Page 1 1.1 IntroductIonThe average introductory geolog.docx

Page | 1
1.1 IntroductIon
The average introductory geology student’s perception of
geology normally in-
volves the memorization of rocks and discussions of natural
disasters, but Geology
contains so much more. Geology is the study of our planet,
which is vital to our ev-
eryday lives from the energy we use, to the growing of the food
we eat, to the foun-
dations of the buildings we live in, to the materials that are used
to make everyday
objects (metals and plastics). The ideal place to start this course
is discussing the
methods that are used to better understand our planet, the
processes that shape it,
and its history.
Science is not a set of facts to remember. Instead it is a method
to discover
the world around us. You are likely already familiar with the
Scientific Method,
but it is worthwhile to review the process. The first step of the
scientific method
is making an observation or learning the background
surrounding the question in
which you are interested. This can be done by taking classes on
a subject matter
as you are doing presently in geology or by simply taking
careful notes about your

surroundings. Based on your knowledge and observations, you
can then make a
hypothesis, which is a testable prediction on how something
works. A hypothesis
should be framed in a way that is easy to test and prove wrong.
This might sound
odd, but science works to rigorously disprove a hypothesis and
only those that
withstand the tests become accepted. The wonderful aspect of
this definition of a
hypothesis is that the testing results in a brand new observation
that can then be
used to formulate a new hypothesis. Therefore, whether the
hypothesis is verified
or rejected it will lead to new information. The next step is
communication to other
scientists. This allows other scientists to repeat the experiment
as well as alter it in
new and unthought-of ways that can then expand on the original
idea. These few
steps encompass the vast majority of the scientific method and
the career of any
individual scientist. As hundreds of related observations and
tested hypotheses
accumulate scientists can formulate a theory. The scientific
meaning of a theory is
an explanation for a natural phenomenon that is supported by a
wealth of scientific
1 Introduction to Physical GeologyBradley Deline
Page | 2
Introductory GeoloGy IntroductIon to physIcal GeoloGy

data. A theory is not yet a law because there still may be some
debate on the exact
workings of the theory or the reasons why a phenomenon
occurs, but there is little
debate on the existence of what is being described.
This leads us back to Geology, the scientific study of the Earth.
There are as-
pects in geology that are directly testable, but others are not and
geologists must
become imaginative in discovering aspects about the earth and
its history that we
will never be able to directly observe. In this laboratory manual
we will discuss the
materials that make up the earth (Minerals and Rocks), earth
processes both deep
inside the earth (Folds and Faults) and on its surface (Rivers
and Climate), as well
as the theory that helps explain how the earth works (Plate
Tectonics). A funda-
mental aspect of understanding the Earth is a grasp of Geologic
Time (the subject
of the first chapter), which helps us think about the rate and
frequency of geologic
events that have formed the planet that we know today.
1.1.2 Learning outcomes
After completing this chapter, you should be able to:
• Discuss the importance of time in the study of Geology
• Discuss the difference between Relative Time and Absolute
Time
• Apply Geologic Laws in the relative dating of geologic events
• Use fossils to date a rock unit
• Use ideas behind radiometric dating to date rock units

1.1.3 Key terms
1.2 GeoLoGIc tIme
The amount of time that is involved in the carving of the
landscape, the forma-
tion of rocks, or the movement of the continents is an important
scientific ques-
• Absolute Dating
• Angular Unconformity
• Carbon-14 Dating
• Daughter Atom
• Disconformity
• Geologic Laws
• Geologic Time Scale
• Half-life
• Index Fossils
• Isotope
• Law of Cross-Cutting
• Law of Faunal Succession
• Law of Original Horizontality
• Law of Superposition
• Nonconformity
• Parent Atom
• Potassium-Argon Dating
• Radiometric Dating
• Relative Dating
• Unconformity
• Uranium Dating
Page | 3

tion. Different hypotheses about the age of the earth can
essentially change our
perspective of the workings of geologic events that molded the
Earth. If the geolog-
ic time is relatively short then catastrophic events would be
required to form the
features we see on the surface of the earth, whereas a vast
amount of time allows
the slow and steady pace that we can easily observe around us
today.
Geologists have used many methods attempting to reconstruct
geologic time
trying to map the major events in earth’s history as well as their
duration. Scientists
studying rocks were able to piece together a progression of
rocks through time to
construct the Geologic Time Scale (Figure 1.1). This time scale
was constructed
by lining up in order rocks that had particular features such as
rock types, environ-
mental indicators, or fossils. Scientists looked at clues within
the rocks and deter-
Figure 1.1 | The geologic time scale. Ma, Million years, K. Yr,
Thousand years
Author: Bradley Deline
Source: Original Work
License: CC BY-SA 3.0
Page | 4

mined the age of these rocks in a comparative sense. This
process is called Relative
Dating, which is the process of determining the comparative age
of two objects or
events. For example, you are younger than your parents. It
doesn’t matter your age
or your parents as long as you can establish that one is older
than the other. As time
progressed, scientists discovered and developed techniques to
date certain rocks as
well as the Earth itself. They discovered the earth was billions
of years old (4.54 bil-
lion years old) and put a time frame to the geologic time scale.
This process is called
Absolute Dating, which is the process of determining the exact
amount of time
that has passed since an object was formed or an event
occurred.
Both absolute and relative dating have advantages and are still
frequently used
by geologists. Dating rocks using relative dating allows a
geologist to reconstruct
a series of events cheaply, often very quickly, and can be used
out in the field on a
rocky outcrop. Relative dating also can be used on many
different types of rocks,
where absolute dating is restricted to certain minerals or
materials. However, ab-
solute dating is the only method that allows scientists to place
an exact age to a
particular rock.

1.2.1 relative time and Geologic Laws
The methods that geologists use to establish relative time scales
are based on
Geologic Laws. A scientific law is something that we
understand and is proven. It
turns out that, unlike math, it is hard to prove ideas in science
and, therefore,
Geologic Laws are often easy to understand and fairly simple.
Before we discuss
the different geologic laws, it would be worthwhile to briefly
introduce the differ-
ent rock types. Sedimentary rocks, like sandstone, are made
from broken pieces
of other rock that are eroded in the high areas of the earth,
transported by wind,
ice, and water to lower areas, and deposited. The cooling and
crystallizing of mol-
ten rock forms igneous rocks. Lastly, the application of heat and
pressure to
rocks creates metamorphic rocks. This distinction is important
because these
three different rock types are formed differently and therefore,
need to be inter-
preted differently.
The Law of Superposition states that
in an undeformed sequence of sedimentary
rocks the oldest rocks will be at the bottom
of the sequence while the youngest will be
on top. Imagine a river carrying sand into an
ocean, the sand will spill out onto the ocean
floor and come to rest on top of the seafloor.
This sand was deposited after the sand of the
seafloor was already deposited. We can then
create a relative time scale of rock layers

from the oldest rocks at the bottom (labeled
#1 in Figure 1.2) to the youngest at the top of
an outcrop (labeled #7 in Figure 1.2).
Figure 1.2 | Block diagram showing the
relative age of sedimentary layers based
on the Law of Superposition.
Page | 5
The Law of Original Horizontality states that undeformed
sedimentary
rock are deposited horizontally. The deposition of sediment is
controlled by gravi-
ty and will pull it downward. If you have muddy water on a
slope, the water will
flow down the slope and pool flat at the base rather than
depositing on the slope
itself. This means that if we see sedimentary rock that is tilted
or folded it was first
deposited flat, then folded or tilted afterward (Figure 1.3).
The Law of Cross-Cutting
states that when two geologic fea-
tures intersect, the one that cuts
across the other is younger. In es-
sence, a feature has to be present
before something can affect it. For
example, if a fault fractures through

a series of sedimentary rocks those
sedimentary rocks must be older
than the fault (Figure 1.4).
One other feature that can be
useful in building relative time
scales is what is missing in a se-
quence of rocks. Unconformi-
ties are surfaces that represent
significant weathering and ero-
sion (the breakdown of rock and
movement of sediment) which re-
sult in missing or erased time.
Erosion often occurs in elevated
areas like continents or moun-
tains so pushing rocks up (called
uplifting) results in erosion and
destroying a part of a geologic se-
quence; much older rocks are then
exposed at the earth’s surface. If
the area sinks (called subsidence),
then much younger rocks will be
deposited overtop of these newly
exposed rocks. The amount of
time missing can be relatively
short or may represent billions of
years. There are three types of unconformities based on the
rocks above and below
the unconformity (Figure 1.5). If the type of rock is different
above and below the
unconformity it is called a Nonconformity. For example,
igneous rock formed
deep in the earth is uplifted and exposed at the surface then
covered with sedimen-
tary rock. If the rocks above and below the erosion surface are
both sedimentary,

Figure 1.3 | Sedimentary rocks are deposited horizontally
such that if the layers are tilted or folded it must have occurred
following deposition.
Figure 1.4 | Block diagrams showing the Law of Cross-Cutting.
In both instances on the right the geological features (fault or
Igneous intrusion) cut across the sedimentary layers and must
then be younger.
Page | 6
then the orientation of the layers is important. If the rocks
below the erosion sur-
face are not parallel with those above, the surface is called an
Angular Uncon-
formity. This is often the result of the rocks below being tilted
or folded prior to
the erosion and deposition of the younger rocks. If the rocks
above and below the
erosion surface are parallel, the surface is called a
Disconformity. This type of
surface is often difficult to detect, but can often be recognized
using other informa-
tion such as the fossils discussed in the next section.

Figure 1.5 | Block diagrams showing the formation of the three
types of Unconformities. The
three unconformities differ based on the type of rock underneath
the erosion surface.
Page | 7
Using these principles we can look at a series of rocks and
determine their rel-
ative ages and even establish a series of events that must have
occurred. Common
events that are often recognized can include 1) Deposition of
sedimentary layers, 2)
Tilting or folding rocks, 3) Uplift and erosion of rocks, 4)
Intrusion of liquid mag-
ma, and 5) Fracturing of rock (faulting). Figures 1.6 and 1.7
show how to piece to-
gether a series of geologic events using relative dating.
Figure 1.6 | An example showing how to determine a relative
dating sequence of events from a block
diagram.
Page | 8

Figure 1.7 | An example showing how to determine a relative
dating sequence of events from a
block diagram.
Page | 9
1.3 LAb exercISe
Part A – relative time
Relative time is an important tool for ge-
ologist to quickly construct series of events,
especially in the field. In the following sec-
tion, apply what you have learned regarding
relative time to the questions below.
1. In Figure 1.8, which of the following rock
layers is the oldest?
a. A b. B c. C
2. Which Geologic Law did you use to come to the conclusion
you made in the
previous question?
a. The Law of Superposition b. The Law of Cross-Cutting

c. The Law of Original Horizontality d. Unconformities
3. In Figure 1.9, which of the following geologic structures is
the youngest?
a. A b. B c. C
Figure 1.8 | Block diagram to use to
answer questions 1 and 2.
Figure 1.9 | Block diagram to use to answer questions 3, 4, and
5. Unconformities are
shown in brown.
Page | 10
you made in the
previous question?
5. Examine unconformities 1 and 2 indicated in Figure 1.9.
Which of the following
statements about them is true?

a. The older unconformity is a Nonconformity, while the
younger is an Angular Unconformity.
b. The older unconformity is a Disconformity, while the
younger is a Nonconformity.
c. The older unconformity is a Nonconformity, while the
younger is a Disconformity.
d. The older unconformity is an Angular Unconformity, while
the younger is a Disconformity.
6. Examine the Unconformity shown in Figure 1.10. What type
of unconformity
is this?
a. Angular Unconformity
b. Nonconformity
c. Disconformity
Figure 1.10 | Block diagram to use to
answer question 6.
Page | 11
Examine Figure 1.11. Note that all of the layers in this block

diagram are com-
posed of sedimentary rock and the unconformities are colored in
red. Using the
geologic laws discussed earlier and following the examples
shown in Figures 1.6
and 1.7, identify the geologic events that occurred in this area.
Then place the fol-
lowing geologic events in the correct relative time sequence.
a. Tilting.
b. Uplift and Erosion (Angular Unconformity).
c. Submergence and deposition of sedimentary layers 10-13.
d. Uplift and Erosion to current position.
e. Submergence and Deposition of sedimentary layers 7-9.
f. Uplift and Erosion (Disconformity)
g. Submergence and deposition of sedimentary layers 1-6.
h. Fault.
Figure 1.11 | Block diagram to use to answer questions 7, 8,
and 9. Unconformities are shown in red.
Page | 12

7. Which of the above geologic events is the second in the
sequence?
a. A b. B c. C d. D
e. E f. F g. G h. H
8. Which of the above geologic events is the fifth in the
sequence?
a. A b. B c. C d. D
e. E f. F g. G h. H
9. Which of the above geologic events is the seventh in the
sequence?
a. A b. B c. C d. D
e. E f. F g. G h. H
1.4 FAunAL SucceSSIon And Index FoSSILS
Another useful tool in relative dating are fossils. Fossils are the
preserved re-
mains of ancient organisms normally found within sedimentary
rocks. Organisms
appear at varying times in geologic history and go extinct at
different times. These
organisms also change in appearance through time. This pattern
of the appear-
ance, change, and extinction of thousands of fossil organisms
creates a recogniz-
able pattern of organisms preserved through geologic time.
Therefore, rocks of the

same age likely contain similar fossils and we can use these
fossils to date sedimen-
tary rocks. This concept is called the Law of Faunal Succession.
Some fossils are particularly useful in telling time, these are
called Index Fos-
sils. These are organisms that we are likely to find because they
were abundant
when they were alive and were likely to become fossils (for
example, having a ro-
bust skeleton). These organisms often have a large geographic
range so they can be
used as an index fossil in many different areas. However, they
should also have a
short geologic range (the amount of time an organism is alive
on Earth), so we can
be more precise in the age of the rock if we find the fossil.
Index fossils are often
the quickest and easiest way to date sedimentary rocks precisely
and accurately.
Page | 13
1.5 LAb exercISe
Part b – Faunal Succession
The use of animals and their preserved remains (fossils) can
help build a high-
ly precise time sequence, often with a higher resolution than
absolute dating. In
the following section, use this principle to answer the following
questions.

Figure 1.12
Page | 14
10. Based on the assemblage of organisms (A-I) in this sample,
what is the age of
this rock?
a. Economy b. Southgate c. McMicken d. Mt. Hope
e. Fairmount f. Bellevue g. Corryville h. Mt. Auburn
11. Which organism was the most useful in coming to this
conclusion (which is the
best index fossil)?
a. Isotelus b. Zygospira c. Cyclonema d. Vinlandostrophia
e. Parvohallopora f. Cincinnetina g. Streptaster h. Ambonychia
12. Which organism was the least useful in coming to this
worst index fossil)?

1.6 AbSoLute tIme And rAdIometrIc dAtInG
Absolute time is a method for determining the age of a rock or
object most often
using radiometric isotopes. Atoms are made of three particles,
protons, electrons,
and neutrons. All three of these particles are important to the
study of geology: the
number of protons defines a particular element, the number of
electrons control how
that element bonds to make compounds, and the number of
neutrons changes the
atomic weight of an element. Isotopes are atoms of an element
that differ in the
number of neutrons in their nucleus and, therefore, their atomic
weight. If an ele-
ment has too many or too few neutrons in its nucleus then the
atom becomes unsta-
ble and breaks down over time, which is called radioactive
decay. The process of
radioactive decay involves the emitting of a particle from a
radioactive atom, called
the parent atom, which changes it to another element, called the
daughter at-
om. We can study and measure the radioactivity of different
elements in the lab and
calculate the rate of decay. Though the rate of decay varies
between isotopes from
milliseconds to billions of years, all radiometric isotopes decay
in a similar way. Ra-
diometric decay follows a curve that is defined by a radiometric
isotope’s half-life.
The half-life is defined as the amount of time it takes for half of
the atoms of the
radiometric parent isotope to decay to the daughter. The half-
life is independent of

the amount of atoms at a given time so it takes the same amount
of time to go from
100% of the parent isotope remaining to 50% as it does to go
from 50% of the parent
isotope remaining to 25%. If we know the length of the half-life
for a particular radio-
Page | 15
metric isotope and we measure the amount of parent and
daughter isotope in a rock,
we can then calculate the age of the rock, which is called
Radiometric Dating.
Given the shape of the decay curve, a material never runs out of
the parent isotope,
but we can only effectively measure the parent up to 10-15 half-
lives.
1.7 LAb exercISe
Part c – radiometric dating
Complete the following chart by calculating the amount of
parent isotope remain-
ing for all of the given half-lives, then plot your findings on the
graph (Figure 1.13).
Make sure you connect the data points on the graph by drawing
in the decay curve.
Use the completed chart and graph to answer the questions
below.
13. How much of the parent isotope would be remaining after 7

half-lives have passed?
a. 6.25% b. 1.56% c. 0.78% d. 0.39%
14. If a radiometric element has a half-life of 425 years, how
old would a rock be
that only had 3.125% of the parent isotope remaining?
a. 2125 years b. 1700 years c. 2550 years d. 3400 years
Figure 1.13
Page | 16
15. Based on your graph above, approximately how much of the
parent isotope
would be remaining after 3.5 half-lives?
a. 16% b. 12% c. 4% d. 8%
16. Based on your graph above, approximately how many half-
lives have passed
when only 35% of the parent isotope is remaining?
a. 0.75 b. 1.5 c. 2.1 d. 2.5
1.8 dAtInG SyStemS

There are several different radiometric isotopes that are
commonly used in
absolute dating. Each of these systems have different uses
within geology in that
they require different materials and can date objects within
specific time frames.
Carbon-14 dating is of limited use within geology, but is still
the system that
is familiar to most people. Carbon-14 (parent isotope) is found
in organic material
including bone, tissue, plants, and fiber. This isotope is found
naturally in small
amounts in the atmosphere within CO2 and is incorporated into
plants during pho-
tosynthesis and then filters throughout the food chain. You
currently have Car-
bon-14 in your body that is decaying to Nitrogen-14 (daughter
isotope), but you
replace it whenever you eat. When an animal stops eating or a
plant stops photosyn-
thesizing, the radioactive carbon starts to decay without being
replaced, which can
be easily measured. Carbon-14 has a very short half-life of
5,730 years and can only
be used to date materials up to approximately 70,000 years.
Given the age of the
Earth is 4.54 billion years, carbon-14 can only be used to date
very recent materials.
Uranium dating involves a complex system of multiple isotopes
that decay
through a chain reaction until it reaches non-radiogenic lead.
Surprising to most
students, uranium can be found in many places, but it is

normally in very miniscule
amounts. Another issue with this system is that the daughter
isotope, lead, is also
found naturally in many different places, which makes it
difficult to differentiate
between lead formed from radiometric decay and lead found
naturally in the envi-
ronment. The mineral zircon solves both of these issues, by
concentrating uranium
and excluding lead from its mineral structure. Therefore, we use
Uranium dating on
zircons found within igneous rocks (such as volcanic ash or
rocks formed deep in the
earth). Uranium has a very long half-life of 4.5 billion years,
which is more than long
enough to date most rocks on Earth. It takes about one million
years for the complex
system to normalize such that Uranium dates of less than that
are unreliable.
Potassium-Argon dating is also a useful method of dating rocks.
Potassium
decays into two separate daughter isotopes, Argon and Calcium.
We measure the
amount of Argon in the rocks because unlike calcium it is rare
within minerals
since it is a Noble Gas and doesn’t normally bond with other
elements. Therefore,
any argon within a mineral is from the decay of potassium. The
use of Argon also
Page | 17

has its drawbacks, for instance a gas can easily escape from a
rock and, therefore,
special care needs to be taken in the lab to prevent this. This
system works well
when there are multiple materials to examine that contain
abundant potassium,
like the rock granite that is full of potassium-rich pink minerals
called feldspars.
The half-life of Potassium is 702 million years, so it is similar
to Uranium in that it
is most useful dating older rocks.
With all of these methods there is still the chance for error such
that it is best to
think of any particular radiometric date as a scientific
hypothesis that needs to be
further tested. Error can come from the addition or subtraction
of either parent or
daughter isotopes in the rock following its formation. This can
be done in several
ways, most commonly through the adding of heat and pressure
(metamorphism).
There are ways to correct for these issues that allows the
scientist to date both the
rock and the metamorphic event as long as the geologic history
is known.
As you may have guessed from the previous exercise, it is rare
to find a rock
that contains an amount of the parent remaining that falls
exactly on one of the
half-lives. In most cases we need to use a simple formula to
calculate the age of a
rock using the length of the half-life and the amount of parent
remaining.

The formula is:
�
1/ 2t = The length of the half-life in years
P = The amount of the parent remaining in decimal form. For
example, if there
is 50% of the parent remaining it would equal 0.5.
Let’s work an example using the equation that we already know
the answer to in
advance. You have a sample of bone that has 25% of the
Carbon-14 (Half-life= 5730
years) remaining, how old is the sample? We can answer this
question in two ways:
1. We know that if there is 25% remaining, two half-lives have
passed and
with each half-life being 5730 the bone would be 11,460 years
old.
2. We could use the above equation and insert both the length of
the half-
life and the amount of the parent remaining:
To solve the equation, take the Natural Log (ln) of 0.25 and
multiply by the
term in the parentheses (make sure to include the negative sign).
If you do this you
will get 11,460 as well.

0.693
)ln(P)
5730
0.693
)ln(0.25)
Page | 18
1.9 LAb exercISe
Part d – Isotopic Systems
Using what you learned in the previous section regarding
absolute dating, de-
termine the most appropriate methods and the ages of the
materials in the follow-
ing questions.
17. An Archeologist finds some cotton cloth at a burial site and
wants to determine
the age of the remains. Which isotopic system should they use?
a. Carbon-14 b. Uranium c. Potassium-Argon
18. The Archeologist determines that there is 16.7% of the
parent isotope remaining
in the cloth sample. How old is the burial site? Hint: you can

find the length of
the half-life in the reading above.
a. 13,559 years b. 14,798 years c. 16,743 years
d. 1.66 billion years e. 1.81 billion years f. 2.05 billion
19. A geologist is trying to date a sequence of sedimentary
rocks with abundant
fossils and sandstones. Within the sequence is a distinctive clay
layer that
under closer inspection is fine-grained volcanic ash. Which of
the following is
the best way to obtain an absolute date for the sequence of
rocks?
a. Carbon date the fossils b. Potassium-Argon date the sands
c. Uranium date the Zircons in the ash d. Identify the index
fossils
20. The geologist determines there is 78.3% of the parent
remaining in the sample
that they examine. How old is the sequence of rocks? Hint: you
can find the
length of the half-life in the reading above.
a. 187.5 million years b. 247.8 million years c. 390.7 million
years
years
Page | 19

1.10 Student reSPonSeS
The following is a summary of the questions in this lab for ease
in submitting
answers online.
1. In Figure 1.8, which of the following rock layers is oldest?
a. A b. B c. C
you made in the
previous question?
youngest?
a. A b. B c. C
you made in the
previous question?

of unconformity
is this?
a. Angular Unconformity b. Nonconformity c. Disconformity
Page | 20
sequence?
a. A b. B c. C d. D
e. E f. F g. G h. H
sequence?
a. A b. B c. C d. D

e. E f. F g. G h. H
sequence?
a. A b. B c. C d. D
e. E f. F g. G h. H
what is the age of
this rock?
best index fossil)?

a. 6.25% b. 1.56% c. 0.78% d. 0.39%
Page | 21
old would a rock be
parent isotope
a. 16% b. 12% c. 4% d. 8%
lives have passed
a. 0.75 b. 1.5 c. 2.1 d. 2.5
wants to determine
a. Carbon-14 b. Uranium c.Potassium-Argon

find the length of
rocks with abundant
layer that
the following is
rocks?
fossils
can find the
years
years

Page | 19
1.10 Student reSPonSeS
The following is a summary of the questions in this lab for ease
in submitting
answers online.
1. In Figure 1.8, which of the following rock layers is oldest?
a. A b. B c. C
you made in the
previous question?
youngest?
a. A b. B c. C
you made in the
previous question?

of unconformity
is this?
a. Angular Unconformity b. Nonconformity c. Disconformity
Page | 20
sequence?
a. A b. B c. C d. D
e. E f. F g. G h. H

sequence?
a. A b. B c. C d. D
e. E f. F g. G h. H
sequence?
a. A b. B c. C d. D
e. E f. F g. G h. H
what is the age of
this rock?
best index fossil)?

a. 6.25% b. 1.56% c. 0.78% d. 0.39%
Page | 21
old would a rock be
parent isotope
a. 16% b. 12% c. 4% d. 8%
lives have passed
a. 0.75 b. 1.5 c. 2.1 d. 2.5
wants to determine

a. Carbon-14 b. Uranium c.Potassium-Argon
find the length of
rocks with abundant
layer that
the following is
rocks?
fossils
can find the
years

years

Page 1 1.1 IntroductIonThe average introductory geolog.docx

More Related Content

Similar to Page 1 1.1 IntroductIonThe average introductory geolog.docx (20)

More from alfred4lewis58146 (20)

Recently uploaded (20)

Page 1 1.1 IntroductIonThe average introductory geolog.docx