Applied Mineral Exploration
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Rapid fluid inclusion data
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The discovery of valuable mineral deposits is a long process, taking into account many aspects including: the structure of the geology, the grade of the ore, mineral processing procedures, the ongoing costs of operation, environmental impacts, plus predictions of future metal prices. Mining feasibility studies are long and costly and can be limited by a lack of geochemical, geophysical, geological and remote sensing exploration techniques available for a given location (Bateman and Jensen 1981). The use of decrepitation techniques to derive information from fluid inclusions in the mineral samples can help to assess suitable locations for mining exploration, improving the economic viability of the venture and potentially minimizing environmental disturbance ( Bateman and Jensen 1981, Craig and Vaughan 1981, Pomārleanu & Mārza 2002)
The study of fluid inclusions can provide valuable data on the nature of the ore fluid (Peach 1949, Roedder & Bodnar 1980, Edwards & Atkinson 1986, Burlinson 2006, 2007a, 2007b). Parameters that can be obtained include the temperature of formation, salinity and chemical composition of the mineral fluid. Upon reheating, the process that forms the fluid inclusions is reversed; this is utilized in the decrepitation study of inclusions (Edwards & Atkinson 1986).
Fluid inclusions are small to microscopic quantities of liquid that are trapped within a mineral as it crystallises (Peach 1949, Roedder & Bodnar 1980).Although the inclusions are usually homogeneous when trapped, once cooled to ambient temperature, they tend to separate into a multiphase inclusion, most commonly vapor and liquid (Roedder & Bodnar 1980). Sometimes during this process, daughter minerals, commonly halite, are formed as the fluid contracts and increases in concentration.
Gold deposits are frequently associated with CO2 rich inclusions, which give a distinctive low temperature decrepitation peak (Partamines & Poutiainen 2001, Mavrogenes et al 1995, Burlinson 2006, 2007a, 2007b). This low decrepitation temperature is caused by the commonly high internal pressures of CO2 rich fluid inclusions (Mavrogenes et al 1995). Vapour rich inclusions also suggest that the fluid was at boiling point at some stage during its accent to its current position (Edwards & Atkinson 1986). Research has shown that areas that are determined to be of epithermal origin are highly likely to have gold and silver mineralisation at some depth below the surface (Mavrogenes et al 1995).
The Late Permian Drake Volcanics has widespread epithermal Gold and Silver mineralisation and has been mined intermittently for Gold, Silver, Copper, Lead and Zinc since the 19th century (Snowden 1987, Bottomer 1986, Clark et al 2001).
The Drake Mineral Field is located within the area of a New England convergent plate boundary leading in the north to calc-alkaline volcanism (Bottomer 1986, Leitch 1975, Cawood 1982). This overlies the Razorback Creek Mudstone which then overlies the Gilgurry Mudstone (Beeson and Borton, 2005). The geology is described on the Drake 1:100,000 map by Thompson, J, 1976. The mineralisation of the Mineral Field is attributed to three styles:
Discordant fissure veins,
Stratabound stockworks and,
Stratabound disseminations.
Most mineral assemblages in the area are made up of a combination of these three styles (Beeson and Borton, 2005). The tectonic relationship of the Drake Volcanics is not fully understood as detailed published studies of this region have been insufficient (Bottomer 1986).
The mineralisation and alteration of the Drake Volcanics has been multistage, most accounts suggest that the depositions occurred over two episodes (Bottomer 1986, Perkins 1997, Smith 1989). The Mt Carrington site has large areas that have undergone pervasive alteration, including intense silica – sericite – pyrite alteration in the central Strauss pit and North Kylo areas (Beeson and Borton, 2005, Smith 1989).
The
study site is located within the Mt Carrington mine site, situated in
the Drake mining area in the Upper Clarence Catchment of Northern
NSW, Australia (Figure 1). The Drake mining area is located within
the New England Fold Belt (Lin et al 2003).
A total of 33 samples were chipped out of insitu quartz veins at three locations (Figure 2) on September 18th 2007. Four samples were collected from North Kylo (S28˚ 54. 449’, E152˚ 22. 331’), 5 samples were from Strauss Pit (S28˚ 54. 579’, E152˚ 22. 382’), and 2 samples from Guy Bell (S28˚ 54. 761’, E152˚ 22. 441’). At each sampling point three replicates were taken from veins occurring within a 1m2 area (Table 1).
| Sample Site |
Sample Location # |
Replicate 1 Sample Number |
Replicate 2 Sample Number |
Replicate 3 Sample Number |
| North Kylo |
1 |
1 |
2 |
3 |
| North Kylo |
2 |
4 |
5 |
6 |
| North Kylo |
3 |
7 |
8 |
9 |
| North Kylo |
4 |
10 |
11 |
12 |
| Strauss Pit |
5 |
13 |
14 |
15 |
| Strauss Pit |
6 |
16 |
17 |
18 |
| Strauss Pit |
7 |
19 |
20 |
21 |
| Strauss Pit |
8 |
22 |
23 |
24 |
| Strauss Pit |
9 |
25 |
26 |
27 |
| Guy Bell |
10 |
28 |
29 |
30 |
| Guy Bell |
11 |
31 |
32 |
33 |
The samples were weighed and photographed after collection. The weight
of the samples varied from 13.7g to
775.9g. A visual assessment determined variation in the width of the
quartz veins to be around 1 to 10cm across. The chemical composition
of the samples also showed variation, from semi-translucent to milky
grey and white, sometimes greenish quartz, jasper was very prominent
is a few of the samples. Other minerals present include galena,
haematite, and some of the samples showed signs of oxidation. The
samples were analysed by Burlinson Geochemical Services in the
Northern Territory on the BGS model 105
decrepitometer, as per methods used in Burlinson 1988 and
described on this website.
The data was curve fitted and de-convoluted using Plot® 0.997
software. Estimates of the position, width and height of Gaussian
peaks were made and entered, the software then iteratively fits these
Gaussian curves. Fitting is assumed complete when further iterations
provide no further improvement of the quality of fit by minimising
the RSD of the fitted envelope curve to the experimental data. An RSD
of <5% was used as a benchmark for a good fit. Chi-squared is also
kept to a minimum, but the overall effectiveness of chi-squared is
more limited as it depends on the degrees of freedom in the sample:
the more Gaussian curves to fit, the higher the degrees of freedom.
The assumption used is that the distributions applicable would be
symmetrical about the point. However, this assumption is shown to be
invalid and skewed-Gaussian distributions should be applied.
After de-convolution was completed, the plots and data were analysed for trends, similarities and differences between sample site curve fits. The temperature of each Gaussian sub-population was recorded and plotted as a frequency distribution at 50˚C intervals: this was done for all samples combined, and for individual sites in the study area.
The results show multiple Gaussian distributions of temperature populations, which occur under curves that range from quite narrow (Figure 3) to very broad (Figure 4)
Samples 10, 11 & 12 were fitted using both symmetrical and asymmetrical distributions (Figures 5- 10). These samples show what is present in most of the other samples, a platy-kurtic population curve leading into a lepto-kurtic population at a slightly higher temperature. This is prominent at just below 400˚C in sample 10 (Figure 5), when refitted allowing for a skewed distribution (Figure 6) the two Gaussian sub-populations become one skewed Gaussian sub-population. This trend is also easy to see in sample 11 (Figure 7) at 300˚C, and again just above 500˚C in sample 12 (Figure 9). This refitting simplified the curve fit, resulting in fewer population distributions within each sample.
Six samples were visually rich in jasper (Appendix 1.2) all displaying high temperature distributions with the low temperature ranges mostly absent (Figures 11-16). The curve shape of each of these samples is very similar, featuring one high intensity temperature peak at around 450˚C.
Although the emplacement for a particular peak may have occurred in one event, there is temperature variation between the pulses of fluid over the duration of the emplacement.
As the vein opens, fluid coming up from below is hotter than the surrounding rock, which chills the fluid. An equilibration occurs between the fluid and the surrounding rock, resulting in what may be detected as a separate distribution beneath a larger curve.
Upon
initial analysis of the raw data it was clear that the Decrepigram
was displaying multiple populations within each sample, as such,
multiple symmetrical Gaussian curves were chosen as the most
appropriate method of statistical analysis. The resulting data plots
from this method were interpreted over a period of time, but it soon
became apparent that there was something
not quite right about the shape and fit of the curves. Possibly due
to the complexity of the software, and limited processing time, it
took some time before the realisation that the distribution of the
data would be better represented by a skewed curve.
This realisation was brought about by the common occurrence of a
sequence of curve shapes. A platy-kurtic population curve leading
into a lepto-kurtic population at a slightly higher temperature was
determined to be a good candidate for a single distribution, which is
skewed toward a ceiling before dropping away.
Samples 10, 11 and 12 were refitted using skewed distributions (Figures 5-10), the curve shape indicated a slow increase in decrepitation followed by a faster increase to a maximum, where the decrepitation counts fell suddenly. The re-fitted curve provided very similar fit parameters in terms of error distribution, but a much simpler fit with fewer distributions underneath the curve.
Due to the variation in wall thickness of the samples an asymmetric distribution makes more sense. Temperature of decrepitation is likely to be affected by the position of the inclusion within the mineral. Inclusions that are surrounded by a thin outer wall mineral are likely to decrepitate earlier, even if the temperature has not yet reached the temperature of emplacement, as the thinner the mineral wall the weaker it invariably is. Inclusions that are embedded deeper within the mineral are likely to decrepitate closer to the actual temperature of mineralisation.
Another factor influencing the early decrepitation of fluid inclusions is the shape of the inclusion itself. Angular inclusions are known to stress at the corners which causes premature decrepitation. Due to the size of most inclusions, tedious preparation and microscope work would be required to determine if this was the case, this would require the traditional methods of ore microscopy be used.
A variation in the wall thickness of the inclusion would explain the tendency toward an asymmetrical skewed distribution. The frequency of the decrepitation pops creeps up as the inclusions with thin walls decrepitate, then the frequency of the decrepitation ceilings as the true temperature is reached, then drops off sharply at the end of the event.
The
results indicate multiple mineralisation events, both in the physical
appearance and in the multiplicity of distributions within the data.
This is consistent with the theories of previous research (Bottomer
1986, Perkins 1997, Smith 1989). The composition
of the fluid is not necessarily changing but the multiple
distributions may be represented by different opening regimes.
Further studies could clarify this issue.
The veins which were embedded within rocks with high levels of jasper generally show high temperature peaks only, low temperature peaks are mostly absent. This indicates first phase mineralisation, as jasper is iron contaminated quartz, formed from high temperature oxidising fluids. The types of veins exhibited here are skewed toward the mesothermal system, due to their high temperature range. These samples are not representative of the full range of temperatures present within the area, but do provide a good representation of the high temperature range.
The results show that there is a high level of variation in the distribution of temperature ranges (Figures 3 &4). The jasper rich veins exhibit temperature ranges that are spread over the high end of the temperature range, with one main peak, whereas other samples have temperature distributions spread over the high and low temperature ranges, some displaying sharp individual peaks, and others displaying very wide distributions that are not as well defined.
There is a noticeable variation of the intensity (frequency) of the decrepitation peaks. Although this study does not focus on decrepitation intensity, this is a point worthy of noting. This variation can be attributed to variations in the number of inclusions present in the sample and their size distribution, and/or the influence of the alpha-beta phase transition.