Full text of DOI:10.1007/BF02875392

Vol. 44 No. 11
SCIENCE IN CHINA (Series D)
November 2001
Three evolutionary stages of the collision orogenic
deformation in the Middle Yangtze Region
SUN Yan (孙 岩)1, SHU Liangshu (舒良树)1, ZHU Wenbin (朱文斌)1,
GUO Jichun (郭继春)1, CHEN Xiangyun (陈祥云)2, M. Faure3, J. Charvet3
& W. Lin3
1. State Key Laboratory of Mineral Deposits, Department of Earth Sciences, Nanjing University, Nanjing 210093, China;
2. Geological Survey Institute of Jiangxi Province, Nanchang 330201, China;
3. Department of Earth Sciences, Orleans University, BP 6759, Orleans, France
Correspondence should be addressed to Sun Yan (email: sunyan003@china.com)
Received August 25, 2000
Abstract A discussion of collision orogenic deformation has been made for the Middle Yangtze
Region. Based on its deformation assemblage orders, three developing stages are classified suc-
cessively as compression thrust uplift, strike-slip escape rheology and tension extension inversion.
The collision orogenesis of the studied region has been divided into three developing periods of
initial, chief and late orogeny. Based on the data from Wugong Mts., Jiuling Mts. and Xuefeng Mts.,
for each stage, its variation of stress and strain axes, the conversion of joint fractures and their
relative tectonic evolution are described, models are plotted and corresponding explanations are
made for the rock chronology dating value in the same tectonic period.
Keywords: collision orogenesis, deformation, tectonic evolution, the Middle Yangtze Region.
—
Since the 1980s, in the course of collision geotectonic research[1 3], Guo et al.[4,5], Hsü et
—
al.[6], Li et al.[7 9] have carried out a further study on the collision orogenesis in South China based
on their studies on plate tectonics and the model shown by Sengör[10]. It is considered that South
China is of Altay style or Turkic type, demonstrating that its characteristics are the regression of
submarine trench toward ocean and island arc magmatism advances toward accretonary complex.
During the 1990s, the Chinese and French geologists carried out geological investigations for
five times in Jiangxi, Hunan and Hubei provinces of the Middle Yangtze Region. Based on the
previous studies with special emphasis on the crust composition, facial belt blocking and macro-
structure of the collision orogenic zone, special attention is paid to the discussion of the stress and
—
strain, the deformation and micro-mechanism of movement properties[11 15]. Based on its defor-
mation assemblage orders, three developing stages are classified successively as compression
thrust uplift, strike-slip escape rheology and tension extension inversion; and the process of the
collision orogenesis are divided into three developing periods of initial, chief and late orogeny.
1
Stage of compression thrust uplift
(1) In the Middle Yangtze Region, the trench, arc and basin systems and geotectonic facies in

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EVOLUTION STAGES OF THE OROGENIC DEFORMATION
991
collision orogenic zone were developed
very completely in the Middle Neopro-
terozoic to early Palaeozoic (fig. 1)[4,5,8,9]
.
During the survey of regional great
sections (fig. 1, Dayong-Lengshuijiang
section in Xuefeng Mts.; Xiushui-Ji’an
section in Jiuling and Wugong Mts.), the
authors found the phenomena of early
inversion and late obversion, tension and
extension produced by bedding slip-
ping[16]. In fact, the inherent law can be
sought from the complete process of col-
lision orogenesis with combination of
explanation to deformation evolutionary
Fig. 1. General distribution sketch of geotectonic facies in collision
orogenic zone, the Middle Yangtze Region (simplified from ref. [7]).
The straight lines are profiles of regional survey.
dynamics[17]
.
(2) In the Middle Yangtze Region, the both collision orogenic zones (Jiuling Mts. and Xue-
feng Mts.) in Neoproterozoic and early Palaeozoic (Wugong Mts.) are linked mountains of fin-
ished and ripe forms. They belong to an evolutionary process of continuous development instead
of being built once only. Either from formation or from deformation, they can be divided into ini-
tial, chief and late orogenic periods, and there might occur superimposed orogenesis or
re-orogenesis when they acted continually. From the viewpoint of deformation, it can be recog-
nized from the alteration of stress axis and strain axis. It is clear that σ 2‖B was altered from
vertical state to horizontal one and then returned back, showing that σ 2‖B is the boundary of
initial period, earlier period and later period of chief orogenesis. However, σ 1‖A of the late oro-
genic period is vertical, bearing characteristics quite different from the previous two periods (table
1). In addition, the plane joint X in early stage and section joint X in late stage also serve as im-
portant recognition marks for the initial period and earlier stage of the chief orogenesis. From
compression to strike-slip, section X, instead of plane joint X (overthrust and thrust faults) is con-
verted to slip structure parallel to the mountain bodies (table 1). In the Middle Yangtze Region,
during the first deformation stage, corresponding to the collision orogenic and developing stages,
e.g., compression thrust uplift stage, the layer-slip and dip-slipping are especially active on dif-
ferent rocks and litho-interfaces, resulting in the formation of ramp and opposite types of struc-
tures (fig. 2) by compressive fold including longitudinal flexed folds of overturn, recumbent,
convolute, thrusting nappe structure (para-autochthonous change of rock plate, imbricate and
poly-superimpostion), different from those of backthrusting and deviate types in the Tianshan Mts.
and Dabie Mts.[18]. Fig. 2 only plots one side of the mountain. From Jiuling Mts. northward to

σ
σ
σ
σ
σ
σ
σ
σ
σ
σ
σ
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EVOLUTION STAGES OF THE OROGENIC DEFORMATION
993
Xiushui (fig. 2(a)), and from Wugong Mts. southward to Yuanbei (fig. 2(b)), ramp types are
formed along the mountains. In the late orogenic period, negative faults shifted to positive move-
ment, being called opposition.
Fig. 2. Tectonic profile from Jiuling Mts. to Fangxi, Changfang to Wugong Mts., northern Jiangxi. Mg, my-
lonitic gneiss; γ , granite; γδ 22 , granodiorite of Middle Proterozoic; 165°/48°, layer or foliation occurrence cor-
responding to surface measurements, showing dip and dip angle (the same below); the trending of early period is
signed by the dotted arrow (the same below).
(3) As late orogenesis may damage, disturb and cover its early tectonic features, the
Sino-French cooperators paid much attention to the study of the following microstructures, their
functions of orientation in defining ductile shear zones to improve the research precision[19,20]: 1)
σ -δ porphyroid rotation and shearing, with δ -type well developed in the studied region; 2) S-C
planar gliding which is rather popular in mylonite and gneissic mylonite; 3) P-Q micro-area dif-
ferentiation, with feldspar and quartz differentiating dynamically and forming pressure shadow
and margin; 4) L-F fabric orientation, with clear and definite lineation and fabric structures. In the
studied area, the former two indicate tendency, and the latter two indicate orientation. The applica-
tion of the composite features of R-P planes in brittle deformation belt is helpful to accurately dif-
ferentiate the middle- and small-sized structures in three deformation stages as well as even some
negative, translational and positive movement of regional structure. On lots of tectonic profiles
from Xiexi, Yichun located on south slope of the Jiuling Mts. to Xiashihe, northward thrusting
features can be found in mylonite gneissic belts, and through σ quartz porphyroid, the trend of
mineral lineation L in foliation can be recognized accurately. More important is that in the slightly
metamorphic strata of the Middle Proterozoic Shuangqiaoshan Group (fig. 3) near Linghuxiang,
early thrusting fractures converted into positive stretching faults in late tectonic period. Near the
distinct fractures parallel to the positive faults, the relict thrusting drag folds are found. Comparing
the thrusting drag of the early fracture with that of the late period, it can be found that the inter-

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SCIENCE IN CHINA (Series D)
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sected angle between axial plane and section from the derived fold is quite small (fig. 3B). This
phenomenon is also evident in the Xuefeng and Wugong Mts. In a word, for the tectonic features
in the stage of compressive thrusting uplift in the studied area, the closer they are to the mountains,
the clearer the features are, and undoubtedly, the thrusting structures on both sides of the moun-
tains must be the products of late orogenic period (fig. 2(b), Changfang area).
Fig. 3. Tectonic profile of Xiexi to Xiashihe in Yichun Region, northern Jiangxi. A, Mould map of
thrust direction; B, C, profiles of local structure details (legends the same as in fig. 2).
2
The stage of strike-slip escape rheology
(1) As the relics of deformation and features in this stage are minor, the sizing and determi-
nation are rather difficult compared with the rest two stages. In the studied area, the strike-slip
structures within the joined zones of island arc and basin, i.e. basin and range intermediate zone,
are pretty evident, and progressively reach a certain scale in the ductile fracture zones from
Pingxiang to Leping of the Middle Proterozoic island and basin system in Jiuling Mts., with a
width of 2—4 km and intermittent extension of 200 km. Taking Wanli-Fangxi section as an exam-
ple, where many times of studies have been made (fig. 4), the rock composition in the section is
mainly mylonitic gneiss, associated with gneissic mylonite and mylonite composed of quartz,
K-feldspar, plagioclase (An 5—20), biotite, muscovite, sericite and penninite, and with or-
thogneiss as primary rock. Within the high strain domains of the ductile shear zone, lineation and
foliation are extremely developed, deformations of different generations are inter-superimposed,
the structures of different types are inter-composed, and the phenomena of spatial and temporal
evolution are plentiful. Based on the field observation and projection analyses on ductile mi-
cro-structures of σ -δ, S-C, P-Q, L-F, it is found that the mineral lineation occurrence is 60°∠
20°, and mylonitic foliation occurrence is 70°∠65°(fig. 5)[15]. In the studied area, most of the

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995
Fig. 4. Geological tectonic sketch map of ductile shear zone in the basin and range joined blocks (Wanli-Fangxi),
northern Jiangxi[15]
.
asymmetric porphyroids are type σ , the por-
phyroids of rigid quartz, feldspar and muscovite
are usually 2—3 mm, with the tail part com-
posed of sericite and chlorite of stress minerals
formed by dynamic metamorphism. For the
penetrative mylonitic foliation of S-C, the closer
to the shear surface, the smaller their inclined
angles will be. With the help of porphyroid sys-
tem and mylonitic foliation, the strike-slip shear
movement translated (strike-slipped) left-later-
ally from southwest to northeast can be accu-
rately determined.
(2) During the late period of chief orogene-
sis, because of the geometric nonlinearity, the Fig. 5. Shi’s projection net map of the ductile shear zone of
the joined blocks in basin and range. ■, Lineation, ▲,
foliation. L and S show the lineation and foliation maximum
unevenness of loading distribution and anisotro-
respectively.
pism of the physical change of rocks around the
collision orogenic boundaries, the nature of the earlier thrusting faults was converted to longitudi-
nal movement along the strike of the mountains. Besides, as far as the whole process of the colli-
sion orogenic dynamics is concerned, the conversion of mechanical energy and thermal energy
weakened the interfacial friction and intensified the rheological creeping[21]. In addition, when the
mineral density difference, linear defect in ductile shear zones and the hidden fissures in ductile
and brittle deformations were pressed in a vertical direction, the stress would be focused on their
ends on the contrary. In this case, movement would occur in a vertical direction with pressure ex-
ertion, i.e., the H.Odë rheology[22], which helped to bring about the new movement of shear glid-
ing and strike slipping.

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In the joined basin and range zones at the south edge of Jiuling Mts., the landmass on south
side of the sinistral strike-slip fracture of ductile shearing was pressed out from SWW to NEE, i.e.
from Pingxiang to Leping. The landmass creeped along strike-slip fracture from high to low stress,
and its resulted deformation was called escape structure[23,24]. In addition, toward Nanchang and
Leping between Jiuling Mts. and Wugong Mts., there was a wedge-shaped block narrow in the
west and wide in the east. Although the dextral strike-slip is not evident in the ductile shear zone
on the south slope of Wugong Mts., it is obviously shown in a large area of cold lineation in the
Middle Palaeozoic along Pingxiang, reflecting exactly the eastward movement of the
wedge-shaped block. This phenomenon is matchable to the escape structure in the Lower Yangtze
Region[25]
.
3
The stage of tension extension inversion
(1) In the studied area, the tension extension tectonic features in the late orogenic period were
better preserved and sized easily compared with those of the former two periods. Fig. 2, fig. 3 and
figs. 6—8 show characteristics of positive extension, especially compression first and then exten-
sion.
Fig. 6. Geological tectonic sketch profile from Yuanshui to Lengshuijiang, western Hunan. Early tendency was
signed by dotted arrow.
Fig. 7. Dip-slip fracture structure of compression first and then extension between Middle Devonian Tiaoma-
jian Fm. and Qiziqiao Fm. by the highway of Longkou, Dongkou region, western Hunan. F1, Primary fracture
plane; F2, late associated fracture plane.
In fig. 7, between the quartz sandstone of the Tiaomajian Fm. (D2t) and siltstone shale of the
Qiziqiao Fm.(D2q), there existed an obvious phenomenon of compression first and then extension
for the dip-slip fracture. A small drag fold is developed in siltstone shale. From transversal view-
point, the occurrences of axial plane are 265º∠46º, 287º∠41º and 290º∠36º respectively and
become gentle in proper order as far away from the section. From longitudinal viewpoint, the dip
angle of axial plane is wavy and gets more gentle from surface layer downward, three series of

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997
Fig. 8. Negative inversion change of the late thrusting fracture zones along lenticule and foliation zones in
Shuangqiao Fm. of Middle Proterozoic by the highway of Diaofeng, Yifeng, northern Jiangxi.
gliding structures could be classified according to its disharmonic development and bedding slip-
ping, and the gliding structures become more gentle when they dip downward. In the blent layer
sections of the Qiziqiao Fm. and Tiaomajian Fm., there is another series of disharmonic folds with
their axial planes nearly horizontal: 85º∠10º and 312º∠10º. Towards the main section, there oc-
cur 2 m of faulted breccia and pudding sandstone with the cleavage destroyed near fault and local
schistosity. They are fine-grained, mylonitic rocks, with stress mineral developed microscopically.
These are resulted from the thrust in the early period. In the above two groups of disharmonic
folds, the former was formed by late tension with axial dipping NWW; the latter was formed by
early thrust and compression, and the late gliding was the source of the disorder of axial dip (the
gliding was also mingled in F1 and F2). Besides, the foliation fabric and porphyroid traces re-
maining on F1 and F2 surfaces can be helpful to discriminate the tendency. The conversion of the
mechanical property is a typical case of the negative inversion tectonics of faults[26]
.
(2) The late orogenic period can be further divided into two sub-periods: layer slip decolle-
ment and gravity decollement tension extension (table 1). The first sub-period is generally devel-
oped in the studied area (fig. 2, fig. 3B and fig. 6), and figs. 7 and 8 also show the dip-slipping
fractures and glide-overburden structures from bedding to tangential, evolving into negative
inversion tectonics along compressive schistose and lenticule zones of thrusting fracture belt (fig.
8). From the folds derived from the faults shown in figs. 7 and 8, it can be observed that the
deeper the folds go downward, the more gentle they become, i.e. a large-sized main decollement
fault could be found in the deeper parts[16]. The second sub-period (gravity decollement), however,
brings about some brittlely deformed tectonics, which are scattered if there are no regional big
decollement faults.
(3) In view that the tension extension inversion stage is the product of late orogenic period, it
inevitably contains some features of the previous two stages, which is also shown clearly in the
micro-fabric diagram (fig. 9). The azimuth of quartz axis c was tested with INEL 309 X-ray tex-
ture gonimeter in the Department of Earth Sciences, Orleans University, France. The fabric dia-
gram for the main part and east and west sides of the Wugong Mts. shows a B-type tectonite of
orthorhombic symmetry, and axis b shows a secondary maximum and present as the remains of

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previous stages.
(4) In the tension extension inversion stage, frontal edge in the orogenic zone can convert
from tension to thrusting to nappe structure and even ramp structure, which is clearly seen be-
tween the Jiuling and Wugong Mts. As shown in fig. 6, the Lower Carboniferous has been evolved
into a klippe. In addition, large-sized regional decollement tectonics are rather popular in the duc-
tilely deformed zones of metamorphic layers, with gentle occurrence. But the horizontal
decollement occuring in the Permian limestone as shown in fig. 3C are rare.
Fig. 9. Simplified maximum diagram of quartz fabric azimuth in ductile deformed layers of the exten-
sional structures, Wugong Mts., northern Jiangxi. The upper three diagrams are the main parts of the moun-
tain range, the lower three are sampled from east and west sides of the mountain rage. WG101, Serial No.
of samples; n, frequency of measurements.
4
Discussion and conclusions
The developing process of southeast China landmass, including collision orogenesis in the
Middle Yangtze Region is complicated, and related marks are abundant [7]. In terms of the defor-
mation rather than the formation, a law of the spatial-temporal evolution of some principal marks
such as thrust and ductile shear zones have been described in this paper.
(1) From the viewpoint of deformation, the collision orogenic period can be divided into ini-
tial, chief and late orogenic developing periods and three evolving stages of compression,
strike-slip and extension. The initial and chief orogenic stages can be merged into the former early
orogenic period (table 1). In space, the variation of tectonic stress field and compound of tectonic
system of the orogenic zone can be compared with the model made for the deformation growing
process of the Wugong Mts. (fig. 10), so the spatial-temporal evolution frame chart of three great
deformation composition orders are constructed.
(2) The deformation evolving period corresponding to the orogenic stage may be divided into
long and short periods based on the analysis of collision orogenesis of the Middle Yangtze Region.
In view of the multi-periods and multi-transmigrations for the region, the long period is relatively

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999
Fig. 10. The tectonic deformation model of collision orogenic zone, the Middle Yangtze Region. γ,
Granite; mr, migmatite; mg, mylonitic gneiss; dd, ductile deformed layers; bd, brittle deformed layers;
St, strike-slip fracture; Sh, scabbard fold; EX, early joint X(fracture); LX, late joint X(fracture); ac, ac
fissure(fracture); a, b, c, coordinate axes.
easy to differentiate. It took a short continuous time for the earlier and later period of the chief
orogenesis to convert from compressive thrusting to strike-slip escape, and the stress and strain
axis σ 2‖B convert from horizontal to vertical. In the synorogenic period, there exists a wide
range of emplaced magmatite and hypo-metamorphic rocks of aggradational metamorphism (table
1), and they may be taken as the substantial foundations for the age determination. However, the
late-orogenic period will be judged by the magmatite of small-range emplacement and the
epi-metamorphic rocks of degradational metamorphism in the tension extension stage of synoro-
genic period. Based on the above principles, with the magmatite emplacement age determination
tested for the chief orogenic period, the age for the Xuefeng, Jiuling and Wugong Mts. in the Mid-
dle Yangtze Region is inferred to be 760[27], 805[15] and 403 Ma1), respectively. The former two
belong to the Neoproterozoic (Pt3) and the last belongs to the Early Devonian in age. The age de-
termination for the later orogenic period will be judged by sample measurement from the Wugong
Mts. with the 40Ar/39Ar method by the Sino-French cooperators at the University of Montpellier,
so the ages are 259.0±3.3 and 233.5±5.0 Ma for magmatites, 229.0±2.9, 225.6±2.9 and
131.7±1.7 Ma for metamorphic rocks. All belong to the Late Permian to Late Triassic in age and
Early Cretaceous for certain specific rocks, over 144 Ma later than the chief orogenic period[28]
.
(3) With regard to the three deformation evolving stages of the collision orogenesis, there has
been a lot of statement on the pattern of compression first and then extension, earlier traction and
later slip as well as the conversion of compression thrusting into tension extension in the orogenic
periods[12,13,22], but the study of strike-slip escape stage between the two stages is not enough[29]
.
The Jiuling Mts. has its age data from the ductile zone of its south edge (figs. 4—6),
410.79±18.69 Ma for dynamic metamorphic rock of Shanggao, and 394 Ma[15] for monzonite of
1) Jiangxi Bureau of Geology and Mineral Resources, Regional Geoloy of Jiangxi Province, The Map of Magmatic Rocks
for Jiangxi Province (1︰50000), 1984.

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nonmylonization from Fengding Mts. by Rb/Sr method, roughly reflecting that the active time of
strike-slip zone in the Jiuling Mts. is prior to the Late Silurian-Early Devonian. In fact, the accu-
rate determination of the tectonics in strike-slip stage needs systematic reconnaissance analysis
and age determination not only on lithorheology, tectonic escape, but also on the change of litho-
sphere and the complete process of the orogenesis.
Acknowledgements This work was supported by the National Natural Science Foundation of China (Grant No.
49972069), the State Key Laboratory of Southwest Petroleum Institute, and Beijing Institute of Geomechanics. Thanks are due to
the academician Guo Lingzhi of the Department of Earth Sciences of Nanjing University and Prof. Li Jiliang of Geological In-
stitute of the Chinese Academy of Sciences for their utmost instructions in the course of research and writing of the paper.
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