Journal of Earth Science, Vol. 24, No. 6, p. 987–996, December 2013
Printed in China
DOI: 10.1007/s12583-013-0392-4
ISSN 1674-487X
Element Response to the Ancient Lake Information
and Its Evolution History of Argillaceous Source
Rocks in the Lucaogou Formation in Sangonghe
Area of Southern Margin of Junggar Basin
Mingming Zhang (张明明), Zhaojun Liu* (刘招君), Shengchuan Xu (许圣传),
Pingchang Sun (孙平昌), Xiaofeng Hu (胡晓峰)
College of Earth Sciences, Jilin University, Changchun 130061, China
ABSTRACT: With the analysis of the element geochemistry characteristics, the ancient lake information evolution history of the argillaceous source rocks in Lucaogou (芦草沟) Formation in Sangonghe (三工河) area is reconstructed. According to the ancient lake information and total organic
matter (TOC) characteristics of argillaceous source rocks, the study section is divided into 6 Subsections. Subsection I mainly developed low-quality source rocks. This is because of the arid climate,
high salinity, low lake productivity, unstable preservation conditions in this Subsection. Subsection II
mainly developed high-quality source rocks. This is because of the humid climate, low salinity, high
lake productivity, stable preservation conditions in this Subsection. Though the paleoclimate was
humid and preservation conditions were stable. Lake productivity and the water salinity changed
frequently. So Subsection III mainly developed medium-quality source rocks. Because of the humid
climate, high lake productivity, medium sedimentary rate and stable preservation conditions,
high-quality source rocks were developed in Subsection IV. The preservation conditions were stable,
but other ancient lake information changed frequently. Therefore, the quality of the formed source
rocks in Subsection V was different. Subsection VI mainly developed high-quality source rocks because of the humid climate, medium sedimentary rate, high lake productivity, low salinity and good
preservation conditions. In summary, the ancient lake information parameters and TOC characteristics of each Subsection are different from each other.
KEY WORDS: Sangonghe area, Lucaogou Formation, argillaceous source rock, ancient lake
information, evolution history.
This study was supported by the National Natural Science
Foundation of China (Nos. 40972076 and 41302075) and the
National Technical Key Special Project of China (No.
2008ZX05018-001-004).
*Corresponding author: [email protected]
© China University of Geosciences and Springer-Verlag Berlin
Heidelberg 2013
Manuscript received November 15, 2012.
Manuscript accepted March 26, 2013.
INTRODUCTION
The argillaceous source rocks in Permian Lucaogou Formation in the northern foot of Bogeda
Mountain are one of the important hydrocarbon source
rocks in the southeastern margin of the Junggar Basin.
The maximum sedimentary thickness of Lucaogou
Formation is in Sangonghe area, which may have
huge hydrocarbon generation potential and abundant
oil shale resources (Kuang et al., 2007; Li et al., 2006).
Mingming Zhang, Zhaojun Liu, Shengchuan Xu, Pingchang Sun and Xiaofeng Hu
988
Precursors have done some research on this region (Li,
2009; Gao, 2008; Kuang et al., 2007; Wang et al.,
2007; Li et al., 2006). But less research has been done
on the ancient lake information evolution history of
argillaceous source rocks. This paper aims to sum up
the evolution history of ancient lake information (such
as paleoclimate, organic matter sedimentary rate, paleosalinity, redox conditions and lake productivity) of
the argillaceous source rocks in the Lucaogou Formation in Sangonghe area.
GEOLOGICAL BACKGROUND AND STUDY
SECTION
Sangonghe area is located in the southeastern margin of Junggar Basin. Tectonically, the structure feature
in this region is very complex. Anticline, syncline and
reverse fault extremely developed in this area. The Permian strata mainly exposed in the south of Sangonghe
area (Fig. 1).
This study section mainly includes Lucaogou Formation and Hongyanchi Formation. The Hongyanchi
Formation is covered on the Lucaogou Formation. The
main lithology in it is grey-green mudstone, and there is
a thin layer of gray-green fine-grained sandstone in the
mudstone. The thickness of Lucaogou Formation (the
argillaceous source rocks) is larger than Hongyanchi
Formation. The main lithology in it is thick gray-black
and black mudstone, oil shale with thin layers of gray
J1-2
Junggar Basin
Bogda Mountain
fine-grained sandstone, siltstone, dolomite, dolomitic
mudstone (Fig. 2).
SAMPLES AND TEST METHODS
According to the lithology distribution and geochemical characteristics of the argillaceous source
rocks section, a total of 23 fresh samples were collected. To avoid the influence of weathering on the
content of the major elements and trace elements in
samples, we use the drilling and sampling machine to
drill 5 m deep to get the fresh samples which almost
not to be subjected to weathering. The sampling location can be shown in Fig. 2. We chiefly tested the
content of the major elements (Fe2O3, FeO, CaO),
trace elements (Sr, Rb, V, Ni, Cr, Mo, U, Ga, B), rare
earth elements (La, Yb) and total organic carbon
(TOC). Ancient lake information of argillaceous
source rocks can be analyzed by the content and ratio
features of these elements. TOC represents the organic
matter content in the argillaceous source rocks. Major
elements were tested on silicate chemistry full analysis. Trace elements and rare earth elements were tested
by inductively coupled plasma mass spectrometry
(ICP-MS). Repetitive samples and standard samples
were analyzed to measure the accuracy of test results.
The qualified rate of repetitive samples is 100%. The
analysis shows that the relative deviation of the elements is less than 5%, which indicates that the overall
C
T
J1-2
C
Sangonghe
area
P2
J1-2
T
P2
Q
J1-2
Urumchi
0
P2
T
10 km
N
P2
J1-2
T
P2
Q
Quaternary
J1-2
Jurassic
T
P2
C
Triassic Permian Carboniferous Anticline Syncline Reverse fault City Research section
Figure 1. Map of Sangonghe area location (revised from Li et al., 2006).
Element Response to the Ancient Lake Information and Its Evolution History
System
Formation
Depth
(m)
Lithology
column
Sample
location
Hongyanchi
100
23
22
21
20
200
Upper
15
14
13
12
300
11
10
Lucaogou
9
8
400
Permian
7
6
5
500
4
3
2
600
1
Oil shale
Mudstone
Marl
Silty
mudstone
Dolomitic
siltstone
Coarse
grained stone
Figure 2. Map of the study cross section column.
analysis results are reliable.Test results are shown in
Table 1.
ANCIENT LAKE INFORMATION ANALYSIS
Ancient lake information analysis on the argilla-
989
ceous source rocks section mainly include paleoclimate and organic matter sedimentary rate, properties
of ancient water (redox conditions, paleosalinity) and
lake productivity.
Paleoclimate and Sedimentary Rate Analysis
Paleoclimate may control the production and
preservation of the organic matter when sedimentary
rocks were formed, and proper sedimentary rate may
also have important influence on the abundance of
organic matter. Therefore, it is necessary to analyze
the paleoclimate and organic matter sedimentary rate
of argillaceous source rocks.
Paleoclimate analysis
Fe is particularly sensitive to the paleoclimate of
sedimentary environment (Jin et al., 2002; Deng and
Qian et al., 1993). Fe2O3/FeO ratio has a good effect
on the instructions of paleoclimate. It is generally
believed that the Fe2O3/FeO value greater than 1.8
indicates arid climate. On the contrary, the value less
than 1.8 indicates humid climate (Wang et al., 2012).
The Fe2O3/FeO value of argillaceous source rocks
section ranges from 0.51 to 5.56, averaging 2.08. This
means that some argillaceous source rocks were
formed in humid climate, and others were formed in
arid climate. In addition, as shown in Fig. 5, the lower
stratum is mainly arid climate, and the upper stratum
is mainly humid climate, but local layers in the upper
stratum are arid climate. This may be the atmospheric
circulation changed occasionally during the deposition of the upper stratum. Some other researchers also
come to the same conclusions about the study strata in
this area (Peng et al., 2012).
Rb/Sr ratio in lake sediments is very sensitive to
the changes of paleoclimate. It is generally believed
that the Rb/Sr value greater than 0.5 indicates arid
climate. On the contrary, the value less than 0.5 indicates humid climate (Hu et al., 2012a; Wang et al.,
2008). Rb/Sr ratio value of argillaceous source rocks
section ranges from 0.15 to 0.98, averaging 0.48. This
also means that some argillaceous source rocks were
formed in humid climate, and others were formed in
arid climate. As shown in Fig. 3a, in addition to the
differences of individual samples, there is a linear
relationship between Fe2O3/FeO and Rb/Sr value. It is
Mingming Zhang, Zhaojun Liu, Shengchuan Xu, Pingchang Sun and Xiaofeng Hu
990
Table 1
Contents of some major elements (wt.%), trace elements, rare earth elements (ppm) in argillaceous source rocks
Fe2O3
FeO
CaO
Rb
Sr
Mo
U
La
Yb
1
3.72
2
5.06
3.74
6.89
28.13
187.5
3.35
20.18
96.48
253.9
3.97
3.3
27.69
2.49
78
96
50.7
17.8
71.86
3.57
2.83
27.8
6.28
126.63
68.99
28.1
23.4
152.00
3
4.11
1.49
15.94
178.35
336.5
3.44
2.33
23.97
2.23
96
120
58.4
28.5
141.48
4
4.17
1.76
21.02
244.60
571.5
1.18
1.34
19.57
1.95
82.74
16.69
40.1
31.4
138.08
5
2.82
0.82
6
2.6
5.04
8.18
174.23
244.7
2.06
2.2
27.83
5.84
78.63
26
26.4
25.4
121.00
11.95
22.64
107.8
5.15
4.11
15.1
1.76
307.16
30.23
53.8
18.3
82.00
7
3.44
2.31
7.94
42.96
143.2
3.58
2.6
10.97
1.2
145.79
21.19
32.2
28.8
135.00
8
4.3
2.76
31.1
95.99
184.6
4.2
2.74
25.54
2.25
131.58
51.47
51.6
32.6
162.00
9
4.46
2.76
10
3.73
2.98
4.24
44.92
290.8
3.12
2.54
16.08
2.01
255.89
27.83
58.2
16.7
45.00
49.21
233.63
561.6
2.51
1.7
17.33
2.1
91.26
24.28
25.6
9.1
54.27
11
4.7
3.12
5.66
30.99
147.6
6.82
5.35
22.41
2.7
124.53
32.71
28.6
28.6
90.23
12
3.57
2.99
3.53
18.11
82.3
4.56
3.65
15.12
1.67
87.89
122
44.6
15.4
40.90
13
14
4.92
2.61
5.45
41.74
95.3
3.96
3.1
17.65
2.44
127.79
32.6
26.3
18.6
52.75
2.95
1.64
4.07
29.27
70.2
4.9
3.19
14.97
1.56
89.68
16.33
20.4
23.4
67.19
15
10.79
2.53
65.27
262.27
299.4
3.43
2.61
21.24
2.82
207.68
44.1
45.6
23.7
156.25
16
5.99
2.32
26.32
112.31
175.2
2.24
1.76
7
1.29
326.63
11.4
53
28.4
137.00
Number
V
Ni
Cr
Ga
B
17
4.84
2.31
13.28
69.03
117
3.56
3.03
12.39
1.73
108.74
32.16
24.6
21.5
100.39
18
3.24
1.15
5.37
223.61
272.7
3.51
2.4
11.24
1.94
79.05
22.56
33.9
23.8
110.00
19
1.83
1.04
44.96
66.11
193.3
4.49
2.6
17.41
2.14
111.79
16.75
24.3
27.8
152.00
20
4.8
4.15
3.84
43.67
150.6
3.79
3
25.26
2.57
109.68
33.9
25.7
24.7
73.00
21
7.33
1.32
11.49
324.43
328.7
3.17
1.9
25.58
3.51
74
89
41
19.8
162.00
22
4.92
3.13
5.37
26.79
76.1
8.3
4.8
14.92
2.07
160.32
42.12
35.6
26.7
77.08
23
2.53
1.12
2.05
80.26
117
3.63
2.18
11.84
1.35
99.47
17.03
23.6
24.6
60.00
The data of Sr and B were cited from Zhang et al., in press.
feasible to comprehensively distinguish the paleoclimate of each sample by the value of Fe2O3/FeO
and Rb/Sr. As shown in Fig. 5, the value of
Fe2O3/FeO and TOC in some samples has negative
correlation in trend, but the other samples do not
comply with this trend. Therefore, it is speculated
that paleoclimate may control the organic matter
enrichment of the argillaceous source rocks to some
degree, but not absolutely.
Sedimentary rate analysis
Parameter w(La)n/w(Yb)n (Ratio of La and Yb
normalized by the North American shale represents
the degree of fractionation of rare earth elements) is
usually used to indicate mudstone sedimentary rate. If
the sedimentary rate is fast, leading the REE (rare
earth elements) differentiation to be weakly, the
w(La)n/w(Yb)n value is closed to 1. If the sedimentary
rate is slow, resulting in the REE differentiation to be
obvious, the w(La)n/w(Yb)n value is significantly less
than 1. The w(La)n/w(Yb)n value is slightly less than 1,
which means that the sedimentary rate is medium (Li
et al., 2008; Chen et al., 2006; Tenger et al., 2006; Qin
et al., 2005). The w(La)n/w(Yb)n value of the samples
in the argillaceous source rocks section ranges from
0.46 to 1.09, and averages 0.79. As shown in Fig. 4,
t h e l i n e a r r e l a t i o n s h i p b e t w e e n TO C a n d
w(La)n/w(Yb)n is not significant. In addition, too fast
or too slow deposition rate (According to the distribution range of w(La)n/w(Yb)n value in samples, the
w(La)n/w(Yb)n value greater than 0.9 represents the
faster sedimentary rate, the value between 0.6 and 0.9
represents moderate deposition rate, the value less
than 0.6 represents the slower sedimentary rate) corresponds to the low TOC value. Moderate sedimentary
rate corresponds to the high TOC value. This is
6
(c)
0
V / Cr
Oxic Dysoxic
Anoxic
5
0.2
0.8
1.0
0.4
0.6
1.2
Fresh water Brackish water Salt water
Ca/(Ca+Fe)
991
7
6
5
4
3
2
1
0
0
(b)
0.4
0.2
Oxic
0.8
1.0
Anoxic
0.6
Dysoxic
V/(V+Ni)
1.2
High
7
6
5
Medium
2
0
4
1
3
Humid Climate
Arid Climate
Fe 2O 3/FeO
Low
10
9
8
7
6
5
4
3
2
1
0
(a)
U content ( 10 - 6) (productivity)
1.0
0.9
0.8
0.7
0.6
0.5
0.4
0.3
0.2
0.1
0
B/Ga
Fresh water Brackish water Salt water
Rb/Sr
Humid climate Arid climate
Element Response to the Ancient Lake Information and Its Evolution History
4
3
2
1
(d)
0
0
1
Low
2
3
4
Medium
5
6
High
7
8
9
10
-6
Mo content (10 ) (productivity)
Figure 3．Discriminant diagram of ancient lake information parameters. (a) Discriminant diagram of
paleoclimate; (b) discriminant diagram of redox conditions; (c) discriminant diagram of paleosalinity; (d)
discriminant diagram of lake productivity.
because that organic matter is gradually consumed
by the oxygen in water with slow deposition rate
leading to the decrease of organic matter content. If
sedimentary rate is too fast, organic matter would be
diluted by inorganic mineral particles, which may
also make the organic matter content decrease.
From above analysis, it is speculated that moderate
sedimentary rate is beneficial to the organic matter
enrichment, too fast or too slow sedimentary rate go
against the preservation of organic matter.
Ancient Water Properties Analysis
Ancient water properties (redox conditions,
paleosalinity) played an important role in the formation of argillaceous source rocks. Therefore, it is
necessary to analyze this ancient lake information.
Redox conditions analysis
Redox conditions are one of the key factors for
the preservation and hydrocarbon generation potential of organic matter. V/Cr ratio is often used to
discriminate the redox conditions. V/Cr value less
than 2.0 indicates oxic environment, the value
ranging from 2.0 to 4.25 indicates dysoxic environment, the value greater than 4.25 indicates
anoxic environment (Li et al., 2011; Wang, 2003;
Jones and Manning, 1994; Hatch and Leventhal,
1992). The V/Cr value of argillaceous source rocks
ranges from 1.53 to 5.71, averaging 3.73. It means
that most samples were formed in the anoxic environment and dysoxic environment. Individual samples were formed in the oxic environment.
V/(V+Ni) ratio also can be used to discriminate the redox conditions. V/(V+Ni) ratio value
greater than 0.6 indicates anoxic environment, and
the value ranging from 0.46 to 0.6 indicates dysoxic
environment. The value less than 0.46 indicates oxic
environment (Li et al., 2011; Wang, 2003; Jones and
Manning et al., 1994; Hatch and Leventhal, 1992).
The V/(V+Ni) ratio value of argillaceous source
rocks ranges from 0.42 to 0.96, averaging 0.75,
which also means that most samples were formed in
the anoxic environment and dysoxic environment.
Individual samples were formed in the oxic
Mingming Zhang, Zhaojun Liu, Shengchuan Xu, Pingchang Sun and Xiaofeng Hu
992
TOC (%)
25
20
15
10
5
0
0.4
Slow
0.6
0.8
Medium
1.0
Fast
1.2
w (La) n/ w (Yb) n
Figure 4．Correlation diagram of w(La)n/w(Yb)n
and TOC.
environment (Fig. 3b). As shown in Fig. 5, most
samples were formed in anoxic environment; only 4
samples were formed in the oxic environment,
which means that the redox conditions of the argillaceous source rocks section is stable. Only the individual layers are oxic environment. In addition,
the correlation between V/(V+Ni) ratio and TOC
value vertical variation curves is not significant.
This means that the redox conditions are not the
decisive control factor for the organic matter content.
Paleosalinity analysis
Appropriate salinity is conductive to the
growth and development of microorganisms in the
lake, which may improve the lake productivity.
Ca/(Ca+Fe) value is sensitive to the changes of paleosalinity. Ca/(Ca+Fe) value greater than 0.8 indicates salt water, the value ranging from 0.4 to 0.8
indicates brackish water. The value less than 0.4
indicate fresh water (Hu et al., 2012a; Lan et al.,
1987). The Ca/(Ca+Fe) value in samples ranges
from 0.3 to 0.96, averaging 0.62. It means that some
argillaceous source rocks were mainly formed in the
brackish water environment and fresh water environment. Other samples were formed in the salt
water environment.
B/Ga ratio is also a good salinity discriminant
parameter. The ratio value greater than 5.0 indicates
salt water, and the value ranging from 3.0 to 5.0
indicates brackish water. The value less than 3.0
indicates fresh water (Hu et al., 2012b; Deng and
Qian, 1993). The B/Ga value in samples ranges
from 2.44 to 8.18, averaging 4.42, which also
means that most samples were formed in the brackish water and fresh water. Other samples were
formed in the salt water environment, as shown in
Fig. 3c. There is a linear relationship between B/Ga
and Ca/(Ca+Fe) value. Therefore, these two parameters can be used to comprehensively judge the
paleosalinity in each sample. It can be seen from
Fig. 5 that the correlation trends between the B/Ga
ratio value and TOC value vertical variation curves
is not obvious. It means that paleosalinity is not the
main control factor for the organic matter enrichment of the argillaceous source rocks either.
Lake Productivity Analysis
The organic matter in sedimentary rocks
mainly comes from the terrigenous organic matter
and the lake endogenous organic matter. The content of the lake endogenous organic matter is far
greater than the injected terrigenous organic matter.
So it is very necessary to study the lake endogenous
productivity of the argillaceous source rocks section.
Elements Mo and U are often used to distinguish the size of the lake endogenous productivity.
Generally, the high abundance represents high
productivity; low abundance represents low productivity (Lyons et al., 2003; Chase et al., 2001; Wilde
et al., 2001). As shown in Fig. 3d, the linear correlation between Mo and U is obvious. Therefore, they
can be used to distinguish the relative size of the
lake productivity in samples comprehensively (according to the distribution range of U and Mo content in samples. Mo less than 3.0 and U less than 2.0
represent the relatively smaller lake productivity,
Mo ranging from 3.0 to 4.0 and U ranging from 2.0
to 3.0 represent the medium lake productivity, Mo
greater than 4.0 and U greater than 3.0 represents
the higher lake productivity). As shown in Fig. 5,
most samples have medium-high lake productivity.
Only individual samples have low lake productivity.
In addition, the vertical variation curves of Mo content and TOC value show the similar trend, which
means that lake productivity plays an important role
in the enrichment of organic matter, while some
samples don’t comply with this law. It also means
Permian
Upper
Lucaogou
1
2
3
4
5
6
7
Mudstone
(Paleosalinity)
Oil shale
11
10
9
8
15
14
13
12
deposition
Marl
(Deposition rate)
Silty mudstone
(Redox conditions)
5
6 0
climate
Arid
climate
Humid
Dolomitic siltstone
Coarse-grained stone
(Productivity)
productivity
Low
(Paleoclimate)
Mo content (%)
6
8
4
Fe2O3/FeO
3 4
2
2
1
productivity
Medium
10 0
Low
5
10
15
TOC (%)
Figure 5．Comprehensive analysis diagram of the ancient lake information in the argillaceous source rocks section.
600
500
400
300
200
22
21
20
environment
water
Fresh
23
environment
water
Brackish
V/(V+Ni)
ω (La) n/ ω (Yb) n
10 0.4 0.5 0.6 0.7 0.8 0.9 1.0 1.1 0.4 0.5 0.6 0.7 0.8 0.9 1.0 0
rate
Medium
8
environment
water
Salt
rate
deposition
Slow
rate
deposition
Rapid
B/Ga
4
6
environment
Oxic
100
2
environment
Dysoxic
Hongyanchi
0
environment
Anoxic
Lithology Sample
column
location
productivity
High
System Formation Depth
(m)
High
20
25
I
II
III
IV
V
VI
Stage
Element Response to the Ancient Lake Information and Its Evolution History
993
Mingming Zhang, Zhaojun Liu, Shengchuan Xu, Pingchang Sun and Xiaofeng Hu
994
Table 2
Number
Ancient lake information evolution features of the argillaceous source rocks section
Paleosalinity
Redox
Depssition
conditions
rate
Paleoclimate
Productivity
TOC
(%)
1
Brackish water
Oxic
Rapid
Humid
Medium
4.54
2
Brackish water
Anoxic
Slow
Arid
Medium
4.45
3
Brackish water
Oxic
Rapid
Arid
Medium
4.05
4
Brackish water
Anoxic
Rapid
Arid
Low
1.83
5
Brackish water
Anoxic
Slow
Arid
Low
5.52
6
Fresh water
Anoxic
Medium
Humid
High
18.24
7
Brackish water
Anoxic
Medium
Humid
Medium
11.29
8
Brackish water
Anoxic
Rapid
Humid
High
6.88
9
Fresh water
Anoxic
Medium
Humid
Medium
8.96
10
Salt water
Anoxic
Medium
Arid
Low
4.99
11
Fresh water
Anoxic
Rapid
Humid
High
8.89
12
Fresh water
Oxic
Medium
Humid
High
21.44
13
Fresh water
Anoxic
Medium
Humid
Medium
10.15
14
Fresh water
Anoxic
Rapid
Humid
High
8.16
15
Salt water
Anoxic
Medium
Arid
Medium
9.98
16
Brackish water
Anoxic
Slow
Arid
Low
5.58
17
Fresh water
Anoxic
Medium
Humid
Medium
8.16
18
Brackish water
Anoxic
Slow
Humid
Medium
5.98
19
Brackish water
Anoxic
Medium
Arid
High
5.71
20
Fresh water
Anoxic
Rapid
Humid
Medium
4.55
21
Salt water
Oxic
Slow
Arid
Medium
4.24
22
Fresh water
Anoxic
Medium
Humid
High
15.6
23
Fresh water
Anoxic
Medium
Humid
Medium
14.2
that this control role is not absolute.
ANCIENT
LAKE
INFORMATION
EVOLUTION HISTORY
With the analysis of ancient lake information
characteristics in argillaceous source rocks section,
the evolution history of it can be described.
The argillaceous source rocks section is divided into 6 Subsections according to the vertical
variation features of ancient lake information and
the TOC value. The ancient lake information parameters characteristics in each Subsection can be
described in Table 2.
The ancient lake evolution history may be described as follows: Subsection I was mainly arid
climate. The water conditions were oxic alternating
with anoxic environment and brackish water envi-
Subsection
I
II
III
IV
V
VI
ronment. Lake productivity was low-medium, leading the TOC value to be low. Subsection II was
mainly humid climate, the water conditions changed
from fresh water to brackish water environment.
Lake productivity was medium to high. Abundant
organic matter with the moderate sedimentary rate
deposited, the high TOC value formed. Subsection
III was humid-arid climate. The water conditions
were fresh water-salt water environment and anoxic
environment. The lake productivity changed greatly
and deposited with medium-fast sedimentary rate.
The argillaceous source rocks with different TOC
value were formed in this Subsection. Subsection
IV was humid climate. The water conditions were
fresh water environment and anoxic environment.
High lake productivity was produced in this Subsection with the moderate-fast sedimentary rate
Element Response to the Ancient Lake Information and Its Evolution History
preserved. The high TOC value argillaceous source
rocks were formed in this Subsection. The evolution
history of the Subsection V was very complex. Paleoclimate ranged from arid to humid, and the water
conditions alternated with fresh water and salt water
environment. The lake productivity of this Subsection changed frequently. Organic matter deposited
with different sedimentary rate. The argillaceous
source rocks with different TOC value were formed
in this Subsection. Subsection VI was humid climate. The water conditions were freshwater environment and anoxic environment. The medium-high
lake productivity slowed down with the moderate
sedimentary rate. The high TOC value was formed
in this Subsection.
995
evolution history of the argillaceous source rocks in
Lucaogou Formation in Sangonghe area is complex.
ACKNOWLEDGMENTS
We appreciate the collaboration and enthusiastic support of Dr. Huijun Chen senior engineer
from Shenyang Geological Survey Center.
REFERENCES CITED
Chase, Z., Anderson, R. F., Fleisher, M. Q., 2001. Evidence
from Authigenic Uranium for Increased Productivity of
the Glacia Subantarctic Ocean. Paleoceanography, 16:
468–478
Chen, J. F., Zhang, Y. C., Sun, S. L., et al., 2006. Main Factors Influencing Marine Carbonate Source Rock Formation. Acta Geologica Sinica, 80(3): 467–472 (in
CONCLUSIONS
The argillaceous source rocks section is divided into 6 Subsections according to the vertical
variation features of ancient lake information and
the TOC value. Subsection I mainly developed
low-quality source rocks. This is because of the arid
climate, high salinity, low lake productivity, unstable preservation conditions in this Subsection. Subsection II mainly developed high-quality source
rocks. This is because of the humid climate, low
salinity, high lake productivity, stable preservation
conditions in this Subsection. Though the paleoclimate was humid and preservation conditions were
stable. Lake productivity and the water salinity
changed frequently. So Subsection III mainly developed medium quality source rocks. Because of
the humid climate, high lake productivity, medium
sedimentary rate, stable preservation conditions,
high-quality source rocks were developed in Subsection IV. The preservation conditions were stable,
but other ancient lake information changed frequently. Therefore, the quality of the formed source
rocks in Subsection V was different. Subsection VI
mainly developed high-quality source rocks because
of the humid climate, medium sedimentary rate,
high lake productivity, low salinity and good preservation conditions. So we can draw the conclusions that the ancient lake information parameters
and TOC characteristics of each Subsection are different form each other, the ancient lake information
Chinese with English Abstract)
Deng, H. W., Qian, K., 1993. Sedimentary Geochemistry
and Environmental Analysis. Gansu Science and Technology Publishing House, Lanzhou. 1–82 (in Chinese)
Gao, J. P., 2008. The Tectonic Characteristics and Petroleum
Geological Conditions of Foreland Thrust Belt in the
Eastern Section of the Southern Junggar Basin: [Dissertation]. Northwest University, Xi’an. 12–46 (in Chinese with English Abstract)
Hatch, J. R., Leventhal, J. S., 1992. Relationship between
Inferred Redox Potential of the Depositional Environment and Geochemistry of the Upper Pennsylvanian
(Missourian) Stark Shale Member of the Dennis Limstone, Wabaunsee Countr, Kansas, U.S.A.. Chemical
Geology, 99: 65–82
Hu, X. F., Liu, Z. J., Liu, R., et al., 2012a. Clay Mineral and
Inorganic Geochemical Characteristics of Eocene Huadian Formation in Huadian Basin and Their Paleoenvironment Implications. Journal of China Coal Society,
37(3): 416–423 (in Chinese with English Abstract)
Hu, X. F., Liu, Z. J., Liu, R., et al., 2012b. Trace Element
Characteristics of Eocence Jijuntun Formation and the
Favorable Metallogenic Conditions of Oil Shale in Fushun Basin. Journal of Jilin University (Earth Science
Edition), 42(Suppl.): 60–71 (in Chinese with English
Abstract)
Jin, B. F., Lin, Z. H., Yang, Q. H., et al., 2002. Application
of Sedimentary Mineralogy to the Environmental
Analysis in Marginal Seas. Marine Geology & Quater-
Mingming Zhang, Zhaojun Liu, Shengchuan Xu, Pingchang Sun and Xiaofeng Hu
996
nary Geology, 22(3): 113–117 (in Chinese with English
the Southeastern Margin of the Junggar Basin and Its
Abstract)
Environmental Implications. Bulletin of Mineralogy,
Jones, B. J., Manning, A. C., 1994. Comparison of Geochemical Indices Used for the Interpretation of Palaeoredox Conditions in Ancient Mudstones. Chemical Geology, 11(11): 111–129
Kuang, L. X., Guo, J. H., Tong, X. L., et al., 2007. Forming
Petrology and Geochemistry, 31(2): 121–157 (in Chinese with English Abstract)
Qin, J. Z., Liu, B. Q., Guo, S. Z., et al., 2005. China Hydrocarbon Source Rocks. Science Publishing House, Beijing. 1–163 (in Chinese)
Conditions and Patterns of Hydrocarbon Reservoirs in
Tenger, Liu, W. H., Xu, Y. C., 2006. Comprehensive Geo-
East of Southern Fringe of Junggar Basin. Earth
chemical Identification of Highly Evolved Marine Hy-
Sciences and Environment, 29(1): 34–40 (in Chinese
drocarbon Source Rocks: Organic Matter, Paleoenvi-
with English Abstract)
ronment and Development of Effective Hydrocarbon
Lan, X. H., Ma, D. X., Xu, M. G., et al., 1987. Some Geochemical Signs and Their Importance for Sedimentary
Facies. Marine Geology and Quaternary Geology, 7(1):
39 (in Chinese with English Abstract)
Source Rocks. Chinese Journal of Geochemistry, 25(4):
332–339
Wang, C. L., Liu, C. L., Hu, H. B., et al., 2012. Sedimentary
Characteristics and Its Environmental Significance of
Li, C. B., Guo, W., Song, Y. Q., et al., 2006. The Genetic
Salt-Bearing Strata of the Member 4 of Paleocene Sha-
Type of the Oil Shale at the Northern Foot of Bogeda
shi Formation in Southern Margin of Jiangling Depres-
Mountain, Xinjiang and Prediction for Favorable Areas.
sion,
Journal of Jilin University (Earth Science Edition),
36(6): 949–953 (in Chinese with English Abstract)
Jianghan
Basin.
Palaeogeography,
14(2):
165–175 (in Chinese with English Abstract)
Wang, S. B., Sun, Y., Zhong, J. H., et al., 2008. The Influ-
Li, J. J., 2009. Study on the Oil Shale Geochemistry of Per-
ence of the Ancient Climate Changes on the Develop-
mian Lucaogou Formation in the Northern Bogda
ment of Sequence Development in the Late Cretaceous
Moutain: [Dissertation]. China University of Geos-
in Songliao Basin. Petroleum Geology and Engineering,
ciences, Beijing. 1–90 (in Chinese with English Ab-
22(4): 29–32 (in Chinese)
stract)
Wang, X. W., Wang, X. W., Ma, Y. S., et al., 2007. The
Li, N., Hu, C. Y., Ma, Z. W., 2011. Main Control Factors of
Tectonic Evolution of Bogda Mountain, Xinjiang
High Quality Hydrocarbon Source Rocks of the Upper
Northwest China and Its Relationship to Oil and Gas
Permian Dalong Formation at Shangsi Section of
Accumulation. Geoscience, 21(1): 116–124 (in Chinese
Guangyuan, Sichuan Province. Palaeogeography, 13(3):
with English Abstract)
347–353 (in Chinese with English Abstract)
Wang, Z. M., 2003. Geochemical Indicators Fordiagnosing
Li, S. J., Xiao, K. H., Wo, Y. J., et al., 2008. REE Geo-
Anoxic Sedimentary Environment. Acta Geologica
chemical Characteristics and Their Geological Signifi-
Gansu, 12(2): 55–58 (in Chinese with English Abstract)
cation in Silurian, West of Hunan Province and North
Wilde, P., Quinby, M. S., Lyons, T. W., 2001. Molybdenum
of Guizhou Province. Geoscience, 22(2): 273–280 (in
as an Indicator of Original Organic Content in Ancient
Chinese with English Abstract)
Anoxic Sediments. Geological Society of American,
Lyons, T. W., Werne, J. P., Holander, D. J., et al., 2003.
33(6): 39 (Abstracts with Programs)
Contrasting Sulfer Geochemistry and Fe/Al And Mo/Al
Zhang, M. M., Liu, Z. J., Xu, S. C., et al., in press. Analysis
Ratios across the Last Oxic-Anoxic Transition in the
for the Paleosalinity and Lake-Level Changes of the Oil
Cariaco Basin, Venezuela. Chemical Geology, 195:
Shale Measures in the Lucaogou Formation in San-
131–157
gonghe Area of Southern Margin, Junggar Basin. Pe-
Peng, X. F., Wang, J. L., Jiang, L. P., 2012. Geochemical
Characteristics of the Lucaogou Formation Oil Shale in
troleum Science and Technology