Geophysical Survey for Placer Prospecting at Mary Creek

Transcription

1 1

2 Geophysical Survey for Placer Prospecting at Mary Creek Cariboo District/Quesnel/BC 2011 N W TENURES , , , , , , , , , , , , METHOD 2D Resistivity FOR Melvin Lee Zeiler Box 188, Wells BC, V0K 2R0 PROVIDED BY Arctic Geophysics Inc. FIELD WORK 3 rd 11 th May 2011 REPORT /DATE Philipp Moll / 25 th Aug 2011 EVENT NUMBERS ,

3 Index 1. Introduction Location List of Claims Mary Creek Location, Tenures, Survey Detail Crew Access Goal Method Use of Geophysical Method Instrumentation Data Acquisition Processing Interpretation Profile image Geology Bedrock Geology Map Geophysical Considerations Profiles Preliminary Note! Mary Creek Line A Mary Creek Line B Conclusion References Literature Maps Qualification GPS Data Attachment 1: Profiles raw Attachment 2: Geological Data Attachment 3: Geophysical Data Attachment 4: Costs

4 1. Introduction This geophysical investigation was done for Melvin Lee Zeiler. The survey using 2D Resistivity was conducted to prospect the ground for placer mining interests. The ground was tested by two 745m measuring lines, depth 100m. 2. Location The survey area is located about 1 kilometer south eastern from the confluence of Mary Creek and Alice Creek.GPS coordinates: N W The line locations were determined by Melvin Lee Zeiler without using any consulting by the service provider Arctic Geophysics Inc.. The measuring lines were well cut by Melvin Lee Zeiler before the field work did start. 3. List of Claims Tenure No Claim Name Map No Issue Date Good To Date Area (ha) LEE #1 093G /oct/ /apr/ LEE #2 093G /oct/ /apr/ LEE #3 093G /oct/ /apr/ MARY GOLD #1 093G /oct/ /apr/ LEE #4 093G /jun/ /apr/ LEE #5 093G /jun/ /apr/ MARY GOLD #2 093G /feb/ /apr/ MG EAST 1 093G 2009/sep/ /apr/ MG EAST 2 093G 2009/sep/ /apr/ MG EAST 3 093G 2010/feb/ /apr/ MG EAST 4 093G 2010/nov/ /apr/ MARY CREEK SOUTH 093G 2011/jan/ /apr/ MARY CREEK SW 093G 2011/jan/ /apr/

5 4. Mary Creek Location, Tenures, Survey Detail 5

6 6

7 7

8 5. Crew Fieldwork Survey Leader Geophysical Prospector: Helper: Processing, Interpretation Managing Director: Scientific Director: Geophysical Prospector: Documentation Managing Director: Stefan Ostermaier Josy Strunden Bud Paling Philipp Moll Stefan Ostermaier Josy Strunden Philipp Moll 6. Access The survey area was accessed via the mining road nearby. 7. Goal The survey was focussed on measuring and interpreting following subsurface characteristics: 1. Depth and topography of bedrock 2. Sedimentary stratification 3. Groundwater table 4. Mining/prospecting history 8. Method Resistivity is not a time domain geophysical method. Resistivity measures a material property. In the Resistivity model the different underground zones are material dependently differentiated according to their electrical conductivity. A measurable data contrast between overburden and bedrock could be stated in 95% of our placer surveys. 1 Resistivity promises good chances in respect of measuring the kind and character of the subsurface materials as well as the groundwater distribution, which would be of interest for placer mining. Measuring of layer interfaces in depths from 0.5m to 100m is possible by varying the electrode spacing. Therefore this prospection concept is based on the use of 2D Resistivity. 1 This likeliness cannot be provided in this survey due to the complexity of the survey area s stratigraphy and lithology. 8

9 9. Use of Geophysical Method 9.1. Instrumentation RESISTIVITY For this survey a lightweight, custom built 2D RESISTIVITY and INDUCED POLARIZATION (IP) imaging system with rapid data acquisition was be used. The system includes: 4 POINT LIGHT EARTH RESISTIVITY METER ELECTRODE CONTROL MODULES STAINLESS STEEL ELECTRODES 4 750m MULTICORE CABLE: CONNECTOR SPACING: 5m 5 This system weighs approximately 120 kg which is about one third of regular standard equipment. It can be run with a 12V lead battery. The equipment facilitates high mobility and rapid data acquisition with a small crew Data Acquisition RESISTIVITY The data acquisition is carried out by the automatic activation of 4 point electrodes. Thus several thousand measurements are taken, one every 1 2 seconds. The AC transmitter current of 0.26 to 30 Hz is amplified by the electrode control modules, up to a maximum of 100mA and 400V peak to peak. The voltage measured at the receiver electrodes (M, N) is also amplified. In this geoelectrical survey the Schlumberger array was used. This array is appropriate to image horizontally running layers as is needed for placer prospecting. Our 2D Resistivity imaging system allows measurements with a depth of up to 130m. With a depth to bedrock of more than 6m we use an electrode spacing of 5m in our placer surveys. This allows us the measuring of large profile lengths in short time with a horizontal measuring resolution of 2.5m. This quantification has proven itself to be reliable in the determination of the bedrock topography and sedimentary arrangement for placer investigation at the most environmental conditions. 2 Constructed and produced by LGM, Erich Lippmann, Kornacker 4, Schaufling, Germany, Phone ++49 (0) , Fax , Lippmann@L GM.de, gm.de 3 Ditto 4 Constructed and produced by Geoanalysis, Am Holderstock 6, Offenburg, Tel (0) ; info@geoanalysis.de, 5 Ditto 9

10 9.3. Processing RESISTIVITY The measured Resistivity/IP data were processed with the RES2DINV inversion program 6. The data scale of the resistivity was not unified because the profiles do not allow the interpretation of a strict correlation between ground material and Resistivity data. And the overburden can be so heterogeneous in the material components, water amount, hardening etc. that the same/similar material does usually not continue over a longer distance. The data usually range by factor 90 and 750, and the data zones in resistivity profiles B are complex: A uniform (averaged) data scale would garble the interfaces. Since this survey is inter alia focussed on the detection of interfaces between sediment layers of different nature within a sedimentary succession, the scales are balanced to make a good compromise between 1) imaging the interfaces and 2) similarity of the scales between the profiles of s series Interpretation The Resistivity profile is the foundation for the interpretation of the subsurface conditions for the placer prospection. It usually allows for good interpretation of bedrock and overburden for finding secondary deposits Profile image In the Resistivity profile the interpreted layer interfaces are marked with a black line. The profiles show ground layers approximately 15% thicker than they are in reality. The thickening of the model layers is caused by the inversion software. The correction factor of 0.85 for the determination of the true layer thickness has been established by the Arctic Geophysics Inc. team on the basis of numerous geoelectrical profiles verified by drilling, trenching, and mining done by our customers. 7 The graphical markings showing the interpreted layer interfaces in the profiles (using a black line) are done accordingly to the data structure in the profile itself. This means: the layers there will also show up approximately 15% thicker than they are in reality. At the measuring sticks and in the interpretation text the layer thicknesses and depths have been recalculated to the expected real values. 6 Designed by GEOTOMO SOFTWARE (Malaysia), 115, Cangkat Minden Jalan 5, Minden Heights, Gelugor, Penang, Malaysia, Tel. : ++60 (0) , Fax : ++60 (0) , geotomo@gmail.com 7 Program settings at the RES2DINV for modifying the layer thickness do frequently not work well for our use and could falsify the profile. That s why this mode was not used. 10

11 10. Geology The survey area was glaciated by most likely two main periods both releasing potentially thick overburden consisting of glacial and pre glacial deposits. During the last glaciations the ice flowed in western direction from the Cariboo Mountains. So old river gravel deposits, which haven t been eroded by the glaciers might have been better conserved in valleys and channel running across to this direction. Thick sequences of glaciofluvial gravel were deposited in braided outwash streams. Ice damming of tributary drainages was common and produced glaciolacustrine deposits of silt and clay. 8 Glaciofluvial and glaciolacustrine deposits might be located mainly on top of till and sometimes on bedrock. Within a glacial deposition cycle, mostly in the upper portions of the overburden, some clay layers were potentially produced which could have reflected the influence of deformable sediments. 9 This way, some deeper, older inter glacial or pre glacial deposits could have been protected against subsequent glacial erosion. Large depositions of stream gravels in the main valleys were followed by river incision. This caused the development of successively lower terraces. 10 In higher regions the glaciers have strongly eroded the overburden on the Mary property. Preglacial placer deposits could probably have survived in bedrock depressions. The bedrock at Mary seems to be dominated by some schistoid bedrock showing good erosion resistance: Some sections of the bedrock seem to be higher metamorphosed and harder. Those rock zones could have acted as a barrier against the ice flow which could have protected placer deposits in lee westerly. The schistoid bedrock is most likely tilted by tectonics and offers some V shaped pockets for placers also potentially protecting placers against the ice. The thrust could have produced trapping zones for placers. 11 The paleo drainage of the area might have run in different directions feeding different water basins. This scenario is still suggested by the current drainage system (see survey map below). The glacial melt water drainage system must have been located on relatively flat ground. The channels did not cut deeply into overburden or bedrock. This multidirectional drainage net might have produced some bedrock depressions which sometimes cannot be differentiated between glaciofluvial channels and melt water basins 8 Levson M. and Timothy R. Giles: Geology of Tertiary and Quaternary Gold Bearing Placers in the Cariboo Region, British Columbia (93A, B G, H), 199: General Geology 9 Technical Review on various exploration licences held by Henning Gold Mines Inc. (Draft 9 th May 2011): 5.5 Local Stratigraphy 10 Levson M. and Timothy R. Giles: Geology of Tertiary and Quaternary Gold Bearing Placers in the Cariboo Region, British Columbia (93A, B G, H), 199: General Geology 11 Some dark schist bedrock has been observed in a test pit near the measuring lines. 11

12 very well. The overburden changes between glacial till, glaciofluvial and glaciolacustrine deposits. 11. Bedrock Geology Map Levson M. and Timothy R. Giles: Geology of Tertiary and Quaternary Gold Bearing Placers in the Cariboo Region, British Columbia (93A, B G, H): Figure 11 12

13 13

14 12. Geophysical Considerations The resistivity or rather conductivity of the sediments is largely controlled by the amount of water saturation as well as the condition of the water. 13 In the survey area glacial till, glaciofluvial and glaciolacustrine deposits contain relatively high amounts of finer sediments such clay, silt, and sand, even in greater depth. Thus its resistivity can be low. Saturated silt can have penetrated into the space between larger sediment particles; this material is called slum. The conductivity of the slum is usually quite homogeneous. Thus, deposits of different type and age are sometimes hard to differentiate. The Resistivity pattern of the profiles potentially indicates glaciofluvial and glaciolacustrine deposits on top of till, as well as glacial till on top of possible river gravel or bedrock. The upwards transition from coarse sediments such as boulders, cobbles and gravels in the depth to pebbles, sand, silt and clay in the upper portions cannot be interpreted in detail in the resistivity profiles. However, clay layers or clay rich layers acting as a water barrier can reveal the layer borders in the sedimentary progression indicating a glacial period. Clay rich layers could also indicate overlying inter glacial and post glacial stream channel placers in the Cottonwood River area [which] have been mined in recent years at Mary and Alice creeks. 14 Layers characterized by clay are sometimes running uneven which might seal sedimentary zones against each other producing resistivity alterations running horizontally and inclinely! Uneven groundwater horizons are frequently assumed in the Resistivity profiles. The interpretation of the Resistivity profiles is mainly focused on the differentiation of layers with different nature, age and origin: 1) glacial till being diamict mostly producing heterogeneous data; glaciofluvial deposits usually being well layered normally producing more homogeneous data. The detailed character of a layer cannot be interpreted seriously in an area showing such a heterogeneous stratigraphy. The interpretation try to differentiate between fine and coarser sediments as well as between sediments which are higher water saturated or less, respectively consolidated (or even cemented) or un consolidated sediments. In some cases the 13 The conductivity in secondary deposits is mainly controlled by following groundwater related influences: Mineral composition of the sediment particles. Pore volume of the deposit correlating with the particle size of the sediments. The smaller the particles the higher is the possible amount of saturation. So potentially clay/silt deposits are better conducting than sand or gravel. Mobility of the water. Sediments being saturated with stationary water do have higher conductivity since ions have time to get solved in groundwater. Weathering increases the conductivity since new (mostly well conducting) minerals are generated and get solved in water. Philipp Moll, Arctic Geophysics Inc. 14 Ditto: Abandoned, Gravel Bed Paleotrunk Valley Deposits 14

15 resistivity models shows a very heterogeneous to bizarre data pattern which might realistically image the complex subsurface. Zones with different resistivity potentially indicate different layers as defined. However, a strong saturation with groundwater can make those layers indistinguishable. A well conducting layer below a lower conducting layer is frequently just a groundwater boundary. But a lower conducting layer below a better conducting layer might indicate two different materials at a higher chance. This scenario could also indicate a clay layer ( false bedrock ) as being a possible base for placers. This survey has confirmed the geological sources referring to various bedrock types. Changes of the resistivity can indicate different rock types or weathered zones. Rock erosion produces porosity which allows for the penetration of water. The rock becomes higher conductive. Frequently the water trapped in rocks is rich in solved minerals which increase the conductivity even more. Especially at fault lines and thrusts the resistivity is elevated usually showing heterogeneous resistivity data. Outside from the hypothetic granitic intrusions at Cottonwood and Mary, the ground materials (sediments, sedimentary rocks, volcanic rocks and clastic rocks) show resistivity data within ranges which does not implicate a strict correlation between ground material and resistivity data. Changes in the bedrock are indicated. And the interfaces between rocks and sediments as well as between rocks and rocks are both running in horizontal direction. The highly changing water saturation increases the heterogeneity of the data. All this makes a harder interpretation. Thus, the interpretation of the profiles in the location specific reports must be ambivalent sometimes. This ambivalence can effectively be terminated by drilling. Drilling will clear the very high information content of this geophysical survey. 13. Profiles Preliminary Note! The subsurface information of this study is an interpretation. 15

16 Mary Creek Line A 2D Resistivity, Schlumberger array 150 Electrodes: spacing 5m, Horizontal measuring resolution 2.5m Horizontal and vertical measure in [meter], Iteration error in [%] Vertical exaggeration in model section display = 0.86 Data acquisition: Stefan Ostermaier, Josy Strunden, 9th May 2011 Processing: Philipp Moll, 10th May 2011; Cariboo Range 16

17 Interpretation At 0 380m, the 2 to 3m thick green/turquois layer below the surface might consist of humus+muck or glacial till being less saturated than the material underneath. The blue well conducting layer is interpreted as overburden highly saturated. This overburden is likely some glacial till containing a significant amount of fine sediment particles, most likely silt (matrix), between the gravels. The high saturation could cover the possible existence of different sediment layers: Possible glaciofluvial deposits on top of the till does not show up in the profile. At m, the red/violet layer is most likely the same material as at the red data zone in profile B. This material is much poorer in water. Its finer sediment particles could have washed out leaving some gravel which cannot hold much water. The hypothetic bedrock depressions below the red layers in profile A and B could indicate alluvial transport of the sediments in former times. This makes the interpretation of naturally washed gravel layers (red) plausible. Around 170m, there might be a larger channel, 38m deep, likely bearing saturated till on top of possible pre glacial river gravel. At 460m, there could be a small channel in the bedrock, depth 57m. However, it is estimated to be less likely. The bedrock interpreted in the profile (green/turquoise zone) is likely some schist containing well conducting minerals. Some dark schist was seen in a test pit nearby the profile. 15 The angular pattern of the resistivity makes this bedrock type likely. Alternatively, the green/turquoise data zone interpreted as bedrock could be some glacial till being less saturated, possibly sealed by a clayrich layer. The geology of this area does have the potential to produce huge piles of glacial till. However, this scenario is estimated to be less likely. The large bedrock depression around 620m could be a pre glacial river channel which did cut deeply into the soft, well conducting bedrock. The deposits in this channel at least being 65m deep are just seen partly; the possible layering of the overburden in the channel is again invisible in the profile because of the high amount of groundwater. Some pre glacial river gravel could have been conserved in this channel. 15 Information: Melvin Lee Zeiler 17

18 Mary Creek Line B 2D Resistivity, Schlumberger array 150 Electrodes: spacing 5m, Horizontal measuring resolution 2.5m Horizontal and vertical measure in [meter], Iteration error in [%] Vertical exaggeration in model section display = 0.89 Data acquisition: Stefan Ostermaier, Josy Strunden, 10th May 2011 Processing: Philipp Moll, 11th May 2011; Cariboo Range 18

19 Interpretation Profile B is running across to profile A, in a distance of about 200m in south eastern direction. The hypothetic large channel in profile A at 620m would run parallel to this profile and thus would not show up in it. The overburden in this profile shows more heterogeneity in the resistivity than in profile A. At 0 240m, the turquoise overburden could be dominated by glaciolacustrine sediments produced by ice damming of tributary drainages when the glacier has started melting. 16 Alternatively, this deposit could just be glacial till with possible commixtures of glaciofluvial sediments. At m, the topmost layer (blue, turquoise) is better conducting than the material below. The topmost material might be higher saturated and possibly sitting on top of a clay rich layer acting as a water barrier. This topmost overburden could be a glaciofluvial deposit on top of glacial till both layers sealed from each other by clay. The brown body at 145m could be a laterally sealed deposit. The red/violet overburden in this profile could be again some naturally washed gravels belonging to a drainage system being inter glacial or pre glacial. At m, the red/violet overburden in this profile could be again some naturally washed gravels belonging to another drainage system than in profile A being inter glacial or pre glacial. The possible channels at 370m and 440m would be 47m and 37m deep. The overburden in these channels look unordered which might be an indication for glacial till. The lower portions of the overburden could be alluvial deposits. At 625m, the channel would be 37m deep. The overburden on top of the channel is well layered. This structure is typical for alluvial deposits. In this section of the profile some pre glacial river gravel could have been conserved. Alternatively, the green/turquoise data zone interpreted as bedrock could be some glacial till being less saturated, possibly sealed by a clayrich layer. The geology of this area does have the potential to produce huge piles of glacial till. However, this scenario is estimated to be less likely. 16 Levson M. and Timothy R. Giles: Geology of Tertiary and Quaternary Gold Bearing Placers in the Cariboo Region, British Columbia (93A, B G, H): Quaternary Geology 19

20 14. Conclusion In the survey area, the overburden could be between 25m and 65m thick. The bedrock depth of the possible paleochannels is 38m, 57m, and 65m at profile A, and 47m, 37m, and 37m at profile B. The interpreted depth of the bedrock could be verified by drilling. Appropriate locations for drilling are marked in the profile images above (red arrows). At profile A, a higher amount of groundwater is strongly assumed which could influence the drilling. It might be reasonable to test this ground using a sonic drill. At profile B less groundwater is expected. The use of an auger drill might be possible to get usable samples. 20

21 15. References Literature Chesterman W. Ch. and Lowe K.E. Field Guide to Rocks and Minerals North America, Chanticleer Press Inc. New York 2007 Evans A.M. Erzlagerstättenkunde, Ferdinand Enke Verlag Stuttgart (1992) Griffiths, D.H.,Turnbull, J. and Olayinka,A.I. Two dimensional resistivity mapping with a computercontrolled array, First Break 8: (1990) Griffiths, D.H. and Barker, R.D. Two dimensional resistivity imaging and modeling in areas of complex geology. Journal of Applied Geophysics 29 : (1993) Keller, G.V.and Frischknecht, F.C. Electrical methods in geophysical prospecting. Oxford: Pergamon Press Inc. (1966) Loke M.H. and Barker R.D. Rapid least squares inversion of apparent resistivity pseudosections by a quasi Newton method. Geophysical Prospecting 44: (1996) Press F., Siever R., Grotzinger J., Thomas H.J. Understanding Earth, W.H. Freeman and Company, New York (2004) Robb L. Introducing to Ore Forming Processes, Backwell Science Ltd., 2005 Literature Location specific Bauer S., Kästner M. Fact Finding Mission and Preliminary Report (2010), Cohen, H. Feasibility Study for HMMC (1980) D.O. Donovan et alii: Technical Review on various exploration licences held by Henning Gold Mines Inc. (Draft 9 th May 2011) about Quesnel Mining area Levson M. and Timothy R. Giles: Geology of Tertiary and Quaternary Gold Bearing Placers in the Cariboo Region, British Columbia (93A, B G, H) Roed M. A., Geology of the Handy Claims (1987) Roed M. A., Preglacial Auriferous Mud Fows of Mary Creek and the Coldspring Volcanic Center, Quesnel Trough, British Columbia (1987) Tremaine, C. W. Feasibility Study: Wingdam Property (1963) 21

22 Maps Levson M. and Timothy R. Giles: Geology of Tertiary and Quaternary Gold Bearing Placers in the Cariboo Region, British Columbia (93A, B G, H): Figure 11 BC Digital Geology Maps Version

23 16. Qualification Philipp Moll Box 747, Dawson City, Yukon, Y0B 1G0 Phone: (Canada) (0) (Germany) Certificate of Qualifications I, Philipp Moll, currently residing at Am Holderstock 7, Offenburg, Germany, do hereby certify that: 1. I have studied Geology at the University of Freiburg, Germany. 2. I have visited of geophysical field courses at the University of Karlsruhe in Germany. 3. I have been working for Arctic Geophysics Inc. since June 2007 (foundation). For this company I have carried out geophysical field surveys using 2D Resistivity, Induced Polarization, and Magnetics: Data acquisition, processing, interpretation, documentation. 4. I have done geophysical surveying for mining exploration in the Yukon since 2005, and geological prospecting for precious metals and minerals in the Yukon, NWTs, and Alaska since I have written the following publications/reports: A) Numerous Assessment Reports about geophysical surveys done for Yukon mining companies, filed at Yukon Mining Recorder, Dawson City and Whitehorse, Yukon. B) Publication about a geophysical survey (45 field days) for the Yukon Government: Yukon Geological Survey: Open Files: Moll, P., & Ostermaier, S., D Resistivity/IP Data Release for Placer Mining and shallow Quartz Mining - Yukon Yukon Geological Survey Miscellaneous Report MR-4. PDF Report [10.3 MB ] & Data Profiles, 45.4 MB ] ] Confirmation I have prepared, along with Fran Macpherson, this report entitled 2D Resistivity Survey on the Mary Property for assessment credit, and reviewed the data contained in the report titled: Geophysical Survey for Placer Prospecting at Mary Creek. The survey was carried out by Arctic Geophysics Inc. Offenburg, Germany, 18th August, 2011 Signed and Sealed Philipp Moll Philipp Moll 23

24 17. GPS Data Mary Creek Line A Electrode No. Location in Profile [m] GPS-Coordinates Latitude/ Longitude [DD MM SS.S ] GPS- Accuracy [m] 1 0 N W * 2 5 N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W * N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W Post [ * ] 24

25 N W N W N W N W N W N W N W N W * N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W * N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W

26 N W N W N W N W N W N W N W N W N W * N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W * N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W

27 N W N W N W N W N W N W N W N W N W N W

28 Mary Creek Line B Electrode No. Location in Profile [m] GPS-Coordinates Latitude/ Longitude [DD MM SS.S '] GPS- Accuracy [m] 1 0 N W * 2 5 N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W * N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W Post [ * ] 28

29 N W N W N W N W N W N W * N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W * N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W

30 N W N W N W N W N W N W N W * N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W * N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W N W

31 N W N W N W N W N W N W N W N W * 31

32 Attachment 1: Profiles raw Profile A 32

33 Profile B 33

34 Attachment 2: Geological Data Levson M. and Timothy R. Giles: Geology of Tertiary and Quaternary Gold Bearing Placers in the Cariboo Region, British Columbia (93A, B G, H),

35 35

36 36

37 37

38 38

39 Particle Seize 39

40 40

41 Attachment 3: Geophysical Data Geophysical Data Table 41

42 42

43 47