Formation of low mass protostars and their circumstellar disks
Geophysical methods brief summary
1. Brief Summary on Geophysical
methods
• Geophysics and
Geophysical prospecting
Collected by:
Jyoti Anischit
Msc in engineering
Geology
TU
2. INTRODUCTION
• Definition
Geophysical prospecting is the study of the structure
of the earth’s crust by physical methods for the
location and surveying of minerals and ores.
It is an integral part of geophysics.
3. OBJECTIVES
• To determine lithology of the area.
• To identify and locate exploitable reservoirs.
• To detect and delineate geothermal resources.
• Estimate geophysical properties of the geothermal
system.
• To determine the ground water conditions in the
regions.
4. CONCEPT OF GEOPHYSICAL EXPLORATION
Exploration geophysics
Definition
Is an applied branch of geophysics, which uses physical
methods at the surface of the Earth to measure the
physical properties of the subsurface, along with the
anomalies in those properties.
Geophysical methods include;
Seismic,
Gravitational,
Magnetic,
Electrical
Electromagnetic
5. CONCEPT OF GEOPHYSICAL EXPL CONT……
These methods identify resources without the need for sampling.
Usually undertaken with minimal surface disturbance.
The survey used in these methods is called Geophysical survey.
Geophysical surveys can be conducted either from ;
The air,
On the ground or
Down drill holes.
6. CONCEPT OF GEOPHYSICAL EXPL CONT….
Airborne geophysical surveys
May comprise of magnetic, radiometric, gravity or
electromagnetic methods.
These surveys provide general geological information for
an area and are often used in the initial stages of
exploration.
These surveys are typically undertaken using low flying
helicopters or light aircraft which fly in a grid pattern.
In airborne survey, instruments may be either mounted on
the aircraft or towed underneath.
The aircraft may fly between 25 and 60m above the
ground, with flight lines spaced between 25 and 200m
apart.
7. CONCEPT OF GEOPHYSICAL EXPL CONT….
DOWN HOLE SURVEYS
These geophysical surveys involve putting geophysical
equipment down exploration drill holes to gather magnetic,
radiometric or electrical information from the rocks adjacent to
the hole.
Also used to determine the exact path of the drill hole.
Occasionally tools with a small radiometric source may be used
and a detailed risk assessment is required to ensure the tool is
not lost down hole.
8. magnetic survey,
Seismic surveys,
Magnetic surveys,
Radiometric surveys,
Ground based surveys
There are a number of types of geophysical surveys
which are undertaken on the ground.
These are include;
Gravity surveys,
Induced Polarization (IP)
surveys,
Electromagnetic (EM)
surveys ,
• CONCEPT OF GEOPHYSICAL EXPL CONT….
Note method used for data collection in above survey is called
geophysical methods.
9. SEISMIC METHOD
The common geophysical method used in Exploration
I. SEISMIC METHOD
Definition
Seismic method refer to method which use seismic
velocities to measure the elastic properties of Earth’s
material.
These techniques provide detailed information about
subsurface layering and subsurface mechanical properties
using seismic waves.
Seismic waves propagate through a rock body at a velocity
which is governed by elastic properties (stress & strain,
Young’s modulus) and density of the geological formation.
10. SEISMIC METHOD CONT..
A seismic source-such as sledgehammer is used to
generate seismic waves, sensed by receivers deployed
along a present geometry (called receiver array), and then
recorded by a digital device called seismograph.
Diagram showing seismograph and geophone array
11. Types of seismic waves
There are two groups of seismic waves such as;
i. Body waves and
ii. Surface waves.
• Body waves- Are the waves that can propagate
through the internal volume of an elastic solid
materials.
• Body wave is divided into two types which are;
Compressional waves (Longitudinal, primary or P-wave)
Shear waves (Transverse, secondary or S-waves).
12. SEISMIC METHOD CONT…
P-wave travel with a velocity that depends on the
elastic properties of the rock through which they travel.
P-wave has the highest velocity than all seismic waves
and thus will reach all the seismograph first.
Particle motion associated with the passage of a
compressional wave involves oscillation, about a fixed
point, in the direction of wave propagation.
S-waves travel through material by shearing it or
changing its shape in the direction perpendicular to the
direction of travel.
S-waves travel slower than the p-wave as reach at the
seismograph after p-waves.
13. SEISMIC METHOD CONT….
Surface waves are the waves which propagate along
the boundary of the solid material on the earth.
Surface behave like S-waves in that they cause up and
down and side to side movement as they pass, but they
travel slower than S-waves and do not travel through the
body of the Earth.
These waves are of two types which are;
• Love waves
• Rayleigh waves
14. SEISMIC METHOD CONT…….
Rayleigh waves propagate along a free surface, or along
the boundary between two dissimilar solid media, the
associated particle motions being elliptical in a plane
perpendicular to the surface and containing the direction
of propagation surface waves.
Love waves are polarized shear waves with a particle
motion parallel to the free surface and perpendicular to the
direction of wave propagation.
16. SEISMIC METHOD CONT……..
SEISMIC WAVE VELOCITY
Additional factors which influence compressional and
shear wave velocities are;
Lithology
Extent of fractures
Temperature
Fluid content
Saturation and
Fluid pressure in the subsurface
17. SEISMIC METHOD CONT……..
• Typical rock velocity
Type of formation P-wave velocity m/s S-wave velocity m/s Density g/cc
Scree, vegetal soil 300-700 100-300 1.7-2.4
Dry sands 400-1200 100-500 1.5-1.7
Wet sands 1500-2000 400-600 1.9-2.1
Saturated shales and clays 1100-2500 200-800 2.0-2.4
Marls 2000-3000 750-1500 2.1-2.6
Porous and saturated sst 2000-3500 800-1800 2.1-2.4
Limestone 3500-6000 2000-3300 2.4-2.7
Chalk 2300-2600 1100-1300 1.8-3.1
Salt 4500-5500 2500-3100 2.1-2.3
Dolomite 3500-6500 1900-3600 2.5-2.9
Granite 4500-6000 2500-3300 2.5-2.7
18. SEISMIC METHOD CONT…….
.
Type of formation P-wave velocity m/s S-wave velocity m/s Density g/cc
Basalt 5000-6000 2800-3400 2.7-3.1
Gneiss 4400-5200 2700-3200 2.7-3.1
Coal 2200-2700 1000-1400 1.3-1.8
Water 1450-1500 - 1.0
Ice 3400-3800 1700-1900 0.9
Oil 1200- 1250 - 0.6-0.9
Note: The Acoustic impendance is defined as the product
of the density and P-wave velocity within a rock unit.
When elastic wave encounters an acoustic impendance
boundary, a portion of the wave energy is Reflected off of
the boundary and a portion is Refracted into the second
medium, according to Snell’s law.
19. SEISMIC METHOD CONT…….
At the critical angle for each interface (energy refracted 90
degrees), the seismic wave will travel along the interface with
a velocity of the underlying layer.
Since P-waves are the fastest portion of the seismic wave,
they represent the first arriving energy at each geophone
(either direct or refracted).
20. SEISMIC METHOD CONT…….
Seismic Reflection method
Seismic reflection is the primary geophysical method
used in oil and gas exploration and operated on density
and elastic module of subsurface materiatials.
The seismic reflection method usually gives better
resolution (i.e., makes it possible to see smaller features)
than other methods, with the exception of measurements
made in close proximity, as with borehole logs.
Seismic Refraction method
Seismic refraction is a method to determine the P-wave
velocity structure of the subsurface.
21. SEISMIC METHOD CONT…….
The refraction method has been used in mineral
investigations to map low-velocity alluvial deposits such
as those that may contain gold, tin or sand and gravel.
Application in geo-environmental work include studying
the structure, thickness, and hydrology of tailings and
extent of Acid mine drainage around mineral deposit.
Note;
Reflection seismic methods provide fine structural detail
and refraction methods provide precise estimates of depth
to lithologies of different Acoustic impendance.
22. SEISMIC METHOD CONT…….
Seismic data and their acquisition, processing, and
interpretation.
Digital seismic data
Seismic data are physical observations, measurements, or
estimates about seismic sources, seismic waves, and their
propagating media.
The form of seismic data varies, and can include analog
graphs, digital time series, maps, text, or even ideas in
some cases.
We focus on the analysis of data on body waves, mostly
P-waves, in their transmission, reflection, diffraction,
refraction, and turning processes.
24. SEISMIC METHOD CONT…….
Data acquisition
Seismic data acquisition in the energy industry employs a
variety of acquisition geometries.
Example of the typical onshore acquisition geometry using
dynamite or Vibroseis technology as sources and geophones as
receivers.
25. SEISMIC METHOD CONT…….
Panel (a) shows a split spread, using a shot located in the
middle and many receivers spread around it.
(b) shows an end-on spread, with a shot located at one
end and all receivers located on one side of the shot.
Quality control, or QC
This involves checking the survey geometry, data format,
and consistency between different components of the
dataset, and assuring that the quality and quantity of the
dataset are satisfactory for the study objectives.
The data QC process is typically part of the pre-
processing.
26. SEISMIC METHOD CONT…….
Data processing
To identify and enhance the desired signal by suppress
various kinds of noise in the data.
The goal of seismic data processing is to help
interpretation, the process of deciphering the useful
information contained in the data.
Data interpretations and Seismic modeling
This is based on processed data and seismic imaging
conducted to produce various forms of imagery for the
interpretation process.
Seismic modeling done after data interpretation and generate
predictions to compare with the real measurements, and thus
verify the interpretation.
28. SEISMIC METHOD CONT…….
APPLICATION OF SEISMIC METHOD
i. Its employed for hydrocarbon exploration
By providing a high resolution map of acoustic impedance and
petroleum geologists and geophysicists interpret potential
petroleum reservoirs easily.
ii. Its used in mineral exploration
By Identifying massive sulphide bodies since massive sulphide
bodies have higher seismic velocities and densities than their
host rocks.
iii. Used to predicts the depth, thickness of geologic strata,
and structural
29. MAGNETIC METHOD
MAGNETIC METHOD
Definition
Magnetic method is the method used to measure the
variations of the Earth’s magnetic field due to the
presence of magnetic minerals. or
It is used to investigate subsurface geology on the basis
of anomalies in the Earth’s magnetic field resulting from
the magnetic properties of the underlying rocks.
Earth's magnetic field refer to magnetic field that
extends from the Earth's interior to where it meets the
solar wind, a stream of charged particles emanating
from the Sun.
30. Thus why the Earth’s
magnetic field varies with
time (it is not constant).
It believed that the earth’s
magnetic field is
originates from the liquid
outer core of the Earth
containing high
concentration of iron.
As the Earth rotates, the outer layers of the ionosphere
interact with the solar wind to cause minor fluctuations
in the magnetic field.
• MAGNETIC METHOD CONT…….
31. MAGNETIC METHOD CONT…….
If the rocks are magnetic (have high susceptibility) they
become magnetized, and their field adds to that of the
earth. Thus the total magnetic field is stronger over
magnetic rocks.
Magnetic fields are measured in Nanoteslas (nT), which
used to be called gammas.
Magnetic rocks contain various combinations of induced
and remanent magnetization that perturb the Earth's
primary field.
The magnitudes of both induced and remanent
magnetization depend on the quantity, composition, and
size of magnetic-mineral grains.
32. MAGNETIC METHOD CONT…….
In order for something to be magnetic, its dipoles must
be aligned with each other, so that they face the same
direction.
The direction they face create a North end, while the
opposite end creates a South end.
Some substances, known as ferromagnetic substances,
have permanently aligned dipoles.
A magnetic high anomaly is where the measured field
strength is higher than the value predicted by the global
model, and a magnetic low is where the measured field
strength is lower than the value predicted by the global
model.
33. MAGNETIC METHOD CONT…….
Anomalies in the earth's magnetic field are caused by
induced or remanent magnetism.
This anomaly created when the Earth’s magnetic field is
disturbed by an object that can be magnetized.
To measure anomalies, magnetometers need a sensitivity of
10 nT or less.
Induced magnetic anomalies are the result of secondary
magnetization induced in a ferrous body by the earth’s
magnetic field.
34. MAGNETIC METHOD CONT…….
Common causes of magnetic anomalies include dykes,
faults and lava flows.
Where the rocks have high magnetic susceptibility, the
local magnetic field will be strong; where they have low
magnetic susceptibility, it will be weaker.
Magnetic gradient anomalies generally give a better
definition of shallow buried features such as buried
tanks and drums, but are less useful for investigating
large geological features.
Sedimentary rocks generally have a very small magnetic
susceptibility compared with igneous or metamorphic
rocks, which tend to have a much higher magnetite
content.
35. MAGNETIC METHOD CONT…….
• INSTRUMENTATION
A magnetometer is a more complex instrument which
measures both the orientation and strength of a magnetic
field.
Magnetometer surveys measure small, localised variations in
the Earth's magnetic field.
Magnetometers are highly accurate instruments, allowing
the local magnetic field to be measured to accuracies of
0.002%.
There are several types of instruments on the market but the
common ones used for commercial applications are the
Proton precession, Fluxgate, Caesium vapour and
Gradiometer magnetometer systems.
36. MAGNETIC METHOD CONT…….
Planning of magnetic survey
Once you have considered all the factors as to the type of
magnetometer survey required, then you are ready to
design and lay out a grid to cover the area of interest
A survey grid usually consists of a base line and one or
several tie lines.
The base line serves as a zero reference line for the grid,
and the tie lines serve to correct the skewness of the
survey lines.
From the base line are drawn survey lines perpendicular
to the base line.
37. MAGNETIC METHOD CONT…….
The following figure below illustrates a typical survey
grid, with base lines at 0 and 40 and survey lines
every two metres.
38. MAGNETIC METHOD CONT…….
DATA ACQUISITION
Ground magnetic measurements are usually made with
portable instruments at regular intervals along more or
less straight and parallel lines which cover the survey
area.
Often the interval between measurement locations
(stations) along the lines is less than the spacing between
lines.
To obtain a representative reading, the sensor should be
operated well above the ground.
In rocky terrain where the rocks have some percentage
of magnetite, sensor heights of up to 4 m have been used
to remove near-surface effects.
39. MAGNETIC METHOD CONT…….
All field readings should be taken twice and the two
readings should differ by no more than 1 nT.
At each station the location, time and reading must be
recorded, as well as any relevant topographic or
geological information and details of any visible or
suspected magnetic sources.
Modern instruments can be linked to a DGPS so that
map coordinates are automatically recorded against the
magnetic reading.
The survey data collected should be corrected at the end
of the survey day or the end of the grid.{see Data
processing in detail}
40. MAGNETIC METHOD CONT…….
DATA PROCESSING
To make accurate magnetic anomaly maps, temporal
changes in the earth’s field during the period of the
survey must be considered.
Normal changes during a day, sometimes called
diurnal drift, are a few tens of nT but changes of
hundreds or thousands of nT may occur over a few
hours during magnetic storms.
Culture noises like buried metal, railroads, pipelines,
bridges and iron fences result error in magnetic data.
There are three ways in which you can remove errors
from magnetic data :
41. MAGNETIC METHOD CONT…….
i. Use a base station magnetometer to record all the
changes in time and then use this data to remove the
change from the readings in the field magnetometer.
This is the most accurate way of doing it, but also it is
more expensive, as two complete instruments are
required.
If time is accurately recorded at both base site and field
location, the field data can be corrected by subtraction of the
variations at the base site.
42. MAGNETIC METHOD CONT…….
ii. Use a tie-point method while doing the total field
survey.
This assumes that the field is changing slowly and evenly
between the first time you measured the value at a station and
the next time you check-in to that station again.
This method is not as accurate as using a base-station, but if
the field is not changing rapidly, it is quite adequate to locate
an anomaly.
Generally the data correction is done automatically while the
survey is carried out in the tie-line mode.
43. MAGNETIC METHOD CONT…….
iii. Perform a vertical gradient survey.
Since you are measuring the rate of change between two
sensors, any changes in the background field will apply to
both sensors and you will not see any of these noise effects.
This technique is quite effective for near-surface anomalies.
Gradiometers measure the magnetic field gradient rather than
total field strength, which allows the removal of background
noise.
44. MAGNETIC METHOD CONT…….
After all corrections have been made, magnetic survey data
are usually displayed as individual profiles (Figure 1) or as
contour maps (Figure 2). Below is a magnetic reading profile
across a dyke
45. MAGNETIC METHOD CONT…….
Magnetic Survey contour map to locate pits containing
buried metallic Containers. Figure 2.
46. MAGNETIC METHOD CONT…….
DATA INTERPRETATION
Data are usually displayed in the form of a contour map
of the magnetic field, but interpretation is often made on
profiles.
From these maps and profiles geoscientists can locate
magnetic bodies (even if they are not outcropping at the
surface), interpret the nature of geological boundaries at
depth, find faults etc.
Like all contoured maps, when the lines are close
together they represent a steep gradient or change in
values.
When lines are widely spaced they represent shallow
gradient or slow change in value.
47. MAGNETIC METHOD CONT…….
A modern technique is to plot the magnetic data as a
color image (red =high, blue=low and all the shades in
between representing the values in between).
When interpreting the aeromagnetic image it is useful to
know that magnetite is found in greater concentrations
in igneous and metamorphic rocks.
Magnetite can also be weathered or leached from rocks
and re-deposited in other locations, such as faults.
In a geothermal environment, this is a very useful
feature as it may indicate the presence of faults, target
for drilling.
49. MAGNETIC METHOD CONT…….
In figure above shows a total field magnetic map from
an area.
The magnetic survey outlined three distinct zones where
the magnetic field ranges from a low of 150 nT (blue
areas) to a high of 500 nT (red areas).
The central part of the grid (blue area) has the lowest
magnetic expression, whereas the areas to the grid north
and grid south (yellows through reds) are more
magnetic.
Generally the magnetic maps are interpreted in terms of
geology therefore on correlating with magnetic map
need to have or know rocks present at the area (or
collect samples).
50. MAGNETIC METHOD CONT…….
Magnetic maps are interpreted in terms of geology.
As low-susceptibility rocks such as limestones show as
areas of low and relatively uniform magnetic fields,
while mafic and ultramafic rocks show as areas of
higher and more variable magnetic fields.
In geophysical displays, deep blues denote the lowest
values, while reds and purples identify the highest
readings.
51. MAGNETIC METHOD CONT…….
APPLICATION OF MAGNETIC METHOD
There are two primary applications for magnetic
measurements:
i. Locating and mapping buried ferrous metals, and
Magnetic measurements can be used for locating and
mapping buried ferrous metals (e.g. waste, drums or
underground structures and utilities).
ii. Mapping geologic structures-Magnetic measurements
can be used for geologic mapping by responding to
the magnetic susceptibility of soil and rock.
52. GRAVITY METHOD
GRAVITY METHOD
Definition
Gravity Survey refer to the survey used to measures the
change of rock density by looking at changes in gravity.
Like all matters, the earth generates gravity field that can
be measured by instrumentation called gravimeter.
The gravimeters are used to precisely measure variations
in the gravity field at different points of the earth.
The strength of the gravitational field is directly
proportional to the density of subsurface materials.
The typical units of gravity field is milligas or gravity
units.
53. GRAVITY METHOD CONT…….
Gravity measurements can be obtained either from
airborne (remote) or ground surveys.
The most sensitive surveys are currently achieved from
the ground.
The force of gravity is not the same all over the world (it
varies from point to point on the Earth).
Things like Mountains, Ocean trenches, tidal
movements, even large buildings, Structures, and
Composition of elements within the Earth’s crust all
cause micro-variation in gravity all over the world.
54. GRAVITY METHOD CONT…….
INSTRUMENTATION
A gravity meter or gravimeter measures the variations in
the earth's gravitational field.
Gravity instruments require careful levelling before a
reading is taken.
This may have to be done manually or it may be
performed by the instrument itself.
The instrument must be placed on solid ground (or a
specially designed plate) so that it does not move or sink.
The common gravimeters on the market are the Worden
gravimeter, the Scintrex and the La Coste Romberg
gravimeter.
55. GRAVITY METHOD CONT…….
The Worden gravimeter is an entirely mechanical and
optical relying only on an AA battery for illuminating
the crosshairs.
The Scintrex Autograv is semi-automated, but although a
bit more expensive, it has been shown to have a higher
stability and experience less tares (a sudden jump in a
gravity reading) over long periods of time.
The Lacoste and Romberg model gravity meter has an
advertised repeatability of 3 microgals (980,000,000
microgals is the Earth's gravitational field) and is one of
the preferred instruments for conducting gravity
surveys in industry.
56. GRAVITY METHOD CONT…….
DATA ACQUISITION
Gravity data acquisition is a relatively simple task that
can be performed by one person or two when
determining location (latitude, longitude and elevation)
of the gravity stations.
Surveys are conducted by taking gravity readings at
regular intervals along a traverse that crosses the
expected location of the target.
Its expected size will determine the distance between
readings (station spacing), with larger station separations
for large target and small separations for small ones.
57. GRAVITY METHOD CONT…….
Obtaining a gravity reading, a horizontal position and
the elevation of the gravity station must be obtained.
Therefore readings are taken by placing the instrument
on the ground and levelling it and this may be automatic
with some instruments, as it is with the Scintrex.
The observed gravity readings obtained from the gravity
survey reflect the gravitational field due to all masses in
the earth and the effect of the earth’s rotation.
Thus the useful gravity values in detailed surveys is to
determine the Earth tide effect as their gravitational
effects may be greater than the gravity field variations
due to the anomalous features being sought.
58. GRAVITY METHOD CONT…….
DATA PROCESSING
The last task of most fieldwork is to determine the
topographic changes and the effects of buildings
surrounding a gravity station.
Both of these effects will be used later in processing the
gravity data.
There are a number of techniques to determine the
elevation changes and these usually involve a
combination of recording elevation changes in the field
and computer computations using digital elevation
models (DEM).
59. GRAVITY METHOD CONT…….
The most common technique is by Hammer where one
records an elevation change in quadrants at set distances
(commonly from 0 to 1000 meters) from the gravity
station.
To interpret gravity data, one must remove all known
gravitational effects not related to the subsurface density
changes.
Each reading has to be corrected for elevation, the
influence of tides, latitude and, if significant local
topography exists, a topographic correction.
60. GRAVITY METHOD CONT…….
Gravity data correction
Because the “weight” of a mass varies with the square of the
distance to the center of the earth, small variations in
elevation of the survey station can greatly affect the
measured value of gravity.
As a result, it is necessary to correct for changes in location
and elevation of the survey stations.
i. Latitude correction
Because the earth rotates, it bulges at the equator, and flattens
at the poles.
Thus gravity is stronger at the poles than at the equator and
increases with increasing in Latitude.
61. GRAVITY METHOD CONT…….
Correction is applied ONLY for relative movement in the N-S
direction.
Correction is added as we move toward the equator and
subtracted as the survey station moves northward.
Latitude correction accounts for rotation and elliptical shape
of the earth.
ii. Free-air correction.
The free-air correction accounts for gravity variations caused
by elevation differences in the observation locations.
Accounts for the 1/r2 decrease in gravity with distance from
the centre of the Earth.
62. GRAVITY METHOD CONT…….
If a station is above the reference datum, the correction is
added to the reading; if the station is below the reference
datum, then the correction is subtracted from the reading.
Free air gravity anomaly is given; gfa = gobs - gn + 0.3086h ;
Where h is the elevation (in meters)
iii. Bouguer correction
The difference between observed gravity (gobs) and theoretical
gravity at any point on the Earth's surface after reducing the
gravity readings to the geoidal surface is known as the
Bouguer gravity anomaly or Bouguer gravity.
63. GRAVITY METHOD CONT…….
This correction accounts for the attraction of material
lying between the station and the reference datum.
The Bouguer correction is {0.04192 x (density of the
intervening material)} per vertical meter.
If the density of the intervening material is the average
rock density of 2.67 grams per cubic centimeter (g/cc)
then the Bouguer correction is 0.112 mgal/meter.
It is applied in the opposite sense to the free air
correction and correction is Subtracted for stations
above the datum and is added for stations below the
datum.
64. GRAVITY METHOD CONT…….
iv. Terrain correction
If the gravity reading is taken on top of a hill, then there is a
deficit of mass on either side of the hill, compared to a
horizontal ground surface.
The figure below need for correction for topography.
65. GRAVITY METHOD CONT…….
The terrain correction is positive regardless of whether
the local topography consists of a mountain or a valley.
Terrain corrections are complex, and, in pre-computer
days, involved enormous amounts of hand calculation.
DATA ANALYSIS AND INTERPRETATION
The final gravity data are usually plotted and contoured
in the same manner as magnetic data.
The grid of gravity values, contour maps or the gravity
profiles can be used to determine the lateral location of
any gravity variations and thus quantify the nature
(depth, geometry, density) of the subsurface feature.
66. GRAVITY METHOD CONT…….
The map generated from gravity data and after
correction is called gravity anomaly map
A gravity anomaly map looks at the difference between
the value of gravity measured at a particular place and
the predicted value for that place.
Gravity anomalies are computed by subtracting a
regional field from the measured field, which result in
gravitational anomalies that correlate with source body
density variations.
Positive gravity anomalies are associated with shallow
high density bodies, whereas gravity lows are associated
with shallow low density bodies.
67. GRAVITY METHOD CONT…….
Thus, deposits of high-density chromite, hematite, and
barite yield gravity highs, whereas deposits of low-
density halite, weathered kimberlite, and diatomaceous
earth yield gravity lows.
Uplifts usually bring denser rocks nearer the surface
and thereby create positive gravity anomalies {denser
rock like-Basalt-Granite-Sandstone}.
Faults that displace rocks of different densities also can
cause gravity anomalies.
Salt domes generally produce negative anomalies
because salt is less dense than the surrounding rocks.
68. GRAVITY METHOD CONT…….
Example of positive and Negative anomaly for anticline
(oil) and salt dome
69. GRAVITY METHOD CONT…….
Contoured data with latitude, free air and Bouguer corrections.
The figure below shows a contour map of gravity data.
The data set has had Latitude, Free air and Bouguer
corrections.
70. GRAVITY METHOD CONT…….
Often gravity results such as these will show a gradual
trend across the area, which will distort local anomalies.
The gradual trend in gravity values can arise from deep
seated geological variations, and can be removed from
the data.
The high gravity at the west end and the low at the east
end both disappear when a linear regional trend is
removed.
Normally such trend removal is carried out by digital
processing.
72. GRAVITY METHOD CONT…….
Sulphide bodies are usually more dense than the host
rocks, and thus yield local high-gravity anomalies.
Graphite, on the other hand, is less dense than sulphides,
and close in density to typical host rocks.
If the survey area is underlain by rocks of different
densities, then gravity can be used to map the
distribution of each rock type.
Where positive anomalies indicate rocks with high
density than crustal average.
Negative anomalies indicate rocks with low density than
the crustal average.
73. GRAVITY METHOD CONT…….
APPLICATION OF GRAVITY METHOD
Typical applications for the gravity profiling include:
i. Mapping karst topography or other subsurface
cavities (natural or man-made)
ii. Map regional geologic structures
iii. Map basement topography and sediment thickness
iv. Exploration for geothermal energy including the
location of heat sources.
74. ELECTROMAGNETIC METHOD
ELECTROMAGNETIC METHOD
Definition
Electromagnetic method provide a means to measure
subsurface electrical conductivity and to identify
subsurface metal objects.
Electrical conductivity is a function of soil and rock type,
porosity and permeability, as well as the composition of
fluids that fill the pore spaces.
Electrical conductivity values are given in units of
milliSiemens/meter (mS/m).
The higher the conductivity, the more current will flow
in the earth for a given electrical field strength.
75. The higher the resistivity, the less current will flow for a
given electrical field strength.
At low frequencies, conductivity and resistivity are
inversely related:
SYSTEM AND OPERATION OF EM
The electromagnetic method consists of Transmitter coil
and Receiver coil.
An AC electric current is applied to a transmitter coil
This generates a primary electromagnetic (EM) field in
the coil or a large loop on surface.
76. This induces small electric currents in the ground,
generating a secondary magnetic field that can be
picked up by a receiver coil. {Please see the illustration
below}.
77. The receiver measures two quantities, the in-phase
component and the quadrature component of the secondary
field, expressed as a percentage of the primary field at the
receiver.
Anomalies from good conductors have large in-phase and
small quadrature components, while weaker conductors
have low in-phase and high quadrature components.
Normally the primary field is much stronger than the
secondary field.
In order to detect the secondary field, a small part of the
primary field is sent from the transmitter via cable to the
receiver, and is used to cancel the primary field at the
receiver, leaving only the secondary field to be detected.
78. Frequency domain electromagnetic methods (FDE)
Measure the electrical conductivity of soil and rock by
measuring the magnitude and phase of an induced
electromagnetic current (ASTM D6639-01).
FDE Provides measurements with depths ranging from a few
feet to 200 feet.
The three common frequency domain electromagnetic
instruments are EM31, EM34, and EM38 as manufactured by
Geonics, Ltd.
79. Time domain electromagnetic (TDEM) methods
Measure the electrical conductivity of soil and rock by
inducing pulsating currents in the ground with a transmitter
coil and monitoring the decay of the induced current over
time with a separate receiver coil (ASTMD6820-02).
The EM47 and EM57 systems manufactured by Geonics, Ltd.
are common TDEM systems.
TDEM penetrate at a depth range of approximately 20 to
3,000 feet.
80. Very Low Frequency (VLF) measurements
These measurements are made by measuring the distortions of
a VLF wave from a distant transmitter.
Distortions of the VLF wave occur due to a local increase in
electrical conductivity usually found within fractures.
The increase in electrical conductivity is a function of the
conductive material, such as water, clay or minerals within
the fracture.
NOTE: Measurements are easily and rapidly made can provide
relatively deep measurements (hundred of feet).
81. EM data is typically collected as point readings of
ground conductivity or in-phase taken at regular
intervals along a survey grid that has been set out over
the site area.
The spacing of the grid-lines and reading stations is
dependent upon the target size.
Generally smaller targets require closer survey lines and
denser spaced readings.
82. PROCESSING & INTERPRETATION
The site data is recorded on a digital data logger for later
downloading to a PC for post-survey processing and
interpretation.
The most commonly used interpretation procedure is
contouring, carried out with specialist interactive software to
produce contour plans.
The contoured data is analyzed in detail by experts to identify
anomalous features relative to the general background.
Once identified, the anomalies are correlated with local
ground conditions.
83.
84. APPLICATION OF ELECTROMAGNETIC METHOD
1. Mineral exploration - metallic elements are found in
highly conductive massive sulfide ore bodies.
2. Groundwater investigations - groundwater contaminants
such as salts and acids significantly increase the
groundwater conductivity.
3. Stratigraphy mapping - rock types may have different
conductivities.
4. Geothermal energy - geothermal alteration due to hot
water increases the conductivity of the host rock.
5. Environmental - locate hazards such as drums and tanks.
6. Locating abandoned mineshafts, crown holes & subsidence
features