利用宇生同位素～（10）Be对青藏高原东南部沙鲁里山第四纪冰期事件的研究
摘要
由于宇宙射线的照射，地面岩石中生成稳定的和放射性的同位素，如~3He、~(10)Be、~(26)Al、~(14)C、~(41)Ca、~(21)Ne、~(36)Cl等，作者称之为宇生核素。岩石中生成的宇生核素的浓度是其生成速率、累积时间、侵蚀速率和地面隆升速率的函数，根据其原理来计算出地貌面的暴露年代。该测年技术已经成熟，特别是利用宇生核素~(10)Be、~(26)Al对年代的计算，该测年技术在国外的应用已相当普遍。本文应用宇生核素~(10)Be对青藏高原冰川地貌面的年代进行计算。由于石英的抗风化性、普遍存在性和成份的单一性，而被普遍运用于宇生核素~(10)Be的提取，并进行年代计算。
在处理的样品中，属于稻城夷平面的有效样品为四组，共7个样品：X6、X7、X13、X8、X9、X15、X16。样品的处理包括石英中~(10)Be的提取和利用质谱加速器对比值进行测定。石英选取了1-0.25mm之间的颗粒，净化后溶解掉20％—30％的石英外壳，以去除大气成因的宇生核素~(10)Be。经实验获得BeO后，由质谱加速器测定出比值。实验精度通过三组数据反映出来，①三个空白样的测量比值(~(10)Be／~9Be)为：0.125*10~(-13)、0.029*10~(-13)、0.037*10~(-13)，质谱加速器的测量本底值为10~(-15)，将空白样的原子数与本组样品中原子数最少的样品相比较，反映出实验过程中外来~(10)Be所造成的最大误差为0.2％；②同一基岩面上相距50cm的两个样品，实验数据分别为6.88886*10~6atoms／g、6.810176*10~6atoms／g，实验误差为1.15％(这一误差也有可能来源于暴露历史)；③相同样品的两次实验，实验数据为4.491689*10~6atoms／g、4.494642*10~6atoms／g，实验误差为0.07％。由此判断，实验数据是精确而可信的。
年代计算过程中存在三个变量：暴露年代、侵蚀速率和高原的隆升速率。侵蚀速率的切入点是砾石覆压下的冰川擦痕与暴露状态的基岩面存在的约9cm的高差，计算获得的花岗岩的侵蚀速率为6.42(±0.41)*10~(-5) cm／a(样品X8、X9)；将这一侵蚀速率应用于不同地点、不同暴露历史的样品将产生误差，对于采自花岗岩羊背石的样品X6来说，由于其形成年代较短，侵蚀速率对年代的影响很小，年代值的决定因素是宇生核素的形成速率，这一侵蚀速率100％的波动所造成的误差仍在1％范围内；对于取自花岗岩漂砾的样品X15、X16来说，由于形成于同
博士学位论文:利用宇生同位素’怕e对青藏高原东南部沙鲁里山第四纪冰期事件的研究
一冰期事件，且两地相距约20公里，应具有相当的侵蚀速率;对于取自老终磺
垄的样品X7、xl3来说，其侵蚀速率通过最大值与最小值来加以界定，取平均值
来进行计算，并逐渐收敛，收敛于1 .53*1。一4 Cm/a。
同时，由于青藏高原隆升观点的差异性，以及隆升存在的阶段性，使得年代
计算存在一定的复杂性。青藏高原的隆升观点总括起来有两种，一是前期隆升观
点，即第四纪以前青藏高原已达到现今高度;一是后期隆升观点，即青藏高原现
今的高度是第四纪以来的阶段性隆升才达到的，但其隆升速率也存在着不同的观
点，总体来说80万年来的阶段性的隆升速率介于0.133cm/a一0.4 cm/a之间。
根据前期隆升观点，计算出老终债垄的形成年代为459.42ka，冰蚀基岩面
的形成年代为122.ska;羊背石的形成年代为18.3 ka。根据80万年来的阶段
性的隆升速率介于0.133 Cm/a一0.4 Cm/a之间，计算出老终债垄的形成年代
为564.96 ka一656.27 ka，取值为610士50伙a;冰蚀基岩面的形成年代为130.85
ka一149.37 ka，取值为140士9 ka;羊背石的形成年代为18.494 ka一18.790 ka，
取值为18.6士0.Zka。由于终债垄是冰盛期结束时遗留下来的，而冰川擦痕面
是冰期结束过程中暴露出来的，因此不同冰川地貌面反映的冰期中的冰力，事件是
不同的。库照日附近的老终债垄形成于M工S16(后期隆升)或MIS12(前期隆升):
老林口道班附近独立山坡上冰蚀基岩面形成于M工56;兔儿山以北的羊背石形成
于MISZ。
一般来说冰川到达的距离越远、冰川的厚度越大，冰期的规模就越大。根据
三组样品所反映的三次冰期来看，形成于倒数第三次冰期的老终垄的保存，以及
形成于倒数第二次冰期的冰川擦痕面的存在，说明最近三次冰期的规模由大到小
依次为倒数第三次冰期、倒数第二次冰期和末次冰期。同时，由于形成于倒数第
二次冰期的冰川擦痕面，位于稻城夷平面上的独立山坡上的基岩面上，相对高度
约30m，它的保存说明末次冰期发育的冰川规模较小，冰川厚度在该地区没有达
到这一高度，同样也说明了关于末次冰期统一大冰盖的观点将稻城夷平面地区包
括在内是错误的。
根据砾石翻转原理得出的年代值1 30ka--150ka反映出，砾石形成于倒数第二
次冰期，期间遭受末次冰期的冰川覆盖。同时说明末次冰期冰川规模较小，冰川
在高原面上的冰蚀作用也小，否则砾石年代值应在末次冰期年代范围之内。
Under cosmic-ray flux, stable cosmogenic nuclides and radioactive
isotopes are created in geomorphic surface, for example 3He 10Be 26Al
14C 41Ca 21Ne 36Cl. The concentration of cosmogenic isotope in rock surface is a function of age, production rate, erosion rate and uplift rate. Using this model, we can calculate the exposed age. This technique for surface dating is ripe now and often be used, especially cosmogenic
isotopes 10Be and 26Al being used to dating. Cosmogenic isotopes Be was
used to date the glacial geomorphic surface of Qinghai-Xizang Plateau in
this paper. We used quartzite grains for Be because qrartzites are close
to being pure Si02, quartzite is very resistant to weathering and easy
found.
Retreating samples included extracting Be from quart grains and
measuring 10Be/9Be ratio by AMS. Quart grains were picked out in the 0.25
to 1.0 mm size fraction and remove atmospheric Be by confining to the
outer portion about 20%-30%. These samples were made into tergers for analysis by AMS at the Tandetron AMS facility at Gif-sur-Yvette, France.
Experimental precision was indicated by three group data. CD 10Be/9Be ratio of three blank samples: 0.125*10-13 0.029*10-13, 0.037*10-15. The lowest ratio
AMS can measure is 10-15. The maximum error of atmospheric contamination
is 0.2% during experimenting. (2) Be concentration of two samples taking
from same rock surface: 6.88886*106 atoms/g 6.810176*106 atoms/g. The
error is 1.15%. (3) Be concentration of two same samples: 4.491689*10?
atoms/g 4. 494642*106 atoms/g. The error is 0.07%. It can be judged that the experimental data is accurate.
There are three variates during dating: exposure age, erosion rate
and uplift rate of plateau. The erosion altitude 9 cm was determined by the glacial rock surface under big stone and surround rock surface. The erosion rate of granite can be calculated : 6. 42*10 cm/a( through samples: X8 X9) . The erosion rate can be used to other granite samples because they are so near. The erosion rate of samples X7 X13 being taken from the old moraine can be restricted using the maximum erosion rate and the minimum erosion rate. During calculating, the mean value of erosion convergent to 1. 53*10 cm/a.
There are different ideas about Qinghai-Xizang Plateau uplift. In brief, there are two situations. One is Qinghai-Xizang Plateau reached modern height before Quaternary, the other is Qinghai-Xizang Plateau uplifted stage to the height since Quaternary. But there are different ideas about Qinghai-Xizang Plateau uplifting rate. The uplift rate changes from 0. 133 cm/a -0.4 cm/a in 800 ka BP.
According to the idea of uplift early, it can be calculated that the old moraine was formed in 459. 42 ka BP, the glacial rock surface was formed in 122. 5 ka BP and the roche moutonnee was formed in 18. 3 ka BP. According to the uplift rate of 0. 133-0.4 cm/a, the old moraine was formed in 610 ?0ka, the glacial rock surface was formed in 140? ka and the roche moutonnee was formed in 18. 6?. 2 ka. Because moraine remained when ice flourished age was over, and glacial rock surface began to expose during ice age is over, they indicate the glaciation event are different. The old moraine near Kuzhaore was formed in MIS16(uplift late) or Misl2(uplift early). The glacial rock surface on the independent hill near Laolinkou Daoban was formed in MIS6. The roche moutonnee in the north of Mountain Tuershang was formed in MIS2.
Normally , the distance glacial reached is further and the height of glacial is bigger, the scale of ice age is bigger. The old moraine formed in the last but two glaciation and the glacial rock surface formed in the
IV
last but one glaciation can be remained, that indicate the scale of ice age is the last but two glaciation, the last but one glaciation and the last glaciation from the largest to the least. The glacial rock surface formed in the last but one glaciation on the independent hill indicates that the last glaciation was not reach the height. It also indicate that the idea about successive ice sheet includ
在处理的样品中，属于稻城夷平面的有效样品为四组，共7个样品：X6、X7、X13、X8、X9、X15、X16。样品的处理包括石英中~(10)Be的提取和利用质谱加速器对比值进行测定。石英选取了1-0.25mm之间的颗粒，净化后溶解掉20％—30％的石英外壳，以去除大气成因的宇生核素~(10)Be。经实验获得BeO后，由质谱加速器测定出比值。实验精度通过三组数据反映出来，①三个空白样的测量比值(~(10)Be／~9Be)为：0.125*10~(-13)、0.029*10~(-13)、0.037*10~(-13)，质谱加速器的测量本底值为10~(-15)，将空白样的原子数与本组样品中原子数最少的样品相比较，反映出实验过程中外来~(10)Be所造成的最大误差为0.2％；②同一基岩面上相距50cm的两个样品，实验数据分别为6.88886*10~6atoms／g、6.810176*10~6atoms／g，实验误差为1.15％(这一误差也有可能来源于暴露历史)；③相同样品的两次实验，实验数据为4.491689*10~6atoms／g、4.494642*10~6atoms／g，实验误差为0.07％。由此判断，实验数据是精确而可信的。
年代计算过程中存在三个变量：暴露年代、侵蚀速率和高原的隆升速率。侵蚀速率的切入点是砾石覆压下的冰川擦痕与暴露状态的基岩面存在的约9cm的高差，计算获得的花岗岩的侵蚀速率为6.42(±0.41)*10~(-5) cm／a(样品X8、X9)；将这一侵蚀速率应用于不同地点、不同暴露历史的样品将产生误差，对于采自花岗岩羊背石的样品X6来说，由于其形成年代较短，侵蚀速率对年代的影响很小，年代值的决定因素是宇生核素的形成速率，这一侵蚀速率100％的波动所造成的误差仍在1％范围内；对于取自花岗岩漂砾的样品X15、X16来说，由于形成于同
博士学位论文:利用宇生同位素’怕e对青藏高原东南部沙鲁里山第四纪冰期事件的研究
一冰期事件，且两地相距约20公里，应具有相当的侵蚀速率;对于取自老终磺
垄的样品X7、xl3来说，其侵蚀速率通过最大值与最小值来加以界定，取平均值
来进行计算，并逐渐收敛，收敛于1 .53*1。一4 Cm/a。
同时，由于青藏高原隆升观点的差异性，以及隆升存在的阶段性，使得年代
计算存在一定的复杂性。青藏高原的隆升观点总括起来有两种，一是前期隆升观
点，即第四纪以前青藏高原已达到现今高度;一是后期隆升观点，即青藏高原现
今的高度是第四纪以来的阶段性隆升才达到的，但其隆升速率也存在着不同的观
点，总体来说80万年来的阶段性的隆升速率介于0.133cm/a一0.4 cm/a之间。
根据前期隆升观点，计算出老终债垄的形成年代为459.42ka，冰蚀基岩面
的形成年代为122.ska;羊背石的形成年代为18.3 ka。根据80万年来的阶段
性的隆升速率介于0.133 Cm/a一0.4 Cm/a之间，计算出老终债垄的形成年代
为564.96 ka一656.27 ka，取值为610士50伙a;冰蚀基岩面的形成年代为130.85
ka一149.37 ka，取值为140士9 ka;羊背石的形成年代为18.494 ka一18.790 ka，
取值为18.6士0.Zka。由于终债垄是冰盛期结束时遗留下来的，而冰川擦痕面
是冰期结束过程中暴露出来的，因此不同冰川地貌面反映的冰期中的冰力，事件是
不同的。库照日附近的老终债垄形成于M工S16(后期隆升)或MIS12(前期隆升):
老林口道班附近独立山坡上冰蚀基岩面形成于M工56;兔儿山以北的羊背石形成
于MISZ。
一般来说冰川到达的距离越远、冰川的厚度越大，冰期的规模就越大。根据
三组样品所反映的三次冰期来看，形成于倒数第三次冰期的老终垄的保存，以及
形成于倒数第二次冰期的冰川擦痕面的存在，说明最近三次冰期的规模由大到小
依次为倒数第三次冰期、倒数第二次冰期和末次冰期。同时，由于形成于倒数第
二次冰期的冰川擦痕面，位于稻城夷平面上的独立山坡上的基岩面上，相对高度
约30m，它的保存说明末次冰期发育的冰川规模较小，冰川厚度在该地区没有达
到这一高度，同样也说明了关于末次冰期统一大冰盖的观点将稻城夷平面地区包
括在内是错误的。
根据砾石翻转原理得出的年代值1 30ka--150ka反映出，砾石形成于倒数第二
次冰期，期间遭受末次冰期的冰川覆盖。同时说明末次冰期冰川规模较小，冰川
在高原面上的冰蚀作用也小，否则砾石年代值应在末次冰期年代范围之内。
Under cosmic-ray flux, stable cosmogenic nuclides and radioactive
isotopes are created in geomorphic surface, for example 3He 10Be 26Al
14C 41Ca 21Ne 36Cl. The concentration of cosmogenic isotope in rock surface is a function of age, production rate, erosion rate and uplift rate. Using this model, we can calculate the exposed age. This technique for surface dating is ripe now and often be used, especially cosmogenic
isotopes 10Be and 26Al being used to dating. Cosmogenic isotopes Be was
used to date the glacial geomorphic surface of Qinghai-Xizang Plateau in
this paper. We used quartzite grains for Be because qrartzites are close
to being pure Si02, quartzite is very resistant to weathering and easy
found.
Retreating samples included extracting Be from quart grains and
measuring 10Be/9Be ratio by AMS. Quart grains were picked out in the 0.25
to 1.0 mm size fraction and remove atmospheric Be by confining to the
outer portion about 20%-30%. These samples were made into tergers for analysis by AMS at the Tandetron AMS facility at Gif-sur-Yvette, France.
Experimental precision was indicated by three group data. CD 10Be/9Be ratio of three blank samples: 0.125*10-13 0.029*10-13, 0.037*10-15. The lowest ratio
AMS can measure is 10-15. The maximum error of atmospheric contamination
is 0.2% during experimenting. (2) Be concentration of two samples taking
from same rock surface: 6.88886*106 atoms/g 6.810176*106 atoms/g. The
error is 1.15%. (3) Be concentration of two same samples: 4.491689*10?
atoms/g 4. 494642*106 atoms/g. The error is 0.07%. It can be judged that the experimental data is accurate.
There are three variates during dating: exposure age, erosion rate
and uplift rate of plateau. The erosion altitude 9 cm was determined by the glacial rock surface under big stone and surround rock surface. The erosion rate of granite can be calculated : 6. 42*10 cm/a( through samples: X8 X9) . The erosion rate can be used to other granite samples because they are so near. The erosion rate of samples X7 X13 being taken from the old moraine can be restricted using the maximum erosion rate and the minimum erosion rate. During calculating, the mean value of erosion convergent to 1. 53*10 cm/a.
There are different ideas about Qinghai-Xizang Plateau uplift. In brief, there are two situations. One is Qinghai-Xizang Plateau reached modern height before Quaternary, the other is Qinghai-Xizang Plateau uplifted stage to the height since Quaternary. But there are different ideas about Qinghai-Xizang Plateau uplifting rate. The uplift rate changes from 0. 133 cm/a -0.4 cm/a in 800 ka BP.
According to the idea of uplift early, it can be calculated that the old moraine was formed in 459. 42 ka BP, the glacial rock surface was formed in 122. 5 ka BP and the roche moutonnee was formed in 18. 3 ka BP. According to the uplift rate of 0. 133-0.4 cm/a, the old moraine was formed in 610 ?0ka, the glacial rock surface was formed in 140? ka and the roche moutonnee was formed in 18. 6?. 2 ka. Because moraine remained when ice flourished age was over, and glacial rock surface began to expose during ice age is over, they indicate the glaciation event are different. The old moraine near Kuzhaore was formed in MIS16(uplift late) or Misl2(uplift early). The glacial rock surface on the independent hill near Laolinkou Daoban was formed in MIS6. The roche moutonnee in the north of Mountain Tuershang was formed in MIS2.
Normally , the distance glacial reached is further and the height of glacial is bigger, the scale of ice age is bigger. The old moraine formed in the last but two glaciation and the glacial rock surface formed in the
IV
last but one glaciation can be remained, that indicate the scale of ice age is the last but two glaciation, the last but one glaciation and the last glaciation from the largest to the least. The glacial rock surface formed in the last but one glaciation on the independent hill indicates that the last glaciation was not reach the height. It also indicate that the idea about successive ice sheet includ
引文
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