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The DRS bands for the studied hematite particles are dominantly controlled by Al substitution.
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In most of the studied profiles, hematite is the dominant magnetic carrier, as indicated by unblocking temperatures that exceed 580°C for about 20 60% of the natural remanent magnetization (NRM).
Magnetic mineral assemblages in the studied samples contain both antiferromagnetic (hematite and goethite) and ferrimagnetic (magnetite and maghemite) minerals with broad grain size distributions, which indicates multiple origins for these iron oxides.
We interpret this characteristic component as carried by a mixture of both magnetite and hematite as part of the detrital fraction of the studied sediments.
The data obtained on fluid inclusions from pyrargyrite and hematite crystals have been integrated by complementary information from X-ray fluorescence analysis using synchrotron radiation (μ-SXRF) under conditions specifically designed for the study of opaque ore minerals.
In addition to the single-stranded DNA damage observed in this study, hematite ENPs also reduced cellular viability in H9T3 cells by 14%; however, only 10 μg/mL elicited reductions that were statistically relevant.
Kinetic parameters were determined for the reactions hematite to magnetite, magnetite to wuestite and wuestite to iron from experimental data.
We apply EIS for studying the interaction between the photosensitizing protein (PC) and hematite using different coating procedures under dark and illuminated conditions using PBS as electrolyte.
The influence of magnetic field intensity, roll speed and feed rate was analyzed for the separation of hematite minerals.
Therefore, P 545 nm and P 535 nm are good indicators for the origin of hematite.
For the formation of hematite with oxygen vacancies, an in situ carbon-thermic process was employed.
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