Geological Interpretation of Reflection Seismic Data

Al-Azhar University Assiut Branch Faculty of Science Geology Department

Research on

The Geological Interpretation of Reflection Seismic Data Prepared by

1. Abdelrhman Mohammed Abdelftah 2. Ahmed Abdelhamed Ali 3. Ahmed Mahmoud Abdelsalam Essay Submitted for Partial Fulfillment of Requirements for B.Sc in Geology

Under supervisor

Dr. AbdelSattar A. Abdellatief Lecturer of Applied Geophysics 2008/2009

Acknowledgements Firstly thanks to "ALLAH" who give us the health and life to finish up this work. We’re grateful to the people who helped with this Research, and to the students and colleagues who have, whether advertently or inadvertently, introduced us to many new learning experiences. We’re particularly grateful to Dr. AbdelSattar for his help. Amid such a mass of small letters, it will not seem surprising that an occasional error of the press should have occurred. But I hope that the number of such errors is small. And special thanks to my parents and my uncle Rabih Elabasere. (Abdelrhman)

ii

Contents Acknowledgements List Of Figures List Of Tables and Boxes Abstract Chapter 1 Introduction 1.1 Introduction 1.2 Milestones in Seismic Industry 1.3 Principle of Seismic Survey 1.4 Modern Seismic Data Acquisition 1.4.1 Land Data Acquisition 1.4.2 Marine Data Acquisition 1.4.3 Transition – Zone Recording 1.5 How Are The Seismic Data Collected? 1.6 What Is The Interpretation Mean? Chapter 2 Fundamentals Of Seismic 2.1 Introduction

ii v vii viii 1 1 1 2 3 3 3 4 4 5 7 7

2.2 The Seismic Wave

7

2.3 Types Of Waves 2.3.1 Compressional Waves (P-waves)

7 7

2.3.2 Shear Waves (S-waves)

8

2.4 Characteristics of Seismic 2.4.1 Reflections

8 8

2.4.2 Critical Reflection

8

2.4.3 Refractions

8

2.4.4 Diffractions

9

2.4.5 Multiples

9

2.4.6 Seismic Noise

9

2.5 Seismic velocities

10

2.6 Seismic Receivers

12

2.6.1 Geophones

12

2.6.2 Hydrophones

13

2.6.3 Dual Sensors

13

2.7 Seismic Data Processing

13

2.7.1 Migration

14

Contents

2.8 Seismic Sections Chapter 3 Steps Of Interpretation Seismic Data 3.1 Introduction 3.2 Identification Of Reflections (Tracing)

14 17 17 18

3.3 Picking And Correlation Of Reflections

18

3.3.1 Correlations 3.4 Continuity 3.5 Unconformities and Seismic Facies Patterns 3.6 Naming

19 20 21 22

3.7 Fault Pattern Determination

22

3.8 Hydrocarbon Indicators

22

3.9 Mapping

24

3.9.1 Construction Of Two-Way Time Map 3.9.2 Construction Of Structural Cross-Sections 3.9.3 Contour Maps 3.9.3.1 Construction Of Geo-Seismic Structural Contour Map 3.9.3.2 Construction Of Isopach Maps Chapter 4 Reflection Data Over Geologic Structures 4.1 Introduction

24 24 24 24 24 25 25

4.2 Anticlines

26

4.3 Faults

27

4.4 Diapirism And Salt Domes

29

4.5 Basement Structure

31

4.6 Pitfalls In Structural Interpretation 4.6.1 Velocity Pitfalls 4.6.2 Geometrical Pitfalls Chapter 5 Example Study Evaluation Of Matruh Basin 5.1 Geological Background 5.2 Basin Analysis 5.3 Seismic Data 5.4 Structural Interpretation 5.4.1 Fault Pattern Interpretation 5.5 Summary And Conclusions Bibliography

32 33 35 36 36 37 38 43 47 47 50 52

List of Figures Fig. 1.1

Sketch of rays reflected from a bed to receiver

5

2.1

Histogram of seismic wave velocities of various classes of rocks (after Grant and West, 1965)

12

2.2

Terminology of wiggles

16

2.3

Vertical trace

16

3.1

Parallel other reflection

21

4.1

Most type of reservoirs and traps

26

4.2 (a)

Anticline from San Joaquin Valley, Calif.: (a) section as automatically migrated by computer;

26

4.2 (b)

(b) immigrated section. The migration has collapsed the 27 many diffraction patterns that concealed the actual structure. (Geocom,Inc.)

4.3

Pattern of faulting

28

4.4

Example of Salt Dome.

30

4.5

Basement effect in a deep-sea area

31

4.6

Identification of basement surface from diffraction patterns on section along traverse In deep water.

32

(United Geophysical Corp, proprietary data.) 4.7

Distortion of sedimentary layers due to forces associated 34 with salt-dome buoyancy. Some of the structures shown, e.g., those below the piercement-type salt dome and salt pillows (like the deep one on the right) are not real but result from velocity effects. (Exxon, Inc.)

4.8

"Anticline" cased by thrusting of high-velocity material over 34 monoclinal layers. Markings on lower section indicate interpreted structure. (From Tucker and Yorston.8)

4.9

Bow-tie effect observed over sharp syncline in the Adriatic Sea. Apparent anticline is actually a diffraction feature.(Geocom, Inc.)

v

35

List of Figures 5.1

Location map of the study area

36

5.2

Basment tectonic map of the north Western Desert of Egypt (Modified after Sultan and Halim, 1988).

37

5.3

The subbasins constituting the northren Western Desert Basin (Modified after Sultan and Halim, 1988).

37

5.4

Isopach map of Bahariya Formation. Matruh Basin, North Western Desert, Egypt (C. I.=50 ft)

40

5.5

Isopach map of Kharita Formation. Matruh Basin, North Western Desert, Egypt (C. I.=200 ft)

40

5.6

Structure contour map of Bahariya Formation. Matruh Basin, North Western Desert, Egypt. Arrows refer to possible hydrocarbon migration pathway (C. I.=200 ft)

41

5.7

Structure contour map of Kharita Formation. Matruh Basin, 41 North Western Desert, Egypt. Arrows refer to possible hydrocarbon migration pathway (C. I.=200 ft)

5.8

Sand to shale ratio map of Bahariya Formation. Matruh Basin, North Western Desert, Egypt.

42

5.9

Sand to shale ratio map of Kharita Formation. Matruh Basin, North Western Desert, Egypt.

42

5.10

Location the seismic lines

43

5.11

Line "q" in the original 3D seismic volume (before applying any intrpretation steps).

44

5.12

Line "f" in the original 3D seismic volume (before applying any intrpretation steps).

45

5.13

Line "k" in the original 3D seismic volume (before applying any intrpretation steps).

46

5.14

Interpreted line number "f"

48

5.15

Interpreted line number"k"

49

5.16

Interpreted part of line number"q"

50

vi

List of Tables Table.

Page

2.1

Average values approximating measurements on polycrystalline bodies

10

2.2

velocities in non-porous sedimentary rocks

11

2.3

Velocity in Porous Rock filled by fluids

11

5.1

Stratigraphic column of matruh basin, Egypt (Modified after Medoil, 1983).

38

5.2

Lithologic constituents of Bahariya and Kharita 39 formations. Matruh Basin, North Western Desert, Egypt.

List of Boxes Box. 2.1

Why Processing?

13

Box. 3.1

Tips for Correlation

19

vii

Abstract This research consists of all these aspects in a brief. Starting from the introduction to the seismic methods in Chapter 1, in Chapter 2, I tried to give a brief introduction about the basics of the different types of waves, and fundamental of seismic data and it's definition like multiples, processing, etc. The next Chapter 3 deals with the steps of geological interpretation to seismic data. Chapter 4 is about the structure interpretation especially the common traps and reservoirs. Where I described pitfalls in structure interpretation. In Chapter 5 i give example study of the interpretation technique from Ph.D explained basic data and aid data used to complete the interpretation. The geophysical method that provides the most detailed picture of subsurface geology is the seismic survey. This involves the natural or artificial generation and propagation of seismic (elastic) waves down into Earth until they encounter a discontinuity (any interruption in sedimentation) and are reflected back to the surface. On-land, seismic “shooting” produces acoustic waves at or near the surface by energy sources such as dynamite, a “Thumper” (a weight dropped on ground surface), a “Dinoseis” (a gas gun), or a “Vibroseis” (which literally vibrates the earth’s surface). Electronic detectors called geophones then pick up the reflected acoustic waves. The signal from the detector is then amplified, filtered to remove excess “noise”, digitized, and then transmitted to a nearby truck to be recorded on magnetic tape or disk. In the early days of offshore exploration, explosive charges suspended from floats were used to generate the necessary sound waves. This method is now banned in many parts of the world because of environmental considerations. One of the most common ways to generate acoustic waves today is an air gun. Air guns contain chambers of compressed gas. When the gas is released under water, it viii

makes a loud “pop” and the seismic waves travel through the rock layers until they are reflected back to the surface where they are picked up by hydrophones, the marine version of geophones, which trail behind the boat. The data recorded on magnetic tape or disk can be displayed in a number of forms for interpretation and research purposes; including visual display forms (photographic and dry paper), a display of the amplitude of arriving seismic waves versus their arrival time, and a common type of display called variable density. The variable-density display is generated by a technique in which light intensity is varied to enhance the different wave amplitudes. For example, low amplitude waves are unshaded and higher amplitude waves are shaded black, thus strong reflections will show up as a black line on the display. Seismic waves travel at known but varying velocities depending upon the kinds of rocks through which they pass and their depth below Earth’s surface. The speed of sound waves through the earth’s crust varies directly with density and inversely with porosity. Through soil, the pulses travel as slowly as 1,000 feet per second, which is comparable to the speed of sound through air at sea level. On the other hand, some metamorphic rocks transmit seismic waves at 20,000 feet (approximately 6 km) per second, or slightly less than 4 miles per second. Some typical average velocities are: shale = 3.6 km/s; sandstone = 4.2 km/s; limestone = 5.0 km/s. If the subsurface lithology is relatively well known from drilling information, it is possible to calculate the amount of time it takes a wave to travel down through the earth to a discontinuity and back to the surface. This information is used to compute the depth of the discontinuity or unconformity. However, the only way of accurately determining depth is by correlating seismic sections to wireline logs. Reflections are generated at unconformities because unconformities separate rocks having different structural attitudes or physical properties, particularly different lithologies. These principles form the basis for application of seismic methods to geologic study. ix

Chapter 1

Introduction 1.1 Introduction The seismic method is one of the geophysical methods of prospecting It has three important/principal applications: a. Delineation of near-surface geology for engineering studies, and coal and mineral exploration within a depth of up to 1km: the seismic method applied to the near surface studies is known as engineering seismology. b. Hydrocarbon exploration and development within a depth of up to 10 km: seismic method applied to the exploration and development of oil and gas fields is known as exploration seismology. c. Investigation of the earth’s crustal structure within a depth of up to 100 km: the seismic method applies to the crustal and an earth quake study is known as earthquake seismology. Definition by Robert E. Sheriff: Seismic survey is a program for mapping geologic structure by observation of seismic waves, especially by creating seismic waves with artificial sources and observing the arrival time of the waves reflected from acoustic impedance contrasts or refracted through high velocity members. 1.2 Milestones in Seismic Industry As the search for oil moved to deeper targets, the technique of using reflected seismic waves, known as the “seismic reflection method”, became more popular during World War II, because it aided delineation of other structural features apart from simple salt domes. During 1960’s the so-called digital revolution ushered in what some historians now are calling the Information Age. This had a tremendous impact on the seismic exploration industry. The ability to record digitized seismic data on magnetic tape, then process that data in a computer, not only greatly improved the productivity of seismic crews 1

but also greatly improved the fidelity with which the processed data imaged earth structure. Modern Seismic Data Acquisition could not have evolved without the digital computer. The late 1970’s saw the development of the 3D seismic survey, in which the data imaged not just a vertical cross-section of earth but an entire volume of earth. The technology improved during the 1980’s, leading to more accurate and realistic imaging of earth. In 1990’s depth section preparation got focused from the prevailing time section preparation after processing the data. In 2000’s data is being acquired with an additional parameter of “time” as the 4th dimension of the existing 3D data acquisition system. This is called 4D data acquisition. As the seismic industry made one breakthrough after another during its history, it also created new challenges for itself. Now we record not just p-waves but also converted s-waves for a wide range of objectives. Using the multi-component seismic method, commonly known as the 4-C seismic method, we are now able to see through gas plumes caused by the reservoir below. We are able to sometimes better image the sub-salt and sub-basalt targets with the 4C seismic method. Using the converted swaves, we are able to detect the oil-water contact, and the top or base of the reservoir unit that we sometimes could not delineate using only pwaves. 1.3 Principle of Seismic Survey Seismic wave are used to give a picture of deep rock structures. The seismic wave travels through the water and strikes the seafloor. Some of the energy of the wave is reflected back to the receivers. The rest of the wave carries on until it reaches another rock layer. The time taken for the waves to travel from the source to the receivers is used to calculate the distance traveled - hence the thickness of the rock layers. The strength of the reflected wave gives information about the density of the reflecting rock. Each time the seismic pulse meets a change in rock properties, for example from a shale to a sand layer, part of the pulse will be reflected back to the surface. This is called an event. By measuring precisely the difference in arrival time of a given event from the nearer and further receivers groups, the velocity of the rock material can be measured. The seismic measurements are made in time, so if the velocity and time are known, geophysicists can work out the depth of the event. In seismic surveys, 2

reflected sound waves, called signals, are combined and interpreted electronically or reproduced on graphic paper recorders. This data gives information on the depth, position and shape of underground geological formations that may contain crude oil or natural gas. 1.4 Modern Seismic Data Acquisition Subsurface geologic structures containing hydrocarbons are found beneath either land or sea. So there is a land data-acquisition method and a marine data-acquisition method. The two methods have a common-goal, imaging the earth. But because the environments differ, so each required unique technology and terminology. 1.4.1 Land Data Acquisition In land acquisition, a shot is fired (i.e., energy is transmitted) and reflections from the boundaries of various Lithological units within the subsurface are recorded at a number of fixed receiver stations on the surface. These geophone stations are usually in-line although the shot source may not be. When the source is in-line with the receivers at either end of the receiver line or positioned in the middle of the receiver line – a two-dimensional (2D) profile through the earth is generated. If the source moves around the receiver line causing reflections to be recorded form points out of the plane of the in line profile, then a three-dimensional (3D) image is possible (the third dimension being distance, orthogonal to the inline receiver-line). The majority of land survey effort is expended in moving the line equipment along and / or across farm fields or through populated communities. Hence, land operations often are conducted only during daylight thus making it a slow process. 1.4.2 Marine Data Acquisition In a marine operation, a ship tows one or more energy sources fastened parallel with one or more towed seismic receiver lines. In this case, the receiver lines take the form of cable called Steamer containing a number of hydrophones. The vessel moves along and fires a shot, with reflections recorded by the streamers. If a single streamer and a single source are used, a single seismic profile may be recorded in like manner to the land operation. If a number of parallel sources and/or streamers are towed at the same time, the result is a number of parallel lines recorded at 3

the same time. If many closely spaced parallel lines are recorded, a 3D data volume is recorded. More than one vessel may be employed to acquire data on 24-hour basis, since there is no need to curtail operations in nights. 1.4.3 Transition – Zone Recording Because ships are limited by the water depth in which they safely can conduct operations, and because land operations must terminate when the source approaches the water edge, or shore lines, transition-zone recording techniques have been developed to provide a continuous seismic coverage required over the land and then into the sea. Geophones that can be placed on the sea bed or used with both marine and land shots fired into them. Techniques have been developed to use both Geophones and hydrophones in the surface area where the shore line / water edge is likely to migrate towards land and sea depending on the tide of sea a day. The combination of such hydrophone / geophones is called a “Dual Sensor”. The advantage of why this is to see that either of the receiver of Dual Sensor pickups the surveyed from the slots recorded using a land or marine source and data gaps all along the coast within the area of prospect. 1.5 How Are The Seismic Data Collected? As the vessel moves along the line, computers control the simultaneous discharge of seismic waves from the sound sources, usually every 10 seconds. The waves travel down through the rock formations. When they encounter a boundary between different formations, some sound waves are reflected back to high-capacity computers, check and store the data collected. The collected data go through several processing steps to improve the quality of the signals and filter out background noise. Geophysicists then interpret the information to develop a detailed picture of the structures and rock formations.

4

Fig. 1.1: Sketch of rays reflected from a bed to receiver 1.6 What Is The Interpretation Mean? The word interpretation has been given many different meanings by geophysicists who handle seismic reflection records and by geologist's who put the information from them to use. To some it is virtually equivalent to data processing and is tied inextricably to computer software. To others it consists of all of the operations we considered as the mechanical transformation of seismic reflection data into a structural picture by the application of corrections, time-depth conversion, and migration. Interpretation can be all of these things, subject to the one inviolable condition that it involves some exercise of judgment based on geological criteria. By this conception, interpretation can begin with planning and programming a seismic reflection survey if they are guided by the geology of the area and by the economic or scientific objectives of the survey. It can involve the choice of field parameters, such as the kind of seismic source to be used, the geometry of source and receiver patterns, and the settings on the panels of the recording instruments, as long as such choices are governed by the geological information desired. The selection of processing procedures and parameters is also an important part of the Interpretation if it is supported by the same considerations. 5

Any purely mechanical operations not requiring discretion on the part of the geophysicist would come under the category of reduction, not interpretation. It is possible to make a seismic map, particularly one in time, without carrying out any real interpretation at all if every stage of its preparation is routine or automatic and no decisions have to be made that involve geological considerations. After a seismic map is constructed, an important part of its interpretation is integrating the seismic data on it with geological information from surface and subsurface sources, e.g., fault traces or geologic contacts. This involves identifying reflections and making ties to wells or surface features. The extent to which this can be done depends on the amount of geologic information available. The computer has made it feasible to use previously unexploited characteristics of seismograms to obtain geological information. Under favorable circumstances, interval velocities can be determined from reflection records with enough precision to permit them to serve as a basis for identifying lithology. Another property of seismic waves that has been employed for studying rock composition is attenuation of seismic-wave amplitudes between successive reflectors, a parameter that can now be measured because of the high dynamic range in modern recording equipment. Thanks to the computer technology.

6

Bibliography Bacon, M., Simm, R., & Redshaw, T. (2003). Geological interpretation. 3-D seismic interpretation. Cambridge, England: Cambridge University Press. Chapman, C. H. (2004). Fundamentals Of Seismic Wave Propagation. Schlumberger Cambridge Research: Cambridge University Press. Coffeen, J. A. (1986). Seismic Exploration Fundamentals. Tulsa, Oklahoma, USA: PennWell Publishing Company. Dobrin, M. B. (1960). Introduction to geophysical prospecting (3th ed.). Singapore: McGraw- Hill Book Company. Gamea, A.S. What do you know about seismic survey? (2009, February). Petroleum Journal: Petroleum Ministry, Egypt. Goulty, N. R. (1997). Lateral resolution of 2D seismic illustrated by a real data example. First Break, 15, 77-80 McQuillin, R., Bacon, M., & Barcly, W. (1979). An Introduction to seismic Interpretation. Graham & Trotman press Othman, W.M. (2007). Evaluate Oil potentiality for Matruh Basin. Applied Geophysics. Ph.D, Faculty of Science: Suez Canal University, Egypt. Talagapu, K. K. (2004). 2D and 3D Land Seismic Data Acquisition and Seismic Data Processing. Andhra Pradesh, India: Geophysics Andhra University. Taner, M . T., Koehler, F & Sheriff R. E. (1979). Complex seismic trace analysis Geophysics, 44, 1041-63. Telford, W. M., Sheriff, R. E. (1980).Reflection Interpretation. Applied Geophysics. pp 260-264 52

‫ﺍﻟﻣﻠﺧﺹ ﺍﻟﻌﺭﺑﻲ‬ ‫ﺍﻟﺗﻔﺳﻳﺭ ﺍﻟﺟﻳﻭﻟﻭﺟﻲ ﻟﻠﺑﻳﺎﻧﺎﺕ ﺍﻟﺳﻳﺯﻣﻳﻪ ﺍﻷﻧﻌﻛﺎﺳﻳﻪ‬ ‫ﻳﻌﺗﺑﺭ ﺍﻟﻣﺳﺢ ﺍﻟﺳﻳﺯﻣﻲ ”‪ “Seismic Survey‬ﻫﻭ ﺍﻟﺧﻁﻭﻩ ﺍﻷﻭﻟﻲ ﻓﻲ ﻋﻣﻠﻳﺎﺕ ﺍﻷﺳﺗﻛﺷﺎﻑ ﻭﺍﻟﺗﻧﻘﻳﺏ‬ ‫ﻋﻥ ﺍﻟﺑﺗﺭﻭﻝ ﻭﻳﻌﺗﺑﺭ ﺣﺟﺭ ﺍﻟﺯﺍﻭﻳﻪ ﻓﻲ ﺗﻠﻙ ﺍﻟﻌﻣﻠﻳﺎﺕ‪ ،‬ﻭﻓﻛﺭﻩ ﺍﻟﻣﺳﺢ ﺍﻟﺳﻳﺯﻣﻲ ﻫﻲ ﺭﺅﻳﺔ ﻣﺎ ﺗﺣﺕ‬ ‫ﺳﻁﺢ ﺍﻷﺭﺽ ﻣﻥ ﺗﺭﺍﻛﻳﺏ ﺟﻳﻭﻟﻭﺟﻳﻪ ﺗﻌﺭﻑ ﺑـ " ‪ "Oil Trap‬ﻣﺻﺎﺋﺩ ﺑﺗﺭﻭﻟﻳﻪ‪ ،‬ﺣﻳﺙ ﺍﻧﻬﺎ ﺗﺣﺗﻭﻱ‬ ‫ﻋﻠﻲ ﺍﻟﺯﻳﺕ ﺃﻭ ﺍﻟﻐﺎﺯ‪.‬‬ ‫ﺗﻘﻭﻡ ﻓﻛﺭﻩ ﺍﻟﻣﺳﺢ ﺍﻟﺳﻳﺯﻣﻲ ﻋﻠﻲ ﺍﺭﺑﻊ ﺧﻁﻭﺍﺕ ‪:‬‬ ‫ﺍﻟﺧﻁﻭﻩ ﺍﻷﻭﻟﻲ ‪ :‬ﺇﻧﺷﺎء ﻣﻭﺟﻪ ﺻﻭﺗﻳﻪ ﻗﻭﻳﻪ ﻓﻭﻕ ﺳﻁﺢ ﺍﻷﺭﺽ ﺑﺄﺳﺗﺧﺩﺍﻡ ﺍﻟﺩﻳﻧﺎﻣﻳﺕ ﺃﻭ ﺍﻟﻌﺭﺑﺎﺕ‬ ‫ﺍﻟﺯﻟﺯﺍﻟﻳﻪ "‪ "Vibroseis‬ﻭﻫﻲ ﺍﻷﻛﺛﺭ ﺷﻳﻭﻋﺎ ً‪.‬‬ ‫ﺍﻟﺧﻁﻭﻩ ﺍﻟﺛﺎﻧﻳﻪ ‪ :‬ﺍﺳﺗﻘﺑﺎﻝ ﺗﻠﻙ ﺍﻟﻣﻭﺟﺎﺕ ﺑﻌﺩ ﺍﻥ ﺗﻧﻌﻛﺱ ﻋﻧﺩ ﺍﻟﺣﺩ ﺍﻟﻔﺎﺻﻝ ﺑﻳﻥ ﺍﻟﻁﺑﻘﺎﺕ ‪interface‬‬ ‫ﺣﻳﺙ ﺍﻷﺧﺗﻼﻑ ﻓﻲ ﺍﻟﻛﺛﺎﻓﻪ )ﻛﺛﺎﻓﻪ ﺍﻟﺻﺧﻭﺭ( ﻟﻠﺣﻭﺽ ﺍﻟﺗﺭﺳﻳﺑﻲ ﻭﻳﺗﻡ ﺭﺻﺩﻫﺎ ﺑﺎﺳﺗﺧﺩﺍﻡ ﺍﺟﻬﺯﺓ‬ ‫ﺣﺳﺎﺳﻪ ﺗﺳﻣﻲ ‪ Receivers‬ﺣﻳﺙ ﺗﻛﻭﻥ ﻣﺗﺻﻠﻪ ﻣﻊ ﺑﻌﺿﻬﺎ ﺍﻟﺑﻌﺽ ﻭﺃﻳﺿﺎ ﻣﺗﺻﻠﻪ ﻣﻊ ﻋﺭﺑﻪ‬ ‫ﺍﻟﺗﺳﺟﻳﻝ "‪. "Recording Unit‬‬ ‫ﺍﻟﺧﻁﻭﻩ ﺍﻟﺛﺎﻟﺛﻪ ‪ :‬ﺗﺳﺟﻳﻝ ﺗﻠﻙ ﺍﻟﻣﻭﺟﺎﺕ ﺍﻟﻣﺭﺗﺩﻩ ﺍﻟﻲ ﺍﻟﺳﻁﺢ ﻣﺭﻩ ﺍﺧﺭﻱ ﺑﺎﺳﺗﺧﺩﺍﻡ ﺍﺟﻬﺯﻩ ﺍﻟﺗﺳﺟﻳﻝ‬ ‫ﻭﺇﺭﺳﺎﻟﻬﺎ ﺍﻟﻲ ﻣﺭﻛﺯ ﺍﻟﻣﻌﺎﻟﺟﻪ ﻹﺟﺭﺍء ﻋﻣﻠﻳﺎﺕ ﺭﻗﻣﻳﻪ ﻋﻠﻳﻬﺎ " ‪ "Digital Processing‬ﻭﻣﻥ ﺛﻡ‬ ‫ﻳﻣﻛﻥ ﺗﺣﻣﻳﻠﻬﺎ ﻋﻠﻲ ﺍﺟﻬﺯﻩ ﺍﻟﻛﻣﺑﻳﻭﺗﺭ ﺍﻟﻣﻌﺩﻩ ﻟﺫﻟﻙ ﺑﺎﺳﺗﺧﺩﺍﻡ ﺑﺭﺍﻣﺞ ﻣﺗﺧﺻﺻﻪ ‪.‬‬ ‫ﺍﻟﺧﻁﻭﻩ ﺍﻷﺧﻳﺭﻩ ‪ :‬ﻫﻲ ﺍﻟﺗﻔﺳﻳﺭ ﺣﻳﺙ ﻳﻘﻭﻡ ﺍﻟﺟﻳﻭﻓﺯﻳﺎﺋﻲ ﻭﺍﻟﺟﻳﻭﻟﻭﺟﻲ ﺑﻌﻣﻝ ﺗﻔﺳﻳﺭﺍﺕ ﺳﻳﺯﻣﻳﻪ ﻟﺗﻠﻙ‬ ‫ﺍﻟﻣﻘﺎﻁﻊ ﻟﺗﺣﺩﻳﺩ ﺍﻟﻣﺻﺎﺋﺩ ﺍﻟﺑﺗﺭﻭﻟﻳﻪ ﻭﻋﻣﻝ ﺧﺭﺍﺋﻁ ﻛﻧﺗﻭﺭﻳﻪ ﻋﻠﻳﻬﺎ ﻟﺗﺣﺩﻳﺩ ﻣﻛﺎﻥ ﺣﻔﺭ ﺍﻟﺑﺋﺭ‪.‬‬

‫‪U‬‬

‫ﻳﺣﺗﻭﻱ ﻫﺫﺍ ﺍﻟﺑﺣﺙ ﻋﻠﻲ ﺍﻷﺗﻲ ﺑﺄﺧﺗﺻﺎﺭ‪:‬‬ ‫ﺍﻟﻔﺻﻝ ﺍﻷﻭﻝ‬ ‫ﻣﻘﺩﻣﻪ ﺗﻌﺭﻳﻔﻳﻪ ﺑﺎﻟﻣﺳﺢ ﺍﻟﺳﻳﺯﻣﻲ ﻭﻛﻳﻔﻳﻪ ﺟﻣﻊ ﺍﻟﺑﻳﺎﻧﺎﺕ ﻭﻣﻌﻧﻲ ﺍﻟﺗﻔﺳﻳﺭ ﺍﻟﺳﻳﺯﻣﻲ‪.‬‬

‫‪1‬‬

‫‪U‬‬

‫ﺍﻟﻔﺻﻝ ﺍﻟﺛﺎﻧﻲ‬ ‫ﻣﺣﺎﻭﻟﻪ ﻟﺗﻘﺩﻳﻡ ﺍﻟﺗﻌﺭﻳﻔﺎﺕ ﻭﺍﻟﻣﻔﺎﻫﻳﻡ ﺍﻷﺳﺎﺳﻳﻪ ﺍﻟﻣﺳﺗﺧﺩﻣﻪ ﻓﻲ ﺍﻟﺗﻔﺳﻳﺭ ﺑﺻﻭﺭﻩ ﻣﺑﺳﻁﻪ ﻣﺛﻝ ﺍﻧﻭﺍﻉ‬ ‫ﺍﻟﻣﻭﺟﺎﺕ ﻭﺍﻟﻔﺭﻕ ﺑﻳﻥ ﺍﻟﻣﻭﺟﺎﺕ ﺍﻷﻧﻌﻛﺎﺳﻳﻪ ﻣﻭﺿﻭﻉ ﺍﻟﺑﺣﺙ ﻭﺍﻟﻣﻭﺟﺎﺕ ﺍﻟﺗﺷﺗﺗﻳﻪ ﻭﺍﻟﺗﻁﺭﻕ ﺍﻟﻲ‬ ‫ﺍﻧﻭﺍﻉ ﺍﻟﻣﺳﺗﻘﺑﻼﺕ‪.‬‬

‫‪U‬‬

‫ﺍﻟﻔﺻﻝ ﺍﻟﺛﺎﻟﺙ‬ ‫ﺗﻘﺩﻳﻡ ﺧﻁﻭﺍﺕ ﻟﻠﺗﻔﺳﻳﺭ ﺍﻟﺟﻳﻭﻟﻭﺟﻲ ﻟﻠﺑﻳﺎﻧﺎﺕ ﺍﻟﺳﻳﺯﻣﻳﻪ ﺍﻷﻧﻌﻛﺎﺳﻳﻪ ﻣﻊ ﺍﻗﺻﺎء ﺍﻟﻣﻌﺎﺩﻻﺕ ﺍﻟﺭﻳﺎﺿﻳﻪ‬ ‫ﺍﻟﻣﻌﻘﺩﻩ ﻭﺍﻟﻧﻅﺭﻳﺎﺕ ﺍﻟﻔﺯﻳﺎﺋﻳﻪ ﺍﻟﻣﻁﻭﻟﻪ ﻭﺍﻟﺗﺭﻛﻳﺯ ﻋﻠﻲ ﺍﻟﻣﻔﻬﻭﻡ ﺍﻟﺟﻳﻭﻟﻭﺟﻲ ﻟﻠﺗﻔﺳﻳﺭ ﻭﻫﺩﻓﻪ‪ ،‬ﺣﻳﺙ‬ ‫ﺗﺿﻣﻧﺕ ﺍﻟﺧﻁﻭﺍﺕ ﺍﻟﻣﺿﺎﻫﺎﻩ ﻭﺭﺳﻡ ﺍﻟﺧﺭﺍﺋﻁ ‪ ………..‬ﺃﻟﺦ‪.‬‬

‫‪U‬‬

‫ﺍﻟﻔﺻﻝ ﺍﻟﺭﺍﺑﻊ‬

‫‪U‬‬

‫ﺩﺭﺍﺳﺔ ﺍﻷﻧﻌﻛﺎﺳﺎﺕ ﺍﻟﺳﻳﺯﻣﻳﻪ ﻓﻭﻕ ﺍﻟﺗﺭﻛﻳﺏ ﺍﻟﺟﻳﻭﻟﻭﺟﻳﻪ ﺍﻟﻣﺧﺗﻠﻔﻪ ﺍﻟﻣﻌﻬﻭﺩ ﺗﻭﺍﺟﺩ ﺍﻟﺑﺗﺭﻭﻝ ﺑﻬﺎ ﻭﻛﻳﻔﻳﻪ‬ ‫ﺗﻔﺳﻳﺭ ﺻﻭﺭﻩ ﺍﻟﻣﻭﺟﺎﺕ ﻓﻭﻕ ﺗﻠﻙ ﺍﻟﺗﺭﺍﻛﻳﺏ ﻣﻊ ﺫﻛﺭ ﺍﻷﺧﻁﺎء ﺍﻟﺗﻲ ﻳﺟﺏ ﺍﻥ ﺗﺗﺟﻧﺏ ﺍﺛﻧﺎء ﺗﻔﺳﻳﺭ ﺗﻠﻙ‬ ‫ﺍﻟﺗﺭﺍﻛﻳﺏ‪.‬‬ ‫ﺍﻟﻔﺻﻝ ﺍﻟﺧﺎﻣﺱ‬ ‫ﺗﻘﺩﻳﻡ ﻧﻣﻭﺫﺝ ﻟﺩﺭﺍﺳﻪ ﻛﺎﻣﻠﻪ ﻋﻠﻲ ﻣﻧﻁﻘﻪ ﺣﻭﺽ ﻣﻁﺭﻭﺡ ﻛﻧﻣﻭﺫﺝ ﻟﺗﻁﺑﻳﻕ ﺧﻁﻭﺍﺕ ﺍﻟﺗﻔﺳﻳﺭ‬ ‫ﺍﻟﺟﻳﻭﻟﻭﺟﻲ ﻋﻠﻲ ﺍﻟﺑﻳﺎﻧﺎﺕ ﺍﻟﺳﻳﺯﻣﻳﻪ ﺍﻷﻧﻌﻛﺎﺳﻳﻪ ﻭﺗﻘﻳﻳﻡ ﺍﻷﺣﺗﻣﺎﻻﺕ ﺍﻟﺑﺗﺭﻭﻟﻳﻪ ﺑﻬﺎ‪.‬‬

‫‪2‬‬

‫ﺑﺴﻢ ﺍﷲ ﺍﻟﺮﲪﻦ ﺍﻟﺮﺣﻴﻢ‬

‫َ ُْ َ ْ َ ْ ُ ْ َ َ َ َ َ ْ َ َ ْ َ ْ ُ َْ َ َ َ‬ ‫ﺖ ﺍﻷﺭﺽ ﺃﺛﻘﺎﻟﻬﺎ *‬ ‫ﺖ ﺍﻷﺭﺽ ِﺯﻟﺰﺍﻟﻬﺎ * ﻭﺃﺧﺮﺟ ِ‬ ‫ِﺇﺫﺍ ﺯﻟ ِﺰﻟ ِ‬ ‫ََ َ ْ َ ُ َ َ َ َ ْ َ ُ َ ﱢ ُ َ َْ َ َ َ ﱠ َﱠ َ‬ ‫ﻭﻗﺎﻝ ﺍﻹِﻧﺴﺎﻥ ﻣﺎ ﻟﻬﺎ * ﻳﻮﻣ ِﺌ ٍﺬ ﺗﺤﺪﺙ ﺃﺧﺒﺎﺭﻫﺎ * ِﺑﺄﻥ ﺭﺑﻚ‬ ‫َ ْ َ ََ َ ْ َ َ ْ ُ ُ ﱠ ُ َ َْ ً ﱢُ َ ْ َ ْ َ َُ ْ َ َ‬ ‫ﺃﻭﺣﻰ ﻟﻬﺎ * ﻳﻮﻣ ِﺌ ٍﺬ ﻳﺼﺪﺭ ﺍﻟﻨﺎﺱ ﺃﺷﺘﺎﺗﺎ ﻟﻴﺮﻭﺍ ﺃﻋﻤﺎﻟﻬﻢ* ﻓﻤﻦ‬

‫َ ْ َ ْ ْ َ َ َ ﱠ َْ ً َ َُ َ َ َ ْ َ ْ ْ َ َ َ ﱠ َ ‪َ َ ‬‬ ‫ﻳﻌﻤﻞ ِﻣﺜﻘﺎﻝ ﺫﺭ ٍﺓ ﺧﻴﺮﺍ ﻳﺮﻩ * ﻭﻣﻦ ﻳﻌﻤﻞ ِﻣﺜﻘﺎﻝ ﺫﺭ ٍﺓ ﺷﺮﺍ ﻳﺮﻩ ُ‬

‫*‬

‫ﺳﻮﺭﺓ ﺍﻟﺰﻟﺰﻟﺔ‬

‫ﺟﺎﻣﻌﻪ ﺍﻷﺯﻫﺭ‬ ‫ﻛﻠﻳﻪ ﺍﻟﻌﻠﻭﻡ ﺑﺄﺳﻳﻭﻁ‬ ‫ﻗﺳﻡ ﺍﻟﺟﻳﻭﻟﻭﺟﻳﺎ‬

‫ﺑﺣﺙ ﻓﻲ‬

‫ﺍﻟﺘﻔﺴﲑ ﺍﳉﻴﻮﻟﻮﺟﻲ ﻟﻠﺒﻴﺎﻧﺎﺕ ﺍﻟﺴﻴﺰﻣﻴﻪ ﺍﻷﻧﻌﻜﺎﺳﻴﻪ‬ ‫ﺇﻋﺩﺍﺩ ﺍﻟﻁﻼﺏ‪:‬‬ ‫‪ .1‬ﺃﺣﻣﺩ ﻋﺑﺩﺍﻟﺣﻣﻳﺩ ﻋﻠﻲ ﻋﺑﺩﺍﻟﺣﺎﻓﻅ‬ ‫‪ .2‬ﺃﺣﻣﺩ ﻣﺣﻣﻭﺩ ﻋﺑﺩﺍﻟﺳﻼﻡ ﺣﺳﻥ‬ ‫‪ .3‬ﻋﺑﺩﺍﻟﺭﺣﻣﻥ ﻣﺣﻣﺩ ﻋﺑﺩﺍﻟﻔﺗﺎﺡ ﺳﻠﻳﻡ‬ ‫ﻷﺳﺗﻛﻣﺎﻝ ﺍﻟﺣﺻﻭﻝ ﻋﻠﻲ ﺑﻛﺎﻟﻭﺭﻳﺎ ﺍﻟﻌﻠﻭﻡ ﺍﻟﺟﻳﻭﻟﻭﺟﻳﻪ‬ ‫ﻟﻠﻌﺎﻡ ‪2009/2008‬‬

‫ﺗﺣﺕ ﺇﺷﺭﺍﻑ‬

‫ﺩ‪/‬ﻋﺑﺩﺍﻟﺳﺗﺎﺭ ﻋﺑﺩﺍﻟﻧﻌﻳﻡ ﻋﺑﺩﺍﻟﻠﻁﻳﻑ‬ ‫ﻣﺣﺎﺿﺭ ﺍﻟﺟﻳﻭﻓﺯﻳﺎء‬