Mineralogical, Rock-Magnetic and Palaeomagnetic Properties of Metadolerites from Central Western Svalbard
Abstract
:1. Introduction
2. Geological Setting
3. Fieldwork and Methods
3.1. Fieldwork
3.2. Petrographic and Mineralogical Methods
3.3. Ferromagnetic Minerals Separation
3.4. Rock-Magnetic, Anisotropy of Magnetic Susceptibility (AMS) and Palaeomagnetic Methods
3.4.1. Rock-Magnetic Procedures
- Vibrating Sample Magnetometer (VSM)The hysteresis parameters including Mrs—saturation magnetization, Mr—saturation remanence, Hc—coercivity, Hcr—remanent coercivity, were determined using precise PMC MicroMag 2900 Series AGM Vibrating Sample Magnetometer (VSM) in maximum field 1 T. Hysteresis loops have been measured for the small particles of “whole rock” samples (up to 0.02 g) as well as the separated magnetic grains. All results were normalized against the mass of the samples.
- Temperature dependence of magnetic susceptibility (κ(T))The maximum unblocking temperatures (Tub max) were estimated from the temperature dependence of magnetic susceptibility κ (T measurements). The experiments were conducted on the MFKA1-FA Kappabridge using the high-temperature CS-3 furnace. Analyses were performed on “whole-rock” powder samples representing each of the palaeomagnetic sites. The κ(T) was monitored during continuous heating in air up to 700 °C and during cooling to room temperature.
- Three component IRM (isothermal remanent magnetization) acquisition curve experiment [41]These procedures produced more detailed information about the ferromagnetic composition. It was possible to observe the contribution of low, medium and high coercivity minerals in the magnetic signal and identify them on the basis of their maximum unblocking temperatures (Tub max). Initially 12 selected cylindrical samples (2 from each of the sites) were magnetized in steps along the z-axis reaching 3 T. To magnetize the samples a MMPM-10 pulse magnetizer was used. After each level of magnetization, the IRM was measured using the Superconducting Quantum Interface Device (SQUID DC, model 755, 2G Enterprise Inc., Sand City, CA, USA) and then plotted on the diagram. In the next step the samples were magnetized along the other perpendicular axis: along the y-axis in 0.4 T and along the x-axis in 0.12 T, respectively. After magnetization, the samples were gradually thermally demagnetized in the MMTD1 magnetic furnace and measured on the SQUID at every temperature step to determine the decrease of magnetic signal.
3.4.2. Palaeomagnetic Procedures
3.4.3. Statistical Procedures and Software
4. Results
4.1. Petrography of Investigated Metadolerites
4.2. Identification of Ferromagnetic Minerals
4.2.1. Mineralogical Methods
4.2.2. Rock-Magnetic Experiments
4.3. Palaeomagnetic Results
- (1)
- A low temperature component (index L) which demagnetized below 250 °C, was calculated using the “free line fit” method of Butler [46]. This was characterized by a steep inclination that was probably influenced by the present-day magnetic field.
- (2)
- A medium temperature component (index M) which demagnetized in the 250–350 °C range of temperatures and calculated using the “free line fit” or the “anchored line fit” methods of Butler [46], was potentially related to pyrrhotite and/or magnetite/maghemite grains of relatively low-Tub, that were identified during the petrological and rock-magnetic experiments.
- (3)
- A high temperature component (index H) which demagnetized above 350 °C and up to 500 °C (before disturbance of the NRM pattern). That component was also calculated using the “free line fit” or the “anchored line fit” methods [46] and is potentially related to magnetite and/or maghemite grains with higher a Tub spectra than was the case for the M component.
5. Discussion
6. Conclusions
- (1)
- The results of rock-magnetic and petrological analyses, including experiments on ferromagnetic separates, reveal a dominance of metamorphic pyrrhotite and Fe-oxides carriers in the metadolerites of SW OIIL and show complete remineralization and reorganization of their ferromagnetic fabric during Caledonian sensu lato metamorphism and younger tectono-thermal events.
- (2)
- Field data together with an analysis of satellite images (available from the NPI Kart over Svalbard) have highlighted the presence previously unreported deformational features such as large and small-scale folding and the presence of high strain (shear) zones in the Daudmannsdalen, Daudmannsøyra, Protectorbreen sites. All of these features have the potential to influence the orientation of the palaeomagnetic signal carriers.
- (3)
- The results of the palaeomagnetic investigations are as follows:
- In five of the six sites the low temperature components (Tub < 250 °C) are characterised by high inclinations (~70°–80°) and are related to Mesozoic–Cenozoic remagnetization, probably influenced by the recent magnetic field.
- In four of the six sites the middle-high temperature components (Tub > 250 °C) were scattered and thus rejected for further consideration. Only from two sites did the middle-high temperature directions qualify. Palaeopoles calculated for these two sites are shifted from combined reference Laurussia–Baltica–Laurentia APWP. At this stage of the study it is not possible to precisely define origin of observed inconsistency. Potentially the shift of the qualified DAU2MH+, DAU4MH+ VGPs from the reference path can be related to L. Mesozoic–Cenozoic listric faulting of the Caledonian basement, postulated in the area of OIIL by Michalski et al. [14]. Additional rotations could be generated by localised shearing and the cumulative effects of localised west-dipping families of small scale faults which were observed in the sampling area.
- (4)
- Finally, it is evident, that to better understand the relationships between the preservation of the palaeomagnetic record and the succession of deformation events recorded in the Caledonian basement of Western Svalbard, further studies are required.
Author Contributions
Funding
Acknowledgments
Conflicts of Interest
Appendix A. Anisotropy of Magnetic Susceptibility
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No. | Samples | Description | Ms (A m2/kg) | Mr (A m2/kg) | Hc (mT) | Hcr (mT) | Mr/Ms | Hcr/Hc |
---|---|---|---|---|---|---|---|---|
1 | Dau0113 | “whole-rock”–metadolerites | 4.09 × 10−3 | 4.55 × 10−4 | 4.02 | 8.34 | 0.11 | 2.07 |
2 | Dau1404 | 1.66 × 10−2 | 8.09 × 10−4 | 3.25 | 8.03 | 0.05 | 2.47 | |
3 | Dau2204 | 3.39 × 10−3 | 3.47 × 10−4 | 13.39 | 29.48 | 0.10 | 2.20 | |
4 | Dau4307 | 5.21 × 10−3 | 4.00 × 10−4 | 3.97 | 9.25 | 0.08 | 2.33 | |
5 | Dau5407 | 2.29 × 10−2 | 6.52 × 10−3 | 2.22 | 7.66 | 0.29 | 3.45 | |
6 | Pro6208 | 3.33 × 10−3 | 4.45 × 10−4 | 7.81 | 35.50 | 0.13 | 4.55 | |
7 | Dau14-63-Po | metadolerite-pyrrhotite 1 | 4.61 × 10−1 | 8.26 × 10−2 | 6.42 | 11.41 | 0.18 | 1.78 |
8 | metadolerite-pyrrhotite 2 | 1.46 × 10−1 | 5.23 × 10−2 | 8.41 | 9.79 | 0.36 | 1.16 | |
9 | metadolerite-pyrrhotite 3 | 2.99 × 10−2 | 9.94 × 10−3 | 6.66 | 9.57 | 0.33 | 1.44 | |
10 | Dau14-63-Py | metadolerite-pyrite 1 | 3.78 × 10−2 | 1.14 × 10−2 | 12.93 | 16.01 | 0.30 | 1.24 |
11 | metadolerite-pyrite 2 | 3.86 × 10−1 | 1.43 × 10−1 | 11.10 | 12.90 | 0.37 | 1.16 |
Site | Site GPS Location | Components | D (°) | I (°) | S/s | N/n | α95 | κ |
---|---|---|---|---|---|---|---|---|
DAU1 | N78°12’32.8 E13°40’24.9 | DAU1L | 42.7 | 85.3 | 6/22 | 4/9 | 4.7 | 120.7 |
DAU2 | N78°12’33.1 E13°40’38.9 | DAU2AFL | 348.4 | 74.5 | 5/5 | 4/4 | 31.0 | 9.73 |
DAU2L | 234.6 | 84.4 | 6/18 | 5/12 | 8.1 | 29.64 | ||
DAU2MH+ | 60.9 | −69.2 | 6/18 | 5/11 | 8.6 | 28.84 | ||
DAU3 | N78°12’33.3 E13°40’48.3 | DAU3L | 310 | 86.5 | 6/18 | 5/8 | 8.5 | 43.21 |
DAU3M+ | 85.8 | −16.8 | 6/18 | 4/9 | 27.0 | 4.58 | ||
DAU4 | N78°12’5.7 E13°41’20.9 | DAU4L | 352.6 | 83.5 | 6/18 | 5/13 | 8.2 | 26.25 |
DAU4MH+ | 94.2 | −25.8 | 6/18 | 5/11 | 16.5 | 8.63 | ||
DAU5 | N78°11’52.4 E13°40’04.1 | DAU5L | 41.3 | 71.2 | 6/18 | 5/10 | 6.7 | 52.65 |
DAU5AFL | 30.7 | 81.3 | 6/7 | 4/4 | 84.5 | 2.17 | ||
DAU5MH+ | 59.2 | −53.2 | 6/18 | 6/12 | 33.2 | 2.67 | ||
PRO6 | N78°13’56.8 E13°41’42.6 | PRO6L | 108.8 | 29.3 | 6/18 | 4/5 | 40.4 | 4.53 |
PRO6H | 114.2 | −13.0 | 6/18 | 4/5 | 37.1 | 5.21 |
VGP Symbol | N | n | P | D (°) | I (°) | α 95 | κ | Φ (°) N | Λ (°) E | Dp/Dm (°) | Plat (°) |
---|---|---|---|---|---|---|---|---|---|---|---|
DAU1L | 4 | 9 | N | 42.7 | 85.3 | 4.7 | 120.7 | 81.88 | 64.68 | 9.2/9.3 | 80.7 |
DAU2L | 5 | 12 | N | 234.6 | 84.4 | 8.1 | 29.64 | 69.50 | 346.89 | 15.8/16.0 | 78.9 |
DAU2MH+ | 5 | 11 | R | 60.9 | −69.2 | 8.6 | 28.84 | −45.86 | 144.12 | 12.5/14.7 | 52.8 |
DAU3L | 5 | 8 | N | 310 | 86.5 | 8.5 | 43.21 | 80.80 | 337.92 | 16.8/16.9 | 83.0 |
DAU4L | 5 | 13 | N | 352.6 | 83.5 | 8.2 | 26.25 | 88.20 | 259.41 | 15.8/16.1 | 77.2 |
DAU4MH+ | 5 | 11 | R | 94.2 | −25.8 | 16.5 | 8.63 | −14.16 | 102.27 | 9.6/17.8 | 13.6 |
DAU5L | 5 | 10 | N | 41.3 | 71.2 | 6.7 | 52.65 | 63.69 | 136.55 | 10.2/11.7 | 55.8 |
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Burzyński, M.; Michalski, K.; Manby, G.; Nejbert, K. Mineralogical, Rock-Magnetic and Palaeomagnetic Properties of Metadolerites from Central Western Svalbard. Minerals 2018, 8, 279. https://doi.org/10.3390/min8070279
Burzyński M, Michalski K, Manby G, Nejbert K. Mineralogical, Rock-Magnetic and Palaeomagnetic Properties of Metadolerites from Central Western Svalbard. Minerals. 2018; 8(7):279. https://doi.org/10.3390/min8070279
Chicago/Turabian StyleBurzyński, Mariusz, Krzysztof Michalski, Geoffrey Manby, and Krzysztof Nejbert. 2018. "Mineralogical, Rock-Magnetic and Palaeomagnetic Properties of Metadolerites from Central Western Svalbard" Minerals 8, no. 7: 279. https://doi.org/10.3390/min8070279