1 A 30 0.00039010 136 61.8 294.9 51.6 A 15 0.00943100 211.3 42.6 34 67.3 A 40 0.00019830 134.7 61.1 296.3 51.3 A 20 0.00747500 210.6 44.3 37.4 68.6 A 50 0.00012280 143 61.9 292.2 54.5 A 25 0.00537400 209.2 44.1 35.6 69.4 A 60 0.00008268 138.6 65.1 289.4 51.2 A 30 0.00392200 208.9 44.4 36.1 69.7 A 70 0.00005347 146.2 65.1 286.4 53.8 A 40 0.00215700 208 43.7 33.5 70 e08109 197 61.00000000 12 90 12 90 A 50 0.00109700 207.5 42.2 29.2 69.5 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 60 0.00056760 207.1 38 19.5 67.3 A 0 0.00531600 187.1 60.2 97.2 86.4 h0703 -74 24.00000000 12 90 12 90 A 5 0.00199000 173.6 49.9 356.2 78.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 10 0.00095640 173.6 46.1 0 74.6 A 0 0.02360000 334.7 -17.4 206.8 -65.5 A 15 0.00058250 174.9 44.3 4.4 73 A 5 0.02104000 333.4 -17.2 206.2 -64.2 A 20 0.00039200 175.2 44 5.3 72.8 A 10 0.01013000 331.2 -16.1 206.9 -61.9 A 25 0.00026180 173.9 44.5 1.9 73.1 A 15 0.00481800 332.3 -16.9 206.1 -63.1 A 30 0.00021160 176.5 46.7 7.3 75.6 A 20 0.00243200 332.8 -16 208.3 -63.3 A 40 0.00014840 174.8 41.4 5.5 70.1 A 25 0.00137300 333.7 -16.6 207.8 -64.3 A 50 0.00012360 173.8 43.8 2.1 72.4 A 30 0.00088090 333.8 -16.5 208.1 -64.3 A 60 0.00007416 180.6 43.1 18.4 72.1 A 40 0.00044800 333.2 -17.4 205.7 -64.1 A 70 0.00007285 168.9 39.8 354 67.7 A 50 0.00023210 333.7 -19 202.4 -65.1 e08309 123 58.00000000 12 90 12 90 A 60 0.00014650 334 -19.3 201.9 -65.4 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 70 0.00009237 330 -20.6 197 -62.1 A 0 0.00472100 220.5 58.6 52 69 h0705 -39 17.00000000 12 90 12 90 A 5 0.00177900 213.3 55.4 39.2 71.7 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 10 0.00083910 210 52.1 26.9 72 A 0 0.03977000 354.4 -39.9 151.9 -66.6 A 15 0.00045710 207.9 51.5 22.9 72.8 A 5 0.03980000 353.7 -39.4 153.5 -66.9 A 20 0.00029440 206.2 47.9 11.4 71.4 A 10 0.03810000 353.6 -37.4 155.2 -68.8 A 25 0.00021530 205.7 45.8 6.2 70.2 A 15 0.02859000 352.8 -36.7 157.5 -69.3 A 30 0.00014410 204.3 42.9 358.7 68.6 A 20 0.01872000 350.2 -38.1 161.2 -67.2 A 40 0.00010990 205.4 37.3 352.8 63.5 A 25 0.01060000 349.8 -35.7 164.9 -69.2 A 50 0.00008016 198.7 40.9 346 69.2 A 30 0.00610900 349.5 -37.5 163.2 -67.5 A 60 0.00006342 204.1 38.8 352.6 65.3 A 40 0.00272000 349.9 -38 161.9 -67.2 A 70 0.00006433 212.3 56.3 41.3 72.6 A 50 0.00122900 349.1 -39.4 161.8 -65.7 f9608 25 62.00000000 12 90 12 90 A 60 0.00067140 347.7 -40 163.4 -64.6 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 70 0.00040030 344.4 -41.3 166.7 -62.2 A 0 0.00969400 125.5 76 55.7 67.3 h0709 31 46.00000000 12 90 12 90 A 5 0.00947500 125.4 75.9 56 67.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 10 0.00888700 125.1 75.8 56.3 67.2 A 0 0.00191800 171.2 -60.6 206.5 -16.8 A 15 0.00778600 124.9 75.8 56.3 67.2 A 5 0.00167300 65.5 -69.5 180.7 -50.8 A 20 0.00646900 125.4 75.7 56.5 67.3 A 10 0.00126200 54.1 -66.1 175.7 -55.4 A 25 0.00462600 125.7 75.4 57.2 67.4 A 15 0.00089830 50 -64.6 173.6 -57.3 A 30 0.00331100 126.2 75.4 57.2 67.6 A 20 0.00062050 49.5 -62.4 169.6 -57.8 A 40 0.00160400 126.8 75.3 57.4 67.7 A 25 0.00044530 52.8 -62.8 170 -56.3 A 50 0.00071180 125.3 74.7 59.1 67.4 A 30 0.00031340 51.5 -62.3 169.2 -56.9 Appendix C, page 1 of 18 Appendix C

A 40 0.00019370 59.8 -56 158.7 -52.3 A 5 0.01795000 155.8 48.7 69.1 68.6 A 50 0.00012110 55 -55.2 156.6 -54.9 A 10 0.01156000 152.1 47.1 65.3 66.1 A 60 0.00006949 71.1 -50.7 154.1 -44.4 A 15 0.00776700 152 47.6 64.6 66.5 A 70 0.00006775 56.7 -44.5 140 -50.9 A 20 0.00460700 151 46.7 64.2 65.3 h0711 -22 47.00000000 12 90 12 90 A 25 0.00263100 151.3 45.3 66.1 64.2 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00147400 151 45.8 65.1 64.5 A 0 0.00334400 284.3 -55.4 208.2 -44.2 A 40 0.00063590 152.3 45.2 67.7 64.4 A 5 0.00264000 310.8 -68.2 189.7 -57.6 A 50 0.00027670 153.6 45.6 69.2 65.2 A 10 0.00176100 332.3 -69.1 180.2 -64 A 60 0.00014000 156.6 41.7 77.2 62.4 A 15 0.00117900 338.9 -68.6 176.8 -65.9 A 70 0.00008538 156.7 40.1 78.5 60.9 A 20 0.00081960 342.7 -68.6 173.9 -66.7 h0730 -49 69.00000000 12 90 12 90 A 25 0.00052060 349 -68.7 168.5 -67.6 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00036260 351.6 -69.1 165.8 -67.5 A 0 0.01576000 144.8 48 73.3 62.8 A 40 0.00019130 5.2 -67.1 152.2 -69.7 A 5 0.01470000 145.4 47.7 74.4 62.8 A 50 0.00011350 9.5 -61.1 140.2 -74.9 A 10 0.01017000 145.7 45.8 76.6 61.1 A 60 0.00004332 37.4 -58.8 109.9 -65 A 15 0.00597700 145.3 44 77.5 59.4 A 70 0.00001983 21 -51.1 92.4 -75.7 A 20 0.00370900 145 45.2 76.2 60.4 h0717 74 72.00000000 12 90 12 90 A 25 0.00204300 146.2 43.6 79 59.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00123600 146.3 43.7 79 59.4 A 0 0.00199800 77 -47.8 171.4 -48.7 A 40 0.00060760 148 43.5 81.4 59.7 A 5 0.00200900 81.7 -54.7 180.8 -53.3 A 50 0.00034000 147 41.7 81.4 57.7 A 10 0.00151700 75.3 -57.6 178.2 -57.7 A 60 0.00020790 147.2 39.1 83.3 55.3 A 15 0.00107800 73.3 -57.7 176.7 -58.4 A 70 0.00013980 149 41.5 84.2 58.1 A 20 0.00078370 73.7 -58.5 177.9 -58.9 h0740 184 76.00000000 12 90 12 90 A 25 0.00055350 73.9 -56.9 176.3 -57.5 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00041400 76.5 -55.8 177.5 -55.8 A 0 0.00890000 209.3 49.4 45 60.9 A 40 0.00024210 80 -52.9 177.9 -52.3 A 5 0.00882100 212.3 48.2 48.2 59.3 A 50 0.00015300 85.2 -51.8 181.4 -49.8 A 10 0.00825800 212.7 47.7 48.5 58.7 A 60 0.00009822 94.3 -44.1 184.4 -40.2 A 15 0.00711400 212 48 47.7 59.1 A 70 0.00009595 99.7 -44.3 189.1 -38.8 A 20 0.00566100 211.4 49 47.5 60.2 h0718 -33 77.00000000 12 90 12 90 A 25 0.00396400 209.7 47.5 44.6 59 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00267800 208.7 48.2 43.6 59.9 A 0 0.00211500 66.7 -23.8 39.7 -28.3 A 40 0.00116900 208.4 48.2 43.2 59.9 A 5 0.00099170 7.2 -17.1 335 -30 A 50 0.00042110 208.3 46 42.1 57.8 A 10 0.00071700 352.5 -10.9 318.9 -23.8 f211 184 10.00000000 12 90 12 90 A 15 0.00047440 350.5 -8.2 316.9 -21 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 20 0.00031700 347.6 -10.8 313.7 -23.5 A 0 0.01386000 3 0.2 200.5 -79.4 A 25 0.00018980 347.9 -9.9 314.1 -22.6 A 5 0.01360000 1.3 0.5 191.1 -79.4 A 30 0.00010740 347.5 -12.9 313.5 -25.6 A 10 0.01104000 0.5 0.7 186.7 -79.3 A 40 0.00006279 344.1 -9.8 310 -22.3 A 15 0.00837600 359.7 0.7 182.4 -79.3 A 50 0.00003860 343.3 -27.7 307.6 -40.1 A 20 0.00616100 359.1 0.9 179.3 -79.1 A 60 0.00002964 335.3 -23.9 299 -35.6 A 25 0.00428200 358.7 0.8 177.1 -79.1 A 70 0.00001882 350.1 -39.9 314.4 -52.7 A 30 0.00306700 358 0.8 173.4 -79 h0721 264 81.00000000 12 90 12 90 A 40 0.00178700 357.9 0.8 172.9 -79 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 50 0.00104900 357.7 0.7 171.8 -79.1 A 0 0.00218000 101.8 -10.3 7.2 -8.3 A 60 0.00068210 358.1 0 173.2 -79.8 A 5 0.00066100 76.7 -2.7 341.3 -4.7 A 70 0.00044690 358.5 0 175.4 -79.9 A 10 0.00031890 65.6 -2 330.2 -5.7 f215 191 24.00000000 12 90 12 90 A 15 0.00015470 60.5 -10.7 326.3 -15 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 20 0.00009589 59.9 -17.1 326.7 -21.4 A 0 0.01174000 351.4 6.4 174.5 -58.5 A 25 0.00005104 57.9 -18.7 324.9 -23.3 A 5 0.01074000 352.3 6 176 -59.1 A 30 0.00004419 51.9 -29 320.4 -34.3 A 10 0.00721100 351.7 5.2 174.4 -59.7 A 40 0.00003180 49.5 -24.5 317.1 -30.1 A 15 0.00455200 351.5 4.7 173.8 -60.1 A 50 0.00001288 46.1 -33.7 315.1 -39.7 A 20 0.00300400 350.9 4.9 172.8 -59.8 A 60 0.00001099 24.5 -16.5 289.9 -24.6 A 25 0.00212900 351 4.5 172.7 -60.2 A 70 0.00001385 55.2 -50.5 329.5 -55 A 30 0.00155700 350.9 4.4 172.5 -60.2 h0726 9 81.00000000 12 90 12 90 A 40 0.00103100 351.1 5 173.2 -59.7 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 50 0.00072430 350.9 4.3 172.4 -60.3 A 0 0.00842800 66.9 72.3 55.3 67.3 A 60 0.00053590 349.9 5.8 171.4 -58.6 A 5 0.00817500 64.3 72.6 53.2 67.3 A 70 0.00039400 349.6 5.5 170.7 -58.8 A 10 0.00697100 64.7 73.5 52.6 68.1 f2110 -77 6.00000000 12 90 12 90 A 15 0.00481300 64.3 73.3 52.5 67.9 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 20 0.00315800 65.5 74.5 52.1 69.1 A 0 0.00438100 349.3 -12 162.7 -77.9 A 25 0.00193000 67.2 74.2 53.6 69 A 5 0.00319200 338 -9.3 183 -68 A 30 0.00107700 68.3 74.1 54.5 69.1 A 10 0.00175100 336.2 -8.1 186.5 -66.3 A 40 0.00047750 66.9 74.2 53.4 69 A 15 0.00121700 336.2 -8.3 186 -66.3 A 50 0.00020410 74.2 73 59.9 68.8 A 20 0.00089150 336.4 -8.5 185.5 -66.5 A 60 0.00010120 79.9 70.8 66.7 67.5 A 25 0.00069470 337.4 -8 186.6 -67.5 A 70 0.00005849 56.5 67.4 51.2 61.5 A 30 0.00056550 337.7 -8.5 185.2 -67.7 h0729 -63 66.00000000 12 90 12 90 A 40 0.00042320 336.7 -9.3 183.4 -66.7 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 50 0.00031310 336.2 -8.5 185.5 -66.3 A 0 0.02078000 157.6 48.4 72.4 68.9 A 60 0.00024720 338.5 -8.2 185.8 -68.6 Appendix C, page 1 of 18 Appendix C

A 70 0.00019200 334.4 -9.9 182.6 -64.4 A 5 0.00094320 322.9 -42.2 204.7 -60.4 f2113 -69 3.00000000 12 90 12 90 A 10 0.00101500 331.2 -46.9 192.3 -65.4 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 15 0.00063830 331.2 -47.5 190.9 -65.2 A 0 0.00306600 345.1 -3.8 197.5 -75.1 A 20 0.00035550 331.1 -45.9 194.6 -65.6 A 5 0.00300200 342 -6.2 190.2 -71.8 A 25 0.00020950 332.4 -46.3 193 -66.4 A 10 0.00177300 339.8 -7 189 -69.5 A 30 0.00013210 335.8 -41.3 204.4 -70 A 15 0.00117900 339.7 -7.2 188.5 -69.4 A 40 0.00006484 334.6 -38.9 211.6 -69.4 A 20 0.00086890 340 -7 188.9 -69.7 k1008 48 47.00000000 12 90 12 90 A 25 0.00065660 339.5 -7.6 187.5 -69.1 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00052880 340.9 -8.9 182.9 -70.1 A 0 0.00132700 327.2 -38.7 325.2 -64.8 A 40 0.00040970 339.9 -7.8 186.7 -69.4 A 5 0.00033410 328.7 -79.3 237.9 -55.8 A 50 0.00029650 339.1 -8.9 184.2 -68.4 A 10 0.00015100 355.2 -73.3 231.1 -63.6 A 60 0.00022680 335.7 -9.9 183.9 -64.9 A 15 0.00008000 349.1 -64.3 243.1 -71.7 A 70 0.00018480 337.2 -9.8 183.2 -66.4 A 20 0.00004325 6.9 -65.2 218.9 -71.4 f2115 -70 0.00000000 12 90 12 90 A 25 0.00002996 348.5 -45.4 325.2 -81.9 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00002543 348 -24.5 20.8 -65.5 A 0 0.00386500 346 -3.4 186.2 -75.6 A 40 0.00002338 345.9 -26.5 14.6 -66.7 A 5 0.00339900 336.7 -4.5 188.7 -66.3 k1108 49 36.00000000 12 90 12 90 A 10 0.00200500 336.4 -4.9 187.9 -65.9 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 15 0.00131200 336 -4.4 189.3 -65.6 A 0 0.00118200 116.9 23 134 34.5 A 20 0.00101800 337.1 -4.9 187.6 -66.6 A 5 0.00016430 144.1 70.7 66.7 50.5 A 25 0.00075130 336.4 -4.1 189.8 -66.1 A 10 0.00002826 245.6 70.7 25.2 41.7 A 30 0.00064270 336.9 -6.4 184 -66.1 A 15 0.00002234 289.1 46.6 7 14.2 A 40 0.00047120 335.4 -4.4 189.5 -65 A 20 0.00002115 295.6 39.5 4.6 6 A 50 0.00035350 334 -6.8 184.8 -63.2 A 25 0.00001512 257.7 38.2 346.6 29.9 A 60 0.00028110 334.2 -3.4 192.2 -64 A 30 0.00001393 279.4 22.3 342.4 5.8 A 70 0.00021710 334.9 -7.6 182.5 -63.8 k1208 46 38.00000000 12 90 12 90 k208 -48 49.00000000 12 90 12 90 IDStep[mT] M[A/m] Dsp Isp Dge Ige IDStep[mT] M[A/m] Dsp Isp Dge Ige A 0 0.00289600 356 35.9 42.6 -16 A 0 0.00814000 340.9 -43.5 237.5 -75.7 A 5 0.00111200 1 -22.2 49.4 -74.2 A 5 0.00609300 340.8 -51 205.5 -77.5 A 10 0.00080240 6 -39.6 156.8 -85.1 A 10 0.00387500 340.1 -53.6 194.1 -76.8 A 15 0.00047380 6.5 -43 183.4 -83 A 15 0.00211400 340.3 -52.1 200.6 -77.1 A 20 0.00026590 1.9 -42.9 210.2 -84.9 A 20 0.00128800 339.1 -53 197.1 -76.3 A 25 0.00015060 1.8 -39.7 187.1 -87.8 A 25 0.00073070 339 -52.2 200.5 -76.3 A 30 0.00010160 7 -46.8 197.9 -79.8 A 30 0.00047510 340.3 -51.4 203.7 -77.2 k1308 85 76.00000000 12 90 12 90 A 40 0.00024140 341.3 -50 210.2 -77.8 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 50 0.00012190 341 -46 228 -76.9 A 0 0.00120700 266.4 -17.3 347.2 -15.9 A 60 0.00006487 335.4 -59.5 176.2 -72.4 A 5 0.00019850 30.9 -40.6 124.4 -52.1 A 70 0.00004288 329.7 -47.2 215.6 -69.8 A 10 0.00010350 36 -49.4 134.5 -59.8 k308 -17 30.00000000 12 90 12 90 A 15 0.00005564 35.3 -43.4 130.7 -54.1 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 20 0.00002724 55.8 -39.1 152.1 -45.8 A 0 0.00390200 352.5 -58.4 171.1 -61.1 A 25 0.00002068 353.4 -64.3 71 -78.1 A 5 0.00471400 345.5 -50.7 186.6 -66.6 A 30 0.00002092 298.3 -47.7 7.4 -52.6 A 10 0.00307900 343.3 -47.6 194.5 -68.2 k1408 45 68.00000000 12 90 12 90 A 15 0.00169500 343.7 -46.6 195.8 -69.1 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 20 0.00092450 342.8 -45.3 199.6 -69.6 A 0 0.00137400 321 49.7 16.6 31.3 A 25 0.00048710 342.7 -44.8 200.9 -69.9 A 5 0.00030620 249.6 40 314.5 44.1 A 30 0.00028990 344.3 -43.9 200.5 -71.3 A 10 0.00008957 241.3 32 301.5 40.1 A 40 0.00014610 344.4 -44.5 199 -71 A 15 0.00003825 232.2 31.1 291.6 42.5 k408 19 63.00000000 12 90 12 90 A 20 0.00002159 241.6 44.6 310.3 51.1 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00000552 123.3 80.6 70.5 71.5 A 0 0.00188800 4.3 -34.1 26.4 -61 A 30 0.00000731 304.3 22.4 354.3 9.1 A 5 0.00162200 16.8 -70.6 165.5 -80 k1608 53 78.00000000 12 90 12 90 A 10 0.00091050 13.4 -76.3 185.9 -76 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 15 0.00049720 9.1 -77.6 191.4 -75.1 A 0 0.00137300 97.2 33 142.3 33.7 A 20 0.00023000 8.8 -73.6 186 -78.9 A 5 0.00016090 90.6 -24.3 148.9 -23.6 A 25 0.00012070 357.4 -71.9 204.2 -81 A 10 0.00009907 89.4 -63.3 165 -61 A 30 0.00006650 3.6 -66.6 177.6 -86.1 A 15 0.00004826 52.2 -70.8 142.8 -74.9 k508 33 70.00000000 12 90 12 90 A 20 0.00003512 54.1 -60.2 128.4 -65.4 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00001135 355.7 -75.6 28.6 -87.4 A 0 0.00779400 80.3 -75.4 172.5 -67.5 A 30 0.00001267 12.7 -37.5 68.5 -49.1 A 5 0.00747200 75.1 -74 167.5 -68.1 k1708 110 73.00000000 12 90 12 90 A 10 0.00463800 76.8 -74.3 168.8 -67.8 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 15 0.00273700 76.2 -74.8 169.8 -68.2 A 0 0.00331800 176.9 79.4 115.1 83.6 A 20 0.00165100 77.6 -75.4 171.7 -68.1 A 5 0.00306300 215 80.1 77.3 79.5 A 25 0.00091440 77.1 -75.6 172 -68.3 A 10 0.00264400 235.4 79.6 71.9 76.1 A 30 0.00055240 75.3 -76.1 172.8 -68.9 A 15 0.00203900 245.2 78.6 69.1 74.1 A 40 0.00028310 72.5 -75 169.2 -69.1 A 20 0.00158900 250.3 78.7 70.5 73.2 k708 -40 35.00000000 12 90 12 90 A 25 0.00115000 253.2 78.6 70.8 72.6 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00078240 255.7 78.4 70.8 72 A 0 0.00132500 199.6 75.2 312.5 48.7 A 40 0.00040950 256.1 78.5 71.2 72 Appendix C, page 1 of 18 Appendix C

A 50 0.00015960 253.7 78 69.1 72.3 A 0 0.00512600 268.9 65.4 64.7 59.6 A 60 0.00004132 227.7 76.4 57.4 77.4 A 5 0.00449200 261.3 71.2 69.4 65.6 A 70 0.00001266 160.8 -64.4 277.7 -48 A 10 0.00317200 258.3 72.3 70.2 67 k1908 130 70.00000000 12 90 12 90 A 15 0.00220000 257.4 73.6 72.7 68 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 20 0.00157200 258.3 74.6 75.3 68.3 A 0 0.00336100 261 65.5 71.4 61.3 A 25 0.00099440 258.3 74.2 74.4 68.1 A 5 0.00316400 252 67.4 69.2 65.3 A 30 0.00066170 260.2 74.4 75.6 67.8 A 10 0.00274200 243.8 68.7 67.3 68.5 A 40 0.00032600 262.4 74.2 76 67.1 A 15 0.00218300 238.9 69.4 66.4 70.4 k2808 76 76.00000000 12 90 12 90 A 20 0.00169700 236.7 70 66.9 71.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00125800 235.2 70.7 68.2 72.1 A 0 0.00558600 240.7 87.6 66.7 77 A 30 0.00088910 234.6 71.3 69.8 72.5 A 5 0.00524100 259 87 63.5 76.3 A 40 0.00046250 229.3 72.5 71.9 74.4 A 10 0.00377600 261.6 86.7 62.3 76.1 A 50 0.00018390 208.7 72.4 67.9 80.5 A 15 0.00270800 260.6 86.8 62.7 76.2 k2008 109 76.00000000 12 90 12 90 A 20 0.00194500 260.3 86.9 63.1 76.2 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00125800 259 86.9 63.1 76.3 A 0 0.00343900 268.9 70.1 52 66.1 A 30 0.00088580 260.7 87 63.5 76.2 A 5 0.00314700 268 73.2 56.5 68.6 A 40 0.00047840 270.5 87.6 66.2 75.8 A 10 0.00265900 270.4 75.2 61.7 69.7 k3008 83 66.00000000 12 90 12 90 A 15 0.00213300 273 76.1 64.8 69.9 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 20 0.00163800 275.5 76.3 66.5 69.6 A 0 0.00844800 224.5 77.8 53.3 72.6 A 25 0.00119600 277.2 76.4 67.5 69.4 A 5 0.00806300 219.9 78.6 57 73.2 A 30 0.00083640 279.3 76.2 68.2 68.9 A 10 0.00651900 218.1 79.3 59.7 73.2 A 40 0.00043490 282.6 75.8 69.1 68.1 A 15 0.00481100 216.5 79.6 61.1 73.2 A 50 0.00016400 284.1 71.8 64.1 64.6 A 20 0.00359200 216 80.2 63 73 k2208 92 75.00000000 12 90 12 90 A 25 0.00245400 214.2 80.3 63.9 73.2 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00175600 214 80.7 65.1 72.9 A 0 0.00439700 250.1 77.7 44.4 74.3 A 40 0.00093200 211 81 66.9 73.1 A 5 0.00418100 257.5 79.2 51.6 73.6 A 50 0.00044740 210.1 80.9 67 73.3 A 10 0.00374300 263.7 80.2 56.5 73.1 k3208 30 70.00000000 12 90 12 90 A 15 0.00311100 266.8 80.5 58.2 72.8 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 20 0.00257600 269.2 80.9 60 72.6 A 0 0.00355100 139.2 82.7 48.5 74.8 A 25 0.00194100 270.8 80.9 60.5 72.4 A 5 0.00340700 121.7 79.3 62.9 73.1 A 30 0.00149600 272.5 81.2 61.8 72.3 A 10 0.00256200 111.3 81.1 56.8 71.4 A 40 0.00078030 274.5 81.2 62.3 72.1 A 15 0.00178200 106.9 82 53.9 70.8 A 50 0.00032820 275.1 80.8 61.4 71.8 A 20 0.00133800 105.3 82.6 52 70.6 A 60 0.00011560 272.9 80.1 58.9 71.7 A 25 0.00087960 103 82.8 51.3 70.4 A 70 0.00002467 244.8 78.7 46.3 75.6 A 30 0.00065070 97.5 83 50.4 69.7 k2308 122 76.00000000 12 90 12 90 A 40 0.00036660 93.3 83.5 48.7 69.4 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 50 0.00017680 93.9 82.8 50.7 69.3 A 0 0.00455300 267.1 74.8 72.1 70 A 60 0.00008767 92.6 80.5 56.5 68.3 A 5 0.00439000 255.7 74.2 64.4 71.8 k3408 104 75.00000000 12 90 12 90 A 10 0.00384800 253.2 73.9 62.2 72.1 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 15 0.00328700 252.3 74.5 63.2 72.7 A 0 0.00829600 194.6 79.4 74.6 84.6 A 20 0.00266600 252.6 74.7 63.9 72.7 A 5 0.00657500 237.8 78.1 54.1 76.8 A 25 0.00206400 252.6 74.7 63.9 72.7 A 10 0.00459600 248 74.6 45.9 73.1 A 30 0.00157200 253.6 75.4 66.3 73 A 15 0.00317800 249.6 73.8 44.6 72.3 A 40 0.00085510 253.6 75.8 67.4 73.2 A 20 0.00214900 251.2 72.8 43 71.3 A 50 0.00037530 249.9 76.1 66.4 74.1 A 25 0.00142200 251 71.7 40.3 70.7 k2408 120 73.00000000 12 90 12 90 A 30 0.00100500 250.2 71.6 39.6 70.8 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 40 0.00053270 247.8 71.6 38 71.3 A 0 0.00441700 245.4 69.7 53.3 69.9 A 50 0.00023670 245.4 71.7 36.7 72 A 5 0.00399100 238.1 68.6 45.8 71.2 k4408 98 80.00000000 12 90 12 90 A 10 0.00323000 238.6 68.9 46.9 71.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 15 0.00234800 238.5 69.4 48.1 71.6 A 0 0.00629700 296.3 80.7 67.1 73.6 A 20 0.00185900 239.8 70.4 51.5 71.8 A 5 0.00581400 294.8 81.2 67.4 74.2 A 25 0.00129100 239.8 70.6 52 72 A 10 0.00475100 288.7 79 59.9 73 A 30 0.00093790 240.7 70.8 53.1 71.8 A 15 0.00367000 290.5 78.4 59.8 72.3 A 40 0.00051840 239 70.9 52.3 72.4 A 20 0.00260800 292 77.4 59 71.2 A 50 0.00023460 239.3 70.7 52 72.2 A 25 0.00188600 293.1 77.6 60 71.3 k2608 141 73.00000000 12 90 12 90 A 30 0.00132100 294.4 77.2 60.1 70.8 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 40 0.00071860 295.9 77.5 61.4 70.9 A 0 0.00488600 229.6 77.5 93.5 77.1 A 50 0.00033960 296.1 76.9 60.7 70.4 A 5 0.00450800 234.6 71.9 73.7 74.1 A 60 0.00017110 294.4 77.6 60.7 71.2 A 10 0.00329900 237.7 70.8 72.2 72.6 k4508 99 88.00000000 12 90 12 90 A 15 0.00208300 237.4 70.6 71.5 72.6 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 20 0.00133200 238.4 70.6 72.1 72.3 A 0 0.00561000 54 74.3 147.7 73 A 25 0.00089800 238.4 71.5 74.6 72.8 A 5 0.00440700 350.7 76.4 90.9 74.4 A 30 0.00058780 238.6 72 76.2 73.1 A 10 0.00277100 330.1 73 72.1 71.2 A 40 0.00029960 237.2 72.9 78.2 73.9 A 15 0.00186700 329 71.7 70.8 70 k2708 120 71.00000000 12 90 12 90 A 20 0.00119000 326.4 70 68.2 68.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00079570 325.7 69.5 67.5 67.8 Appendix C, page 1 of 18 Appendix C

A 30 0.00056990 326.4 69.2 68.1 67.5 k7508 13 85.00000000 12 90 12 90 A 40 0.00030310 328.2 67.6 69.6 65.9 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 50 0.00015540 330.7 66.5 71.8 64.7 A 0 0.01900000 189.4 75.7 207.3 80.6 k4708 36 83.00000000 12 90 12 90 A 5 0.01748000 171.3 79 177.3 83.9 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 10 0.01265000 164.5 79.5 164.4 84.2 A 0 0.01181000 246.4 -74.3 263.8 -70.4 A 15 0.00846000 162.8 79.3 161.9 83.9 A 5 0.01174000 243.9 -77.1 258.8 -72.8 A 20 0.00568800 162.1 79.3 160.7 83.9 A 10 0.01128000 242.6 -79.2 255 -74.7 A 25 0.00359800 163.9 78.3 165.7 83 A 15 0.00984700 241.9 -80.2 252.9 -75.5 A 30 0.00214900 165.1 77.1 169.2 81.8 A 20 0.00763500 243.9 -80.7 253.3 -76.1 A 40 0.00098030 167.6 74.1 175.2 78.9 A 25 0.00518000 244.3 -80.8 253.3 -76.2 A 50 0.00045330 169.9 69.6 179.8 74.5 A 30 0.00357100 247.2 -81.7 253.1 -77.2 k7708 9 82.00000000 12 90 12 90 A 40 0.00165800 251.2 -82.3 253.8 -78.1 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 50 0.00070650 254.6 -82.7 254.4 -78.6 A 0 0.02413000 207.1 68.5 229.8 75.2 A 60 0.00033400 254.7 -83.7 251.2 -79.4 A 5 0.02321000 205.8 70.1 229.6 76.9 k4908 87 65.00000000 12 90 12 90 A 10 0.02061000 204.5 71 228.8 77.8 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 15 0.01699000 202.9 71.1 226.6 78.1 A 0 0.01516000 37.2 -70.5 215 -75.2 A 20 0.01406000 201.5 71.7 225.2 78.8 A 5 0.01490000 36.3 -71.9 220.5 -75.3 A 25 0.01017000 199.8 71.7 222.5 78.9 A 10 0.01362000 34.3 -72.8 224.6 -75.7 A 30 0.00752100 198.7 71.7 220.8 79 A 15 0.01100000 32 -73.5 228.2 -76.1 A 40 0.00392500 196.5 71.4 216.9 78.8 A 20 0.00836400 30.6 -74.3 231.9 -76.2 A 50 0.00174100 194.9 70.7 213.7 78.3 A 25 0.00589400 28.1 -74.4 233.6 -76.7 A 60 0.00067010 194.4 69.6 212 77.2 A 30 0.00408100 26.7 -75.7 239.1 -76.3 k8108 156 69.00000000 12 90 12 90 A 40 0.00224600 22.5 -76.9 245.6 -76.2 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 50 0.00107000 14.3 -77.9 254.3 -76.4 A 0 0.00276300 47.8 -45.3 226.3 -56.4 k6208 188 80.00000000 12 90 12 90 A 5 0.00184400 352.2 -68 81.6 -87 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 10 0.00099140 343.7 -68.6 62.3 -84.1 A 0 0.00666800 24.3 -82.7 326.1 -85.5 A 15 0.00055230 345.8 -69.1 58.2 -84.9 A 5 0.00691300 33.3 -72.6 251.9 -79.5 A 20 0.00035370 344 -69 58.5 -84.3 A 10 0.00516300 33.5 -71.7 249.8 -78.7 A 25 0.00023880 339.9 -67.8 65.8 -82.5 A 15 0.00269100 31 -70.8 244.1 -78.2 A 30 0.00017650 338.6 -67.8 64.6 -82.1 A 20 0.00164900 31.4 -73.3 251.3 -80.4 k8308 159 65.00000000 12 90 12 90 A 25 0.00086250 31.4 -73.3 251.3 -80.4 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00056280 29.6 -73.8 250.4 -81.1 A 0 0.00235600 44.3 -45.7 231.8 -59.3 A 40 0.00027670 34.3 -74.8 260.8 -81.1 A 5 0.00200100 9.4 -56.2 190.9 -80.1 k6408 225 81.00000000 12 90 12 90 A 10 0.00130300 359.1 -56.8 155.5 -81.8 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 15 0.00076820 356.6 -55.5 147.4 -80.4 A 0 0.00669900 6.7 -52.8 233.6 -61.7 A 20 0.00050380 355.5 -56.4 142.6 -81.1 A 5 0.00598400 7.4 -62.6 235.8 -71.5 A 25 0.00033490 355.3 -54.9 143.8 -79.6 A 10 0.00419600 5.5 -64.7 233.4 -73.6 A 30 0.00023810 353.7 -55.9 137.4 -80.4 A 15 0.00239400 2.1 -65.3 228.2 -74.3 A 40 0.00014210 352 -53.2 136.3 -77.5 A 20 0.00145500 0.2 -66.8 225.3 -75.8 A 50 0.00009081 351.7 -53.3 135.4 -77.6 A 25 0.00083700 359.1 -67.5 223.5 -76.5 k9008 163 80.00000000 12 90 12 90 A 30 0.00056600 358.6 -69 222.6 -78 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 40 0.00029060 359.2 -71.1 223.5 -80.1 A 0 0.00151500 242.3 53 58.6 56.6 k6608 1 71.00000000 12 90 12 90 A 5 0.00146100 241.7 59.4 61.9 62.8 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 10 0.00141600 249.8 69.9 81.2 71 A 0 0.02740000 115.6 75 49.2 71.8 A 15 0.00123900 259.9 74.2 97.1 72.9 A 5 0.02719000 111.6 75.1 47.7 70.8 A 20 0.00104700 266.3 75.7 104.8 73.1 A 10 0.02668000 109.1 75.1 46.9 70.2 A 25 0.00076720 270.1 75.9 107.7 72.8 A 15 0.02576000 107.9 75 46.8 69.9 A 30 0.00059680 272.8 76.2 110.1 72.6 A 20 0.02463000 107.4 75 46.7 69.8 A 40 0.00035070 274.6 76.3 111.4 72.5 A 25 0.02250000 107.2 75 46.6 69.8 A 50 0.00018380 277.3 75.6 111.9 71.5 A 30 0.01927000 107.4 75.2 46.1 69.9 A 60 0.00009023 278.9 74.2 110.8 70.1 A 40 0.01256000 108.9 76.3 43.6 70.7 k9308 155 80.00000000 12 90 12 90 A 50 0.00614300 111.7 78.3 38.2 71.9 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 60 0.00253100 122.4 83.9 19.4 73.5 A 0 0.00449200 123.2 -77.2 302.3 -69.9 A 70 0.00107900 274.1 79.6 332.6 67.8 A 5 0.00445200 129.4 -76.9 305.6 -69.1 k6808 3 85.00000000 12 90 12 90 A 10 0.00393600 129.3 -76.8 305.4 -69 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 15 0.00323600 129.4 -76.5 305.2 -68.7 A 0 0.02312000 41.7 77.8 33.1 73.7 A 20 0.00279600 129.7 -76.4 305.3 -68.6 A 5 0.02304000 39.9 77.9 31.7 73.7 A 25 0.00226800 129.9 -76 305 -68.2 A 10 0.02264000 38.7 78.4 30.5 74.2 A 30 0.00184000 130.5 -76.2 305.5 -68.4 A 15 0.02201000 37.3 78.7 29.3 74.4 A 40 0.00110400 131.8 -76.4 306.5 -68.4 A 20 0.02102000 36 79 28.1 74.7 A 50 0.00062330 132.2 -78.1 308.5 -70 A 25 0.01925000 34.4 79.1 26.9 74.7 A 60 0.00041650 129.7 -81.3 311.4 -73.1 A 30 0.01665000 32.8 79.4 25.6 75 k10208 127 30.00000000 12 90 12 90 A 40 0.01060000 26.2 80 20.6 75.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 50 0.00493700 12.4 79.8 11.4 74.9 A 0 0.00660700 188.5 30 39.1 82.6 A 60 0.00170100 345.7 76.6 352.5 71.7 A 5 0.00549400 188.8 29.3 34 82.3 A 70 0.00039100 315.7 44.9 321.9 41.2 A 10 0.00397000 187.5 29.8 37.1 83.5 Appendix C, page 1 of 18 Appendix C

A 15 0.00259200 186.2 29.1 29.1 84.5 k11108 32 35.00000000 12 90 12 90 A 20 0.00170100 185.1 30.3 42.2 85.6 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00113900 184.6 29.2 26.8 85.9 A 0 0.00459600 189.1 46.7 4.4 76.4 A 30 0.00078980 184.4 29.5 30.6 86.1 A 5 0.00414800 189.1 46.7 4.4 76.4 A 40 0.00047000 184.6 29.7 33.8 86 A 10 0.00313000 188.7 48.1 8.4 75.4 A 50 0.00031260 185.3 30.2 40.8 85.4 A 15 0.00199600 187.9 46.4 6.8 77.1 k10408 111 37.00000000 12 90 12 90 A 20 0.00131800 186.8 47 11 77 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00087560 186.4 46.1 10.4 77.9 A 0 0.00554300 191.7 38.5 33.8 80.6 A 30 0.00060010 186.2 46 10.8 78 A 5 0.00462900 186.5 37.9 32.9 84.8 A 40 0.00035650 186.3 45.9 10.3 78.1 A 10 0.00287700 184.6 38.7 47.5 86 A 50 0.00022050 186.7 45 6.9 78.8 A 15 0.00168500 183.5 38.2 45.5 87 k11308 1 22.00000000 12 90 12 90 A 20 0.00113600 183.3 38.4 50.2 87 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00080610 183.4 38.6 52.8 86.9 A 0 0.00601000 183.3 32.2 345.7 79.4 A 30 0.00060640 183.6 38.2 44.9 86.9 A 5 0.00529600 182.6 32.3 348.9 79.4 A 40 0.00042400 184.1 37.8 36 86.6 A 10 0.00372000 181.4 32.2 354.3 79.7 A 50 0.00031230 185.5 38.3 39.3 85.5 A 15 0.00246500 180.5 31.2 358.3 80.8 k10508 71 40.00000000 12 90 12 90 A 20 0.00160500 179.1 31.8 5.5 80.2 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00110800 179.2 31.2 5.3 80.8 A 0 0.00489000 196.6 43.1 0.4 77.2 A 30 0.00079470 178.4 31 9.7 80.9 A 5 0.00400700 198.2 44.9 7.1 75.7 A 40 0.00050830 179.3 31.4 4.7 80.6 A 10 0.00270600 196.8 44.5 6.4 76.8 A 50 0.00034220 179 31.6 6.1 80.4 A 15 0.00178600 195.2 44.5 7.8 77.9 k11508 -6 47.00000000 12 90 12 90 A 20 0.00121900 194.8 44.9 10.1 78.1 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00089230 194.8 44.6 8.7 78.1 A 0 0.00511000 180.8 51.4 347.5 85.6 A 30 0.00064970 194.9 44.9 9.9 78 A 5 0.00412500 184.8 55 335.2 81.5 A 40 0.00044480 195.8 45.1 9.9 77.3 A 10 0.00249200 184 54.6 337.1 82 A 50 0.00031530 197.5 45.2 8.8 76.1 A 15 0.00141400 183.9 52.4 330.4 84 k10608 52 22.00000000 12 90 12 90 A 20 0.00095070 184.2 52.9 331 83.5 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00069400 183.1 52.8 336.2 83.9 A 0 0.00451600 174.6 31.1 78.8 79.7 A 30 0.00054920 185 53.5 329.7 82.8 A 5 0.00351800 173.5 31.8 81.2 78.6 A 40 0.00039800 183.1 54.1 339.7 82.6 A 10 0.00245500 172.7 30.8 87 79 A 50 0.00029290 184.1 54.7 337 81.9 A 15 0.00162500 171.7 29.4 95.6 79.5 k11608 12 51.00000000 12 90 12 90 A 20 0.00109400 170.8 29.9 96.4 78.6 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00078410 170.3 29.2 100.5 78.7 A 0 0.00476900 186.4 57.3 343.8 82.7 A 30 0.00059580 170.5 29.1 100.4 78.9 A 5 0.00376800 185.4 57.2 347.1 83 A 40 0.00041230 170.2 29.1 101.2 78.7 A 10 0.00241400 184.3 57.6 352.9 82.9 A 50 0.00030240 171 30 95.4 78.6 A 15 0.00134100 183 56.9 356.5 83.8 k10708 100 66.00000000 12 90 12 90 A 20 0.00083940 182.4 57.3 0.4 83.5 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00051730 182.2 55.8 357.6 85 A 0 0.00369300 210.9 72.7 55.5 77.4 A 30 0.00034870 182.4 56 357 84.8 A 5 0.00337400 199.8 70.3 49.2 81.5 A 40 0.00021320 182.2 55.8 357.6 85 A 10 0.00233400 198.2 70.1 49.3 82.1 A 50 0.00014130 182.5 57.2 359.7 83.6 A 15 0.00161500 196.6 70.6 54.4 82.4 k11808 59 55.00000000 12 90 12 90 A 20 0.00106800 196.5 70.8 55.8 82.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00077700 195.9 70.8 56.6 82.5 A 0 0.01078000 185.5 42.4 257.2 76.9 A 30 0.00057470 194.9 71.1 59.9 82.6 A 5 0.00612900 198.2 61 8.4 78.7 A 40 0.00039870 196.6 71.6 60.6 81.8 A 10 0.00324100 198.3 61 8.3 78.7 A 50 0.00028630 199.1 71.8 58.8 81.1 A 15 0.00164000 196.2 63 19.6 78.5 k10808 94 72.00000000 12 90 12 90 A 20 0.00075320 194.6 62.6 20.2 79.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00031350 192.4 63.2 26.4 79.7 A 0 0.00403300 210.2 67 353.4 78.5 A 30 0.00015500 182.9 61.4 46.8 83.4 A 5 0.00319200 201.6 74 31.7 83.4 A 40 0.00005701 183.2 62.8 48.4 82 A 10 0.00221300 199.9 74.2 34.2 83.8 A 50 0.00003407 187.3 65.4 42.9 79 A 15 0.00151000 198.1 74.3 36.2 84.3 k12008 52 83.00000000 12 90 12 90 A 20 0.00101600 197.6 75.3 45.9 84.1 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00066420 196.3 75.2 46.5 84.4 A 0 0.01216000 338.5 84.7 42.7 77.9 A 30 0.00046930 195.2 75.9 54 84.3 A 5 0.01092000 330.9 82.7 37 76.2 A 40 0.00028320 197.7 76.7 56.8 83.4 A 10 0.00762600 326.1 81.7 33.4 75.4 A 50 0.00019210 197 76 52.5 83.9 A 15 0.00459700 323.6 81.5 31.8 75.3 k10908 17 50.00000000 12 90 12 90 A 20 0.00244600 322 80.8 30.1 74.7 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00130600 321.7 80.8 30 74.7 A 0 0.00454600 211.7 59.9 328 69.6 A 30 0.00071810 322.6 80.1 29.8 74 A 5 0.00394600 208.2 58 323.8 71.8 A 40 0.00028580 328.9 80.3 33.7 73.9 A 10 0.00269100 206.1 57.3 322.5 73 A 50 0.00010980 347.1 78 43.8 71.1 A 15 0.00175900 204.6 56.7 321.1 74 k12208 214 74.00000000 12 90 12 90 A 20 0.00114300 203.9 56.8 321.8 74.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00074520 203.2 56.5 321.1 74.8 A 0 0.01405000 161.2 58.2 359.3 72.6 A 30 0.00053460 203.3 56.8 322.2 74.6 A 5 0.01122000 168.4 61.3 9.3 76.6 A 40 0.00032510 203.3 56.7 321.8 74.7 A 10 0.00755500 169.4 61.8 10.9 77.2 A 50 0.00021020 203.2 56 319.3 74.9 A 15 0.00444100 169.2 60.9 11.3 76.3 Appendix C, page 1 of 18 Appendix C

A 20 0.00252400 166.7 62.4 4.6 77.5 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00123900 166.6 60 7.1 75.1 A 0 0.00612300 201.7 52.1 98.8 76.3 A 30 0.00065440 165.2 59.9 4.6 74.9 A 5 0.00517900 193 49.9 73.8 78.9 A 40 0.00023990 166.8 58.8 8.6 74 A 10 0.00365100 190.4 47.3 59.8 77.6 A 50 0.00009069 173.8 52.3 23.8 68.1 A 15 0.00212200 187.6 45.9 49.2 77 k12308 212 70.00000000 12 90 12 90 A 20 0.00118700 185.4 47.7 44.8 79.2 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00058130 183.6 44.8 36.1 76.6 A 0 0.01102000 171.8 61.4 6.8 80.8 A 30 0.00029500 181.6 45 30 77 A 5 0.01016000 174.7 58 18.6 77.8 A 40 0.00008334 179.2 36 23.3 68 A 10 0.00720600 173.4 57.6 15.8 77.3 A 50 0.00002781 181 5.7 26.3 37.7 A 15 0.00408200 171.7 56.1 13.1 75.6 s208 234 69.00000000 12 90 12 90 A 20 0.00215200 170 55.7 9.7 75 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00106800 169.5 53.9 10.2 73.2 A 0 0.00020360 331.7 39.6 211 20.6 A 30 0.00052920 167.1 53.9 5.5 72.9 A 5 0.00019500 339.7 9.6 213.7 -10.1 A 40 0.00019300 170.9 51.4 14.4 70.9 A 10 0.00019010 340.9 -10.6 212.1 -30.3 A 50 0.00007793 176.2 44.5 25.7 64.4 A 15 0.00014900 340.9 -14.8 211.4 -34.5 k12508 211 56.00000000 12 90 12 90 A 20 0.00009779 337.3 -16.2 207 -35.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00005837 337.1 -15 207 -34.1 A 0 0.01019000 176.4 45.9 16.9 79.7 A 30 0.00003484 335.7 -14.7 205.5 -33.6 A 5 0.00839300 181.3 45 35.8 79 A 40 0.00001285 338.3 -22.9 206.7 -42.1 A 10 0.00533000 180.9 43.8 34.1 77.8 A 50 0.00000658 340.8 -22 209.9 -41.6 A 15 0.00303400 178.8 43.3 27 77.3 s00209 226 78.00000000 12 90 12 90 A 20 0.00153200 176.1 43.6 18 77.4 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00077130 173.7 42.5 11.6 75.9 A 0 0.00001885 299.8 64.2 182.6 56.7 A 30 0.00039330 171.8 42.4 6.3 75.4 A 5 0.00001788 341 15.9 207.7 4.5 A 40 0.00015730 171.9 38.9 10.1 72.1 A 10 0.00001475 343.9 -2 209.4 -13.5 A 50 0.00008175 180.7 38.1 32.8 72.1 A 15 0.00001256 341.6 -10.5 206.5 -21.9 k12808 238 55.00000000 12 90 12 90 A 20 0.00001128 340.3 -11.8 205 -23.1 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 25 0.00001055 341.4 -15.3 205.9 -26.6 A 0 0.00164800 193.3 64.1 207.1 78.7 A 30 0.00000750 344.4 -30.2 207.9 -41.7 A 5 0.00199300 186.4 43 79.8 77.3 A 40 0.00000797 346.7 -25.5 210.9 -37.1 A 10 0.00157800 186.1 42.4 78.1 76.8 A 50 0.00000651 0.2 -23.4 226.2 -35.4 A 15 0.00107300 184.8 42 73.6 76.6 A 60 0.00000639 340.1 -17 204.3 -28.2 A 20 0.00065290 183.3 42.6 69.2 77.4 A 70 0.00000495 351.5 -36.9 215.7 -48.7 A 25 0.00037450 182.7 41.5 66.6 76.4 A 80 0.00000550 340.6 -23.4 204.3 -34.6 A 30 0.00021190 181.7 39.7 62.9 74.7 A 90 0.00000471 2.2 2.2 228.2 -9.8 A 40 0.00009124 183 37.1 65.8 72 s308 232 67.00000000 12 90 12 90 A 50 0.00003781 185.1 22.9 66.8 57.7 IDStep[mT] M[A/m] Dsp Isp Dge Ige k12908 224 50.00000000 12 90 12 90 A 0 0.00020130 340.4 -2.4 210.5 -24 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 5 0.00022120 349.4 -6.4 219.9 -29 A 0 0.00630400 187.3 40.9 76 79.6 A 10 0.00021290 351.8 -12.9 222.2 -35.6 A 5 0.00595500 190.6 39.8 84.2 77.4 A 15 0.00016800 352.3 -15.5 222.5 -38.3 A 10 0.00448700 189.6 40.1 81.9 78 A 20 0.00011010 350.4 -17.2 220 -39.8 A 15 0.00295900 187.2 40.6 74.9 79.3 A 23 0.00008103 349.9 -15.9 219.6 -38.5 A 20 0.00181100 184.8 41.5 67.3 80.9 A 26 0.00005998 347.4 -15.9 216.5 -38.2 A 25 0.00099230 182.8 37.6 54.3 77.4 A 29 0.00004244 347.2 -17.3 216.1 -39.6 A 30 0.00052950 180.6 36.9 46.1 76.9 A 32 0.00002962 346.3 -19.8 214.6 -42 A 40 0.00018460 179.7 28.6 43.3 68.6 A 35 0.00002014 344.2 -24.1 211 -46 A 50 0.00006093 183.5 14.4 49.8 54.3 A 40 0.00001462 347.7 -29.8 214.5 -52.1 k13008 -84 53.00000000 12 90 12 90 A 50 0.00000788 357.9 -15.7 229.4 -38.7 IDStep[mT] M[A/m] Dsp Isp Dge Ige s608 223 70.00000000 12 90 12 90 A 5 0.00135400 187 38.1 116.8 74.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 10 0.00115000 185.8 42.7 118.9 79 A 0 0.00017720 152.8 67.5 314.3 79.9 A 15 0.00066540 185.9 43.5 120.7 79.7 A 5 0.00009645 141.1 70.2 293.8 77 A 20 0.00036690 188.3 45.2 134.1 80.5 A 10 0.00003549 81.9 76.6 255.3 64.5 A 25 0.00018350 192.6 43 141 77 A 15 0.00001800 9.4 63.3 228.8 43.5 A 30 0.00009224 200.6 41.9 155.5 72.3 A 20 0.00001192 8.4 28.9 230.4 9.1 A 40 0.00003208 205.8 26.7 142.3 57.4 A 25 0.00001092 0.2 13.8 223.2 -6.2 A 50 0.00001963 194.9 16.7 119.5 51.9 A 30 0.00001172 353.2 -0.6 215.7 -20.5 A 60 0.00001863 184.1 7.6 101.7 44.5 A 40 0.00000992 358.6 -5.6 221.5 -25.6 k13208 205 58.00000000 12 90 12 90 s708 224 70.00000000 12 90 12 90 IDStep[mT] M[A/m] Dsp Isp Dge Ige IDStep[mT] M[A/m] Dsp Isp Dge Ige A 0 0.00286300 190.9 60.1 140.2 84 A 0 0.00012210 124.2 63.5 303.2 67.9 A 5 0.00274800 202.1 48 87.3 73.5 A 5 0.00007235 156.5 65.4 330.1 80.1 A 10 0.00201700 197.2 44.7 71 73 A 10 0.00003169 155.4 66.7 322.2 80.4 A 15 0.00131300 193.5 44.2 62 73.9 A 15 0.00001887 159.5 68.9 313 82.8 A 20 0.00082910 191.5 45.3 59 75.5 A 20 0.00001166 172.4 69.9 312.6 87.4 A 25 0.00045710 188.8 43.3 49.3 74.3 A 23 0.00000789 177.3 58 37.1 77.9 A 30 0.00027440 188.2 41.2 45.8 72.4 A 26 0.00000561 157.6 64.3 336.5 79.7 A 40 0.00010920 185.8 35.7 37.3 67.4 A 29 0.00000426 196.7 72.4 165.8 84.1 A 50 0.00004283 187 26.7 37 58.3 A 32 0.00000405 111.6 71 279.2 68.4 k13608 205 58.00000000 12 90 12 90 s00809 206 79.00000000 12 90 12 90 Appendix C, page 1 of 18 Appendix C

IDStep[mT] M[A/m] Dsp Isp Dge Ige A 100 0.00000436 357.9 15 195.7 -30 A 0 0.00005353 24 41.7 226.9 31.5 A 110 0.00000486 355.8 25.8 194 -19.1 A 5 0.00004676 22.6 3.8 228.7 -6.4 s1808 158 68.00000000 12 90 12 90 A 10 0.00003576 19.3 -10.9 226.4 -21.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 15 0.00002614 18.3 -15.3 225.6 -25.7 A 0 0.00010750 167.6 69.4 225 85.3 A 20 0.00001872 19.3 -16.4 226.8 -26.7 A 5 0.00004608 108.4 62.6 223.6 61.4 A 25 0.00001558 14 -17.8 221.2 -28.4 A 10 0.00001918 81.2 30.1 228 24.5 A 30 0.00001373 17.4 -17.7 224.9 -28.2 A 15 0.00001106 71.1 6 228.2 -1.4 A 40 0.00001089 15.1 -26.3 223 -36.9 A 20 0.00000888 66.4 -1.1 226.3 -9.7 A 50 0.00000955 14.4 -26.1 222.2 -36.7 A 25 0.00000725 64.7 -27.3 235.4 -34.6 A 60 0.00000927 13.6 -29.8 221.6 -40.4 A 30 0.00000796 63.8 -15.7 229.3 -24.2 A 70 0.00000659 20.3 -25.3 228.7 -35.5 s01809 204 80.00000000 12 90 12 90 A 80 0.00000497 38.3 -27.7 248.8 -36.1 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 90 0.00000639 6.1 -19.2 212.7 -30.1 A 0 0.00104200 346.5 -24.7 189.1 -34.4 s908 206 66.00000000 12 90 12 90 A 5 0.00115200 358.7 -28.7 202.5 -38.7 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 10 0.00081220 0 -29.2 204 -39.2 A 0 0.00007778 161.7 62.3 312.4 81.2 A 15 0.00049540 0.1 -27.6 204.1 -37.6 A 5 0.00005325 166.4 55.2 348.2 77.4 A 20 0.00028410 359.1 -28.8 203 -38.8 A 10 0.00003082 169.8 49.4 3.4 72.6 A 25 0.00017000 360 -27.2 204 -37.2 A 15 0.00001959 172.8 42.8 12.7 66.5 A 30 0.00010180 0.3 -30.6 204.3 -40.6 A 20 0.00001325 177.2 48.2 19.9 72.1 A 40 0.00004901 2.6 -34.3 207 -44.3 A 25 0.00001079 180.8 46.8 27.7 70.8 A 50 0.00003010 8.4 -41.2 214.1 -51.1 A 30 0.00000708 188 35.7 38.8 59.3 A 60 0.00001458 2.8 -48.9 207.6 -58.9 A 40 0.00000376 206.4 26.8 62 47.5 A 70 0.00001420 16.7 -52.5 225.8 -62 s01109 141 78.00000000 12 90 12 90 s1908 -48 31.00000000 12 90 12 90 IDStep[mT] M[A/m] Dsp Isp Dge Ige IDStep[mT] M[A/m] Dsp Isp Dge Ige A 0 0.00006162 204 51.9 353.9 62.5 A 0 0.01490000 161.4 36.8 16.4 73.5 A 5 0.00006348 216.9 56.8 13.3 65.4 A 5 0.01483000 162.9 36.7 15.5 74.7 A 10 0.00004142 219.2 53.9 14.2 62.3 A 10 0.01336000 162.6 36.7 15.8 74.5 A 15 0.00002971 228.1 49.6 22.2 56.6 A 15 0.01102000 162.4 36.5 16.6 74.4 A 20 0.00001905 232 51.2 27.4 57.4 A 20 0.00814800 161.2 36.4 17.9 73.5 A 25 0.00001213 225.8 52.6 21.2 59.9 A 25 0.00514100 160.1 34.2 25.9 73 A 30 0.00000632 206.8 62.4 4.5 72.3 A 30 0.00300900 158.4 34 26.9 71.6 A 40 0.00000239 70 43.8 201.4 38.7 A 40 0.00130500 156.9 33.1 29.8 70.3 A 50 0.00000531 39.3 -22.5 184.4 -31.5 A 50 0.00049860 154.6 28.2 42.8 67.8 A 60 0.00000689 55.6 -28.7 203 -34.9 s01909 223 82.00000000 12 90 12 90 A 70 0.00000538 44.9 -23.3 190.5 -31.5 IDStep[mT] M[A/m] Dsp Isp Dge Ige s1408 200 55.00000000 12 90 12 90 A 0 0.00164500 337.9 -34.8 198.4 -42.1 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 5 0.00141000 346.1 -32.3 207.6 -40 A 0 0.00012600 232.7 41.5 110.8 53.4 A 10 0.00090610 345.4 -30.4 207 -38.1 A 5 0.00005447 10.3 9.4 211.2 -25 A 15 0.00054310 345.6 -30.3 207.2 -38 A 10 0.00006557 9.7 -1.8 212 -36.2 A 20 0.00032670 344.8 -30.8 206.3 -38.5 A 15 0.00006181 8.7 -6.1 211.4 -40.6 A 25 0.00018830 345.3 -29.4 206.9 -37.1 A 20 0.00005873 7.8 -6.4 210.3 -41 A 30 0.00012210 345.5 -31 207 -38.7 A 23 0.00005550 6.7 -6.7 208.9 -41.4 A 40 0.00006778 347.6 -31.7 209.3 -39.5 A 26 0.00005315 6.6 -7.3 208.8 -42 A 50 0.00003946 351.9 -35.7 213.9 -43.6 A 29 0.00005071 6.9 -9.5 209.5 -44.2 A 60 0.00002308 348 -28.8 209.9 -36.6 A 32 0.00004803 5.1 -9.3 207 -44.1 A 70 0.00001694 351.3 -39.5 213.1 -47.4 A 35 0.00004480 8.5 -8.4 211.5 -42.9 s02009 231 84.00000000 12 90 12 90 A 40 0.00004322 6 -7.5 208 -42.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 50 0.00003466 5.4 -9.1 207.4 -43.9 A 0 0.00139600 338.3 -26.3 208 -31.9 A 60 0.00003084 7.7 -11.1 210.8 -45.7 A 5 0.00122500 339.9 -30.1 209.5 -35.7 A 70 0.00002796 3.7 -13.2 205.4 -48.1 A 10 0.00081480 338.4 -30.9 207.9 -36.5 A 80 0.00002311 5.4 -11.9 207.7 -46.7 A 15 0.00048240 339.3 -30.8 208.8 -36.4 A 90 0.00001948 7.3 -9.5 210.1 -44.1 A 20 0.00029660 337.4 -32.8 206.7 -38.3 A 100 0.00001672 6.4 -13.5 209.4 -48.2 A 25 0.00017430 338.9 -30.2 208.5 -35.8 A 110 0.00001657 9 -12.2 212.9 -46.6 A 30 0.00011400 338.8 -34.1 208.1 -39.7 s1608 198 45.00000000 12 90 12 90 A 40 0.00006328 339.4 -34.1 208.8 -39.7 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 50 0.00003136 342.7 -37 212.1 -42.7 A 0 0.00008263 152.8 85.4 201.2 49 A 60 0.00002247 331.6 -44.5 199.4 -49.7 A 5 0.00004744 17.5 53.7 208.4 9.8 A 70 0.00001616 341.1 -34.9 210.5 -40.6 A 10 0.00003829 11.3 25.5 208.8 -18.7 s02209 5 67.00000000 12 90 12 90 A 15 0.00003057 6.6 17.9 205 -26.8 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 20 0.00002482 9.9 13.4 209.2 -30.9 A 0 0.00032940 215.2 74.2 322.5 76.6 A 25 0.00002150 6.8 8.5 206.3 -36.2 A 5 0.00030070 214.2 74 321.9 76.9 A 30 0.00001501 5.7 5.2 205.4 -39.5 A 10 0.00024450 214.2 75.4 327.7 76.5 A 40 0.00001248 1.3 2.3 199.8 -42.7 A 15 0.00020230 211.9 77.4 336.3 76.1 A 50 0.00000856 17.6 20.7 215.8 -22.4 A 20 0.00017180 208.7 78.5 341.7 76 A 60 0.00000915 1.1 2.6 199.5 -42.4 A 25 0.00014710 206 79.7 346.7 75.6 A 70 0.00000731 23 2.7 227.7 -38.1 A 30 0.00012300 203.2 80.4 349.9 75.4 A 80 0.00000701 13.6 -2 217.5 -45.4 A 40 0.00008031 203.9 81.5 352.1 74.4 A 90 0.00000599 10.1 19.4 208.5 -24.9 A 50 0.00003986 202.9 82.3 354.2 73.8 Appendix C, page 1 of 18 Appendix C

A 60 0.00001589 219.1 77.8 335 74.5 A 50 0.00046220 196.5 48.1 342.9 70.1 A 70 0.00000412 226 56.6 271.3 66.6 s03509 18 68.00000000 12 90 12 90 A 80 0.00000260 239.5 15.4 252.3 25.8 IDStep[mT] M[A/m] Dsp Isp Dge Ige s2308 -38 73.00000000 12 90 12 90 A 0 0.00012150 227.3 56.9 283.8 66.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 5 0.00007149 221.5 49.7 267.1 62.7 A 0 0.01317000 132.6 74.8 21.8 77.1 A 10 0.00003144 219.1 30.7 249.8 46.3 A 5 0.01276000 126.2 78.7 3.9 76.3 A 15 0.00001719 216.6 -3.4 235.9 14.2 A 10 0.01110000 124.1 79.6 0.1 76 A 20 0.00001286 216.8 -26.5 230.8 -8.4 A 15 0.00790800 123.9 79.5 0.5 75.9 A 25 0.00001168 216.1 -41.6 226.6 -22.9 A 20 0.00545000 124.8 80.1 358 76.1 A 30 0.00000991 216.4 -55.9 222.5 -36.8 A 25 0.00283400 126.5 79.3 1.4 76.4 A 40 0.00000872 204.5 -63 212.7 -42.2 A 30 0.00163700 126.9 79 2.7 76.5 A 50 0.00000840 203.6 -68.1 210.7 -47.1 A 40 0.00061360 128.7 78.4 5.4 76.8 A 60 0.00000587 184 -78.7 199.4 -56.7 A 50 0.00022450 129.6 74.7 21.2 76.3 A 70 0.00000477 191.4 -79 202 -57.1 s02309 -2 62.00000000 12 90 12 90 A 80 0.00000386 230.1 -60.4 229.5 -43.4 IDStep[mT] M[A/m] Dsp Isp Dge Ige s03709 62 75.00000000 12 90 12 90 A 0 0.00026980 196 67.8 315.6 81.1 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 5 0.00024100 195.5 67 311.7 81.7 A 0 0.00013310 221.9 72.5 340.7 78.3 A 10 0.00018380 195.5 67.7 315.7 81.3 A 5 0.00008837 206.2 70.8 316.4 81.3 A 15 0.00014380 194.3 68.5 321.7 81.2 A 10 0.00003713 183.8 58.2 248.9 73.1 A 20 0.00012050 192.2 70.5 333.5 80.2 A 15 0.00001800 172.9 31 233.2 45.9 A 25 0.00009838 188.5 72 343.5 79.5 A 20 0.00001202 163.3 2.1 224.6 16.4 A 30 0.00008266 184.8 72.7 350.4 79.1 A 25 0.00001088 154.9 -22.9 218.7 -9.2 A 40 0.00005462 184.2 73.1 351.7 78.8 A 30 0.00001035 159.7 -40 224.8 -25.8 A 50 0.00002670 185 69.7 345.4 82 A 40 0.00000882 138.5 -56.9 211.4 -44.7 A 60 0.00001139 194.2 68.5 321.9 81.2 A 50 0.00000831 150.1 -58.8 220.5 -45.2 s02509 5 72.00000000 12 90 12 90 A 60 0.00000765 135.6 -66.4 213.4 -54.2 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 70 0.00000735 121.5 -59.5 199.9 -49.8 A 0 0.00028470 219.7 58.5 255.4 69.3 A 80 0.00000642 129.1 -76.7 217.5 -64.5 A 5 0.00024610 219.1 57.3 252.9 68.4 s04809 30 78.00000000 12 90 12 90 A 10 0.00020020 219.8 62.7 263.4 72.6 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 15 0.00016720 218.1 68.1 276.9 76.7 A 0 0.00008158 181.2 -55 210.9 -43 A 20 0.00014450 218.8 72.3 294.9 78.3 A 5 0.00010370 177.9 -62.5 208.5 -50.5 A 25 0.00012110 216.1 75.1 308.7 79.5 A 10 0.00010910 176.6 -64.3 207.6 -52.3 A 30 0.00010020 214.6 76.6 317.2 79.8 A 15 0.00010190 175.4 -64.9 206.8 -52.9 A 40 0.00006449 216.9 78 324.1 79 A 20 0.00008791 173.8 -65.2 205.7 -53.2 A 50 0.00003230 208 76.7 319.9 81.2 A 25 0.00007218 172.3 -65.5 204.6 -53.6 A 60 0.00001203 204.3 74.4 305.2 82.6 A 30 0.00005549 172 -65.5 204.4 -53.6 A 70 0.00000406 220.8 39.8 239.7 52 A 40 0.00003419 171 -66.3 203.8 -54.4 s02609 7 70.00000000 12 90 12 90 A 50 0.00002026 169.4 -67.3 202.8 -55.4 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 60 0.00001218 171.9 -69.8 204.8 -57.9 A 0 0.00032510 209.5 73.1 309 80.3 A 70 0.00000767 165.6 -70.7 200.8 -58.9 A 5 0.00030140 208.5 73.5 311.6 80.5 A 80 0.00000563 163.8 -70.1 199.6 -58.4 A 10 0.00023310 207.9 74.6 318.3 80.5 s04909 30 83.00000000 12 90 12 90 A 15 0.00018790 205.3 76.6 330.9 80.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 20 0.00015770 202.9 78.9 343.1 79.3 A 0 0.00005960 192.5 0.6 222.6 7.4 A 25 0.00012890 198.6 80.5 351.5 78.6 A 5 0.00005856 193.1 -5.1 223.1 1.7 A 30 0.00010800 193.4 81.5 357.4 78.1 A 10 0.00006116 194.3 -19.8 223.8 -13 A 40 0.00007010 190.4 83.1 1.6 76.7 A 15 0.00006866 194.8 -35.7 223.7 -28.9 A 50 0.00003256 201.1 82.3 354.7 76.9 A 20 0.00007402 194.8 -45.5 223.3 -38.7 A 60 0.00001262 187.3 79.9 359.7 79.9 A 25 0.00007166 193.8 -51.1 222.1 -44.3 s2808 133 55.00000000 12 90 12 90 A 30 0.00006604 193.1 -53.9 221.3 -47.1 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 40 0.00005117 191.2 -57 219.5 -50.1 A 0 0.01468000 206.2 49.4 34.5 73.1 A 50 0.00003433 189.6 -58.8 218 -51.9 A 5 0.01393000 205.1 48.3 30 73.2 A 60 0.00002180 189.2 -61.3 217.6 -54.4 A 10 0.01239000 204.6 48.3 29.4 73.4 A 70 0.00001336 186.5 -61.4 215.3 -54.4 A 15 0.00987400 203.4 48.8 29.3 74.4 A 80 0.00000857 189.2 -62.9 217.5 -56 A 20 0.00691300 202.3 49.6 30.5 75.4 A 90 0.00000532 181 -69.3 210.8 -62.3 A 25 0.00425700 199.7 47.9 21 75.9 s05409 -20 79.00000000 12 90 12 90 A 30 0.00251200 198.6 50.6 29.2 78 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 40 0.00103400 196.1 51.8 31.2 79.9 A 0 0.00004164 220 -7.2 199.6 1.3 A 50 0.00038650 194 48.8 13 79.4 A 5 0.00004912 223.5 -31.2 199.8 -23 s3008 129 66.00000000 12 90 12 90 A 10 0.00005579 229 -42.6 202.6 -34.9 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 15 0.00005999 232 -49.2 203.7 -41.8 A 0 0.01532000 207.4 47.6 0.5 66.7 A 20 0.00005927 233.5 -52.5 204 -45.2 A 5 0.01456000 206.4 47 358.3 66.4 A 25 0.00005519 233.7 -54.5 203.5 -47.2 A 10 0.01270000 206.3 46.7 357.8 66.2 A 30 0.00004914 234.7 -56.2 203.8 -49 A 15 0.01040000 205.3 47.3 357 67 A 40 0.00003786 234.6 -57.9 203 -50.6 A 20 0.00761500 204.5 48.9 357.6 68.7 A 50 0.00002544 235.9 -58.5 203.9 -51.4 A 25 0.00482000 202.4 48.5 353.7 69 A 60 0.00001601 236.3 -58.7 204.1 -51.6 A 30 0.00291300 201.1 49.4 352.6 70.1 A 70 0.00000981 240.6 -62.9 205.5 -56.2 A 40 0.00118800 199 50.2 349.9 71.4 A 80 0.00000631 243.5 -66.1 205.9 -59.7 Appendix C, page 1 of 18 Appendix C

A 90 0.00000402 245.5 -69.1 205.1 -62.7 IDStep[mT] M[A/m] Dsp Isp Dge Ige s05609 21 76.00000000 12 90 12 90 A 0 0.00113800 357.3 -34.2 206.9 -44.2 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 5 0.00116800 3.6 -30.7 214.1 -40.7 A 0 0.00003695 183.3 -59.4 203.4 -45.4 A 10 0.00075380 1.4 -28.7 211.6 -38.7 A 5 0.00003553 185.6 -58.9 205.1 -44.9 A 15 0.00042540 359.6 -28.2 209.6 -38.2 A 10 0.00003606 188.3 -60 207 -46.1 A 20 0.00024430 357.9 -29.5 207.6 -39.5 A 15 0.00003614 189.9 -61.7 208 -47.8 A 25 0.00013890 358.3 -29.5 208.1 -39.5 A 20 0.00003457 189.9 -62.9 207.9 -49 A 30 0.00009363 356.3 -28 205.9 -38 A 25 0.00003140 189.7 -63.5 207.7 -49.6 A 40 0.00005171 355 -26.5 204.4 -36.5 A 30 0.00002767 189.1 -64.4 207.2 -50.5 A 50 0.00003093 2.1 -26.5 212.3 -36.5 A 40 0.00002030 187.2 -65.5 205.8 -51.6 A 60 0.00002276 3.2 -32.6 213.7 -42.6 A 50 0.00001269 185.8 -66.2 204.8 -52.2 A 70 0.00001517 352.2 -14.9 201.7 -24.8 A 60 0.00000767 185.9 -65.8 204.9 -51.8 s3009 22 70.00000000 12 90 12 90 A 70 0.00000437 175.5 -67.7 198.1 -53.7 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 80 0.00000296 181.5 -73.9 201.8 -59.9 A 0 0.00018230 232.5 48.8 279.1 57.6 A 90 0.00000158 175.4 -69.2 198.1 -55.2 A 10 0.00005522 230.5 38.3 269 48.9 s07909 -18 75.00000000 12 90 12 90 A 20 0.00001922 229.8 33.9 265.7 45 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00000770 236.9 22.2 268 31.9 A 0 0.00004977 255.2 -58.3 217.4 -51.9 A 40 0.00000316 226.5 -14.7 246.6 -0.6 A 5 0.00004970 256.2 -55.9 219.8 -49.9 A 45 0.00000439 212.4 -22.3 231.9 -5.1 A 10 0.00005627 252.9 -55.8 217.2 -49.1 A 50 0.00000412 165.8 -57.5 192.4 -37.9 A 15 0.00005761 252.1 -58.3 215 -51.3 A 55 0.00000199 175 -50.3 198.3 -30.4 A 20 0.00005447 251.8 -60.4 213.4 -53.1 A 60 0.00000319 238.9 -54 243.8 -41 A 25 0.00004853 252.2 -61.8 212.7 -54.5 A 65 0.00000356 180.8 -42.8 202.6 -22.8 A 30 0.00004183 250.8 -63 210.8 -55.3 A 70 0.00000324 262.3 -80.3 227 -66.7 A 40 0.00002929 252.6 -64.4 211 -56.9 s3209 40 73.00000000 12 90 12 90 A 50 0.00001865 251.3 -66.4 208.4 -58.4 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 60 0.00001164 251.3 -67.6 207.3 -59.5 A 0 0.00013420 153.3 63.6 160.6 76.6 A 70 0.00000708 252.1 -69 206.4 -60.8 A 10 0.00003293 153.9 39.4 184.6 54.1 A 80 0.00000467 272.7 -75.2 208.9 -69.6 A 20 0.00001238 156 -6.9 195.9 8.6 s08009 -34 73.00000000 12 90 12 90 A 30 0.00000796 151.1 -37.1 195.5 -21.9 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 40 0.00000709 153.8 -51.3 200.2 -35.6 A 0 0.00011300 266.3 -50.5 213.4 -46.5 A 45 0.00000727 164.5 -67.5 210.7 -50.9 A 5 0.00011750 269.8 -53.9 214 -50.5 A 50 0.00000650 170.4 -67.9 214.3 -51 A 10 0.00012130 270.5 -56 213 -52.6 A 55 0.00000623 87.7 -79.1 186 -70.3 A 15 0.00012010 270.6 -57.7 211.7 -54.1 A 60 0.00000358 144.6 -63.5 197 -48.5 A 20 0.00011420 271.3 -58.9 211.2 -55.3 A 65 0.00000485 132.8 -69.6 192.9 -55.8 A 25 0.00010410 271.4 -60 210.2 -56.3 A 70 0.00000268 66.3 -69.2 152.8 -69.3 A 30 0.00009068 272.5 -60.7 210.4 -57.2 s3309 50 76.00000000 12 90 12 90 A 40 0.00006830 273.7 -61.4 210.6 -58.1 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 50 0.00004492 276.3 -63.1 210.6 -60.2 A 0 0.00011510 154.6 46.8 195.3 59 A 60 0.00002870 276.3 -63.8 209.8 -60.7 A 10 0.00004441 154.1 11.2 202.1 23.7 A 70 0.00001777 276.8 -64.5 209.3 -61.4 A 20 0.00002869 156 -28.1 208.2 -15.2 A 80 0.00001120 277.3 -70.2 201.2 -65.8 A 30 0.00002069 156.3 -41.9 210 -28.9 A 90 0.00000721 276.9 -68 204.5 -64.1 A 40 0.00001663 155.3 -47.5 210 -34.5 s21009 222 82.00000000 12 90 12 90 A 45 0.00001416 159.3 -50 213.5 -36.7 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 50 0.00001233 162.8 -53.1 216.7 -39.6 A 0 0.00105200 351.9 -35.9 212.9 -43.8 A 55 0.00001126 168.7 -60.3 221.9 -46.5 A 5 0.00101100 352 -32.1 213.1 -40 A 60 0.00000870 155.6 -61.9 212.8 -48.8 A 10 0.00068340 349.8 -32.8 210.7 -40.7 A 65 0.00000762 137.6 -56.8 198.2 -45.6 A 15 0.00044110 350.3 -32.1 211.3 -40 A 70 0.00000804 166.4 -58.1 220 -44.4 A 20 0.00027740 349.6 -32.9 210.5 -40.8 s3809 42 67.00000000 12 90 12 90 A 25 0.00017470 349 -32.5 209.8 -40.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00011750 349 -33.8 209.8 -41.6 A 0 0.00011780 196.8 59.2 274 79.2 A 40 0.00006916 351.9 -33.9 213 -41.8 A 5 0.00008407 194.3 54.5 257.7 75.8 A 50 0.00004169 353.7 -34.1 215 -42 A 10 0.00004406 188.8 43.2 237.7 65.7 A 60 0.00002635 358.1 -39.5 219.8 -47.5 A 15 0.00002394 186.9 17.1 230.6 39.9 A 70 0.00002087 3.1 -34.3 225.5 -42.3 A 20 0.00001652 182.3 0.6 224.5 23.6 s21209 210 81.00000000 12 90 12 90 A 25 0.00001369 177.5 -23.3 219.7 -0.3 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 30 0.00001101 176.7 -27.3 219.1 -4.3 A 0 0.00150900 344.8 -27.9 193.2 -36.6 A 35 0.00001080 172.3 -38.6 215.8 -15.8 A 5 0.00130400 354.4 -29.3 203.8 -38.3 A 40 0.00000920 161.4 -49.4 208.5 -27.3 A 10 0.00084010 354.3 -29.4 203.7 -38.4 A 45 0.00000868 181.3 -55.1 222.9 -32.1 A 15 0.00046540 354 -28.8 203.3 -37.7 A 50 0.00000808 172.9 -56.4 217.3 -33.5 A 20 0.00025750 352.2 -29.4 201.3 -38.3 A 55 0.00000811 163.6 -60.7 211.9 -38.3 A 25 0.00014300 352.2 -30.3 201.3 -39.2 A 60 0.00000670 165.9 -60 213.2 -37.4 A 30 0.00009345 352 -30.3 201.1 -39.2 A 65 0.00000549 149.4 -61.9 203.5 -40.8 A 40 0.00005031 358.7 -28.4 208.6 -37.4 A 70 0.00000520 181.3 -57.9 222.8 -34.9 A 50 0.00002404 6.7 -25.4 217.3 -34.3 s4009 16 67.00000000 12 90 12 90 A 60 0.00001551 5.9 -26.5 216.5 -35.4 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 70 0.00001171 30.2 -25.2 242.8 -32.9 A 0 0.00012440 148.1 53.1 132.3 69.3 s21309 210 80.00000000 12 90 12 90 A 10 0.00004877 154.6 32.6 159.6 52.5 Appendix C, page 1 of 18 Appendix C

A 20 0.00001874 158.8 0.8 173 22.2 A 30 0.00001137 167 -26.3 184.3 -3.8 A 40 0.00000767 167 -36.9 185.3 -14.4 A 45 0.00000622 184.5 -44.8 199.4 -21.9 A 50 0.00000566 183.8 -55.8 198.5 -32.8 A 55 0.00000381 165.1 -62 187 -39.5 A 60 0.00000363 191.5 -74.3 201 -51.5 A 65 0.00000390 216.7 -77.7 209.3 -56.4 A 70 0.00000356 348.1 -76.7 211.3 -79.7 s4109 28 73.00000000 12 90 12 90 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 0 0.00015710 201.3 69 278.4 82.1 A 10 0.00007229 199.7 62.2 252.3 77 A 20 0.00002646 198.4 43.4 234.6 59.2 A 30 0.00001356 200.2 25.5 232.5 41.3 A 40 0.00000710 203.4 12 234 27.5 A 50 0.00000522 203.8 -24.8 229.8 -9.1 A 55 0.00000483 167.6 -25.8 196.7 -9.2 A 60 0.00000308 207 -62.7 225.7 -46.9 A 65 0.00000256 173.1 -79.3 205.2 -62.3 A 70 0.00000231 110.1 -42.6 150.5 -35 A 75 0.00000271 154.3 -41 186.8 -25.4 A 80 0.00000260 98.2 -66.7 157.5 -59.5 s4209 13 72.00000000 12 90 12 90 IDStep[mT] M[A/m] Dsp Isp Dge Ige A 0 0.00013350 180.2 70 195 88 A 10 0.00004988 184.4 54.2 201.4 72.1 A 20 0.00001687 191 4.5 204.9 22.1 A 30 0.00001201 198.4 -30 209.3 -12.8 A 40 0.00000876 189.8 -49.2 200.5 -31.4 A 50 0.00000730 198.5 -60.4 205.4 -43 A 55 0.00000528 197.7 -60.4 204.8 -43 A 60 0.00000619 195.5 -70.5 201.5 -52.9 A 65 0.00000488 178.7 -68.8 192.3 -50.8 A 70 0.00000506 190.5 -56.5 200.4 -38.7 A 75 0.00000388 152.8 -74.4 179.8 -57.4

Appendix C, page 1 of 18 Appendix D

S57.09 A10.09 parametervalue unit parameter value unit Ms 7.67E-02 Am2 Ms 9.66E-06 Am2 Mr 1.03E-02 Am2 Mr 1.21E-06 Am2 Hc 1.15E-02 T Hc 5.67E-03 T Mr/Ms ratio3.78E-02 Mr/Ms ratio 7.63E-02 Hcr3.03E+01 mT Hcr 1.16E+01 mT

S13.08 A56.09 parametervalue unit parameter value unit Ms 6.09E-01 Am2 Ms 8.29E-06 Am2 Mr 2.96E-02 Am2 Mr 8.38E-07 Am2 Hc 4.72E-03 T Hc 4.41E-03 T Mr/Ms ratio2.15E-02 Mr/Ms ratio 4.80E-02 Hcr1.56E+01 mT Hcr 9.98E+00 mT

S20.09 B20.09 parametervalue unit parameter value unit Ms 1.10E+00 Am2 Ms 1.29E-05 Am2 Mr 1.52E-01 Am2 Mr 1.37E-06 Am2 Hc 8.54E-03 T Hc 5.40E-03 T Mr/Ms ratio3.56E-02 Mr/Ms ratio 4.59E-02 Hcr1.59E+01 mT Hcr 1.14E+01 mT

S24.09 B4.09 parametervalue unit parameter value unit Ms 5.39E-01 Am2 Ms 3.60E-05 Am2 Mr 4.71E-02 Am2 Mr 3.59E-06 Am2 Hc 5.99E-03 T Hc 4.11E-03 T Mr/Ms ratio2.54E-02 Mr/Ms ratio 7.22E-02 Hcr1.65E+01 mT Hcr 8.22E+00 mT

S52.09 B26.09 parametervalue unit parameter value unit Ms 4.66E-06 Am2 Ms 2.47E-05 Am2 Mr 4.18E-07 Am2 Mr 5.64E-06 Am2 Hc 8.52E-03 T Hc 1.66E-02 T Mr/Ms ratio2.03E-02 Mr/Ms ratio 7.55E-02 Hcr2.66E+01 mT Hcr 2.93E+01 mT

A70.09 D36.09 parametervalue unit parameter value unit Ms 1.31E-05 Am2 Ms 3.24E-05 Am2 Mr 1.49E-06 Am2 Mr 1.78E-06 Am2 Hc 7.27E-03 T Hc 2.86E-03 T Mr/Ms ratio3.95E-02 Mr/Ms ratio 2.15E-02 Hcr1.68E+01 mT Hcr 9.07E+00 mT

A15.09 D17.09 parametervalue unit parameter value unit Ms 0 Am2 Ms 1.14E-05 Am2 Mr 0 Am2 Mr 2.94E-06 Am2 Hc 0.01 T Hc 1.90E-02 T Mr/Ms ratio0.1 Mr/Ms ratio 1.11E-01 Hcr12.02 mT Hcr 2.99E+01 mT

Appendix D, page 1 of 2 Appendix D

E53.09 F95.08 parametervalue unit parameter value unit Ms 4.16E-05 Am2 Ms 3.13E-05 Am2 Mr 3.27E-06 Am2 Mr 7.62E-06 Am2 Hc 4.18E-03 T Hc 1.96E-02 T Mr/Ms ratio4.73E-02 Mr/Ms ratio 9.06E-02 Hcr1.07E+01 mT Hcr 3.23E+01 mT

E33.09 S25.08 parametervalue unit parameter value unit Ms 1.87E-05 Am2 Ms 2.66E-05 Am2 Mr 1.43E-06 Am2 Mr 5.63E-06 Am2 Hc 3.74E-03 T Hc 1.52E-02 T Mr/Ms ratio5.40E-02 Mr/Ms ratio 9.81E-02 Hcr8.51E+00 mT Hcr 2.42E+01 mT

E78.09 parameter value unit Ms 2.09E-05 Am2 Mr 1.56E-06 Am2 Hc 4.17E-03 T Mr/Ms ratio 5.35E-02 Hcr 1.13E+01 mT

E67.09 parameter value unit Ms 8.10E-06 Am2 Mr 1.05E-06 Am2 Hc 3.97E-03 T Mr/Ms ratio 4.26E-02 Hcr 8.58E+00 mT

K31.08 parameter value unit Ms 1.30E-05 Am2 Mr 1.03E-06 Am2 Hc 4.27E-03 T Mr/Ms ratio 4.96E-02 Hcr 1.04E+01 mT

K24.08 parameter value unit Ms 6.76E-06 Am2 Mr 1.34E-06 Am2 Hc 9.29E-03 T Mr/Ms ratio 4.16E-02 Hcr 1.75E+01 mT

K2.08 parameter value unit Ms 1.92E-05 Am2 Mr 1.96E-06 Am2 Hc 5.11E-03 T Mr/Ms ratio 5.58E-02 Hcr 1.18E+01 mT

Appendix D, page 2 of 2