NOTES
2. Manabe, S., Broccoli, A. J., Mountains and arid climate of middle
latitudes, Science, 1990, 247: 192.
3. Molar, P., England, P., Marlinod, J., Mantle dynamics, uplift of the
Tibetan Plateau and Indian monsoon, Rev. Geophys., 1993, 31:
357.
4. Zhang Linyuan, The Qinghai-Tibetan Plateau formed process and
the epoch of the climate evaluation in Cenozoic in China, Study-
ing of Qinghai-Tibetan Plateau, Environment Vicissitude and
Ecology System (ed. Sun. H. L.) (in Chinese with English ab-
rate is 0.12 mm/a (the elevation difference) or 0.14 mm/a
(the mineral pair). The average uplift rates based on the
elevation difference (table 2 and fig. 4) have shown some
changes as slow, fast, slow and fast for different epochs. It
is like that the uplift rate is less than 0.05 mm/a from 68.2
to 48.0 Ma; 0.18 mm/a from 48.0 to 45.1 Ma, 0.017 mm/a
from 35.7 to 30.3 Ma, and 0.1 mm/a from 30.5 to 17.8 Ma.
The uplifting of the Hua Shan seems to be accelerated
since 17.8 MaBP, with an average uplift rate of 0.19 mm/a,
and the geomorphologic relief in the Hua Shan reveals the
uplift accelerates in the Late Cenozoic. Based on the data
obtained from the mineral pair (table 3 and fig. 5), the
uplift rate of the Hua Shan has not been much changed for
different epochs, and the uplift rates are less distinct than
those estimated by the elevation difference. The reason for
the distinction of the uplift rates, which were calculated
by the elevation difference method and by the mineral pair
method respectively, may be caused by two factors. One is
that the time interval taken for calculation of the uplift
rate is not the same for two methods. The other may be
the fission track ages of zircon with a large uncertainty.
For a period from 68.2 MaBP to the present, however, the
average uplift rates estimated by the two methods are in
good agreement.
stract), Beijing: Science Press, 1994, 267ü281.
5. Liu Tungsheng, Ding Menglin, Derbyshir, E., Gravel deposits on
the margins of the Qinghai-Tibetan Plateau and their environ-
mental significance, Palaeo-Geography, -Climatology, -Ecology,
1996, 120: 159.
6. Ramstein, G., Fluteau, F., Besse, J. et al., Effect of orogeny: Plate
motion and land-sea distribution on Eurasian climate change over
the past 30 million years, Nature, 1997, 386: 788.
7. The Editorial Committee of China Physical Geography, CAS,
China Physical Geography: Paleogeography (first) (in Chinese),
Beijing: Science Press, 1984, 43ü47.
8. Zhang Guowei, Meng Qingren, Lai Shaocon, tectonics and struc-
ture of the Qinling orogenic belt, Science in China, Ser. B, 1995,
38(11): 1379.
9. Zhao Zongpu, An intracontinental type orogenyüüevidence
from the Qinling-Dabei Orogenic Belt, Scientia Geological Sinica
(in Chinese with English abstract), 1995, 30(1): 19.
10. Zhang Guowei, Meng Qingren, Liu Shoufong et al., Huge in-
tracontinential subduction zone at south margin of the North
China Block and the present 3-D lithosperic framework of the
Qinling orogenic belt, Geological Journal of China University (in
Chinese with English abstract), 1997, 3(20): 129.
11. Cerveny, P. F., Naeser, C. W., Kelemen, P. B. et al., Zircon fission
track ages from the Gasherbrum Diorite, Karakoram Range,
Northern Pakistan, Geology, 1989, 17: 1044.
12. Thomson, S. N., Fission-track analysis and provenance studies in
Calabrian Arc sedimentary rocks, Southern Italy, J. Geol. Society,
1994, 151: 463.
13. Ding Lin, Zhong Dalei, Pan Yusheng, The evidences of fission
track for the fast uplift in east Himalaya from Pliocene epoch,
Chinese Science Bulletin (in Chinese), 1995, 40: 1497.
14. The Study Team of “Active Faults Zone in Ordos Surrounding
Areas”, Active Faults Zone in Ordos Surrounding Areas (in Chi-
There are many summit levels in the Qinling Moun-
tain. The two summit levels in the Hua Shan range are the
south peak (2000ü2200 m) and the north peak (1600ü
1800 m) of the Hua Shan. If the uplift is very slow, and
the exhumation is very intense, and the range must be
very smooth. Based on the uplift rate of the granite mass
in the Hua Shan, it would be suggested that the two
summit levels in the Hua Shan range were formed later
than 48.0 MaBP and earlier than 17.8 MaBP respectively.
nese), Beijing: Seismological Press, 1988, 114ü136.
15. The Northwest Bureau of Geology, MGM, The Geology Report of
Luonan (1:200000) (in Chinese), Beijing: Geological Publishing
House, 1965.
4
Conclusion
Based on the fission track dates of both apatite and
16. The Collaboration Team of Institute of Atomic Energy and Insti-
tute of Geochemistry, CAS, Dating muscovite and glass meteorite
by fission track technique, Geochemica, 1976, (1).
17. Green P. F, Duddy I. R, Laslett G.M., Thermal annealing of fission
tracks in apatite 4. Quantitative modeling techniques and exten-
sion to geological time scales, Chemical Geology (Isotope Geo-
science Section), 1989, 79: 155.
zircon separated from six granite samples from the Hua
Shan, the uplifting of the Hua Shan range started at least
as early as 68.2 MaBP and then the uplift process has
alternated between slow and fast. The uplift of the range
seems to be in the period of faster uplift from (17.8f2.0)
MaBP to the present, with the average uplift rate of about
0.19 mm/a. The two summit levels in the Hua Shan range
might be formed later than 48.0 MaBP and earlier than
17.8 MaBP respectively.
18. Naeser, C.W., Fission-track dating and geologic annealing of fis-
sion track, Lectures in Isotope Geology (eds. Jager, E., Hunziker, J.
C.), New York: Springer-Verlag, 1979, 154ü169.
19. Harrison, T. M., Armstrong, R. L., Naeser C. W., Geochronology
and thermal history of the Coast Plutonic complex, near Prince
Rupert, BC: Canadian Journal of Earth Sciences, 1979, 16: 400.
20. Hurford, A. J., Cooling and uplift patters in the Lepontine Alps,
south-central Switzerland, and an age of vertical movement on the
Insubric fault line, Contributions to Mineralogy and Petrology,
1986, 92: 413.
Acknowledgements The authors thank Zhao Chunhua for separating
minerals from granite samples. This work was supported by the National
Natural Science Foundation of China (Grant Nos. 49732090 and
49872062).
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(Received April 5, 2001)
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Chinese Science Bulletin Vol. 46 No. 19 October 2001