<table><tr><td>10DX140-34</td><td>Qz5 b</td><td>26.1 131 608 86.7</td><td>v.d.</td><td>21.8</td><td>v.d.</td><td>v.d.</td><td>0.435</td><td>&lt;0.00</td><td>0.137</td><td>2.92</td><td>v.d.</td><td>v.d.</td><td>0.266</td><td>2.30</td><td>v.d.</td><td>0.56</td><td>1086</td><td>0.1</td><td>0.5</td><td>411</td><td>419</td></tr><tr><td>10DX140-37</td><td>Qz5 b</td><td>29.4 52.5 375 42.8</td><td>317</td><td>11.2</td><td>0.757</td><td>v.d.</td><td>0.830</td><td>&lt;0.95</td><td>0.202</td><td>2.94</td><td>1.64</td><td>1.56</td><td>&lt;0.06<br>3</td><td>1.97</td><td>0.589</td><td>0.56</td><td>670</td><td>0.1</td><td>0.5</td><td>372</td><td>380</td></tr><tr><td>10DX140-43</td><td>Qz5 b</td><td>30.6 29.5 v.d. v.d.</td><td>256</td><td>11.2</td><td>1.62</td><td>v.d.</td><td>0.720</td><td>&lt;0.53</td><td>0.0840</td><td>2.14</td><td>1.48</td><td>v.d.</td><td>0.369</td><td>1.18</td><td>1.22</td><td>0.56</td><td>v.d.</td><td>0.1</td><td>0.5</td><td>243</td><td>249</td></tr><tr><td>10DX140-44</td><td>Qz5 b</td><td>7.24 64.1 98.2 25.2</td><td>&lt;54.86</td><td>8.12</td><td>v.d.</td><td>v.d.</td><td>v.d.</td><td>3.10</td><td>&lt;0.013<br>1</td><td>2.31</td><td>1.28</td><td>0.62</td><td>0.154</td><td>0.761</td><td>0.995</td><td>0.56</td><td>175</td><td>0.1</td><td>0.5</td><td>264</td><td>270</td></tr><tr><td>10DX140-46</td><td>Qz5 b</td><td>46.8 73.5 410 29.7</td><td>v.d.</td><td>14.9</td><td>0.0480</td><td>v.d.</td><td>&lt;0.15<br>5</td><td>&lt;0.00</td><td>0.068</td><td>2.62</td><td>0.350</td><td>0.359</td><td>0.050<br>0</td><td>0.637</td><td>0.752</td><td>0.56</td><td>731</td><td>0.1</td><td>0.5</td><td>373</td><td>380</td></tr><tr><td>10DX140-47</td><td>Qz5 b</td><td>23.4 48.1 334 17.2</td><td>&lt;67.59</td><td>9.10</td><td>&lt;0.031</td><td>v.d.</td><td>0.343</td><td>1.14</td><td>0.254</td><td>6.24</td><td>2.17</td><td>v.d.</td><td>0.156</td><td>0.900</td><td>0.571</td><td>0.56</td><td>597</td><td>0.1</td><td>0.5</td><td>355</td><td>362</td></tr><tr><td>10DX140-48</td><td>Qz5 b</td><td>23.7 70.0 364 17.8</td><td>&lt;67.44</td><td>12.0</td><td>0.0510</td><td>5.10</td><td>&lt;0.14<br>6</td><td>&lt;0.55</td><td>&lt;0.00</td><td>3.46</td><td>3.34</td><td>1.75</td><td>0.165</td><td>0.950</td><td>0.865</td><td>0.56</td><td>651</td><td>0.1</td><td>0.5</td><td>389</td><td>396</td></tr><tr><td>10DX145-4</td><td>Qz5 b</td><td>40.3 99.4 119<br>0</td><td>31.2</td><td>220</td><td>3.21</td><td>0.0600</td><td>1.19</td><td>0.850</td><td>&lt;0.64</td><td>1.17</td><td>4.65</td><td>5.40</td><td>0.275</td><td>0.084</td><td>v.d.</td><td>0.139</td><td>0.62</td><td>1919</td><td>0.1</td><td>0.5</td><td>361</td><td>369</td></tr><tr><td>10DX145-5</td><td>Qz5 b</td><td>20.2 31.2 527 38.9</td><td>&lt;147.6<br>6</td><td>2.61</td><td>&lt;0.101</td><td>2.11</td><td>0.870</td><td>2.01</td><td>0.118</td><td>3.06</td><td>1.10</td><td>0.277</td><td>&lt;0.09<br>8</td><td>2.52</td><td>&lt;0.097</td><td>0.62</td><td>851</td><td>0.1</td><td>0.5</td><td>376</td><td>384</td></tr><tr><td>10DX145-12</td><td>Qz5 b</td><td>28.8 41.3 868 241</td><td>&lt;48.18</td><td>2.87</td><td>0.304</td><td>6.85</td><td>0.780</td><td>0.410</td><td>0.229</td><td>3.57</td><td>2.19</td><td>0.073</td><td>0.427</td><td>2.02</td><td>0.082</td><td>0.62</td><td>1399</td><td>0.1</td><td>0.5</td><td>310</td><td>316</td></tr><tr><td>10DX145-14</td><td>Qz5 b</td><td>36.3 93.2 v.d. v.d.</td><td>108</td><td>8.58</td><td>0.822</td><td>v.d.</td><td>1.75</td><td>1.04</td><td>0.159</td><td>4.01</td><td>2.40</td><td>0.431</td><td>0.176</td><td>2.00</td><td>&lt;0.055</td><td>0.62</td><td>v.d.</td><td>0.1</td><td>0.5</td><td>300</td><td>307</td></tr><tr><td>10DX145-15</td><td>Qz5 b</td><td>49.5 69.3 112<br>8</td><td>17.4</td><td>&lt;99.11</td><td>8.63</td><td>0.109</td><td>3.36</td><td>&lt;0.22</td><td>0.890</td><td>0.563</td><td>2.50</td><td>2.57</td><td>0.048<br>1</td><td>0.152</td><td>2.98</td><td>0.178</td><td>0.62</td><td>1819</td><td>0.1</td><td>0.5</td><td>305</td><td>311</td></tr><tr><td>10DX145-17</td><td>Qz5 b</td><td>45.6 95.4 937 22.0</td><td>&lt;64.58</td><td>5.99</td><td>1.86</td><td>7.14</td><td>0.880</td><td>&lt;0.44</td><td>0.214</td><td>4.44</td><td>4.9</td><td>0.195</td><td>0.077</td><td>2.39</td><td>0.071</td><td>0.62</td><td>1512</td><td>0.1</td><td>0.5</td><td>358</td><td>365</td></tr><tr><td>10DX145-22</td><td>Qz5 b</td><td>28.4 12.4 457 7.88</td><td>75.2</td><td>2.84</td><td>0.330</td><td>6.18</td><td>&lt;0.15</td><td>&lt;0.75</td><td>0.348</td><td>4.91</td><td>4.13</td><td>0.055</td><td>0.072</td><td>3.13</td><td>0.385</td><td>0.62</td><td>736</td><td>0.1</td><td>0.5</td><td>358</td><td>366</td></tr><tr><td>10DX145-26</td><td>Qz5 b</td><td>26.1 52.9 392 11.3</td><td>&lt;72.40</td><td>4.30</td><td>2.02</td><td>v.d.</td><td>1.33</td><td>&lt;0.50</td><td>0.374</td><td>4.27</td><td>2.33</td><td>0.832</td><td>&lt;0.04<br>7</td><td>2.56</td><td>0.336</td><td>0.62</td><td>632</td><td>0.1</td><td>0.5</td><td>340</td><td>347</td></tr><tr><td>10DX145-31</td><td>Qz5 b</td><td>30.2 &lt;3.7<br>7</td><td>634</td><td>&lt;6.78</td><td>&lt;123.3<br>0</td><td>3.68</td><td>&lt;0.091</td><td>1.42</td><td>&lt;0.30</td><td>&lt;0.75</td><td>0.407</td><td>2.52</td><td>2.53</td><td>&lt;0.03<br>4</td><td>0.175</td><td>0.731</td><td>0.076</td><td>0.62</td><td>1023</td><td>0.1</td><td>0.5</td><td>304</td><td>311</td></tr><tr><td>10DX145-32</td><td>Qz5 b</td><td>26.1 &lt;3.8<br>8</td><td>522</td><td>&lt;7.31</td><td>&lt;137.5<br>1</td><td>2.39</td><td>&lt;0.060</td><td>&lt;0.23</td><td>0.690</td><td>0.580</td><td>0.400</td><td>2.60</td><td>0.730</td><td>1.30</td><td>0.145</td><td>0.457</td><td>&lt;0.085</td><td>0.62</td><td>841</td><td>0.1</td><td>0.5</td><td>323</td><td>330</td></tr><tr><td>10DX145-34</td><td>Qz5 b</td><td>13.1 49.0 217 13.4</td><td>143</td><td>6.67</td><td>0.114</td><td>2.45</td><td>0.917</td><td>&lt;0.38</td><td>0.0402</td><td>1.85</td><td>0.410</td><td>0.335</td><td>0.078</td><td>0.257</td><td>0.042</td><td>0.62</td><td>350</td><td>0.1</td><td>0.5</td><td>316</td><td>323</td></tr></table>
<table><tr><td>10DX140-34</td><td>Qz5 b</td><td>26.1 131 608 86.7</td><td>v.d.</td><td>21.8</td><td>v.d.</td><td>v.d.</td><td>0.435</td><td>&lt;0.00</td><td>0.137</td><td>2.92</td><td>v.d.</td><td>v.d.</td><td>0.266</td><td>2.30</td><td>v.d.</td><td>0.56</td><td>1086</td><td>0.1</td><td>0.5</td><td>411</td><td>419</td></tr><tr><td>10DX140-37</td><td>Qz5 b</td><td>29.4 52.5 375 42.8</td><td>317</td><td>11.2</td><td>0.757</td><td>v.d.</td><td>0.830</td><td>&lt;0.95</td><td>0.202</td><td>2.94</td><td>1.64</td><td>1.56</td><td>&lt;0.06<br>3</td><td>1.97</td><td>0.589</td><td>0.56</td><td>670</td><td>0.1</td><td>0.5</td><td>372</td><td>380</td></tr><tr><td>10DX140-43</td><td>Qz5 b</td><td>30.6 29.5 v.d. v.d.</td><td>256</td><td>11.2</td><td>1.62</td><td>v.d.</td><td>0.720</td><td>&lt;0.53</td><td>0.0840</td><td>2.14</td><td>1.48</td><td>v.d.</td><td>0.369</td><td>1.18</td><td>1.22</td><td>0.56</td><td>v.d.</td><td>0.1</td><td>0.5</td><td>243</td><td>249</td></tr><tr><td>10DX140-44</td><td>Qz5 b</td><td>7.24 64.1 98.2 25.2</td><td>&lt;54.86</td><td>8.12</td><td>v.d.</td><td>v.d.</td><td>v.d.</td><td>3.10</td><td>&lt;0.013<br>1</td><td>2.31</td><td>1.28</td><td>0.62</td><td>0.154</td><td>0.761</td><td>0.995</td><td>0.56</td><td>175</td><td>0.1</td><td>0.5</td><td>264</td><td>270</td></tr><tr><td>10DX140-46</td><td>Qz5 b</td><td>46.8 73.5 410 29.7</td><td>v.d.</td><td>14.9</td><td>0.0480</td><td>v.d.</td><td>&lt;0.15<br>5</td><td>&lt;0.00</td><td>0.068</td><td>2.62</td><td>0.350</td><td>0.359</td><td>0.050<br>0</td><td>0.637</td><td>0.752</td><td>0.56</td><td>731</td><td>0.1</td><td>0.5</td><td>373</td><td>380</td></tr><tr><td>10DX140-47</td><td>Qz5 b</td><td>23.4 48.1 334 17.2</td><td>&lt;67.59</td><td>9.10</td><td>&lt;0.031</td><td>v.d.</td><td>0.343</td><td>1.14</td><td>0.254</td><td>6.24</td><td>2.17</td><td>v.d.</td><td>0.156</td><td>0.900</td><td>0.571</td><td>0.56</td><td>597</td><td>0.1</td><td>0.5</td><td>355</td><td>362</td></tr><tr><td>10DX140-48</td><td>Qz5 b</td><td>23.7 70.0 364 17.8</td><td>&lt;67.44</td><td>12.0</td><td>0.0510</td><td>5.10</td><td>&lt;0.14<br>6</td><td>&lt;0.55</td><td>&lt;0.00</td><td>3.46</td><td>3.34</td><td>1.75</td><td>0.165</td><td>0.950</td><td>0.865</td><td>0.56</td><td>651</td><td>0.1</td><td>0.5</td><td>389</td><td>396</td></tr><tr><td>10DX145-4</td><td>Qz5 b</td><td>40.3 99.4 119<br>0</td><td>31.2</td><td>220</td><td>3.21</td><td>0.0600</td><td>1.19</td><td>0.850</td><td>&lt;0.64</td><td>1.17</td><td>4.65</td><td>5.40</td><td>0.275</td><td>0.084</td><td>v.d.</td><td>0.139</td><td>0.62</td><td>1919</td><td>0.1</td><td>0.5</td><td>361</td><td>369</td></tr><tr><td>10DX145-5</td><td>Qz5 b</td><td>20.2 31.2 527 38.9</td><td>&lt;147.6<br>6</td><td>2.61</td><td>&lt;0.101</td><td>2.11</td><td>0.870</td><td>2.01</td><td>0.118</td><td>3.06</td><td>1.10</td><td>0.277</td><td>&lt;0.09<br>8</td><td>2.52</td><td>&lt;0.097</td><td>0.62</td><td>851</td><td>0.1</td><td>0.5</td><td>376</td><td>384</td></tr><tr><td>10DX145-12</td><td>Qz5 b</td><td>28.8 41.3 868 241</td><td>&lt;48.18</td><td>2.87</td><td>0.304</td><td>6.85</td><td>0.780</td><td>0.410</td><td>0.229</td><td>3.57</td><td>2.19</td><td>0.073</td><td>0.427</td><td>2.02</td><td>0.082</td><td>0.62</td><td>1399</td><td>0.1</td><td>0.5</td><td>310</td><td>316</td></tr><tr><td>10DX145-14</td><td>Qz5 b</td><td>36.3 93.2 v.d. v.d.</td><td>108</td><td>8.58</td><td>0.822</td><td>v.d.</td><td>1.75</td><td>1.04</td><td>0.159</td><td>4.01</td><td>2.40</td><td>0.431</td><td>0.176</td><td>2.00</td><td>&lt;0.055</td><td>0.62</td><td>v.d.</td><td>0.1</td><td>0.5</td><td>300</td><td>307</td></tr><tr><td>10DX145-15</td><td>Qz5 b</td><td>49.5 69.3 112<br>8</td><td>17.4</td><td>&lt;99.11</td><td>8.63</td><td>0.109</td><td>3.36</td><td>&lt;0.22</td><td>0.890</td><td>0.563</td><td>2.50</td><td>2.57</td><td>0.048<br>1</td><td>0.152</td><td>2.98</td><td>0.178</td><td>0.62</td><td>1819</td><td>0.1</td><td>0.5</td><td>305</td><td>311</td></tr><tr><td>10DX145-17</td><td>Qz5 b</td><td>45.6 95.4 937 22.0</td><td>&lt;64.58</td><td>5.99</td><td>1.86</td><td>7.14</td><td>0.880</td><td>&lt;0.44</td><td>0.214</td><td>4.44</td><td>4.9</td><td>0.195</td><td>0.077</td><td>2.39</td><td>0.071</td><td>0.62</td><td>1512</td><td>0.1</td><td>0.5</td><td>358</td><td>365</td></tr><tr><td>10DX145-22</td><td>Qz5 b</td><td>28.4 12.4 457 7.88</td><td>75.2</td><td>2.84</td><td>0.330</td><td>6.18</td><td>&lt;0.15</td><td>&lt;0.75</td><td>0.348</td><td>4.91</td><td>4.13</td><td>0.055</td><td>0.072</td><td>3.13</td><td>0.385</td><td>0.62</td><td>736</td><td>0.1</td><td>0.5</td><td>358</td><td>366</td></tr><tr><td>10DX145-26</td><td>Qz5 b</td><td>26.1 52.9 392 11.3</td><td>&lt;72.40</td><td>4.30</td><td>2.02</td><td>v.d.</td><td>1.33</td><td>&lt;0.50</td><td>0.374</td><td>4.27</td><td>2.33</td><td>0.832</td><td>&lt;0.04<br>7</td><td>2.56</td><td>0.336</td><td>0.62</td><td>632</td><td>0.1</td><td>0.5</td><td>340</td><td>347</td></tr><tr><td>10DX145-31</td><td>Qz5 b</td><td>30.2 &lt;3.7<br>7</td><td>634</td><td>&lt;6.78</td><td>&lt;123.3<br>0</td><td>3.68</td><td>&lt;0.091</td><td>1.42</td><td>&lt;0.30</td><td>&lt;0.75</td><td>0.407</td><td>2.52</td><td>2.53</td><td>&lt;0.03<br>4</td><td>0.175</td><td>0.731</td><td>0.076</td><td>0.62</td><td>1023</td><td>0.1</td><td>0.5</td><td>304</td><td>311</td></tr><tr><td>10DX145-32</td><td>Qz5 b</td><td>26.1 &lt;3.8<br>8</td><td>522</td><td>&lt;7.31</td><td>&lt;137.5<br>1</td><td>2.39</td><td>&lt;0.060</td><td>&lt;0.23</td><td>0.690</td><td>0.580</td><td>0.400</td><td>2.60</td><td>0.730</td><td>1.30</td><td>0.145</td><td>0.457</td><td>&lt;0.085</td><td>0.62</td><td>841</td><td>0.1</td><td>0.5</td><td>323</td><td>330</td></tr><tr><td>10DX145-34</td><td>Qz5 b</td><td>13.1 49.0 217 13.4</td><td>143</td><td>6.67</td><td>0.114</td><td>2.45</td><td>0.917</td><td>&lt;0.38</td><td>0.0402</td><td>1.85</td><td>0.410</td><td>0.335</td><td>0.078</td><td>0.257</td><td>0.042</td><td>0.62</td><td>350</td><td>0.1</td><td>0.5</td><td>316</td><td>323</td></tr></table>
<table><tr><td>10DX145-35</td><td>Qz5 b</td><td>28.7 9.82 691</td><td>140</td><td>&lt;89.15 2.75 0.209 7.74 0.230 &lt;0.68 0.144 3.17 1.93 0.161 0.747 1.31 0.098</td><td>0.62</td><td>1114</td><td>0.1</td><td>0.5</td><td>297</td><td>303</td></tr><tr><td>10DX145-36</td><td>Qz5 b</td><td>44.9 25.8 155 9</td><td>328</td><td>&lt;68.26 5.70 0.609 v.d. 0.470 &lt;0.00 0.491 v.d. v.d. v.d. 0.169 v.d. 0.237</td><td>0.62</td><td>2514</td><td>0.1</td><td>0.5</td><td>345</td><td>352</td></tr><tr><td>10DX145-37</td><td>Qz5 b</td><td>51.6 68.5 143 5</td><td>42.6</td><td>&lt;57.96 10.9 0.199 2.21 0.910 &lt;0.29 0.009 3.64 1.28 0.417 0.094 3.68 0.09</td><td>0.62</td><td>2314</td><td>0.1</td><td>0.5</td><td>303</td><td>309</td></tr><tr><td>10DX145-38</td><td>Qz5 b</td><td>29.6 11.1 600</td><td>12.0</td><td>&lt;80.65 3.70 &lt;0.047 0.705 &lt;0.17 1.35 0.0280 1.81 0.140 1.71 0.078 2.05 0.166</td><td>0.62</td><td>968</td><td>0.1</td><td>0.5</td><td>337</td><td>344</td></tr><tr><td>10DX145-39</td><td>Qz5 b</td><td>39.1 93.0 120 2</td><td>251</td><td>106 4.38 0.129 v.d. 0.520 &lt;0.85 0.726 3.31 0.190 v.d. 0.133 0.91 &lt;0.068</td><td>0.62</td><td>1939</td><td>0.1</td><td>0.5</td><td>371</td><td>378</td></tr><tr><td>10DX145-45</td><td>Qz5 b</td><td>8.17 v.d. 415</td><td>120</td><td>v.d. 7.27 1.702 v.d. 1.58 &lt;0.52 0.0520 2.87 1.09 v.d. 0.414 1.94 1.78</td><td>0.62</td><td>669</td><td>0.1</td><td>0.5</td><td>316</td><td>323</td></tr><tr><td>10DX158-5</td><td>Qz5 b</td><td>8.64 99.0 167</td><td>37.2</td><td>168 3.67 0.309 0.893 0.952 &lt;0.31 0.0920 2.82 4.07 0.859 0.086 3.71 0.176</td><td>0.52</td><td>321</td><td>0.1</td><td>0.5</td><td>324</td><td>331</td></tr><tr><td>10DX158-7</td><td>Qz5 b</td><td>0.93 102 47.2 13.8</td><td>&lt;60.44 3.15 0.120 0.368 0.599 &lt;0.38 0.0562 2.78 3.01 v.d. 0.056 2.87 0.048</td><td>0.52</td><td>90.7</td><td>0.1</td><td>0.5</td><td>350</td><td>357</td></tr><tr><td>10DX158-21</td><td>Qz5 b</td><td>5.21 76.1 123</td><td>36.9</td><td>68.2 5.69 v.d. v.d. v.d. &lt;0.39 1.10 3.37 5.51 v.d. 0.242 7.29 0.766</td><td>0.52</td><td>236</td><td>0.1</td><td>0.5</td><td>316</td><td>323</td></tr><tr><td>10DX158-22</td><td>Qz5 b</td><td>6.19 78.3 100</td><td>32.8</td><td>120 3.07 1.06 2.35 0.986 &lt;0.35 0.0182 3.03 2.11 1.35 &lt;0.04 2.83 0.12</td><td>0.52</td><td>192</td><td>0.1</td><td>0.5</td><td>309</td><td>316</td></tr><tr><td>10DX164-2</td><td>Qz5 b</td><td>v.d. 42.3 v.d. &lt;4.18 &lt;83.61 6.07 1.27 3.83 1.41 0.890 0.0200 2.50 1.02 0.338 &lt;0.07 1.02 0.116</td><td>0.66</td><td>v.d.</td><td>0.1</td><td>0.5</td><td>337</td><td>344</td></tr><tr><td>10DX164-4</td><td>Qz5 b</td><td>23.0 37.7 173</td><td>19.2</td><td>118 6.51 0.0870 1.88 0.207 &lt;0.38 0.118 2.50 1.55 0.377 0.084 2.02 0.112</td><td>0.66</td><td>263</td><td>0.1</td><td>0.5</td><td>308</td><td>314</td></tr><tr><td>10DX164-10</td><td>Qz5 b</td><td>17.5 11.5 101 v.d.</td><td>v.d.</td><td>14.3 0.2900 4.59 0.353 &lt;1.27 &lt;0.028 3.06 0.790 1.83 0.113 0.503 0.331</td><td>0.66</td><td>152</td><td>0.1</td><td>0.5</td><td>340</td><td>347</td></tr><tr><td>10DX164-11</td><td>Qz5 b</td><td>19.5 31.8 145 v.d.</td><td>v.d.</td><td>8.83 0.655 3.90 3.32 1.76 0.0490 2.51 1.38 2.41 0.182 0.323 0.346</td><td>0.66</td><td>219</td><td>0.1</td><td>0.5</td><td>344</td><td>351</td></tr><tr><td>10DX164-12</td><td>Qz5 b</td><td>29.0 v.d. 191 v.d.</td><td>107 13.7 1.41 4.32 1.29 &lt;0.28 0.0490 3.46 2.37 1.8 0.087 2.18 0.296</td><td>0.66</td><td>290</td><td>0.1</td><td>0.5</td><td>386</td><td>394</td></tr><tr><td>10DX164-14</td><td>Qz5 b</td><td>10.7 126 158 31.5 v.d.</td><td>8.15 1.11 v.d.</td><td>1.30 v.d. 0.0220 2.88 4.81 v.d. 0.190 4.73 1.52</td><td>0.66</td><td>239</td><td>0.1</td><td>0.5</td><td>360</td><td>367</td></tr><tr><td>10DX164-15</td><td>Qz5 b</td><td>27.8 78.7 211</td><td>6.48 &lt;85.47 7.51 &lt;0.059 1.56 0.424 0.850 0.0730 4.37 3.07 v.d. 0.112 3.41 &lt;0.056</td><td>0.66</td><td>319</td><td>0.1</td><td>0.5</td><td>384</td><td>391</td></tr><tr><td>10DX164-17</td><td>Qz5 b</td><td>12.4 62.6 115 29.8 v.d.</td><td>7.27 0.902 4.09 0.62 1.25 0.0200 1.90 &lt;0.23 v.d. &lt;0.06 0.475 0.117</td><td>0.66</td><td>175</td><td>0.1</td><td>0.5</td><td>355</td><td>363</td></tr></table>
<table><tr><td>10DX145-35</td><td>Qz5 b</td><td>28.7 9.82 691</td><td>140</td><td>&lt;89.15 2.75 0.209 7.74 0.230 &lt;0.68 0.144 3.17 1.93 0.161 0.747 1.31 0.098</td><td>0.62</td><td>1114</td><td>0.1</td><td>0.5</td><td>297</td><td>303</td></tr><tr><td>10DX145-36</td><td>Qz5 b</td><td>44.9 25.8 155 9</td><td>328</td><td>&lt;68.26 5.70 0.609 v.d. 0.470 &lt;0.00 0.491 v.d. v.d. v.d. 0.169 v.d. 0.237</td><td>0.62</td><td>2514</td><td>0.1</td><td>0.5</td><td>345</td><td>352</td></tr><tr><td>10DX145-37</td><td>Qz5 b</td><td>51.6 68.5 143 5</td><td>42.6</td><td>&lt;57.96 10.9 0.199 2.21 0.910 &lt;0.29 0.009 3.64 1.28 0.417 0.094 0.368 0.09</td><td>0.62</td><td>2314</td><td>0.1</td><td>0.5</td><td>303</td><td>309</td></tr><tr><td>10DX145-38</td><td>Qz5 b</td><td>29.6 11.1 600</td><td>12.0</td><td>&lt;80.65 3.70 &lt;0.047 0.705 &lt;0.17 1.35 0.0280 1.81 0.140 1.71 0.078 0.205 0.166</td><td>0.62</td><td>968</td><td>0.1</td><td>0.5</td><td>337</td><td>344</td></tr><tr><td>10DX145-39</td><td>Qz5 b</td><td>39.1 93.0 120 2</td><td>251</td><td>106 4.38 0.129 v.d. 0.520 &lt;0.85 0.726 3.31 0.190 v.d. 0.133 0.91 &lt;0.068</td><td>0.62</td><td>1939</td><td>0.1</td><td>0.5</td><td>371</td><td>378</td></tr><tr><td>10DX145-45</td><td>Qz5 b</td><td>8.17 v.d. 415</td><td>120</td><td>v.d. 7.27 1.702 v.d. 1.58 &lt;0.52 0.0520 2.87 1.09 v.d. 0.414 1.94 1.78</td><td>0.62</td><td>669</td><td>0.1</td><td>0.5</td><td>316</td><td>323</td></tr><tr><td>10DX158-5</td><td>Qz5 b</td><td>8.64 99.0 167</td><td>37.2</td><td>168 3.67 0.309 0.893 0.952 &lt;0.31 0.0920 2.82 4.07 0.859 0.086 3.71 0.176</td><td>0.52</td><td>321</td><td>0.1</td><td>0.5</td><td>324</td><td>331</td></tr><tr><td>10DX158-7</td><td>Qz5 b</td><td>0.93 102 47.2 13.8</td><td>&lt;60.44 3.15 0.120 0.368 0.599 &lt;0.38 0.0562 2.78 3.01 v.d. 0.056 2.87 0.048</td><td>0.52</td><td>90.7</td><td>0.1</td><td>0.5</td><td>350</td><td>357</td></tr><tr><td>10DX158-21</td><td>Qz5 b</td><td>5.21 76.1 123</td><td>36.9</td><td>68.2 5.69 v.d. v.d. v.d. &lt;0.39 1.10 3.37 5.51 v.d. 0.242 7.29 0.766</td><td>0.52</td><td>236</td><td>0.1</td><td>0.5</td><td>316</td><td>323</td></tr><tr><td>10DX158-22</td><td>Qz5 b</td><td>6.19 78.3 100</td><td>32.8</td><td>120 3.07 1.06 2.35 0.986 &lt;0.35 0.0182 3.03 2.11 1.35 &lt;0.04 0.283 0.12</td><td>0.52</td><td>192</td><td>0.1</td><td>0.5</td><td>309</td><td>316</td></tr><tr><td>10DX164-2</td><td>Qz5 b</td><td>v.d. 42.3 v.d. &lt;4.18 &lt;83.61 6.07 1.27 3.83 1.41 0.890 0.0200 2.50 1.02 0.338 &lt;0.07 0.102 0.116</td><td>0.66</td><td>v.d.</td><td>0.1</td><td>0.5</td><td>337</td><td>344</td></tr><tr><td>10DX164-4</td><td>Qz5 b</td><td>23.0 37.7 173</td><td>19.2</td><td>118 6.51 0.0870 1.88 0.207 &lt;0.38 0.118 2.50 1.55 0.377 0.084 2.02 0.112</td><td>0.66</td><td>263</td><td>0.1</td><td>0.5</td><td>308</td><td>314</td></tr><tr><td>10DX164-10</td><td>Qz5 b</td><td>17.5 11.5 101 v.d.</td><td>v.d.</td><td>14.3 0.2900 4.59 0.353 &lt;1.27 &lt;0.028 3.06 0.790 1.83 0.113 0.503 0.331</td><td>0.66</td><td>152</td><td>0.1</td><td>0.5</td><td>340</td><td>347</td></tr><tr><td>10DX164-11</td><td>Qz5 b</td><td>19.5 31.8 145 v.d.</td><td>v.d.</td><td>8.83 0.655 3.90 3.32 1.76 0.0490 2.51 1.38 2.41 0.182 0.323 0.346</td><td>0.66</td><td>219</td><td>0.1</td><td>0.5</td><td>344</td><td>351</td></tr><tr><td>10DX164-12</td><td>Qz5 b</td><td>29.0 v.d. 191 v.d.</td><td>107 13.7 1.41 4.32 1.29 &lt;0.28 0.0490 3.46 2.37 1.8 0.087 0.218 0.296</td><td>0.66</td><td>290</td><td>0.1</td><td>0.5</td><td>386</td><td>394</td></tr><tr><td>10DX164-14</td><td>Qz5 b</td><td>10.7 126 158 31.5</td><td>v.d.</td><td>8.15 1.11 v.d. 1.30 v.d. 0.0220 2.88 4.81 v.d. 0.190 4.73 1.52</td><td>0.66</td><td>239</td><td>0.1</td><td>0.5</td><td>360</td><td>367</td></tr><tr><td>10DX164-15</td><td>Qz5 b</td><td>27.8 78.7 211</td><td>6.48 &lt;85.47 7.51 &lt;0.059 1.56 0.424 0.850 0.0730 4.37 3.07 v.d. 0.112 3.41 &lt;0.056</td><td>0.66</td><td>319</td><td>0.1</td><td>0.5</td><td>384</td><td>391</td></tr><tr><td>10DX164-17</td><td>Qz5 b</td><td>12.4 62.6 115 29.8</td><td>v.d.</td><td>7.27 0.902 4.09 0.62 1.25 0.0200 1.90 &lt;0.23 v.d. &lt;0.06 0.475 0.117</td><td>0.66</td><td>175</td><td>0.1</td><td>0.5</td><td>355</td><td>363</td></tr></table>
<table><tr><td>10DX164-21</td><td>Qz5 b</td><td>11.3 18.4 108 11.5</td><td>101</td><td>5.42</td><td>&lt;0.048</td><td>0.268</td><td>0.249</td><td>0.540</td><td>0.0084</td><td>1.47</td><td>0.57</td><td>v.d.</td><td>0.080 0.259 0.089</td><td>0.66</td><td>163</td><td>0.1</td><td>0.5</td><td>351</td><td>358</td></tr><tr><td>10DX164-24</td><td>Qz5 b</td><td>14.1 27.1 126 26.9</td><td>&lt;86.99</td><td>10.7</td><td>0.577</td><td>4.09</td><td>2.73</td><td>&lt;1.01</td><td>0.183</td><td>2.02</td><td>&lt;0.24 0.055</td><td>&lt;0.07 0.272</td><td>0.160</td><td>0.66</td><td>190</td><td>0.1</td><td>0.5</td><td>350</td><td>357</td></tr><tr><td>10DX164-25</td><td>Qz5 b</td><td>14.1 52.8 397 136</td><td>220</td><td>11.4</td><td>0.299</td><td>6.99</td><td>1.87</td><td>&lt;1.31</td><td>0.260</td><td>3.13</td><td>3.49</td><td>1.25</td><td>&lt;0.08 16.3</td><td>&lt;0.077</td><td>0.66</td><td>601</td><td>0.1</td><td>0.5</td><td>335</td><td>342</td></tr><tr><td>10DX164-42</td><td>Qz5 b</td><td>10.0 44.4 181 33.4</td><td>&lt;145.6 6.95</td><td>0.221</td><td>6.91</td><td>1.36</td><td>0.550</td><td>0.0860</td><td>2.99</td><td>0.720</td><td>0.597</td><td>0.110</td><td>1.75</td><td>0.210</td><td>0.66</td><td>275</td><td>0.1</td><td>0.5</td><td>370</td><td>377</td></tr><tr><td>10DX164-43</td><td>Qz5 b</td><td>24.5 145 v.d. v.d.</td><td>v.d.</td><td>9.55</td><td>0.402</td><td>v.d.</td><td>v.d.</td><td>&lt;0.00</td><td>1.43</td><td>3.91</td><td>3.91</td><td>v.d.</td><td>0.739</td><td>5.04</td><td>0.784</td><td>0.66</td><td>v.d.</td><td>0.1</td><td>0.5</td><td>373</td><td>381</td></tr><tr><td>10DX164-44</td><td>Qz5 b</td><td>18.5 77.9 254 94.2</td><td>&lt;113.2 6.42</td><td>0.972</td><td>v.d.</td><td>1.50</td><td>&lt;1.15</td><td>0.194</td><td>2.52</td><td>1.49</td><td>0.284</td><td>0.095</td><td>1.20</td><td>0.379</td><td>0.66</td><td>385</td><td>0.1</td><td>0.5</td><td>347</td><td>354</td></tr><tr><td>10DX164-45</td><td>Qz5 b</td><td>11.8 99.5 187 49.8</td><td>295</td><td>5.17</td><td>0.480</td><td>3.45</td><td>2.73</td><td>&lt;0.00</td><td>0.106</td><td>3.07</td><td>0.350</td><td>0.512</td><td>&lt;0.09 0.659</td><td>0.141</td><td>0.66</td><td>283</td><td>0.1</td><td>0.5</td><td>364</td><td>371</td></tr><tr><td>10DX164-46</td><td>Qz5 b</td><td>13.8 141 166 68.7</td><td>v.d.</td><td>9.84</td><td>0.372</td><td>v.d.</td><td>v.d.</td><td>&lt;0.37</td><td>0.500</td><td>3.39</td><td>2.96</td><td>v.d.</td><td>0.662</td><td>2.48</td><td>v.d.</td><td>0.66</td><td>251</td><td>0.1</td><td>0.5</td><td>343</td><td>350</td></tr><tr><td>10DX164-48</td><td>Qz5 b</td><td>11.0 53.3 108 28.7</td><td>v.d.</td><td>4.75</td><td>0.157</td><td>4.26</td><td>0.436</td><td>&lt;0.61</td><td>0.109</td><td>2.57</td><td>1.47</td><td>v.d.</td><td>0.109</td><td>1.70</td><td>1.90</td><td>0.66</td><td>163</td><td>0.1</td><td>0.5</td><td>332</td><td>339</td></tr><tr><td>10DX164-48A</td><td>Qz5 b</td><td>13.9 32.6 151 53.5</td><td>&lt;259.2 9.14</td><td>&lt;0.173</td><td>0.790</td><td>0.700</td><td>1.66</td><td>&lt;0.00</td><td>2.01</td><td>&lt;0.79</td><td>0.097</td><td>&lt;0.20</td><td>0.940</td><td>0.200</td><td>0.66</td><td>228</td><td>0.1</td><td>0.5</td><td>366</td><td>373</td></tr><tr><td>10DX164-49</td><td>Qz5 b</td><td>14.0 85.9 91.9 6.96</td><td>&lt;67.44</td><td>11.6</td><td>0.352</td><td>5.76</td><td>0.75</td><td>0.840</td><td>0.0970</td><td>3.85</td><td>1.92</td><td>0.755</td><td>0.226</td><td>1.11</td><td>0.115</td><td>0.66</td><td>139</td><td>0.1</td><td>0.5</td><td>328</td><td>335</td></tr><tr><td>10DX164-55</td><td>Qz5 b</td><td>8.13 165 41.6 12.2</td><td>v.d.</td><td>3.60</td><td>0.575</td><td>v.d.</td><td>4.40</td><td>0.970</td><td>0.0500</td><td>2.05</td><td>1.58</td><td>v.d.</td><td>0.067 0.401</td><td>0.190</td><td>0.66</td><td>63.0</td><td>0.1</td><td>0.5</td><td>362</td><td>369</td></tr><tr><td>10DX164-56</td><td>Qz5 b</td><td>16.0 76.6 97.2 23.4</td><td>&lt;50.69</td><td>9.74</td><td>1.19</td><td>v.d.</td><td>5.76</td><td>&lt;0.48</td><td>0.0490</td><td>2.96</td><td>2.09</td><td>0.234</td><td>0.099 3.56</td><td>0.411</td><td>0.66</td><td>147</td><td>0.1</td><td>0.5</td><td>375</td><td>382</td></tr><tr><td>10DX164-57</td><td>Qz5 b</td><td>29.5 19.8 173 10.0</td><td>&lt;58.72</td><td>13.8</td><td>0.237</td><td>1.52</td><td>&lt;0.11 0.51</td><td>0.0530</td><td>2.7</td><td>2.16</td><td>0.041 0.134</td><td>2.25</td><td>0.074</td><td>0.66</td><td>263</td><td>0.1</td><td>0.5</td><td>315</td><td>322</td></tr><tr><td>10DX220-29</td><td>Qz5 b</td><td>21.9 33.2 139 9.55</td><td>v.d.</td><td>4.77</td><td>0.255</td><td>7.67</td><td>&lt;0.27</td><td>&lt;1.46</td><td>1.14</td><td>2.59</td><td>2.08</td><td>v.d.</td><td>1.57</td><td>1.03</td><td>v.d.</td><td>0.66</td><td>211</td><td>0.1</td><td>0.5</td><td>365</td><td>372</td></tr><tr><td>10DX220-30</td><td>Qz5 b</td><td>30.1 40.9 421 14.1 9</td><td>254</td><td>10.9</td><td>&lt;0.172</td><td>2.69</td><td>0.980</td><td>2.66</td><td>1.00</td><td>3.41</td><td>2.39</td><td>1.64</td><td>0.450</td><td>0.590</td><td>v.d.</td><td>0.66</td><td>638</td><td>0.1</td><td>0.5</td><td>384</td><td>392</td></tr><tr><td>10DX201-12</td><td>Qz5 b</td><td>54.4 160 112 581</td><td>&lt;33.50</td><td>6.91</td><td>0.661</td><td>7.70</td><td>1.93</td><td>&lt;0.30 0.9</td><td>2.34</td><td>9.99</td><td>45.6</td><td>0.691</td><td>0.152</td><td>64.0</td><td>0.168</td><td>0.61</td><td>1849</td><td>0.1</td><td>0.5</td><td>328</td><td>335</td></tr><tr><td>10DX201-13</td><td>Qz5 b</td><td>29.5 106 255 57.2</td><td>78</td><td>5.42</td><td>0.159</td><td>2.17</td><td>1.27</td><td>0.91</td><td>0.153</td><td>4.71</td><td>4.45</td><td>1.15</td><td>0.130</td><td>5.72</td><td>0.294</td><td>0.61</td><td>418</td><td>0.1</td><td>0.5</td><td>371</td><td>378</td></tr></table>
<table><tr><td>10DX164-21</td><td>Qz5<br>b</td><td>11.3</td><td>18.4</td><td>108</td><td>11.5</td><td>101</td><td>5.42</td><td>&lt;0.048</td><td>0.268</td><td>0.249</td><td>0.540</td><td>0.0084</td><td>1.47</td><td>0.57</td><td>v.d.</td><td>0.080<br>0</td><td>0.259</td><td>0.089</td><td>0.66</td><td>163</td><td>0.1</td><td>0.5</td><td>351</td><td>358</td></tr><tr><td>10DX164-24</td><td>Qz5<br>b</td><td>14.1</td><td>27.1</td><td>126</td><td>26.9</td><td>&lt;86.99</td><td>10.7</td><td>0.577</td><td>4.09</td><td>2.73</td><td>&lt;1.01</td><td>0.183</td><td>2.02</td><td>&lt;0.24<br>9</td><td>0.055</td><td>&lt;0.07<br>4</td><td>0.272</td><td>0.160</td><td>0.66</td><td>190</td><td>0.1</td><td>0.5</td><td>350</td><td>357</td></tr><tr><td>10DX164-25</td><td>Qz5<br>b</td><td>14.1</td><td>52.8</td><td>397</td><td>136</td><td>220</td><td>11.4</td><td>0.299</td><td>6.99</td><td>1.87</td><td>&lt;1.31</td><td>0.260</td><td>3.13</td><td>3.49</td><td>1.25</td><td>&lt;0.08<br>5</td><td>16.3</td><td>&lt;0.077</td><td>0.66</td><td>601</td><td>0.1</td><td>0.5</td><td>335</td><td>342</td></tr><tr><td>10DX164-42</td><td>Qz5<br>b</td><td>10.0</td><td>44.4</td><td>181</td><td>33.4</td><td>&lt;145.6<br>9</td><td>6.95</td><td>0.221</td><td>6.91</td><td>1.36</td><td>0.550</td><td>0.0860</td><td>2.99</td><td>0.720</td><td>0.597</td><td>0.110</td><td>1.75</td><td>0.210</td><td>0.66</td><td>275</td><td>0.1</td><td>0.5</td><td>370</td><td>377</td></tr><tr><td>10DX164-43</td><td>Qz5<br>b</td><td>24.5</td><td>145</td><td>v.d.</td><td>v.d.</td><td>v.d.</td><td>9.55</td><td>0.402</td><td>v.d.</td><td>v.d.</td>< &lt;0.00</td><td>1.43</td><td>3.91</td><td>3.91</td><td>v.d.</td><td>0.739</td><td>5.04</td><td>0.784</td><td>0.66</td><td>v.d.</td><td>0.1</td><td>0.5</td><td>373</td><td>381</td></tr><tr><td>10DX164-44</td><td>Qz5<br>b</td><td>18.5</td><td>77.9</td><td>254</td><td>94.2</td><td>&lt;113.2<br>2</td><td>6.42</td><td>0.972</td><td>v.d.</td><td>1.50</td>< &lt;1.15</td><td>0.194</td><td>2.52</td><td>1.49</td><td>0.284</td><td>0.095</td><td>1.20</td><td>0.379</td><td>0.66</td><td>385</td><td>0.1</td><td>0.5</td><td>347</td><td>354</td></tr><tr><td>10DX164-45</td><td>Qz5<br>b</td><td>11.8</td><td>99.5</td><td>187</td><td>49.8</td><td>295</td><td>5.17</td><td>0.480</td><td>3.45</td><td>2.73</td>< &lt;0.00</td><td>0.106</td><td>3.07</td><td>0.350</td><td>0.512</td><td>&lt;0.09<br>1</td><td>0.659</td><td>0.141</td><td>0.66</td><td>283</td><td>0.1</td><td>0.5</td><td>364</td><td>371</td></tr><tr><td>10DX164-46</td><td>Qz5<br>b</td><td>13.8</td><td>141</td><td>166</td><td>68.7</td><td>v.d.</td><td>9.84</td><td>0.372</td><td>v.d.</td><td>v.d.</td>< &lt;0.37</td><td>0.500</td><td>3.39</td><td>2.96</td><td>v.d.</td><td>0.662</td><td>2.48</td><td>v.d.</td><td>0.66</td><td>251</td><td>0.1</td><td>0.5</td><td>343</td><td>350</td></tr><tr><td>10DX164-48</td><td>Qz5<br>b</td><td>11.0</td><td>53.3</td><td>108</td><td>28.7</td><td>v.d.</td><td>4.75</td><td>0.157</td><td>4.26</td><td>0.436</td>< &lt;0.61</td><td>0.109</td><td>2.57</td><td>1.47</td><td>v.d.</td><td>0.109</td><td>1.70</td><td>1.90</td><td>0.66</td><td>163</td><td>0.1</td><td>0.5</td><td>332</td><td>339</td></tr><tr><td>10DX164-48A</td><td>Qz5<br>b</td><td>13.9</td><td>32.6</td><td>151</td><td>53.5</td><td>&lt;259.2<br>9</td><td>9.14</td><td>&lt;0.173</td><td>0.790</td><td>0.700</td>< 1.66</td>< &lt;0.00</td><td>2.01</td><td>&lt;0.79</td><td>0.097</td><td>&lt;0.20</td><td>0.940</td><td>0.200</td><td>0.66</td><td>228</td><td>0.1</td><td>0.5</td><td>366</td><td>373</td></tr><tr><td>10DX164-49</td><td>Qz5<br>b</td><td>14.0</td><td>85.9</td><td>91.9</td><td>6.96</td><td>&lt;67.44</td><td>11.6</td><td>0.352</td><td>5.76</td><td>0.75</td>< 0.840</td>< 0.0970</td><td>3.85</td><td>1.92</td><td>0.755</td><td>0.226</td><td>1.11</td><td>0.115</td><td>0.66</td><td>139</td><td>0.1</td><td>0.5</td><td>328</td><td>335</td></tr><tr><td>10DX164-55</td><td>Qz5<br>b</td><td>8.13</td><td>165</td><td>41.6</td><td>12.2</td><td>v.d.</td><td>3.60</td><td>0.575</td><td>v.d.</td><td>4.40</td>< 0.970</td>< 0.0500</td><td>2.05</td><td>1.58</td><td>v.d.</td><td>0.067<br>0</td><td>0.401</td><td>0.190</td><td>0.66</td><td>63.0</td><td>0.1</td><td>0.5</td><td>362</td><td>369</td></tr><tr><td>10DX164-56</td><td>Qz5<br>b</td><td>16.0</td><td>76.6</td><td>97.2</td><td>23.4</td><td>&lt;50.69</td><td>9.74</td><td>1.19</td><td>v.d.</td><td>5.76</td>< &lt;0.48</td>< 0.0490</td><td>2.96</td><td>2.09</td><td>0.234</td><td>0.099<br>0</td><td>3.56</td><td>0.411</td><td>0.66</td><td>147</td><td>0.1</td><td>0.5</td><td>375</td><td>382</td></tr><tr><td>10DX164-57</td><td>Qz5<br>b</td><td>29.5</td><td>19.8</td><td>173</td><td>10.0</td><td>&lt;58.72</td><td>13.8</td><td>0.237</td><td>1.52</td>< &lt;0.11<br>9</td>< &lt;0.51</td>< 0.0530</td><td>2.7</td><td>2.16</td><td>0.041<br>5</td><td>0.134</td><td>2.25</td><td>0.074</td><td>0.66</td><td>263</td><td>0.1</td><td>0.5</td><td>315</td><td>322</td></tr><tr><td>10DX220-29</td><td>Qz5<br>b</td><td>21.9</td><td>33.2</td><td>139</td><td>9.55</td><td>v.d.</td><td>4.77</td><td>0.255</td><td>7.67</td>< &lt;0.27</td>< &lt;1.46</td>< 1.14</td><td>2.59</td><td>2.08</td><td>v.d.</td><td>1.57</td><td>1.03</td><td>v.d.</td><td>0.66</td><td>211</td><td>0.1</td><td>0.5</td><td>365</td><td>372</td></tr><tr><td>10DX220-30</td><td>Qz5<br>b</td><td>30.1</td><td>40.9</td><td>421</td><td>&lt;14.1<br>9</td><td>254</td><td>10.9</td><td>&lt;0.172</td><td>2.69</td>< 0.980</td>< 2.66</td>< 1.00</td><td>3.41</td><td>2.39</td><td>1.64</td><td>0.450</td><td>0.590</td><td>v.d.</td><td>0.66</td><td>638</td><td>0.1</td><td>0.5</td><td>384</td><td>392</td></tr><tr><td>10DX201-12</td><td>Qz5<br>b</td><td>54.4</td><td>160</td><td>112<br>8</td><td>581</td><td>&lt;33.50</td><td>6.91</td><td>0.661</td><td>7.70</td>< 1.93</td>< &lt;0.30<br>9</td>< 2.34</td><td>9.99</td><td>45.6</td><td>0.691</td><td>0.152</td><td>64.0</td><td>0.168</td><td>0.61</td><td>1849</td><td>0.1</td><td>0.5</td><td>328</td><td>335</td></tr><tr><td>10DX201-13</td><td>Qz5<br>b</td><td>29.5</td><td>106</td><td>255</td><td>57.2</td><td>78</td><td>5.42</td><td>0.159</td><td>2.17</td>< 1.27</td>< 0.91</td>< 0.153</td><td>4.71</td><td>4.45</td><td>1.15</td><td>0.130</td><td>5.72</td><td>0.294</td><td>0.61</td><td>418</td><td>0.1</td><td>0.5</td><td>371</td><td>378</td></tr></table>
<table><tr><td>10DX201-14</td><td>Qz5<br>b</td><td>28.5 75.5 251 30.2</td><td>&lt;73.36 5.61 0.0580 0.585 0.391 0.35 0.211 3.72 2.97</td><td>1.12 0.054<br>0 7.42 0.074</td><td>0.61</td><td>412</td><td>0.1</td><td>0.5</td><td>347</td><td>354</td></tr><tr><td>10DX140-39</td><td>Qz6<br>a</td><td>26.6 164 943 206</td><td>151 0.63<br>0 0.964 v.d. 0.770 &lt;0.55 0.262 17.8 83.3</td><td>v.d. &lt;0.04<br>3 106 0.46</td><td>0.56</td><td>1684</td><td>0.1</td><td>0.5</td><td>335</td><td>342</td></tr><tr><td>10DX140-40</td><td>Qz6<br>a</td><td>56.4 276 152<br>3 375</td><td>158 1.09 0.404 5.17</td><td>v.d. &lt;0.46 0.0580 24.6 84.9</td><td>v.d. 0.130 109 0.913</td><td>0.56</td><td>2721</td><td>0.1</td><td>0.5</td><td>336</td><td>343</td></tr><tr><td>10DX140-71</td><td>Qz6<br>a</td><td>0.38<br>2 16.8 81.2 33.9</td><td>&lt;45.85 0.65<br>0 0.0400 0.903</td><td>&lt;0.09<br>0 &lt;0.40 1.167 12.3 98.0</td><td>0.057<br>5 0.139 107 0.046</td><td>0.56</td><td>145</td><td>0.01</td><td>0.5</td><td>209</td><td>239</td></tr><tr><td>10DX164-22</td><td>Qz6<br>a</td><td>3.94 73.8 112 23.4</td><td>&lt;95.32 3.50 v.d. v.d. v.d. 1.04 &lt;0.00 1.77 1.48</td><td>v.d. 0.267 0.419 0.467</td><td>0.66</td><td>169</td><td>0.01</td><td>0.5</td><td>243</td><td>277</td></tr><tr><td>10DX164-1</td><td>Qz6<br>a</td><td>4.11 41.7 68.9 16.8</td><td>528.3 3.64 &lt;0.045 0.747 1.21 &lt;0.59 0.112 2.48 0.290</td><td>0.381 0.144 0.749 0.111</td><td>0.66</td><td>104</td><td>0.01</td><td>0.5</td><td>312</td><td>355</td></tr><tr><td>10DX164-61</td><td>Qz6<br>a</td><td>1.54 62.9 28.8 17.19</td><td>&lt;163.7<br>8 5.75 0.712 4.75 3.68 &lt;1.27 &lt;0.040 1.73 &lt;0.46 0.125</td><td>&lt;0.12<br>0 0.590 &lt;0.106</td><td>0.66</td><td>43.6</td><td>0.01</td><td>0.5</td><td>314</td><td>357</td></tr><tr><td>10DX164-62</td><td>Qz6<br>a</td><td>1.40 104.<br>4 40.5 22.9<br>9 4.82 1.70</td><td>&lt;428.2<br>5</td><td>v.d. v.d. 2.63 &lt;0.106 1.81 1.12 0.092 &lt;0.29 &lt;0.26 &lt;0.24</td><td>0.66</td><td>61.3</td><td>0.01</td><td>0.5</td><td>336</td><td>382</td></tr><tr><td>10DX201-1</td><td>Qz6<br>a</td><td>124 156. 131<br>5 9 309</td><td>60.5 0.84<br>0 0.887 v.d. v.d. &lt;0.00 0.0350 18.0 17.88</td><td>v.d. 0.067<br>0 27.8 0.202</td><td>0.61</td><td>2163</td><td>0.01</td><td>0.5</td><td>327</td><td>372</td></tr><tr><td>10DX201-4</td><td>Qz6<br>a</td><td>184 147. 115<br>7 3 155</td><td>&lt;60.33 1.07 0.180 0.952 0.225 &lt;0.33 0.0460 32.5 9.36</td><td>1.61 0.063<br>0 13.6 0.083</td><td>0.61</td><td>1890</td><td>0.01</td><td>0.5</td><td>253</td><td>288</td></tr><tr><td>10DX201-5</td><td>Qz6<br>a</td><td>201 132. 166<br>6 0 147</td><td>&lt;105.5<br>8 1.15 0.424 1.89 0.390 0.89 &lt;0.022 17.3 4.13</td><td>1.17 0.208 3.43 &lt;0.038</td><td>0.61</td><td>2721</td><td>0.01</td><td>0.5</td><td>262</td><td>298</td></tr><tr><td>10DX201-6</td><td>Qz6<br>a</td><td>245 121. 133<br>7 6 106</td><td>172 0.65<br>0 0.386 v.d. 0.516 &lt;0.49 1.249 14.5 2.61</td><td>v.d. 0.069 2.03 0.331</td><td>0.61</td><td>2191</td><td>0.01</td><td>0.5</td><td>265</td><td>301</td></tr><tr><td>10DX201-9</td><td>Qz6<br>a</td><td>102 77.6 709 44.3</td><td>&lt;91.39 2.42 0.0700 0.456 3.15 0.48 0.0460 13.3 7.15</td><td>0.557 0.125 18.1 0.117</td><td>0.61</td><td>1162</td><td>0.01</td><td>0.5</td><td>243</td><td>277</td></tr><tr><td>10DX201-10</td><td>Qz6<br>a</td><td>46.9 78.4 287 87.3</td><td>v.d. 1.20 0.424 v.d. 2.51 &lt;0.27 0.484 5.65 11.6 6.32</td><td>0.146 11.4 0.878</td><td>0.61</td><td>470</td><td>0.01</td><td>0.5</td><td>296</td><td>336</td></tr><tr><td>10DX201-11</td><td>Qz6<br>a</td><td>15.0 54.2 155 27.6</td><td>&lt;82.02 0.89<br>0 0.0860 0.371 0.710 &lt;0.67 0.257 3.39 5.61</td><td>0.627 &lt;0.06<br>4 7.95 0.17</td><td>0.61</td><td>254</td><td>0.01</td><td>0.5</td><td>266</td><td>303</td></tr><tr><td>10DX201-23</td><td>Qz6<br>a</td><td>149 82.6 908 39.9</td><td>&lt;74.56 2.05 &lt;0.042 1.07 0.183 &lt;0.43 0.0650 11.5 8.23</td><td>0.445 &lt;0.05<br>7 28.6 0.072</td><td>0.61</td><td>1489</td><td>0.01</td><td>0.5</td><td>255</td><td>290</td></tr><tr><td>10DX201-24</td><td>Qz6<br>a</td><td>108 114 957 165</td><td>&lt;66.57 2.61 0.929 v.d. 0.663 &lt;0.70 0.0760 12.6 10.6 1.63</td><td>&lt;0.04<br>7 20.3 0.122 2.39</td><td>0.61</td><td>1568</td><td>0.01</td><td>0.5</td><td>288</td><td>328</td></tr><tr><td>10DX201-26</td><td>Qz6<br>a</td><td>17.5 41.7 125 &lt;4.40 123</td><td>7.17 0.0860 1.35 3.59 &lt;0.40 0.0700 2.34 1.53 0.537</td><td>0.122 2.39 0.172</td><td>0.61</td><td>204</td><td>0.01</td><td>0.5</td><td>299</td><td>340</td></tr></table>
<table><tr><td>10DX201-14</td><td>Qz5<br>b</td><td>28.5 75.5 251 30.2</td><td>&lt;73.36 5.61 0.0580 0.585 0.391 0.35 0.211 3.72 2.97</td><td>1.12 0.054<br>0 7.42 0.074</td><td>0.61</td><td>412</td><td>0.1</td><td>0.5</td><td>347</td><td>354</td></tr><tr><td>10DX140-39</td><td>Qz6<br>a</td><td>26.6 164 943 206</td><td>151 0.63<br>0 0.964 v.d. 0.770 &lt;0.55 0.262 17.8 83.3</td><td>v.d. &lt;0.04<br>3 106 0.46</td><td>0.56</td><td>1684</td><td>0.1</td><td>0.5</td><td>335</td><td>342</td></tr><tr><td>10DX140-40</td><td>Qz6<br>a</td><td>56.4 276 152<br>3 375</td><td>158 1.09 0.404 5.17</td><td>v.d. &lt;0.46 0.0580 24.6 84.9</td><td>v.d. 0.130 109 0.913</td><td>0.56</td><td>2721</td><td>0.1</td><td>0.5</td><td>336</td><td>343</td></tr><tr><td>10DX140-71</td><td>Qz6<br>a</td><td>0.38<br>2 16.8 81.2 33.9</td><td>&lt;45.85 0.65<br>0 0.0400 0.903</td><td>&lt;0.09<br>0 &lt;0.40 1.167 12.3 98.0</td><td>0.057<br>5 0.139 107 0.046</td><td>0.56</td><td>145</td><td>0.01</td><td>0.5</td><td>209</td><td>239</td></tr><tr><td>10DX164-22</td><td>Qz6<br>a</td><td>3.94 73.8 112 23.4</td><td>&lt;95.32 3.50 v.d.</td><td>v.d. v.d. 1.04 &lt;0.00 1.77 1.48</td><td>v.d. 0.267 0.419 0.467</td><td>0.66</td><td>169</td><td>0.01</td><td>0.5</td><td>243</td><td>277</td></tr><tr><td>10DX164-1</td><td>Qz6<br>a</td><td>4.11 41.7 68.9 16.8</td><td>528.3 3.64 &lt;0.045 0.747 1.21</td><td>&lt;0.59 0.112 2.48 0.290 0.381 0.144 0.749 0.111</td><td>0.66</td><td>104</td><td>0.01</td><td>0.5</td><td>312</td><td>355</td></tr><tr><td>10DX164-61</td><td>Qz6<br>a</td><td>1.54 62.9 28.8 17.19</td><td>&lt;163.7<br>8 5.75 0.712 4.75</td><td>3.68 &lt;1.27 &lt;0.040 1.73 &lt;0.46 0.125</td><td>&lt;0.12<br>0 0.590 &lt;0.106</td><td>0.66</td><td>43.6</td><td>0.01</td><td>0.5</td><td>314</td><td>357</td></tr><tr><td>10DX164-62</td><td>Qz6<br>a</td><td>1.40 104.<br>4 40.5 22.9<br>9 5</td><td>&lt;428.2<br>4.82 1.70 v.d.</td><td>v.d. 2.63 &lt;0.106 1.81 1.12 0.092</td><td>&lt;0.29 &lt;0.26 &lt;0.24</td><td>0.66</td><td>61.3</td><td>0.01</td><td>0.5</td><td>336</td><td>382</td></tr><tr><td>10DX201-1</td><td>Qz6<br>a</td><td>124 156. 131<br>5 9 309</td><td>60.5 0.84<br>0 0.887 v.d.</td><td>v.d. &lt;0.00 0.0350 18.0 17.88</td><td>v.d. 0.067<br>0 27.8 0.202</td><td>0.61</td><td>2163</td><td>0.01</td><td>0.5</td><td>327</td><td>372</td></tr><tr><td>10DX201-4</td><td>Qz6<br>a</td><td>184 147. 115<br>7 3 155</td><td>&lt;60.33 1.07 0.180 0.952 0.225</td><td>&lt;0.33 0.0460 32.5 9.36</td><td>0.063<br>0 13.6 0.083</td><td>0.61</td><td>1890</td><td>0.01</td><td>0.5</td><td>253</td><td>288</td></tr><tr><td>10DX201-5</td><td>Qz6<br>a</td><td>201 132. 166<br>6 0 147</td><td>&lt;105.5<br>8 1.15 0.424 1.89 0.390</td><td>0.89 &lt;0.022 17.3 4.13</td><td>0.208 3.43 &lt;0.038</td><td>0.61</td><td>2721</td><td>0.01</td><td>0.5</td><td>262</td><td>298</td></tr><tr><td>10DX201-6</td><td>Qz6<br>a</td><td>245 121. 133<br>7 6 106</td><td>172 0.65<br>0 0.386 v.d.</td><td>0.516 &lt;0.49 1.249 14.5 2.61</td><td>v.d. 0.069 2.03 0.331</td><td>0.61</td><td>2191</td><td>0.01</td><td>0.5</td><td>265</td><td>301</td></tr><tr><td>10DX201-9</td><td>Qz6<br>a</td><td>102 77.6 709 44.3</td><td>&lt;91.39 2.42 0.0700 0.456 3.15</td><td>0.48 0.0460 13.3 7.15</td><td>0.557 0.125 18.1 0.117</td><td>0.61</td><td>1162</td><td>0.01</td><td>0.5</td><td>243</td><td>277</td></tr><tr><td>10DX201-10</td><td>Qz6<br>a</td><td>46.9 78.4 287 87.3</td><td>v.d. 1.20 0.424 v.d.</td><td>2.51 &lt;0.27 0.484 5.65 11.6</td><td>6.32 0.146 11.4 0.878</td><td>0.61</td><td>470</td><td>0.01</td><td>0.5</td><td>296</td><td>336</td></tr><tr><td>10DX201-11</td><td>Qz6<br>a</td><td>15.0 54.2 155 27.6</td><td>&lt;82.02 0.89<br>0 0.0860 0.371 0.710</td><td>&lt;0.67 0.257 3.39 5.61</td><td>0.627 &lt;0.06<br>4 7.95 0.17</td><td>0.61</td><td>254</td><td>0.01</td><td>0.5</td><td>266</td><td>303</td></tr><tr><td>10DX201-23</td><td>Qz6<br>a</td><td>149 82.6 908 39.9</td><td>&lt;74.56 2.05 &lt;0.042 1.07 0.183</td><td>&lt;0.43 0.0650 11.5 8.23</td><td>0.445 &lt;0.05<br>7 28.6 0.072</td><td>0.61</td><td>1489</td><td>0.01</td><td>0.5</td><td>255</td><td>290</td></tr><tr><td>10DX201-24</td><td>Qz6<br>a</td><td>108 114 957 165</td><td>&lt;66.57 2.61 0.929 v.d.</td><td>0.663 &lt;0.70 0.0760 12.6 10.6</td><td>1.63 &lt;0.04<br>7 20.3 0.122</td><td>0.61</td><td>1568</td><td>0.01</td><td>0.5</td><td>288</td><td>328</td></tr><tr><td>10DX201-26</td><td>Qz6<br>a</td><td>17.5 41.7 125 &lt;4.40 123</td><td>7.17 0.0860 1.35 3.59</td><td>&lt;0.40 0.0700 2.34 1.53</td><td>0.537 0.122 2.39 0.172</td><td>0.61</td><td>204</td><td>0.01</td><td>0.5</td><td>299</td><td>340</td></tr></table>
<table><tr><td>10DX201-27</td><td>Qz6 a</td><td>45.2</td><td>120</td><td>933</td><td>235</td><td>&lt;66.20</td><td>7.80</td><td>0.688</td><td>4.72</td><td>0.578</td><td>&lt;0.00</td><td>1.01</td><td>8.26</td><td>36.0</td><td>0.842</td><td>&lt;0.04 6</td><td>50.0</td><td>0.223</td><td>0.61</td><td>1530</td><td>0.01</td><td>0.5</td><td>347</td><td>395</td></tr><tr><td>10DX201-30</td><td>Qz6 a</td><td>10.6</td><td>48.0</td><td>119</td><td>13.5</td><td>87.63</td><td>2.78</td><td>0.158</td><td>1.08</td><td>1.26</td><td>&lt;0.64</td><td>0.0150</td><td>3.08</td><td>2.1</td><td>0.758</td><td>0.066</td><td>2.96</td><td>0.138</td><td>0.61</td><td>195</td><td>0.01</td><td>0.5</td><td>352</td><td>400</td></tr><tr><td>10DX140-70</td><td>Qz6 b</td><td>4.69</td><td>21.1</td><td>139</td><td>30.0</td><td>142</td><td>0.24 0</td><td>0.0970</td><td>0.883</td><td>0.218</td><td>&lt;0.61</td><td>0.474</td><td>6.47</td><td>44.1</td><td>0.155</td><td>0.096 0</td><td>34.5</td><td>0.062</td><td>0.56</td><td>248</td><td>0.01</td><td>0.5</td><td>302</td><td>343</td></tr><tr><td>10DX158-6</td><td>Qz6 b</td><td>14.2</td><td>31.9</td><td>229</td><td>16.0</td><td>&lt;87.68</td><td>0.34 0</td><td>0.808</td><td>v.d.</td><td>0.890</td><td>1.02</td><td>&lt;0.023</td><td>4.45</td><td>2.73</td><td>1.52</td><td>&lt;0.07 1</td><td>4.50</td><td>0.126</td><td>0.52</td><td>441</td><td>0.01</td><td>0.5</td><td>221</td><td>252</td></tr><tr><td>10DX158-8</td><td>Qz6 b</td><td>2.85</td><td>48.7</td><td>114</td><td>11.1</td><td>&lt;73.62</td><td>0.40 0</td><td>0.226</td><td>0.57</td><td>0.399</td><td>&lt;0.63</td><td>0.0750</td><td>2.62</td><td>2.24</td><td>0.983</td><td>0.073</td><td>3.14</td><td>0.036</td><td>0.52</td><td>219</td><td>0.01</td><td>0.5</td><td>226</td><td>258</td></tr><tr><td>10DX158-9</td><td>Qz6 b</td><td>16.8</td><td>121</td><td>530</td><td>131</td><td>&lt;81.87</td><td>0.46 0</td><td>0.463</td><td>1.27</td><td>0.570</td><td>0.700</td><td>0.0340</td><td>9.35</td><td>16.3</td><td>1.37</td><td>0.098 0</td><td>25.0</td><td>&lt;0.023</td><td>0.52</td><td>1020</td><td>0.01</td><td>0.5</td><td>231</td><td>264</td></tr><tr><td>10DX158-10</td><td>Qz6 b</td><td>42.1</td><td>107</td><td>566</td><td>124</td><td>&lt;46.76</td><td>0.73 0</td><td>0.331</td><td>5.83</td><td>1.02</td><td>&lt;0.44</td><td>&lt;0.007 7</td><td>10.5</td><td>13.7</td><td>0.705</td><td>0.070 0</td><td>20.4</td><td>0.095</td><td>0.52</td><td>1089</td><td>0.01</td><td>0.5</td><td>247</td><td>282</td></tr><tr><td>10DX158-11</td><td>Qz6 b</td><td>37.6</td><td>136</td><td>713</td><td>220</td><td>104</td><td>0.63 0</td><td>0.970</td><td>3.56</td><td>1.02</td><td>&lt;0.47</td><td>0.0510</td><td>10.6</td><td>10.3</td><td>2.49</td><td>&lt;0.05 3</td><td>12.5</td><td>0.116</td><td>0.52</td><td>1371</td><td>0.01</td><td>0.5</td><td>242</td><td>276</td></tr><tr><td>10DX158-17</td><td>Qz6 b</td><td>31.3</td><td>101</td><td>361</td><td>81.2</td><td>127</td><td>2.18</td><td>0.476</td><td>6.42</td><td>0.610</td><td>0.960</td><td>0.392</td><td>4.72</td><td>6.09</td><td>0.483</td><td>&lt;0.07 2</td><td>13.2</td><td>0.875</td><td>0.52</td><td>693</td><td>0.01</td><td>0.5</td><td>291</td><td>331</td></tr><tr><td>10DX158-23</td><td>Qz6 b</td><td>1.67</td><td>63.7</td><td>55.1</td><td>15.8</td><td>87.7</td><td>0.52 0</td><td>0.350</td><td>4.22</td><td>0.512</td><td>&lt;0.63</td><td>0.0760</td><td>2.27</td><td>1.66</td><td>1.29</td><td>0.100</td><td>2.23</td><td>0.03</td><td>0.52</td><td>106</td><td>0.01</td><td>0.5</td><td>235</td><td>268</td></tr><tr><td>10DX158-24</td><td>Qz6 b</td><td>8.20</td><td>40.2</td><td>79.4</td><td>7.05</td><td>&lt;64.56</td><td>1.27</td><td>0.054</td><td>0.294</td><td>&lt;0.13 8</td><td>0.540</td><td>0.0399</td><td>2.85</td><td>1.21</td><td>0.227</td><td>0.098 0</td><td>2.54</td><td>0.08</td><td>0.52</td><td>153</td><td>0.01</td><td>0.5</td><td>269</td><td>306</td></tr><tr><td>10DX158-25</td><td>Qz6 b</td><td>56.3</td><td>84.6</td><td>701</td><td>149</td><td>&lt;42.59</td><td>0.99 0</td><td>0.126</td><td>0.637</td><td>0.131</td><td>&lt;0.27 9</td><td>0.0590</td><td>12.4</td><td>6.94</td><td>v.d.</td><td>0.092 0</td><td>7.36</td><td>0.043</td><td>0.52</td><td>1349</td><td>0.01</td><td>0.5</td><td>259</td><td>295</td></tr><tr><td>10DX164-40</td><td>Qz6 b</td><td>80.3</td><td>104</td><td>122 6</td><td>187</td><td>&lt;111.0 1</td><td>1.47</td><td>0.215</td><td>2.96</td><td>1.30</td><td>1.92</td><td>&lt;0.00</td><td>5.06</td><td>11.1</td><td>v.d.</td><td>0.188</td><td>22.2</td><td>0.720</td><td>0.66</td><td>1857</td><td>0.01</td><td>0.5</td><td>275</td><td>313</td></tr><tr><td>10DX164-41</td><td>Qz6 b</td><td>132</td><td>126</td><td>113 9</td><td>278</td><td>141.7</td><td>1.03</td><td>0.0900</td><td>2.29</td><td>1.75</td><td>0.460</td><td>&lt;0.00</td><td>21.6</td><td>13.6</td><td>v.d.</td><td>0.176</td><td>27.7</td><td>0.392</td><td>0.66</td><td>1726</td><td>0.01</td><td>0.5</td><td>260</td><td>297</td></tr><tr><td>10DX201-2</td><td>Qz6 b</td><td>1.67</td><td>18.8</td><td>33.9</td><td>&lt;3.50</td><td>&lt;63.53</td><td>0.60 0</td><td>&lt;0.033</td><td>&lt;0.11 2</td><td>0.336</td><td>&lt;0.68</td><td>&lt;0.022</td><td>32.3</td><td>74.9</td><td>0.776</td><td>0.134</td><td>897</td><td>0.033</td><td>0.61</td><td>55.6</td><td>0.01</td><td>0.5</td><td>240</td><td>274</td></tr><tr><td>10DX201-3</td><td>Qz6 b</td><td>7.39</td><td>47.7</td><td>105</td><td>19.7</td><td>&lt;46.03</td><td>0.46 0</td><td>0.0630</td><td>0.303</td><td>&lt;0.11 7</td><td>&lt;0.36</td><td>0.096</td><td>19.2</td><td>66.0</td><td>0.887</td><td>0.070 0</td><td>875</td><td>0.031</td><td>0.61</td><td>173</td><td>0.01</td><td>0.5</td><td>231</td><td>264</td></tr><tr><td>10DX201-7</td><td>Qz6 b</td><td>1.17</td><td>20.3</td><td>26.6</td><td>&lt;2.62</td><td>&lt;46.57</td><td>0.53 0</td><td>&lt;0.024</td><td>0.339</td><td>0.362</td><td>&lt;0.36</td><td>0.0560</td><td>11.5</td><td>18.8</td><td>0.157</td><td>&lt;0.03 0</td><td>58.3</td><td>0.031</td><td>0.61</td><td>43.7</td><td>0.01</td><td>0.5</td><td>236</td><td>269</td></tr><tr><td>10DX201-8</td><td>Qz6 b</td><td>1.10</td><td>14.9</td><td>26.9</td><td>&lt;4.62</td><td>&lt;79.68</td><td>0.35 0</td><td>&lt;0.046</td><td>0.13 7</td><td>&lt;0.15 6</td><td>&lt;0.68</td><td>0.0520</td><td>16.1</td><td>60.9</td><td>v.d.</td><td>&lt;0.07 1</td><td>172</td><td>0.029</td><td>0.61</td><td>44.1</td><td>0.01</td><td>0.5</td><td>222</td><td>253</td></tr></table>
<table><tr><td>10DX201-27</td><td>Qz6<br>a</td><td>45.2</td><td>120</td><td>933</td><td>235</td><td>&lt;66.20</td><td>7.80</td><td>0.688</td><td>4.72</td><td>0.578</td><td>&lt;0.00</td><td>1.01</td><td>8.26</td><td>36.0</td><td>0.842</td><td>&lt;0.04<br>6</td><td>50.0</td><td>0.223</td><td>0.61</td><td>1530</td><td>0.01</td><td>0.5</td><td>347</td><td>395</td></tr><tr><td>10DX201-30</td><td>Qz6<br>a</td><td>10.6</td><td>48.0</td><td>119</td><td>13.5</td><td>87.63</td><td>2.78</td><td>0.158</td><td>1.08</td><td>1.26</td><td>&lt;0.64</td><td>0.0150</td><td>3.08</td><td>2.1</td><td>0.758</td><td>0.066</td><td>2.96</td><td>0.138</td><td>0.61</td><td>195</td><td>0.01</td><td>0.5</td><td>352</td><td>400</td></tr><tr><td>10DX140-70</td><td>Qz6<br>b</td><td>4.69</td><td>21.1</td><td>139</td><td>30.0</td><td>142</td><td>0.24<br>0</td><td>0.0970</td><td>0.883</td><td>0.218</td><td>&lt;0.61</td><td>0.474</td><td>6.47</td><td>44.1</td><td>0.155</td><td>0.096<br>0</td><td>34.5</td><td>0.062</td><td>0.56</td><td>248</td><td>0.01</td><td>0.5</td><td>302</td><td>343</td></tr><tr><td>10DX158-6</td><td>Qz6<br>b</td><td>14.2</td><td>31.9</td><td>229</td><td>16.0</td><td>&lt;87.68</td><td>0.34<br>0</td><td>0.808</td><td>v.d.</td><td>0.890</td><td>1.02</td><td>&lt;0.023</td><td>4.45</td><td>2.73</td><td>1.52</td><td>&lt;0.07<br>1</td><td>4.50</td><td>0.126</td><td>0.52</td><td>441</td><td>0.01</td><td>0.5</td><td>221</td><td>252</td></tr><tr><td>10DX158-8</td><td>Qz6<br>b</td><td>2.85</td><td>48.7</td><td>114</td><td>11.1</td><td>&lt;73.62</td><td>0.40<br>0</td><td>0.226</td><td>0.57</td><td>0.399</td><td>&lt;0.63</td><td>0.0750</td><td>2.62</td><td>2.24</td><td>0.983</td><td>0.073</td><td>3.14</td><td>0.036</td><td>0.52</td><td>219</td><td>0.01</td><td>0.5</td><td>226</td><td>258</td></tr><tr><td>10DX158-9</td><td>Qz6<br>b</td><td>16.8</td><td>121</td><td>530</td><td>131</td><td>&lt;81.87</td><td>0.46<br>0</td><td>0.463</td><td>1.27</td><td>0.570</td><td>0.700</td><td>0.0340</td><td>9.35</td><td>16.3</td><td>1.37</td><td>0.098<br>0</td><td>25.0</td><td>&lt;0.023</td><td>0.52</td><td>1020</td><td>0.01</td><td>0.5</td><td>231</td><td>264</td></tr><tr><td>10DX158-10</td><td>Qz6<br>b</td><td>42.1</td><td>107</td><td>566</td><td>124</td><td>&lt;46.76</td><td>0.73<br>0</td><td>0.331</td><td>5.83</td><td>1.02</td><td>&lt;0.44</td><td>&lt;0.007<br>7</td><td>10.5</td><td>13.7</td><td>0.705</td><td>0.070<br>0</td><td>20.4</td><td>0.095</td><td>0.52</td><td>1089</td><td>0.01</td><td>0.5</td><td>247</td><td>282</td></tr><tr><td>10DX158-11</td><td>Qz6<br>b</td><td>37.6</td><td>136</td><td>713</td><td>220</td><td>104</td><td>0.63<br>0</td><td>0.970</td><td>3.56</td><td>1.02</td><td>&lt;0.47</td><td>0.0510</td><td>10.6</td><td>10.3</td><td>2.49</td><td>&lt;0.05<br>3</td><td>12.5</td><td>0.116</td><td>0.52</td><td>1371</td><td>0.01</td><td>0.5</td><td>242</td><td>276</td></tr><tr><td>10DX158-17</td><td>Qz6<br>b</td><td>31.3</td><td>101</td><td>361</td><td>81.2</td><td>127</td><td>2.18</td><td>0.476</td><td>6.42</td><td>0.610</td><td>0.960</td><td>0.392</td><td>4.72</td><td>6.09</td><td>0.483</td><td>&lt;0.07<br>2</td><td>13.2</td><td>0.875</td><td>0.52</td><td>693</td><td>0.01</td><td>0.5</td><td>291</td><td>331</td></tr><tr><td>10DX158-23</td><td>Qz6<br>b</td><td>1.67</td><td>63.7</td><td>55.1</td><td>15.8</td><td>87.7</td><td>0.52<br>0</td><td>0.350</td><td>4.22</td><td>0.512</td><td>&lt;0.63</td><td>0.0760</td><td>2.27</td><td>1.66</td><td>1.29</td><td>0.100</td><td>2.23</td><td>0.03</td><td>0.52</td><td>106</td><td>0.01</td><td>0.5</td><td>235</td><td>268</td></tr><tr><td>10DX158-24</td><td>Qz6<br>b</td><td>8.20</td><td>40.2</td><td>79.4</td><td>7.05</td><td>&lt;64.56</td><td>1.27</td><td>0.054</td><td>0.294</td><td>&lt;0.13<br>8</td><td>0.540</td><td>0.0399</td><td>2.85</td><td>1.21</td><td>0.227</td><td>0.098<br>0</td><td>2.54</td><td>0.08</td><td>0.52</td><td>153</td><td>0.01</td><td>0.5</td><td>269</td><td>306</td></tr><tr><td>10DX158-25</td><td>Qz6<br>b</td><td>56.3</td><td>84.6</td><td>701</td><td>149</td><td>&lt;42.59</td><td>0.99<br>0</td><td>0.126</td><td>0.637</td><td>0.131</td><td>&lt;0.27<br>9</td><td>0.0590</td><td>12.4</td><td>6.94</td><td>v.d.</td><td>0.092<br>0</td><td>7.36</td><td>0.043</td><td>0.52</td><td>1349</td><td>0.01</td><td>0.5</td><td>259</td><td>295</td></tr><tr><td>10DX164-40</td><td>Qz6<br>b</td><td>80.3</td><td>104</td><td>122<br>6</td><td>187</td><td>&lt;111.0<br>1</td><td>1.47</td><td>0.215</td><td>2.96</td><td>1.30</td><td>1.92</td><td>&lt;0.00</td><td>5.06</td><td>11.1</td><td>v.d.</td><td>0.188</td><td>22.2</td><td>0.720</td><td>0.66</td><td>1857</td><td>0.01</td><td>0.5</td><td>275</td><td>313</td></tr><tr><td>10DX164-41</td><td>Qz6<br>b</td><td>132</td><td>126</td><td>113<br>9</td><td>278</td><td>141.7</td><td>1.03</td><td>0.0900</td><td>2.29</td><td>1.75</td><td>0.460</td><td>&lt;0.00</td><td>21.6</td><td>13.6</td><td>v.d.</td><td>0.176</td><td>27.7</td><td>0.392</td><td>0.66</td><td>1726</td><td>0.01</td><td>0.5</td><td>260</td><td>297</td></tr><tr><td>10DX201-2</td><td>Qz6<br>b</td><td>1.67</td><td>18.8</td><td>33.9</td><td>&lt;3.50</td><td>&lt;63.53</td><td>0.60<br>0</td><td>&lt;0.033</td><td>&lt;0.11<br>2</td><td>0.336</td><td>&lt;0.68</td><td>&lt;0.022</td><td>32.3</td><td>74.9</td><td>0.776</td><td>0.134</td><td>897</td><td>0.033</td><td>0.61</td><td>55.6</td><td>0.01</td><td>0.5</td><td>240</td><td>274</td></tr><tr><td>10DX201-3</td><td>Qz6<br>b</td><td>7.39</td><td>47.7</td><td>105</td><td>19.7</td><td>&lt;46.03</td><td>0.46<br>0</td><td>0.0630</td><td>0.303</td><td>&lt;0.11<br>7</td><td>&lt;0.36</td><td>0.096</td><td>19.2</td><td>66.0</td><td>0.887</td><td>0.070<br>0</td><td>875</td><td>0.031</td><td>0.61</td><td>173</td><td>0.01</td><td>0.5</td><td>231</td><td>264</td></tr><tr><td>10DX201-7</td><td>Qz6<br>b</td><td>1.17</td><td>20.3</td><td>26.6</td><td>&lt;2.62</td><td>&lt;46.57</td><td>0.53<br>0</td><td>&lt;0.024</td><td>0.339</td><td>0.362</td><td>&lt;0.36</td><td>0.0560</td><td>11.5</td><td>18.8</td><td>0.157</td><td>&lt;0.03<br>0</td><td>58.3</td><td>0.031</td><td>0.61</td><td>43.7</td><td>0.01</td><td>0.5</td><td>236</td><td>269</td></tr><tr><td>10DX201-8</td><td>Qz6<br>b</td><td>1.10</td><td>14.9</td><td>26.9</td><td>&lt;4.62</td><td>&lt;79.68</td><td>0.35<br>0</td><td>&lt;0.046</td><td>&lt;0.13<br>7</td><td>&lt;0.15<br>6</td><td>&lt;0.68</td><td>0.0520</td><td>16.1</td><td>60.9</td><td>v.d.</td><td>&lt;0.07<br>1</td><td>172</td><td>0.029</td><td>0.61</td><td>44.1</td><td>0.01</td><td>0.5</td><td>222</td><td>253</td></tr></table>
<table><tr><td>10DX201-19</td><td>Qz6<br>b</td><td>3.06</td><td>25.9</td><td>102</td><td>18.5</td><td>&lt;51.18</td><td>0.43<br>0</td><td>&lt;0.027</td><td>0.279</td><td>&lt;0.09<br>8</td><td>0.390</td><td>0.289</td><td>13.4</td><td>47.4</td><td>0.275</td><td>0.043</td><td>232</td><td>&lt;0.018<br>9</td><td>0.61</td><td>167</td><td>0.01</td><td>0.5</td><td>229</td><td>261</td></tr><tr><td>10DX201-20</td><td>Qz6<br>b</td><td>8.32</td><td>17.9</td><td>92.5</td><td>12.4</td><td>96.72</td><td>0.37<br>0</td><td>0.024</td><td>0.172</td><td>0.189</td><td>&lt;0.31</td><td>0.133</td><td>13.7</td><td>50.3</td><td>0.127</td><td>0.076</td><td>285</td><td>0.02</td><td>0.61</td><td>152</td><td>0.01</td><td>0.5</td><td>223</td><td>255</td></tr><tr><td>10DX201-21</td><td>Qz6<br>b</td><td>1.47</td><td>24.4</td><td>23.7</td><td>&lt;2.79</td><td>&lt;50.10</td><td>0.46<br>0</td><td>&lt;0.021<br>9</td><td>&lt;0.08<br>6</td><td>0.109</td><td>&lt;0.29</td><td>0.205</td><td>22.0</td><td>79.4</td><td>0.040<br>9</td><td>0.099</td><td>279</td><td>&lt;0.022<br>9</td><td>0.61</td><td>38.8</td><td>0.01</td><td>0.5</td><td>231</td><td>264</td></tr><tr><td>10DX201-22</td><td>Qz6<br>b</td><td>3.19</td><td>57.2</td><td>143</td><td>13.2</td><td>&lt;60.40</td><td>0.49<br>0</td><td>0.234</td><td>5.02</td><td>0.160</td><td>&lt;0.47</td><td>0.350</td><td>30.9</td><td>81.4</td><td>0.374</td><td>0.066</td><td>877</td><td>0.052</td><td>0.61</td><td>234</td><td>0.01</td><td>0.5</td><td>233</td><td>266</td></tr><tr><td>10DX201-25</td><td>Qz6<br>b</td><td>126</td><td>196</td><td>209<br>6</td><td>656</td><td>&lt;44.32</td><td>0.73<br>0</td><td>v.d.</td><td>v.d.</td><td>1.47</td><td>0.840</td><td>0.0990</td><td>29.5</td><td>53.8</td><td>v.d.</td><td>0.122</td><td>333</td><td>0.878</td><td>0.61</td><td>3436</td><td>0.01</td><td>0.5</td><td>247</td><td>282</td></tr></table>

v.d.: value discarded; values below detection limit are denoted with a "<" sign.
<table><tr><td>10DX201-19</td><td>Qz6<br>b</td><td>3.06 25.9 102 18.5</td><td>&lt;51.18</td><td>0.43<br>0</td><td>&lt;0.027 0.279</td><td>&lt;0.09<br>8</td><td>0.390 0.289 13.4 47.4</td><td>0.275 0.043 232</td><td>&lt;0.018<br>9</td><td>0.61</td><td>167</td><td>0.01</td><td>0.5</td><td>229</td><td>261</td></tr><tr><td>10DX201-20</td><td>Qz6<br>b</td><td>8.32 17.9 92.5 12.4</td><td>96.72</td><td>0.37<br>0</td><td>0.024 0.172 0.189</td><td>&lt;0.31</td><td>0.133 13.7 50.3</td><td>0.127 0.076 285</td><td>0.02</td><td>0.61</td><td>152</td><td>0.01</td><td>0.5</td><td>223</td><td>255</td></tr><tr><td>10DX201-21</td><td>Qz6<br>b</td><td>1.47 24.4 23.7 &lt;2.79</td><td>&lt;50.10</td><td>0.46<br>0</td><td>&lt;0.021 0.08<br>9 6</td><td>0.109 &lt;0.29</td><td>0.205 22.0 79.4</td><td>0.040<br>9 0.099 279</td><td>&lt;0.022<br>9</td><td>0.61</td><td>38.8</td><td>0.01</td><td>0.5</td><td>231</td><td>264</td></tr><tr><td>10DX201-22</td><td>Qz6<br>b</td><td>3.19 57.2 143 13.2</td><td>&lt;60.40</td><td>0.49<br>0</td><td>0.234 5.02</td><td>0.160 &lt;0.47</td><td>0.350 30.9 81.4</td><td>0.374 0.066 877</td><td>0.052</td><td>0.61</td><td>234</td><td>0.01</td><td>0.5</td><td>233</td><td>266</td></tr><tr><td>10DX201-25</td><td>Qz6<br>b</td><td>126 196 209<br>6 656</td><td>&lt;44.32</td><td>0.73<br>0</td><td>v.d. v.d.</td><td>1.47 0.840 0.0990 29.5</td><td>53.8 v.d.</td><td>0.122 333</td><td>0.878</td><td>0.61</td><td>3436</td><td>0.01</td><td>0.5</td><td>247</td><td>282</td></tr></table>

v.d.: value discarded; values below detection limit are denoted with a "<" sign.
### 5.4. Temperature Estimation

At a chemical equilibrium, the incorporation of Ti in quartz is dependent on pressure and temperature. The dependency has been devised as a geothermometer known as Tita-niQ by various experiments [23,26,27,75,76]. Different calibration equations have been de-rived [77], but one developed by [26], as shown below, was selected in this study based on the arguments presented in [76]. An overview of the arguments is out of the scope of this study; interested readers are referred to the publications mentioned above.

$$RT\ln X_{TiO_2}^{quartz} = -60952(\pm3122) + 1.52(\pm0.04) \times T - 1741(\pm63) \times P + RT\ln a_{TiO_2}$$

At a given Ti activity ($a_{TiO_2}$), the mole fraction of Ti in quartz ($X_{TiO_2}^{quartz}$) increases with T but decreases with P. In a P-T space, equal $X_{TiO_2}^{quartz}$ (isopleth) defines vertical lines that have increasing slopes (Figure 10). For the Tongchang deposit, $a_{TiO_2} = 1$ can be assumed for Qz2-, Qz3- and Qz4- and Qz5-depositing fluids since the rutile was coprecipitated. For Qz1 and Qz6, $a_{TiO_2} = 0.5$ and 1, are used to calculate two isopleths for each $X_{TiO_2}^{quartz}$.

Exact pressures and temperatures can be obtained by combining TitaniQ and other geothermobarometers. Fluid inclusion isochores are an option but, unfortunately, they are only available for Qz3 and Qz4. B15HS inclusions in Qz1 and Qz2 are not used since their origin remains unclear [19] and their isochores intersect with TitaniQ isopleths at unreasonably high pressures (Figure 10). For the remaining quartz generations, a range of geologically reasonable pressures are assumed, i.e., 1500–500 bars for Qz1, Qz2, and Qz3a, 500–100 bars for Qz5, and 500–10 bars for Qz6. The assumption of decreasing pressures is supported by the increasing Al and Li contents consistent with a recent study by [78]. At a constant pressure, temperature is negatively related to $a_{TiO_2}$. The minimum temperatures for Qz1 and Qz6 are calculated with $a_{TiO_2} = 1$ and minimum pressure, and maximum temperatures are calculated with $a_{TiO_2} = 0.5$ and maximum pressure. Accordingly, the following averaged temperature ranges are obtained for different quartz generations (Figure 10; Table 4): Qz1 425–495 °C; Qz2a 529–618 °C; Qz2b 473–551 °C; Qz3a 374–420; Qz3b 350–450 °C; Qz4 310–390 °C; Qz5a 356–385 °C; Qz5b 344–351 °C; Qz6a 287–327 °C; Qz6b 242–276 °C.

<figure><img src="image_15.png" /><figcaption>**Figure 10.** Pressure and temperature estimates by combining TitaniQ isopleths (dash-dotted lines in red) and fluid inclusion isochores (dash lines in black). Ti isopleths of 1 ppm, 10 ppm, 30 ppm, 50 ppm, and 100 ppm are shown; isochores of B15HS inclusions in both Qz2a and Qz2b, B50 inclusions in Qz3b, B30 inclusions in Qz4, and B10 inclusions are shown. The minimum and maximum range (solid open diamonds in colors) as well as an averaged range (solid color-filled) of Ti contents for all quartz generations are shown. Orange indicates Qz1, red indicates Qz2a, pink indicates Qz2b, yellow indicates Qz3a, green indicates Qz3b, blue indicates Qz4, dark brown indicates Qz5b, purple</figcaption></figure>
5.4. Temperature Estimation

At a chemical equilibrium, the incorporation of Ti in quartz is dependent on pressure and temperature. The dependency has been devised as a geothermometer known as Tita- niQ by various experiments [23,26,27,75,76]. Different calibration equations have been de- rived [77], but one developed by [26], as shown below, was selected in this study based on the arguments presented in [76]. An overview of the arguments is out of the scope of this study; interested readers are referred to the publications mentioned above.

$$RT\ln X_{TiO_2}^{quartz} = -60952(\pm3122) + 1.52(\pm0.04) \times T - 1741(\pm63) \times P + RT\ln a_{TiO_2}$$

At a given Ti activity ($a_{TiO_2}$), the mole fraction of Ti in quartz ($X_{TiO_2}^{quartz}$) increases with T but decreases with P. In a P-T space, equal $X_{TiO_2}^{quartz}$ (isopleth) defines vertical lines that have increasing slopes (Figure 10). For the Tongchang deposit, $a_{TiO_2}$ = 1 can be assumed for Qz2-, Qz3- and Qz4- and Qz5-depositing fluids since the rutile was coprecipitated. For Qz1 and Qz6, $a_{TiO_2}$ = 0.5 and 1, are used to calculate two isopleths for each $X_{TiO_2}^{quartz}$.

Exact pressures and temperatures can be obtained by combining TitaniQ and other geothermobarometers. Fluid inclusion isochores are an option but, unfortunately, they are only available for Qz3 and Qz4. B15HS inclusions in Qz1 and Qz2 are not used since their origin remains unclear [19] and their isochores intersect with TitaniQ isopleths at unrea- sonably high pressures (Figure 10). For the remaining quartz generations, a range of geo- logically reasonable pressures are assumed, i.e., 1500–500 bars for Qz1, Qz2, and Qz3a, 500–100 bars for Qz5, and 500–10 bars for Qz6. The assumption of decreasing pressures is supported by the increasing Al and Li contents consistent with a recent study by [78]. At a constant pressure, temperature is negatively related to $a_{TiO_2}$. The minimum tempera- tures for Qz1 and Qz6 are calculated with $a_{TiO_2}$ = 1 and minimum pressure, and maxi- mum temperatures are calculated with $a_{TiO_2}$ = 0.5 and maximum pressure. Accordingly, the following averaged temperature ranges are obtained for different quartz generations (Figure 10; Table 4): Qz1 425–495 °C; Qz2a 529–618 °C; Qz2b 473–551 °C; Qz3a 374–420; Qz3b 350–450 °C; Qz4 310–390 °C; Qz5a 356–385 °C; Qz5b 344–351 °C; Qz6a 287–327 °C; Qz6b 242–276 °C.

<figure><img src="image_15.png" /><figcaption>**Figure 10.** Pressure and temperature estimates by combining TitaniQ isopleths (dash-dotted lines in red) and fluid inclusion isochores (dash lines in black). Ti isopleths of 1 ppm, 10 ppm, 30 ppm, 50 ppm, and 100 ppm are shown; isochores of B15HS inclusions in both Qz2a and Qz2b, B50 inclusions in Qz3b, B30 inclusions in Qz4, and B10 inclusions are shown. The minimum and maximum range (solid open diamonds in colors) as well as an averaged range (solid color-filled) of Ti contents for all quartz generations are shown. Orange indicates Qz1, red indicates Qz2a, pink indicates Qz2b, yellow indicates Qz3a, green indicates Qz3b, blue indicates Qz4, dark brown indicates Qz5b, purple</figcaption></figure>
indicates Qz6a, and grey indicates Qz6b. Note that only Qz3a and Qz4 had reliable fluid inclusion
isochore data that allowed for the use of the interception method. For other quartz generations, a
pressure range was assumed to produce a reliable temperature estimate.

**6. Discussion**

6.1. *An Improved Timeline Based on Quartz CL Sequencing*

Vein crosscut relations are often used to sort fluid events in the porphyry deposits
[8]. However, this technique could be imparted by the existence of reopened veins. In
those cases, a detailed look into mineral microstructures could help construct a reliable time-
line of superimposed fluid events.

CL microstructures in hydrothermal quartz falls in two general categories: primary crystallization textures and secondary modification textures attributable to quartz deposition, dissolution, and deformation processes [79,80]. Concentric and euhedral oscillatory zoning in the Qz2a, Qz3, Qz5, and Qz6 grains belong to the primary crystallization textures, indicating a direct deposition from hydrothermal fluids. Mottled CL in the Qz1 and Qz2b grains is indicative of fluid-aided dynamic recrystallization. Similar Ti contents in both quartz generations might indicate a common event of recrystallization. The seemingly contradictory coexistence of un-recrystallized Qz2a and recrystallized Qz2b is likely linked to a difference in crystal sizes and shapes and resultant preferential deformation, as proposed for the Butte porphyry Cu-Mo deposit [22]. Qz2b resorbing Qz2a, "splatter" and "cobweb" in the Qz1 and Qz2 grains as well as overgrowth of Qz3 on earlier quartz gains indicate quartz dissolution. Qz3 and Qz4 fragments and fracture-filling Qz5 grains are indicative of brittle fracturing.

Based on these pieces of textural evidence, a refined timeline of fluid evolution is proposed for the Tongchang deposit. The early stage involved the deposition of the Qz1 precursor, Qz2a, and the Qz2b precursor followed by dynamic recrystallization and a first-time dissolution. The subsequent intermediate stage started with dissolution of earlier quartz grains followed by progressive deposition of Qz3a, Qz3b, and Qz4. The late stage commenced with the fracturing and brecciation of earlier quartz grains followed by the progressive deposition of Qz5 and Qz6.

Petrographic observations suggest that the early Qz1- and Qz2-depositing stage also precipitated hematite and anhydrite (Anh1) in the veins, and bornite, chalcopyrite, and potassic silicates in the alteration halos. The early intermediate stage precipitated pyrite, chalcopyrite, anhydrite (Anh3), chlorite, and sericite, along with Qz3 quartz, as well as chlorite-sericite alteration halos. The late intermediate stage precipitated abundant chalcopyrite, pyrite, anhydrite (Anh4), chlorite, sericite, and calcite in the veins. The late stages generated pyrite and sericite with Qz5 and Qz6 grains.

6.2. *Fluid Cooling and Compression during Quartz Deposition, Recrystallization, and Dissolution*

6.2.1. Quartz Deposition

TitaniQ thermobarometry has been widely utilized to estimate the P-T conditions of quartz deposition in magmatic [81,82] and hydrothermal environments [22,74,83]. Quartz solubility in various fluid compositions at varied P-T conditions can be used to investigate the fluid processes responsible for quartz deposition and dissolution, and, by inference, vein formation processes [31,32,84].

According to TitaniQ temperatures, early quartz deposition (Qz2a) occurred at
around 529–618 °C; early intermediate quartz deposition (Qz3a and Qz3b) occurred at
around 350–450 °C; late intermediate quartz deposition (Qz4) occurred at around 310–400
°C; and late quartz deposition (Qz5 and Qz6) occurred at around 240–400 °C. On a P-T
phase diagram for H₂O-NaCl overlapped with quartz solubility curves (Figure 11), the
quartz deposition temperature ranges are located in the single liquid phase region where
quartz solubility decreases dramatically with temperature, and much less with pressure.
indicates Qz6a, and grey indicates Qz6b. Note that only Qz3a and Qz4 had reliable fluid inclusion
isochore data that allowed for the use of the interception method. For other quartz generations, a
pressure range was assumed to produce a reliable temperature estimate.

6. Discussion

6.1. *An Improved Timeline Based on Quartz CL Sequencing*

Vein crosscut relations are often used to sort fluid events in the porphyry deposits
[8]. However, this technique could be imparted by the existence of reopened veins. In
those cases, a detailed look into mineral microstructures could help construct a reliable time-
line of superimposed fluid events.

CL microstructures in hydrothermal quartz falls in two general categories: primary crystallization textures and secondary modification textures attributable to quartz deposition, dissolution, and deformation processes [79,80]. Concentric and euhedral oscillatory zoning in the Qz2a, Qz3, Qz5, and Qz6 grains belong to the primary crystallization textures, indicating a direct deposition from hydrothermal fluids. Mottled CL in the Qz1 and Qz2b grains is indicative of fluid-aided dynamic recrystallization. Similar Ti contents in both quartz generations might indicate a common event of recrystallization. The seemingly contradictory coexistence of un-recrystallized Qz2a and recrystallized Qz2b is likely linked to a difference in crystal sizes and shapes and resultant preferential deformation, as proposed for the Butte porphyry Cu-Mo deposit [22]. Qz2b resorbing Qz2a, "splatter" and "cobweb" in the Qz1 and Qz2 grains as well as overgrowth of Qz3 on earlier quartz gains indicate quartz dissolution. Qz3 and Qz4 fragments and fracture-filling Qz5 grains are indicative of brittle fracturing.

Based on these pieces of textural evidence, a refined timeline of fluid evolution is proposed for the Tongchang deposit. The early stage involved the deposition of the Qz1 precursor, Qz2a, and the Qz2b precursor followed by dynamic recrystallization and a first-time dissolution. The subsequent intermediate stage started with dissolution of earlier quartz grains followed by progressive deposition of Qz3a, Qz3b, and Qz4. The late stage commenced with the fracturing and brecciation of earlier quartz grains followed by the progressive deposition of Qz5 and Qz6.

Petrographic observations suggest that the early Qz1- and Qz2-depositing stage also precipitated hematite and anhydrite (Anh1) in the veins, and bornite, chalcopyrite, and potassic silicates in the alteration halos. The early intermediate stage precipitated pyrite, chalcopyrite, anhydrite (Anh3), chlorite, and sericite, along with Qz3 quartz, as well as chlorite-sericite alteration halos. The late intermediate stage precipitated abundant chalcopyrite, pyrite, anhydrite (Anh4), chlorite, sericite, and calcite in the veins. The late stages generated pyrite and sericite with Qz5 and Qz6 grains.

6.2. *Fluid Cooling and Compression during Quartz Deposition, Recrystallization, and Dissolution*

6.2.1. Quartz Deposition

TitaniQ thermobarometry has been widely utilized to estimate the P-T conditions of quartz deposition in magmatic [81,82] and hydrothermal environments [22,74,83]. Quartz solubility in various fluid compositions at varied P-T conditions can be used to investigate the fluid processes responsible for quartz deposition and dissolution, and, by inference, vein formation processes [31,32,84].

According to TitaniQ temperatures, early quartz deposition (Qz2a) occurred at
around 529–618 °C; early intermediate quartz deposition (Qz3a and Qz3b) occurred at
around 350–450 °C; late intermediate quartz deposition (Qz4) occurred at around 310–400
°C; and late quartz deposition (Qz5 and Qz6) occurred at around 240–400 °C. On a P-T
phase diagram for H₂O-NaCl overlapped with quartz solubility curves (Figure 11), the
quartz deposition temperature ranges are located in the single liquid phase region where
quartz solubility decreases dramatically with temperature, and much less with pressure.
It is inferred that the quartz deposition is mainly the result of fluid cooling. Anhydrite has a similar prograde solubility behavior at temperatures above 350 °C in H₂O-10wt.%NaCl solutions, but shows retrograde solubility below that temperature (the grey region in the Figure 11). Increasing salinity tends to decrease the deflection point of the temperature, thus shifting the retrograde region to lower temperatures. H₂O-NaCl fluids containing silica and calcium sulfate would precipitate quartz and anhydrite upon cooling to 350 °C. Below 350 °C, quartz would continue to precipitate, whereas anhydrite deposition would cease. This inference is consistent with the coprecipitation of quartz and anhydrite in the early to intermediate stage and the disappearance of anhydrite in the late stage in the Tongchang deposit.

<figure><img src="image_16.png" /><figcaption>**Figure 11.** P-T phase diagrams for H₂O-10 wt.% NaCl and H₂O-20 wt.% NaCl aqueous systems, contoured with quartz and anhydrite solubilities (red: quartz; green: anhydrite; solid curve: H₂O-20 wt.% NaCl; dashed curve: H₂O-10 wt.% NaCl. Anhydrite data are from [85]; and quartz data are from [31]. The two areas in grey color are the retrograde solubility regions of anhydrite (AnhRS) and quartz (QzRS). The color-filled rectangles accompanied with error bars represent the deposition conditions of quartz and anhydrite (colors are the same as the in the Figure 10). The thick arrows (decompression cooling in red; quasi-isothermal compression in black) and connecting dash lines represent the possible P-T paths of the hydrothermal ore fluids. Note that the quasi-isothermal fluid overpressure occurred prior to precipitation of Qz3/Anh2, which was followed by pressure fluctuations. Pressure fluctuations also happened during the formation of Qz5. Solubility values (in mm/kgH₂O) are marked on the curves. GD solidus: H₂O-saturated granodioritic melt solidus; CP10/20: critical point for H₂O-10 wt.% NaCl or H₂O-20 wt.% NaCl. L: liquid; V: vapor; H: halite.</figcaption></figure>

### 6.2.2. Quartz Recrystallization

Like many other minerals, quartz undergoes dynamic recrystallization during deformation to minimize free strain energy [86]. Three distinctive recrystallization mechanisms have been recognized [87], i.e., bulging recrystallization (BLG), subgrain rotation (SGR), and grain boundary migration (GBM). These mechanisms occur at different temperature regimes and result in characteristic microstructures [22]. BLG occurs at temperatures between 250 °C and 400 °C, resulting in small, recrystallized grains surrounding large, un-
It is inferred that the quartz deposition is mainly the result of fluid cooling. Anhydrite has a similar prograde solubility behavior at temperatures above 350 °C in H₂O-10wt.%NaCl solutions, but shows retrograde solubility below that temperature (the grey region in the Figure 11). Increasing salinity tends to decrease the deflection point of the temperature, thus shifting the retrograde region to lower temperatures. H₂O-NaCl fluids containing silica and calcium sulfate would precipitate quartz and anhydrite upon cooling to 350 °C. Below 350 °C, quartz would continue to precipitate, whereas anhydrite deposition would cease. This inference is consistent with the coprecipitation of quartz and anhydrite in the early to intermediate stage and the disappearance of anhydrite in the late stage in the Tongchang deposit.

<figure><img src="image_16.png" /><figcaption>**Figure 11.** P-T phase diagrams for H₂O-10 wt.% NaCl and H₂O-20 wt.% NaCl aqueous systems, contoured with quartz and anhydrite solubilities (red: quartz; green: anhydrite; solid curve: H₂O-20 wt.% NaCl; dashed curve: H₂O-10 wt.% NaCl. Anhydrite data are from [85]; and quartz data are from [31]. The two areas in grey color are the retrograde solubility regions of anhydrite (AnhRS) and quartz (QzRS). The color-filled rectangles accompanied with error bars represent the deposition conditions of quartz and anhydrite (colors are the same as the in the Figure 10). The thick arrows (decompression cooling in red; quasi-isothermal compression in black) and connecting dash lines represent the possible P-T paths of the hydrothermal ore fluids. Note that the quasi-isothermal fluid overpressure occurred prior to precipitation of Qz3/Anh2, which was followed by pressure fluctuations. Pressure fluctuations also happened during the formation of Qz5. Solubility values (in mm/kgH₂O) are marked on the curves. GD solidus: H₂O-saturated granodioritic melt solidus; CP10/20: critical point for H₂O-10 wt.% NaCl or H₂O-20 wt.% NaCl. L: liquid; V: vapor; H: halite.</figcaption></figure>

### 6.2.2. Quartz Recrystallization

Like many other minerals, quartz undergoes dynamic recrystallization during deformation to minimize free strain energy [86]. Three distinctive recrystallization mechanisms have been recognized [87], i.e., bulging recrystallization (BLG), subgrain rotation (SGR), and grain boundary migration (GBM). These mechanisms occur at different temperature regimes and result in characteristic microstructures [22]. BLG occurs at temperatures between 250 °C and 400 °C, resulting in small, recrystallized grains surrounding large, un-
recrystallized grains. SGR occurs at temperatures between 400 °C and 500 °C, generating straight and commonly polygonal grain boundaries. GBM occurs at temperatures between 500 °C and 600 °C, producing lobate grain boundaries. TitaniQ applied in a metamorphic environment [88] and experiments [76,89,90] suggests that SGR and GBM could re-equilibrate Ti in quartz, and thus that TitaniQ would record the temperature of recrystallization.

The grain boundaries shown in Qz1 and Qz2b grains are similar to those of SGR (Figure 6a,b). TitaniQ temperatures of 400–550 °C suggest SGR/GBM recrystallization consistent with the microstructures. A noteworthy feature is that less-recrystallized Qz2a grains are commonly rimmed by CL-dark edges. A similar feature in B-type veins of the Butte porphyry deposit was proposed to be a result of mismatch in lattice alignment of adjacent crystals during competitive grain growth [22]. However, we noted that the CL-dark rims in the Qz2a grains are comparable to those quartz experimentally deformed with the presence of fluid [76]. We infer that the CL-dark rims in Qz2 (Figure 6b) may have been a product of fluid-mediated dissolution-reprecipitation during dynamic recrystallization. If this inference is correct, the quartz dissolution event requires an increase in silica solubility, which cannot be explained by a drop in fluid pressure in a deflating magma chamber as proposed by [22]. Conversely, we consider it more likely to reflect an increase in fluid pressure and/or temperature based on a solubility analysis (Figure 11). Fluid compression is a plausible process in that overpressure in the overlying carapace that could be caused by fluid exsolution and accumulation, which is common for the deposition of early quartz veins [91]. In addition, silica solubility can be enhanced by new pulses of mafic recharge, which may introduce hotter fluids. A possible magmatic recharge was suggested by a geochemical study of the mafic enclaves of the Tongchang deposit [20].

### 6.2.3. Quartz Dissolution and Fracturing

Immediately after the deposition of Qz2b, a quartz- and anhydrite-dissolution took place prior to the deposition of Qz3 and Anh2 at lower temperatures (350–450 °C) and fluctuating pressures. The temperature constraints indicate a transition from lithostatic to hydrostatic regimes (Figure 11). The quartz dissolution was previously attributed to quasi-isobaric cooling through the retrograde quartz solubility region [17,31,92]. However, this explanation is not likely for Tongchang because quasi-isobaric cooling would cause lower Ti contents in later deposited Qz3b, which is inconsistent with higher Ti contents in Qz3b (around 15 ppm) than in Qz3a (around 10 ppm). Another observation not in favor of quasi-isobaric cooling is that anhydrite displays prograde solubility in the quartz retrograde solubility field, which cannot account for the coeval dissolution of anhydrite and quartz (Figure 11). Therefore, it is inferred that fluid pressurization is seemingly the only viable way to elevate the solubility for both minerals.

Quartz and anhydrite show a similar solubility behavior at temperatures between 350 °C and 400 °C and pressures below 2000 bars, corresponding to a hydrostatic regime [92]. Under hydrostatic conditions, quartz and anhydrite deforms in a brittle fashion, which is consistent with early anhydrite breccia cemented by Anh4 (Figure 7h). The quartz micro-breccia enclosed in Qz5 suggests the occurrence of another episode of fluid overpressure. With the space created by brecciation, pressure fluctuated in response to fluid exsolution and mineral precipitation, resulting in the zoning patterns in Qz5b (Figure 11).

Preexisting veins can be reopened during a later fluid event by dissolution, mechanical breaking, brecciation, and recrystallization [17]. At Tongchang, these phenomena are abundant and occurred at different stages. Dissolution and recrystallization occurred in the early to transitional stage when host rock behaved in ductile fashion, whereas breaking and brecciation occurred in the late stage when host rocks behaved in a brittle fashion.

### 6.3. Vein Growth Via Reopening

Hydrothermal veins in porphyry Cu deposits are commonly grouped into early quartz (A-type), transitional molybdenite quartz (B-type), and late pyrite (D-type) veins
recrystallized grains. SGR occurs at temperatures between 400 °C and 500 °C, generating straight and commonly polygonal grain boundaries. GBM occurs at temperatures between 500 °C and 600 °C, producing lobate grain boundaries. TitaniQ applied in a metamorphic environment [88] and experiments [76,89,90] suggests that SGR and GBM could re-equilibrate Ti in quartz, and thus that TitaniQ would record the temperature of recrystallization.

The grain boundaries shown in Qz1 and Qz2b grains are similar to those of SGR (Figure 6a,b). TitaniQ temperatures of 400–550 °C suggest SGR/GBM recrystallization consistent with the microstructures. A noteworthy feature is that less-recrystallized Qz2a grains are commonly rimmed by CL-dark edges. A similar feature in B-type veins of the Butte porphyry deposit was proposed to be a result of mismatch in lattice alignment of adjacent crystals during competitive grain growth [22]. However, we noted that the CL-dark rims in the Qz2a grains are comparable to those quartz experimentally deformed with the presence of fluid [76]. We infer that the CL-dark rims in Qz2 (Figure 6b) may have been a product of fluid-mediated dissolution-reprecipitation during dynamic recrystallization. If this inference is correct, the quartz dissolution event requires an increase in silica solubility, which cannot be explained by a drop in fluid pressure in a deflating magma chamber as proposed by [22]. Conversely, we consider it more likely to reflect an increase in fluid pressure and/or temperature based on a solubility analysis (Figure 11). Fluid compression is a plausible process in that overpressure in the overlying carapace that could be caused by fluid exsolution and accumulation, which is common for the deposition of early quartz veins [91]. In addition, silica solubility can be enhanced by new pulses of mafic recharge, which may introduce hotter fluids. A possible magmatic recharge was suggested by a geochemical study of the mafic enclaves of the Tongchang deposit [20].

### 6.2.3. Quartz Dissolution and Fracturing

Immediately after the deposition of Qz2b, a quartz- and anhydrite-dissolution took place prior to the deposition of Qz3 and Anh2 at lower temperatures (350–450 °C) and fluctuating pressures. The temperature constraints indicate a transition from lithostatic to hydrostatic regimes (Figure 11). The quartz dissolution was previously attributed to quasi-isobaric cooling through the retrograde quartz solubility region [17,31,92]. However, this explanation is not likely for Tongchang because quasi-isobaric cooling would cause lower Ti contents in later deposited Qz3b, which is inconsistent with higher Ti contents in Qz3b (around 15 ppm) than in Qz3a (around 10 ppm). Another observation not in favor of quasi-isobaric cooling is that anhydrite displays prograde solubility in the quartz retrograde solubility field, which cannot account for the coeval dissolution of anhydrite and quartz (Figure 11). Therefore, it is inferred that fluid pressurization is seemingly the only viable way to elevate the solubility for both minerals.

Quartz and anhydrite show a similar solubility behavior at temperatures between 350 °C and 400 °C and pressures below 2000 bars, corresponding to a hydrostatic regime [92]. Under hydrostatic conditions, quartz and anhydrite deforms in a brittle fashion, which is consistent with early anhydrite breccia cemented by Anh4 (Figure 7h). The quartz micro-breccia enclosed in Qz5 suggests the occurrence of another episode of fluid overpressure. With the space created by brecciation, pressure fluctuated in response to fluid exsolution and mineral precipitation, resulting in the zoning patterns in Qz5b (Figure 11).

Preexisting veins can be reopened during a later fluid event by dissolution, mechanical breaking, brecciation, and recrystallization [17]. At Tongchang, these phenomena are abundant and occurred at different stages. Dissolution and recrystallization occurred in the early to transitional stage when host rock behaved in ductile fashion, whereas breaking and brecciation occurred in the late stage when host rocks behaved in a brittle fashion.

### 6.3. Vein Growth Via Reopening

Hydrothermal veins in porphyry Cu deposits are commonly grouped into early quartz (A-type), transitional molybdenite quartz (B-type), and late pyrite (D-type) veins
[93]. This model was later modified with the addition of several subordinate vein types, including early magnetite (M-type) [94], early biotitic (EB-type) [95], late chalcopyrite-sericite (C-type) [95,96](Dilles et al., 1992, and epithermal (E-type) veins [97]. Although widely used, the model faces challenges with regard to vein overprints [12].

The Tongchang porphyry deposit presents a good example of such challenges. According to their deposition temperatures, Qz1-2, Qz3 and Qz5 can be considered as indigenous quartz of A-, B-, and D- type veins [31]. Three fourths of the examined veins contain quartz that precipitated earlier or later than the vein formation defined by vein classification (Figure 12). Visual estimates suggested that the early A veins, except the A.V<sub>kq</sub> vein in 10DX197, contain younger quartz (Qz3 and Qz4) in volumes <50%. The B veins particularly involve the addition of younger Qz4 quartz to older quartz. For instance, the B.V<sub>macpq</sub> vein in 12DX328 comprises a central lining of pyrite, chalcopyrite, Qz4, Anh4 and carbonates, which is sandwiched by Qz1 and Qz2 quartz. Overprints in late veins are dramatic, and are characterized by the presence of earlier relict quartz (Qz1-3) and minor younger Qz6 quartz. Qz4 quartz are typically absent. D.V<sub>mqp</sub> is only different from D.V<sub>pd</sub> veins in that it has a larger amount of relict quartz.

<figure><img src="image_17.png" /></figure>

**Figure 12.** A qualitative estimation diagram of quartz types contained in A-type, B-type, and D-type veins examined in this study. All examined veins (17 in total) contained quartz younger or older than the vein formation, except two A-type veins. All vein contained early quartz (Qz1, Qz2a, and Qz2b), regardless of vein types. The presence of younger quartz in A-type veins indicates low-degree vein reopening, whereas the presence of older quartz in B-type and D-type veins indicates high-degree vein reopening. Note that there were two veins in the sample 12LDX37. The A.V<sub>hq</sub> vein is named as 12LDX37-1, and the B.V<sub>cpq</sub> vein is named 12LDX37-2.

A striking feature of the studied veins is that they all contain early quartz (Qz1-2), regardless of vein types. If these samples are representative of veining processes at Tongchang, it is plausible to infer that all the vein types are reopening early quartz-dominated veins. The present early veins are the product of slight overprints. The chalcopyrite veins (B.V<sub>cpq</sub> and B.V<sub>macpq</sub>) may be produced by the reopening of the earlier quartz veins by Qz4-depositing fluids, which is consistent with the conclusion of [31]. The late pyritic veins (D.V<sub>mqp</sub> and D.V<sub>pd</sub>) are products of overprints by Qz5-depositing fluids on earlier quartz veins.

## 6.4. Implications for Cu Sulfide Deposition
[93]. This model was later modified with the addition of several subordinate vein types, including early magnetite (M-type) [94], early biotitic (EB-type) [95], late chalcopyrite-sericite (C-type) [95,96](Dilles et al., 1992, and epithermal (E-type) veins [97]. Although widely used, the model faces challenges with regard to vein overprints [12].

The Tongchang porphyry deposit presents a good example of such challenges. According to their deposition temperatures, Qz1-2, Qz3 and Qz5 can be considered as indig'enous quartz of A-, B-, and D- type veins [31]. Three fourths of the examined veins contain quartz that precipitated earlier or later than the vein formation defined by vein classifica-tion (Figure 12). Visual estimates suggested that the early A veins, except the A.V<sub>kq</sub> vein in 10DX197, contain younger quartz (Qz3 and Qz4) in volumes <50%. The B veins partic-ularly involve the addition of younger Qz4 quartz to older quartz. For instance, the B.V<sub>macpq</sub> vein in 12DX328 comprises a central lining of pyrite, chalcopyrite, Qz4, Anh4 and carbonates, which is sandwiched by Qz1 and Qz2 quartz. Overprints in late veins are dra-matic, and are characterized by the presence of earlier relict quartz (Qz1-3) and minor younger Qz6 quartz. Qz4 quartz are typically absent. D.V<sub>mqp</sub> is only different from D.V<sub>pd</sub> veins in that it has a larger amount of relict quartz.

<figure><img src="image_17.png" /></figure>

**Figure 12.** A qualitative estimation diagram of quartz types contained in A-type, B-type, and D-type veins examined in this study. All examined veins (17 in total) contained quartz younger or older than the vein formation, except two A-type veins. All vein contained early quartz (Qz1, Qz2a, and Qz2b), regardless of vein types. The presence of younger quartz in A-type veins indicates low-degree vein reopening, whereas the presence of older quartz in B-type and D-type veins indicates high-degree vein reopening. Note that there were two veins in the sample 12LDX37. The A.Vhq vein is named as 12LDX37-1, and the B.Vcpq vein is named 12LDX37-2.

A striking feature of the studied veins is that they all contain early quartz (Qz1-2), regardless of vein types. If these samples are representative of veining processes at Tongchang, it is plausible to infer that all the vein types are reopening early quartz-dominated veins. The present early veins are the product of slight overprints. The chalcopyrite veins (B.Vcpq and B.Vmacpq) may be produced by the reopening of the earlier quartz veins by Qz4-depositing fluids, which is consistent with the conclusion of [31]. The late pyritic veins (D.Vmqp and D.Vpd) are products of overprints by Qz5-depositing fluids on earlier quartz veins.

## 6.4. Implications for Cu Sulfide Deposition
In the early fluid stage, hematite and anhydrite with little sulfide were deposited in the A.Vhq veins (Figure 13), attesting to oxidized sulfur species (SO₂, SO₄²⁻) at high temperatures [98,99]. In the potassic altered rocks, however, the low-sulfidation assemblage of chalcopyrite, bornite, magnetite and hematite developed [100]. These Fe-Cu sulfides were formed coevally with Qz1 and Qz2 at high temperatures (650 °C to 450 °C) (Figure 13), and the required H₂S was probably produced through the chemical reduction of sulfate in the fluids by mafic minerals such as biotite and hornblende [101]. It is worth mentioning that potassic ores of Tongchang are much less significant than in usual porphyry deposits [74], likely due to sulfide remobilization [1].

<figure><img src="image_18.png" /></figure>

**Figure 13.** A mineral to vein scale model illustrating hydrothermal alterations, veins, and vein reo-pening over four fluid stages encompassed in the Tongchang porphyry Cu deposit. It also summarizes the temporal evolution of P-T conditions and sulfide assemblages. Hem: hematite; Bn: bornite; Cpy: chalcopyrite; Mag: magnetite; Qz: quartz; Anh: anhydrite; Py: pyrite; Ten: tennantite; diss: disseminated.

The first overprint is characterized by the deposition of pyrite ± chalcopyrite in the Qz3-Anh2 veins and chlorite-sericite alterations (Figure 13). The disappearance of ferric iron oxides and the appearance of pyrite indicate an increase in the sulfidation state with continuous cooling [100]. The H₂S required for sulfide deposition is likely derived from the SO₂ disproportionation favored by fluid cooling (350 °C to 450 °C) [98]. The remobilization of early-stage sulfides might not be a significant source of H₂S because chalcopyrite solubility is significantly impeded during this process [102]. In the alteration halos, the precipitation of anhydrite (Anh2) occurred coevally with sulfide deposition and the hydrolysis of feldspars, indicating a potential chemisorption reaction between SO₂-bearing fluids and andesine [10].

Cu sulfides of the Tongchang deposit were mainly deposited in the vein assemblage of pyrite—chalcopyrite—Qz4—Anh4 at 300 °C–380 °C (Figure 13). The increased availability of Cu may be a result of the dissociation of CuCl₂⁻ complexes caused by fluid dilution in response to the entrainment of groundwaters and metamorphic fluids [103]. Another contributing factor might be the remobilization of existing sulfides associated with potassic alteration. Inflow of air saturated groundwater may significantly elevate the oxidation state and acidity of the magmatic fluids, which are favorable for chalcopyrite dissolution [102].
In the early fluid stage, hematite and anhydrite with little sulfide were deposited in the A.Vhq veins (Figure 13), attesting to oxidized sulfur species (SO₂, SO₄²⁻) at high temperatures [98,99]. In the potassic altered rocks, however, the low-sulfidation assemblage of chalcopyrite, bornite, magnetite and hematite developed [100]. These Fe-Cu sulfides were formed coevally with Qz1 and Qz2 at high temperatures (650 °C to 450 °C) (Figure 13), and the required H₂S was probably produced through the chemical reduction of sulfate in the fluids by mafic minerals such as biotite and hornblende [101]. It is worth mentioning that potassic ores of Tongchang are much less significant than in usual porphyry deposits [74], likely due to sulfide remobilization [1].

<figure><img src="image_18.png" /></figure>

**Figure 13.** A mineral to vein scale model illustrating hydrothermal alterations, veins, and vein reo-pening over four fluid stages encompassed in the Tongchang porphyry Cu deposit. It also summarizes the temporal evolution of P-T conditions and sulfide assemblages. Hem: hematite; Bn: bornite; Cpy: chalcopyrite; Mag: magnetite; Qz: quartz; Anh: anhydrite; Py: pyrite; Ten: tennantite; diss: disseminated.

The first overprint is characterized by the deposition of pyrite ± chalcopyrite in the Qz3-Anh2 veins and chlorite-sericite alterations (Figure 13). The disappearance of ferric iron oxides and the appearance of pyrite indicate an increase in the sulfidation state with continuous cooling [100]. The H₂S required for sulfide deposition is likely derived from the SO₂ disproportionation favored by fluid cooling (350 °C to 450 °C) [98]. The remobilization of early-stage sulfides might not be a significant source of H₂S because chalcopyrite solubility is significantly impeded during this process [102]. In the alteration halos, the precipitation of anhydrite (Anh2) occurred coevally with sulfide deposition and the hydrolysis of feldspars, indicating a potential chemisorption reaction between SO₂-bearing fluids and andesine [10].

Cu sulfides of the Tongchang deposit were mainly deposited in the vein assemblage of pyrite—chalcopyrite—Qz4—Anh4 at 300 °C–380 °C (Figure 13). The increased availability of Cu may be a result of the dissociation of CuCl₂⁻ complexes caused by fluid dilution in response to the entrainment of groundwaters and metamorphic fluids [103]. Another contributing factor might be the remobilization of existing sulfides associated with potassic alteration. Inflow of air saturated groundwater may significantly elevate the oxidation state and acidity of the magmatic fluids, which are favorable for chalcopyrite dissolution [102].
Although a large proportion of Cu sulfides are hosted in sericitic alteration zones, petrographic evidence of chalcopyrite inclusions and high-sulfidation assemblage of pyrite and tennantite indicates that they are remobilized from earlier ores (Figure 13). The mineral assemblage in the phyllic altered rocks reflects the stability of muscovite, quartz and pyrite, and the instability of chlorite, feldspars, mafic minerals, and chalcopyrite. This is similar to the Butte porphyry deposit, where the early ores (chalcopyrite-pyrite-magnetite) with potassic-chloritic alterations were remobilized by circulating oxidized groundwaters and re-deposited as chalcocite and covellite [104].

## 7. Conclusions

The Tongchang porphyry deposit represents a rare case of a porphyry copper deposit resulting from a single magmatic intrusion. It was expected that it would have undergone less fluid overprint compared to multi-intrusion counterparts. However, CL imaging of vein quartz and anhydrite revealed vein overprints as complicated (if not more complicated) as those in multi-intrusion deposits. This observation suggests that vein overprinting is likely an intrinsic property of porphyry deposits, regardless of intrusive history and other geological factors. The failure to recognize such vein overprints may result in erroneous fluid chronology and the incorrect interpretation of geochemical data (e.g., fluid inclusion and isotopes). Therefore, one should be careful when conducting geochemical analysis based on macroscopic features and a conventional vein model. Whenever possible, detailed CL imaging is an imperative.

As expected, the P-T history of Tongchang is characterized by an overall cooling and decompression trajectory. However, in contrast to monotonic cooling model, the P-T analysis of Tongchang porphyry deposit uncovered two significant episodes of fluid compression, likely corresponding to two periods of magmatic fluid accumulation under lithostatic and lithostatic to hydrostatic regimes. There might have been an increase in temperature during the second episode of compression. These irregularities in pressure should be considered for fluid models of porphyry deposits.

The Cu deposition process is better elucidated with the aid of CL petrography and integrated geothermometry. It was clearly shown that the high oxidation state of early high temperature fluids precludes Cu sulfide deposition in veins. However, Cu sulfide could be deposited via a chemical reaction with mafic minerals. The Cu sulfide deposition commences at temperatures lower than 450 °C when SO₂ disproportionation starts. Most chalcopyrite was precipitated at lower temperatures of 350 °C to 300 °C.

**Author Contributions:** X.L. and B.G.R. initiated the idea and work plan; X.L. performed the experiments; X.L., A.R., J.P. and B.G.R. interpreted the data; X.L. prepared the manuscript; A.R., J.P. and B.G.R. edited the manuscript. X.L. and J.P. acquired research funds. All authors have read and agreed to the published version of the manuscript.

**Funding:** This study was supported collectively by the National Natural Science Foundation of China (project N.O. 41402083), the China Scholarship Council (a visiting scholar fellowship granted to X.L.), and the Extra & Co project (Valorisation-Instituts Carnot n°ANR-15-CNRT-003).

**Informed Consent Statement:** Not applicable.

**Data Availability Statement:** All data generated or analyzed during this study are included in this published article and Appendix A.

**Acknowledgments:** Hongrui Fan, Fangfang Hu, Kuifeng Yang and Bojie Wen are acknowledged for their assistance with the fieldwork and sample preparation. Charles Wandler and Andreï Lecomte are thanked for their help during the SEM analyses. Kyle Mikkelsen and Tingguang Lan are acknowledged for their assistance during the LA-ICP-MS analyses. van Hoan Le assisted with the solubility curves construction. Two anonymous reviewers are sincerely thanked for their detailed reviews and comments.

**Conflicts of Interest:** The authors declare no conflict of interest.
Although a large proportion of Cu sulfides are hosted in sericitic alteration zones, petrographic evidence of chalcopyrite inclusions and high-sulfidation assemblage of pyrite and tennantite indicates that they are remobilized from earlier ores (Figure 13). The mineral assemblage in the phyllic altered rocks reflects the stability of muscovite, quartz and pyrite, and the instability of chlorite, feldspars, mafic minerals, and chalcopyrite. This is similar to the Butte porphyry deposit, where the early ores (chalcopyrite-pyrite-magnetite) with potassic-chloritic alterations were remobilized by circulating oxidized groundwaters and re-deposited as chalcocite and covellite [104].

## 7. Conclusions

The Tongchang porphyry deposit represents a rare case of a porphyry copper deposit resulting from a single magmatic intrusion. It was expected that it would have undergone less fluid overprint compared to multi-intrusion counterparts. However, CL imaging of vein quartz and anhydrite revealed vein overprints as complicated (if not more complicated) as those in multi-intrusion deposits. This observation suggests that vein overprinting is likely an intrinsic property of porphyry deposits, regardless of intrusive history and other geological factors. The failure to recognize such vein overprints may result in erroneous fluid chronology and the incorrect interpretation of geochemical data (e.g., fluid inclusion and isotopes). Therefore, one should be careful when conducting geochemical analysis based on macroscopic features and a conventional vein model. Whenever possible, detailed CL imaging is an imperative.

As expected, the P-T history of Tongchang is characterized by an overall cooling and decompression trajectory. However, in contrast to monotonic cooling model, the P-T analysis of Tongchang porphyry deposit uncovered two significant episodes of fluid compression, likely corresponding to two periods of magmatic fluid accumulation under lithostatic and lithostatic to hydrostatic regimes. There might have been an increase in temperature during the second episode of compression. These irregularities in pressure should be considered for fluid models of porphyry deposits.

The Cu deposition process is better elucidated with the aid of CL petrography and integrated geothermometry. It was clearly shown that the high oxidation state of early high temperature fluids precludes Cu sulfide deposition in veins. However, Cu sulfide could be deposited via a chemical reaction with mafic minerals. The Cu sulfide deposition commences at temperatures lower than 450 °C when SO₂ disproportionation starts. Most chalcopyrite was precipitated at lower temperatures of 350 °C to 300 °C.

**Author Contributions:** X.L. and B.G.R. initiated the idea and work plan; X.L. performed the experiments; X.L., A.R., J.P. and B.G.R. interpreted the data; X.L. prepared the manuscript; A.R., J.P. and B.G.R. edited the manuscript. X.L. and J.P. acquired research funds. All authors have read and agreed to the published version of the manuscript.

**Funding:** This study was supported collectively by the National Natural Science Foundation of China (project N.O. 41402083), the China Scholarship Council (a visiting scholar fellowship granted to X.L.), and the Extra & Co project (Valorisation-Instituts Carnot n°ANR-15-CNRT-003).

**Informed Consent Statement:** Not applicable.

**Data Availability Statement:** All data generated or analyzed during this study are included in this published article and Appendix A.

**Acknowledgments:** Hongrui Fan, Fangfang Hu, Kuifeng Yang and Bojie Wen are acknowledged for their assistance with the fieldwork and sample preparation. Charles Wandler and Andreï Lecomte are thanked for their help during the SEM analyses. Kyle Mikkelsen and Tingguang Lan are acknowledged for their assistance during the LA-ICP-MS analyses. van Hoan Le assisted with the solubility curves construction. Two anonymous reviewers are sincerely thanked for their detailed reviews and comments.

**Conflicts of Interest:** The authors declare no conflict of interest.
Appendix A

<figure><img src="image_19.png" /></figure>

**Figure A1.** Petrography of studied samples. Selected vein samples and photos of the thick sections. (a) 1- hematite quartz vein; 2- muscovite chlorite chalcopyrite pyrite quartz vein; 3- chunk of chlorite, hematite, sericite and muscovite; 4- large chunk of hematite; 5- feldspar replaced by sericite; 6- residue quartz; 7- groundmass containing disseminated chalcopyrite; 8- groundmass containing abundant hematite and chalcopyrite; 9- green aggregation consisting of chlorite and sericite; (b) 1- K-feldspar partly altered by muscovite and chlorite; 2- sericite - chlorite pseudomorph after plagioclase; 3- chunk of sericite, chlorite, muscovite, chalcopyrite and rutile; 4- chunk of chlorite, chalcopyrite and rutile; 5- chalcopyrite with pyrite inclusions; 6- chunk of rutile, chalcopyrite and muscovite; 7- muscovite - chlorite - rutile - quartz after biotite; 8- chunk of muscovite, chalcopyrite, pyrite and rutile; 9- chlorite (center) - sericite (rim) after feldspar; 10- chunk of chlorite and rutile; 11- chunk of pyrite, chlorite, rutile and epidote; 12- chunk of chlorite, rutile and calcite; (c) 1- altered porphyry by chlorite, sericite, rutile and pyrite; 2- anhydrite, epidote and chlorite; 3- carbonate vein; 4- anhydrite epidote veinlet; 5- chunk of molybdenite; 6- K-feldspar partly altered by sericite, chlorite and epidote; 7- sericite pseudomorph after K-feldspar; 8- pyrite crosscut by chalcopyrite veinlets; 9- dirty quartz with abundant fluid inclusions; 10- clear quartz; 11- anhydrite; (d) 1-fresh biotite; 2- biotite slightly altered by chlorite; 3- biotite slightly altered by quartz, sericite, chlorite, hematite and magnetite; 4- chunks of secondary biotite; 5- plagioclase slightly altered by sericite; 6- residue quartz with overgrowth; 7- sericite pseudomorph after feldspar; 8- groundmass of small quartz, sericite and chlorite; 9- vein quartz and anhydrite; (e) 1- quartz vein; 2- altered porphyry; 3- chlorite hematite calcite vein; 4- chlorite muscovite chalcopyrite pyrite vein; 5- chalcopyrite pyrite chlorite quartz veinlets; 6- biotite replaced by chlorite sericite chalcopyrite and rutile; 7- feldspar completely
Appendix A

<figure><img src="image_19.png" /></figure>

**Figure A1.** Petrography of studied samples. Selected vein samples and photos of the thick sections. (a) 1- hematite quartz vein; 2- muscovite chlorite chalcopyrite pyrite quartz vein; 3- chunk of chlorite, hematite, sericite and muscovite; 4- large chunk of hematite; 5- feldspar replaced by sericite; 6- residue quartz; 7- groundmass containing disseminated chalcopyrite; 8- groundmass containing abundant hematite and chalcopyrite; 9- green aggregation consisting of chlorite and sericite; (b) 1- K-feldspar partly altered by muscovite and chlorite; 2- sericite - chlorite pseudomorph after plagioclase; 3- chunk of sericite, chlorite, muscovite, chalcopyrite and rutile; 4- chunk of chlorite, chalcopyrite and rutile; 5- chalcopyrite with pyrite inclusions; 6- chunk of rutile, chalcopyrite and muscovite; 7- muscovite - chlorite - rutile - quartz after biotite; 8- chunk of muscovite, chalcopyrite, pyrite and rutile; 9- chlorite (center) - sericite (rim) after feldspar; 10- chunk of chlorite and rutile; 11- chunk of pyrite, chlorite, rutile and epidote; 12- chunk of chlorite, rutile and calcite; (c) 1- altered porphyry by chlorite, sericite, rutile and pyrite; 2- anhydrite, epidote and chlorite; 3- carbonate vein; 4- anhydrite epidote veinlet; 5- chunk of molybdenite; 6- K-feldspar partly altered by sericite, chlorite and epidote; 7- sericite pseudomorph after K-feldspar; 8- pyrite crosscut by chalcopyrite veinlets; 9- dirty quartz with abundant fluid inclusions; 10- clear quartz; 11- anhydrite; (d) 1-fresh biotite; 2- biotite slightly altered by chlorite; 3- biotite slightly altered by quartz, sericite, chlorite, hematite and magnetite; 4- chunks of secondary biotite; 5- plagioclase slightly altered by sericite; 6- residue quartz with overgrowth; 7- sericite pseudomorph after feldspar; 8- groundmass of small quartz, sericite and chlorite; 9- vein quartz and anhydrite; (e) 1- quartz vein; 2- altered porphyry; 3- chlorite hematite calcite vein; 4- chlorite muscovite chalcopyrite pyrite vein; 5- chalcopyrite pyrite chlorite quartz veinlets; 6- biotite replaced by chlorite sericite chalcopyrite and rutile; 7- feldspar completely
replaced by sericite and muscovite; (f) 1- slightly altered porphyry; 2- illitic chlorite - sericite altered porphyry; 3- sericite (rim)-chlorite (center) pseudomorph after feldspar; 4- chlorite-chalcopyrite pseudomorph after biotite; 5- sericite-rutile pseudomorph after biotite; 6- chunk of chalcopyrite, muscovite and anhydrite; 7- residue anhydrite; 8- anhydrite chalcopyrite veinlet; 9- anhydrite chalcopyrite pyrite vein; 10- chalcopyrite veinlet; (g) 1- slightly altered porphyry; 2- sericitic altered porphyry; 3- residue quartz; 4- chunk of muscovite and pyrite; 5- pyrite, muscovite and rutile pseudomorph after biotite; 6- muscovite, rutile, quartz and pyrite pseudomorph after biotite; 7- vein pyrite crosscut by carbonate veinlets; 8- quartz, muscovite, molybdenite, rutile layer; 9- fine-grained quartz and large muscovite in equal amount; (h) 1- silicified phyllite with oriented sericite, quartz and rutile; 2- pyrite quartz vein; 3- pyrite dominated vein; 4- aggregation of chlorite; 5- aggregation of quartz. Areas mapped with SEM-CL are also shown.

<figure><img src="image_20.png" /><figcaption>**Figure A2.** Tukey Boxplot of trace elements in vein quartz of the Tongchang porphyry Cu deposit.</figcaption></figure>

## References

1. Sillitoe, R.H. Porphyry copper systems. *Econ. Geol.* **2010**, *105*, 3–41.

2. Michaux, S.P. Assessment of the Extra Capacity Required of Alternative Energy Electrical Power Systems to Completely Replace Fossil Fuels. Geological Survey of Finland (GTK) Open Report 42. 2021. Available online: https://tupa.gtk.fi/raportti/arkisto/42_2021.pdf (accessed on 29 March 2022).

3. Hedenquist, J.W.; Lowenstern, J.B. The role of magmas in the formation of hydrothermal ore deposits. *Nature* **1994**, *370*, 519.
replaced by sericite and muscovite; (f) 1- slightly altered porphyry; 2- illitic chlorite - sericite altered porphyry; 3- sericite (rim)-chlorite (center) pseudomorph after feldspar; 4- chlorite-chalcopyrite pseudomorph after biotite; 5- sericite-rutile pseudomorph after biotite; 6- chunk of chalcopyrite, muscovite and anhydrite; 7- residue anhydrite; 8- anhydrite chalcopyrite veinlet; 9- anhydrite chalcopyrite pyrite vein; 10- chalcopyrite veinlet; (g) 1- slightly altered porphyry; 2- sericitic altered porphyry; 3- residue quartz; 4- chunk of muscovite and pyrite; 5- pyrite, muscovite and rutile pseudomorph after biotite; 6- muscovite, rutile, quartz and pyrite pseudomorph after biotite; 7- vein pyrite crosscut by carbonate veinlets; 8- quartz, muscovite, molybdenite, rutile layer; 9- fine-grained quartz and large muscovite in equal amount; (h) 1- silicified phyllite with oriented sericite, quartz and rutile; 2- pyrite quartz vein; 3- pyrite dominated vein; 4- aggregation of chlorite; 5- aggregation of quartz. Areas mapped with SEM-CL are also shown.

<figure><img src="image_20.png" /><figcaption>**Figure A2.** Tukey Boxplot of trace elements in vein quartz of the Tongchang porphyry Cu deposit.</figcaption></figure>

## References

1. Sillitoe, R.H. Porphyry copper systems. *Econ. Geol.* **2010**, *105*, 3–41.

2. Michaux, S.P. Assessment of the Extra Capacity Required of Alternative Energy Electrical Power Systems to Completely Replace Fossil Fuels. Geological Survey of Finland (GTK) Open Report 42. 2021. Available online: https://tupa.gtk.fi/raportti/arkisto/42_2021.pdf (accessed on 29 March 2022).

3. Hedenquist, J.W.; Lowenstern, J.B. The role of magmas in the formation of hydrothermal ore deposits. *Nature* **1994**, *370*, 519.
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15. Qiu, K.F.; Deng, J.; Yu, H.C.; Wu, M.Q.; Wang, Y.; Zhang, L.; Goldfarb, R. Identifying hydrothermal quartz vein generations in the Taiyangshan porphyry Cu-Mo deposit (West Qinling, China) using cathodoluminescence, trace element geochemistry, and fluid inclusions. *Ore Geol. Rev.* **2021**, *128*, 103882.

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21. Götze, J.; Pan, Y.; Müller, A. Mineralogy and mineral chemistry of quartz: A review. *Miner. Mag.* **2021**, *85*, 639–664.

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32. Wei, Q.; Fan, H.; Pironon, J.; Liu, X. Auriferous Quartz Veining Due to CO₂ Content Variations and Decompressional Cooling, Revealed by Quartz Solubility, SEM-CL and Fluid Inclusion Analyses (The Linglong Goldfield, Jiaodong). *Minerals* **2020**, *10*, 417.

33. Cloos, M. Bubbling magma chambers, cupolas, and porphyry copper deposits. *Int. Geol. Rev.* **2001**, *43*, 285–311.
4. Richards, J.P. Magmatic to hydrothermal metal fluxes in convergent and collided margins. Ore Geology Reviews, **2011**, *40*, 1–26.

5. Richards, J.P. Giant ore deposits formed by optimal alignments and combinations of geological processes. *Nat. Geosci.* **2013**, *6*, 911–916.

6. Vigneresse, J.-L.; Ballouard, C.; Liu, X.; Richard, A. Toward a global conceptual model for metal enrichment in felsic, mafic-ultramafic, and alkaline-carbonatitic magmas. *Ore Geol. Rev.* **2020**, *129*, 103925.

7. Vigneresse, J.-L.; Truche, L.; Richard, A. How do metals escape from magmas to form porphyry-type ore deposits? *Ore Geol. Rev.* **2018**, *105*, 310–336.

8. Seedorff, E.; Dilles, J.H.; Proffett, J.M.; Einaudi, M.T. Porphyry deposits: Characteristics and origin of hypogene features. *Econ. Geol.* **100th Anniv. Vol.** 2005, 251-298.

9. Blundy, J.; Mavrogenes, J.; Tattitch, B.; Sparks, S.; Gilmer, A. Generation of porphyry copper deposits by gas-brine reaction in volcanic arcs. *Nat. Geosci.* **2015**, *8*, nge02351.

10. Henley, R.W.; King, P.L.; Wykes, J.L.; Renggli, C.J.; Brink, F.J.; Clark, D.A.; Troitzsch. Porphyry copper deposit formation by sub-volcanic sulphur dioxide flux and chemisorption. *Nat. Geosci.* **2015**, *8*, 210–215.

11. Wilkinson, J.J. Triggers for the formation of porphyry ore deposits in magmatic arcs. *Nat. Geosci.* **2013**, *6*, 917–925.

12. Bennett, M.M. Cathodoluminescence and Fluid Inclusion Characteristics of Hydrothermal Quartz from Porphyry Deposits. Doctoral Dissertation, Colorado School of Mines, Arthur Lakes Library, Colorado, USA, 2014.

13. Landtwing, M.R.; Pettke, T.; Halter, W.E.; Heinrich, C.A.; Redmond, P.B.; Einaudi, M.T.; Kunze, K. Copper deposition during quartz dissolution by cooling magmatic-hydrothermal fluids: The Bingham porphyry. *Earth Planet. Sci. Lett.* **2005**, *235*, 229–243.

14. Landtwing, M.R.; Furrer, C.; Redmond, P.B.; Pettke, T.; Guillong, M.; Heinrich, C.A. The Bingham Canyon Porphyry Cu-Mo-Au Deposit. III. Zoned Copper-Gold Ore Deposition by Magmatic Vapor Expansion. *Econ. Geol.* **2010**, *105*, 91–118.

15. Qiu, K.F.; Deng, J.; Yu, H.C.; Wu, M.Q.; Wang, Y.; Zhang, L.; Goldfarb, R. Identifying hydrothermal quartz vein generations in the Taiyangshan porphyry Cu-Mo deposit (West Qinling, China) using cathodoluminescence, trace element geochemistry, and fluid inclusions. *Ore Geol. Rev.* **2021**, *128*, 103882.

16. Redmond, P.B.; Einaudi, M.T.; Inan, E.E.; Landtwing, M.R.; Heinrich, C.A. Copper deposition by fluid cooling in intrusion-centered systems: New insights from the Bingham porphyry ore deposit, Utah. *Geology* **2004**, *32*, 217–220.

17. Rusk, B.; Reed, M. Scanning electron microscope—Cathodoluminescence analysis of quartz reveals complex growth histories in veins from the Butte porphyry copper deposit, Montana. *Geology* **2002**, *30*, 727–730.

18. Frelinger, S.N.; Ledvina, M.D.; Kyle, J.R.; Zhao, D. Scanning electron microscopy cathodoluminescence of quartz: Principles, techniques and applications in ore geology. *Ore Geol. Rev.* **2015**, *65*, 840–852.

19. Liu, X.; Fan, H.R.; Hu, F.F.; Yang, K.F.; Wen, B.J. Nature and evolution of the ore-forming fluids in the giant Dexing porphyry Cu-Mo-Au deposit, Southeastern China. *J. Geochem. Explor.* **2016**, *171*, 83–95.

20. Hou, Z.; Pan, X.; Li, Q.; Yang, Z.; Song, Y. The giant Dexing porphyry Cu–Mo–Au deposit in east China: Product of melting of juvenile lower crust in an intracontinental setting. *Miner. Deposta* **2013**, *48*, 1019–1045.

21. Götze, J.; Pan, Y.; Müller, A. Mineralogy and mineral chemistry of quartz: A review. *Miner. Mag.* **2021**, *85*, 639–664.

22. Acosta, M.D.; Reed, M.H.; Watkins, J.M. Quartz Vein Formation and Deformation during Porphyry Cu Deposit Formation: A Microstructural and Geochemical Analysis of the Butte, Montana, Ore Deposit. *Lithosphere* **2022**, 2022, 3196601.

23. Huang, R.; Audétat, A. The titanium-in-quartz (TitaniQ) thermobarometer: A critical examination and re-calibration. *Geochim. Cosmochim. Acta* **2012**, *84*, 75–89.

24. Maydagán, L.; Franchini, M.; Rusk, B.; Lentz, D.R.; McFarlane, C.; Impiccini, A.; Ríos, F.J.; Rey, R. Porphyry to epithermal transition in the altar Cu-(Au-Mo) deposit, Argentina, studied by cathodoluminescence, LA-ICP-MS, and fluid inclusion analysis. *Econ. Geol.* **2015**, *110*, 889–923.

25. Mao, W.; Rusk, B.; Yang, F.; Zhang, M. Physical and Chemical Evolution of the Dabaoshan Porphyry Mo Deposit, South China: Insights from Fluid Inclusions, Cathodoluminescence, and Trace Elements in Quartz. *Econ. Geol.* **2017**, *112*, 889–918.

26. Thomas, J.B.; Watson, E.B.; Spear, F.S.; Shemella, P.T.; Nayak, S.K.; Lanzirrotti, A. TitaniQ under pressure: The effect of pressure and temperature on the solubility of Ti in quartz. *Contrib. Mineral. Petrol.* **2010**, *160*, 743–759.

27. Wark, D.A.; Watson, E.B. TitaniQ: A titanium-in-quartz geothermometer. *Contrib. Mineral. Petrol.* **2006**, *152*, 743–754.

28. Boiron, M.C.; Essarraj, S.; Cathelineau, L.P. Identification of fluid inclusions in relation to their host microstructural domains in quartz by cathodoluminescence. *Geochim. Cosmochim. Acta* **1992**, *56*, 175–185.

29. Ni, P.; Pan, J.Y.; Wang, G.G.; Chi, Z.; Qin, H.; Ding, J.Y.; Chen, H. A CO₂-rich porphyry ore-forming fluid system constrained from a combined cathodoluminescence imaging and fluid inclusion studies of quartz veins from the Tongcun Mo deposit, South China. *Ore Geol. Rev.* **2017**, *81*, 856–870.

30. Van den Kerkhof, A.M.; Hein, U.F. Fluid inclusion petrography. *Lithos* **2001**, *55*, 27–47.

31. Monecke, T.; Monecke, J.; Reynolds, T.J.; Tsuruoka, S.; Bennett, M.M.; Skewes, W.B.; Palin, R.M. Quartz solubility in the H₂O-NaCl system: A framework for understanding vein formation in porphyry copper deposits. *Econ. Geol.* **2018**, *113*, 1007–1046.

32. Wei, Q.; Fan, H.; Pironon, J.; Liu, X. Auriferous Quartz Veining Due to CO₂ Content Variations and Decompressional Cooling, Revealed by Quartz Solubility, SEM-CL and Fluid Inclusion Analyses (The Linglong Goldfield, Jiaodong). *Minerals* **2020**, *10*, 417.

33. Cloos, M. Bubbling magma chambers, cupolas, and porphyry copper deposits. *Int. Geol. Rev.* **2001**, *43*, 285–311.
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36. Gilder, S.A.; Gill, J.; Coe, R.S.; Zhao, X.; Liu, Z.; Wang, G.; Yuan, K.; Liu, W.; Kuang, G.; Wu, H. Isotopic and paleomagnetic constraints on the Mesozoic tectonic evolution of south China. *Journal of Geophysical Research. Solid Earth* **1996**, *101*, 16137–16154.

37. Zhao, G.; Cawood, P.A. Precambrian geology of China. *Precambrian Res.* **2012**, 222-223, 13–54.

38. Liu, X.; Fan, H.R.; Santosh, M.; Hu, F.F.; Yang, K.F.; Li, Q.L.; Yang, Y.H.; Liu, Y. Remelting of Neoproterozoic relict volcanic arcs in the Middle Jurassic: Implication for the formation of the Dexing porphyry copper deposit, Southeastern China. *Lithos* **2012**, *150*, 85–100.

39. Liu, X.; Fan, H.R.; Santosh, M.; Hu, F.F.; Yang, K.F.; Wen, B.J.; Yang, Y.H.; Liu, Y. Origin of the Yinshan epithermal-porphyry Cu-Au-Pb-Zn-Ag deposit, southeastern China: Insights from geochemistry, Sr-Nd and zircon U-Pb-Hf-O isotopes. *International Geology Review*, **2013**, *55*, 1835–1864.

40. Charvet, J. The neoproterozoic–early paleozoic tectonic evolution of the South China Block: An overview. *J. Asian Earth Sci.* **2013**, *74*, 198–209.

41. Wang, X.-L.; Zhou, J.-C.; Griffin, W.; Zhao, G.; Yu, J.-H.; Qiu, J.-S.; Zhang, Y.-J.; Xing, G.-F. Geochemical zonation across a Neoproterozoic orogenic belt: Isotopic evidence from granitoids and metasedimentary rocks of the Jiangnan orogen, China. *Precambrian Res.* **2014**, *242*, 154–171.

42. Yao, J.; Shu, L.; Cawood, P.A.; Zhao, G. Differentiating continental and oceanic arc systems and retro-arc basins in the Jiangnan orogenic belt, South China. *Geol. Mag.* **2019**, *156*, 2001–2016.

43. Li, X.H.; Li, W.X.; Li, Z.X.; Lo, C.H.; Wang, J.; Ye, M.F.; Yang, Y.H. Amalgamation between the Yangtze and Cathaysia Blocks in South China: Constraints from SHRIMP U-Pb zircon ages, geochemistry and Nd-Hf isotopes of the Shuangxiwu volcanic rocks. *Precambrian Res.* **2009**, *174*, 117–128.

44. Charvet, J.; Shu, L.; Shi, Y.; Guo, L.; Faure, M. The building of south China: Collision of Yangzi and Cathaysia blocks, problems and tentative answers. *J. Southeast Asian Earth Sci.* **1996**, *13*, 223–235.

45. Yang, C.; Li, X.H.; Wang, X.C.; Lan, Z. Mid-Neoproterozoic angular unconformity in the Yangtze Block revisited: Insights from detrital zircon U-Pb age and Hf-O isotopes. *Precambrian Res.* **2015**, *266*, 165–178.

46. Wang, X.-L.; Zhao, G.; Zhou, J.-C.; Liu, Y.; Hu, J. Geochronology and Hf isotopes of zircon from volcanic rocks of the Shuangqiaoshan Group, South China: Implications for the Neoproterozoic tectonic evolution of the eastern Jiangnan orogen. *Gondwana Res.* **2008**, *14*, 355–367.

47. Xia, Y.; Xu, X. A Fragment of Columbia Supercontinent: Insight for Cathaysia Block Basement From Tectono-Magmatic Evolution and Mantle Heterogeneity. *Geophys. Res. Lett.* **2019**, *46*, 2012–2024.

48. Wang, Y.; Zhang, A.; Cawood, P.A.; Fan, W.; Xu, J.; Zhang, G.; Zhang, Y. Geochronological, geochemical and Nd-Hf-Os isotopic fingerprinting of an early Neoproterozoic arc-back-arc system in South China and its accretionary assembly along the margin of Rodinia. *Precambrian Res.* **2013b**, *231*, 343–371.

49. Zheng, J.; Griffin, W.; Li, L.; O'Reilly, S.Y.; Pearson, N.; Tang, H.; Liu, G.; Zhao, J.; Yu, C.; Su, Y. Highly evolved Archean basement beneath the western Cathaysia Block, South China. *Geochim. Cosmochim. Acta* **2010**, *75*, 242–255.

50. Li, Z.; Li, X.; Kinny, P.; Wang, J.; Zhang, S.; Zhou, H. Geochronology of Neoproterozoic syn-rift magmatism in the Yangtze Craton, South China and correlations with other continents: Evidence for a mantle superplume that broke up Rodinia. *Precambrian Res.* **2003**, *122*, 85–109.

51. Zhao, G. Jiangnan Orogen in South China: Developing from divergent double subduction. *Gondwana Res.* **2015**, *27*, 1173–1180.

52. Shu, L.; Faure, M.; Wang, B.; Zhou, X.; Song, B. Late Palaeozoic–Early Mesozoic geological features of South China: Response to the Indosinian collision events in Southeast Asia. *Comptes Rendus Geosci.* **2008**, *340*, 151–165.

53. Zhou, X.; Sun, T.; Shen, W.; Shu, L.; Niu, Y. Petrogenesis of Mesozoic granitoids and volcanic rocks in South China: A response to tectonic evolution. *Episodes* **2006**, *29*, 26–33.

54. Mao, J.W.; Chen, Y.B.; Chen, M.H.; Pirajno, F. Major types and time-space distribution of Mesozoic ore deposits in South China and their geodynamic settings. *Miner. Depos.* **2013**, *48*, 267–294.

55. Chu, Y.; Faure, M.; Lin, W.; Wang, Q. Early Mesozoic tectonics of the South China block: Insights from the Xuefengshan intracontinental orogen. *J. Asian Earth Sci.* **2012**, *61*, 199–220.

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35. Cawood, P.A.; Zhao, G.; Yao, J.; Wang, W.; Xu, Y.; Wang, Y. Reconstructing South China in phanerozoic and precambrian supercontinents. *Earth-Sci. Rev.* **2018**, *186*, 173–194.

36. Gilder, S.A.; Gill, J.; Coe, R.S.; Zhao, X.; Liu, Z.; Wang, G.; Yuan, K.; Liu, W.; Kuang, G.; Wu, H. Isotopic and paleomagnetic constraints on the Mesozoic tectonic evolution of south China. *Journal of Geophysical Research. Solid Earth* **1996**, *101*, 16137–16154.

37. Zhao, G.; Cawood, P.A. Precambrian geology of China. *Precambrian Res.* **2012**, 222-223, 13–54.

38. Liu, X.; Fan, H.R.; Santosh, M.; Hu, F.F.; Yang, K.F.; Li, Q.L.; Yang, Y.H.; Liu, Y. Remelting of Neoproterozoic relict volcanic arcs in the Middle Jurassic: Implication for the formation of the Dexing porphyry copper deposit, Southeastern China. *Lithos* **2012**, *150*, 85–100.

39. Liu, X.; Fan, H.R.; Santosh, M.; Hu, F.F.; Yang, K.F.; Wen, B.J.; Yang, Y.H.; Liu, Y. Origin of the Yinshan epithermal-porphyry Cu-Au-Pb-Zn-Ag deposit, southeastern China: Insights from geochemistry, Sr-Nd and zircon U-Pb-Hf-O isotopes. *International Geology Review*, **2013**, *55*, 1835–1864.

40. Charvet, J. The neoproterozoic–early paleozoic tectonic evolution of the South China Block: An overview. *J. Asian Earth Sci.* **2013**, *74*, 198–209.

41. Wang, X.-L.; Zhou, J.-C.; Griffin, W.; Zhao, G.; Yu, J.-H.; Qiu, J.-S.; Zhang, Y.-J.; Xing, G.-F. Geochemical zonation across a Neoproterozoic orogenic belt: Isotopic evidence from granitoids and metasedimentary rocks of the Jiangnan orogen, China. *Precambrian Res.* **2014**, *242*, 154–171.

42. Yao, J.; Shu, L.; Cawood, P.A.; Zhao, G. Differentiating continental and oceanic arc systems and retro-arc basins in the Jiangnan orogenic belt, South China. *Geol. Mag.* **2019**, *156*, 2001–2016.

43. Li, X.H.; Li, W.X.; Li, Z.X.; Lo, C.H.; Wang, J.; Ye, M.F.; Yang, Y.H. Amalgamation between the Yangtze and Cathaysia Blocks in South China: Constraints from SHRIMP U-Pb zircon ages, geochemistry and Nd-Hf isotopes of the Shuangxiwu volcanic rocks. *Precambrian Res.* **2009**, *174*, 117–128.

44. Charvet, J.; Shu, L.; Shi, Y.; Guo, L.; Faure, M. The building of south China: Collision of Yangzi and Cathaysia blocks, problems and tentative answers. *J. Southeast Asian Earth Sci.* **1996**, *13*, 223–235.

45. Yang, C.; Li, X.H.; Wang, X.C.; Lan, Z. Mid-Neoproterozoic angular unconformity in the Yangtze Block revisited: Insights from detrital zircon U-Pb age and Hf-O isotopes. *Precambrian Res.* **2015**, *266*, 165–178.

46. Wang, X.-L.; Zhao, G.; Zhou, J.-C.; Liu, Y.; Hu, J. Geochronology and Hf isotopes of zircon from volcanic rocks of the Shuangqiaoshan Group, South China: Implications for the Neoproterozoic tectonic evolution of the eastern Jiangnan orogen. *Gondwana Res.* **2008**, *14*, 355–367.

47. Xia, Y.; Xu, X. A Fragment of Columbia Supercontinent: Insight for Cathaysia Block Basement From Tectono-Magmatic Evolution and Mantle Heterogeneity. *Geophys. Res. Lett.* **2019**, *46*, 2012–2024.

48. Wang, Y.; Zhang, A.; Cawood, P.A.; Fan, W.; Xu, J.; Zhang, G.; Zhang, Y. Geochronological, geochemical and Nd-Hf-Os isotopic fingerprinting of an early Neoproterozoic arc-back-arc system in South China and its accretionary assembly along the margin of Rodinia. *Precambrian Res.* **2013b**, *231*, 343–371.

49. Zheng, J.; Griffin, W.; Li, L.; O'Reilly, S.Y.; Pearson, N.; Tang, H.; Liu, G.; Zhao, J.; Yu, C.; Su, Y. Highly evolved Archean basement beneath the western Cathaysia Block, South China. *Geochim. Cosmochim. Acta* **2010**, *75*, 242–255.

50. Li, Z.; Li, X.; Kinny, P.; Wang, J.; Zhang, S.; Zhou, H. Geochronology of Neoproterozoic syn-rift magmatism in the Yangtze Craton, South China and correlations with other continents: Evidence for a mantle superplume that broke up Rodinia. *Precambrian Res.* **2003**, *122*, 85–109.

51. Zhao, G. Jiangnan Orogen in South China: Developing from divergent double subduction. *Gondwana Res.* **2015**, *27*, 1173–1180.

52. Shu, L.; Faure, M.; Wang, B.; Zhou, X.; Song, B. Late Palaeozoic–Early Mesozoic geological features of South China: Response to the Indosinian collision events in Southeast Asia. *Comptes Rendus Geosci.* **2008**, *340*, 151–165.

53. Zhou, X.; Sun, T.; Shen, W.; Shu, L.; Niu, Y. Petrogenesis of Mesozoic granitoids and volcanic rocks in South China: A response to tectonic evolution. *Episodes* **2006**, *29*, 26–33.

54. Mao, J.W.; Chen, Y.B.; Chen, M.H.; Pirajno, F. Major types and time-space distribution of Mesozoic ore deposits in South China and their geodynamic settings. *Miner. Depos.* **2013**, *48*, 267–294.

55. Chu, Y.; Faure, M.; Lin, W.; Wang, Q. Early Mesozoic tectonics of the South China block: Insights from the Xuefengshan intracontinental orogen. *J. Asian Earth Sci.* **2012**, *61*, 199–220.

56. Dong, S.; Zhang, Y.; Zhang, F.; Cui, J.; Chen, X.; Zhang, S.; Miao, L.; Li, J.; Shi, W.; Li, Z.; et al. Late Jurassic–Early Cretaceous continental convergence and intracontinental orogenesis in East Asia: A synthesis of the Yanshan Revolution. *J. Asian Earth Sci.* **2015**, *114*, 750–770.

57. Faure, M.; Lin, W.; Chu, Y.; Lepvrier, C. Triassic tectonics of the southern margin of the South China Block. *Comptes Rendus Geosci.* **2016**, *348*, 5–14.

58. Ji, W.; Faure, M.; Lin, W.; Chen, Y.; Chu, Y.; Xue, Z. Multiple Emplacement and Exhumation History of the Late Mesozoic Dayunshan-Mufushan Batholith in Southeast China and Its Tectonic Significance: 1. Structural Analysis and Geochronological Constraints. *J. Geophys. Res. Solid Earth* **2018**, *123*, 689–710.
59. Li, Z.X.; Li, X.H.; Chung, S.L.; Lo, C.H.; Xu, X.; Li, W.X. Magmatic switch-on and switch-off along the South China continental margin since the Permian: Transition from an Andean-type to a Western Pacific-type plate boundary. *Tectonophysics* **2012**, *532*, 271–290.

60. Li, J.; Dong, S.; Cawood, P.A.; Zhao, G.; Johnston, S.T.; Zhang, Y.; Xin, Y. An Andean-type retro-arc foreland system beneath northwest South China revealed by SINOPROBE profiling. *Earth Planet. Sci. Lett.* **2018**, *490*, 170–179.

61. Xu, C.; Zhang, L.; Shi, H.; Brix, M.R.; Huhma, H.; Chen, L.; Zhang, M.; Zhou, Z. Tracing an Early Jurassic magmatic arc from South to East China Seas. *Tectonics* **2017**, *36*, 466–492.

62. Yui, T.F.; Chu, H.T.; Suga, K.; Lan, C.Y.; Chung, S.H.; Wang, K.L.; Grove, M. Subduction-related 200 Ma Talun metagranite, SE Taiwan: An age constraint for palaeo-Pacific plate subduction beneath South China Block during the Mesozoic. *Int. Geol. Rev.* **2016**, *59*, 333–334.

63. Wang, Q.; Xu, J.-F.; Jian, P.; Bao, Z.-W.; Zhao, Z.-H.; Li, C.-F.; Xiong, X.-L.; Ma, J.-L. Petrogenesis of Adakitic Porphyries in an Extensional Tectonic Setting, Dexing, South China: Implications for the Genesis of Porphyry Copper Mineralization. *J. Pet. 2006*, *47*, 119–144.

64. Liu, X.; Fan, H.-R.; Evans, N.J.; Batt, G.E.; McInnes, B.I.A.; Yang, K.-F.; Qin, K.-Z. Cooling and exhumation of the mid-Jurassic porphyry copper systems in Dexing City, SE China: Insights from geo- and thermochronology. *Miner. Deposita* **2014**, *49*, 809–819.

65. Zhou, Q.; Jiang, Y.H.; Liao, S.Y.; Zhao, P.; Jin, G.D.; Jia, R.Y.; Liu, Z.; Xu, S.M. SHRIMP zircon U-Pb dating and Hf isotope studies of the diorite porphyrite from the Dexing copper deposit. *Acta Geol. Sin.* **2012**, *86*, 1726–1734. (In Chinese with English Abstract).

66. Gao, F.Z. Alteration of Dexing porphyry copper (molybdenum). *Shanghai Geol. 1992*, *2*, 24–35. (In Chinese with English abstract).

67. Pan, X.F.; Song, Y.C.; Wang, S.X.; Li, Z.Q.; Yang, Z.M.; Hou, Z.Q. Evolution of hydrothermal fluid of Dexing Tongchang copper-gold porphyry deposit. *Acta Geol. Sin.* **2009**, *12*, 1929–1950. (In Chinese with English abstract).

68. Rui, Z.Y.; Huang, C.K.; Qi, G.M.; Xu, Y.; Zhang, H.T. Porphyry Copper (Molybdenite) Deposits of China; Geological Publishing House: Beijing, China, 1984; pp. 242–252 (in Chinese with English abstract).

69. Jochum, K.P.; Weis, U.; Stoll, B.; Kuzmin, D.; Yang, Q.; Raczek, I.; Jacob, D.E.; Stracke, A.; Birbaum, K.; Frick, D.A.; et al. Determination of Reference Values for NIST SRM 610-617 Glasses Following ISO Guidelines. *Geostand. Geoanalytical Res.* **2011**, *35*, 397–429.

70. Audôtat, A.; Garbe-Schönberg, D.; Kronz, A.; Pettke, T.; Rusk, B.; Donovan, J.J.; Lowers, H.A. Characterisation of a natural quartz crystal as a reference material for microanalytical determination of Ti, Al, Li, Fe, Mn, Ga and Ge. *Geostand. Geoanalytical Res.* **2015**, *39*, 171–184.

71. Liu, Y.; Hu, Z.; Gao, S.; Günther, D.; Xu, J.; Gao, C.; Chen, H. In situ analysis of major and trace elements of anhydrous minerals by LA-ICP-MS without applying an internal standard. *Chem. Geol.* **2008**, *257*, 34–43.

72. Roedder, E. Fluid inclusions. *Rev. Mineral.* **1984**, *12*, 11-16.

73. Steele-MacInnis, M.; Lecumberri-Sanchez, P.; Bodnar, R.J. HokieFlincs_H₂O-NaCl: A Microsoft Excel spreadsheet for interpreting microthermometric data from fluid inclusions based on the PVTX properties of H₂O-NaCl. *Comput. Geosci.* **2012**, *49*, 334–337.

74. Rusk, B.G.; Reed, M.H.; Dilles, J.H. Fluid Inclusion Evidence for Magmatic-Hydrothermal Fluid Evolution in the Porphyry Copper-Molybdenum Deposit at Butte, Montana. *Econ. Geol.* **2008**, *103*, 307–334.

75. Ostapenko, G.T.; Tarashchan, A.N.; Mitsyuk, B.M. Rutile-quartz geothermobarometer. *Geochem. Int.* **2007**, *45*, 506–508.

76. Thomas, J.B.; Watson, E.B.; Spear, F.S.; Wark, D.A. TitaniQ recrystallized: Experimental confirmation of the original Ti-in-quartz calibrations. *Contrib. Mineral. Petrol.* **2015**, *169*, 27.

77. Acosta, M.D. Titanium in Quartz during Growth and Deformation under Hydrothermal-Magmatic Conditions. Doctoral Dissertation, University of Oregon, Eugene, OR, USA, 2020.

78. Raimbourg, H.; Famin, V.; Canizarès, A.; Le Trong, E. Fluid pressure changes recorded by trace elements in quartz. *Geochem. Geophys. Geosystems* **2022**, *23*, e2022GC010346.

79. Rusk, B.; Reed, M.; Bignall, G.; Tsuchiya, N. Natural and synthetic quartz growth and dissolution revealed by scanning electron microscope cathodoluminescence. In Proceedings of the 14th International Conference on the Properties of Water and Steam, Kyoto, Japan, 29 August–3 September 2004.

80. Rusk, B. Cathodoluminescent Textures and Trace Elements in Hydrothermal Quartz. In *Quartz: Deposits, Mineralogy and Análtyics*; Springer Geology: Berlin/Heidelberg, Germany, 2012; pp. 307–329.

81. Vasyukova, O.V.; Kamenetsky, V.S.; Goemann, K.; Davidson, P. Diversity of primary CL textures in quartz from porphyry environments: Implication for origin of quartz eyes. *Contrib. Miner. Pet.* **2013**, *166*, 1253–1268.

82. Monnier, L.; Lach, P.; Salvi, S.; Melleton, J.; Bailly, L.; Béziat, D.; Monnier, Y.; Gouy, S. Quartz trace-element composition by LA-ICP-MS as proxy for granite differentiation, hydrothermal episodes, and related mineralization: The Beauvoir Granite (Echassières district), France. *Lithos* **2018**, *320*, 355–377.

83. Tanner, D.; Henley, R.W.; Mavrogenes, J.A.; Holden, P. Combining in situ isotopic, trace element and textural analyses of quartz from four magmatic-hydrothermal ore deposits. *Contrib. Mineral. Petrol.* **2013**, *166*, 1119–1142.

84. Li, X.-H.; Klyukin, Y.; Steele-MacInnis, M.; Fan, H.-R.; Yang, K.-F.; Zoheir, B. Phase equilibria, thermodynamic properties, and solubility of quartz in saline-aqueous-carbonic fluids: Application to orogenic and intrusion-related gold deposits. *Geochim. Cosmochim. Acta* **2020**, *283*, 201–221.
59. Li, Z.X.; Li, X.H.; Chung, S.L.; Lo, C.H.; Xu, X.; Li, W.X. Magmatic switch-on and switch-off along the South China continental margin since the Permian: Transition from an Andean-type to a Western Pacific-type plate boundary. *Tectonophysics* **2012**, *532*, 271–290.

60. Li, J.; Dong, S.; Cawood, P.A.; Zhao, G.; Johnston, S.T.; Zhang, Y.; Xin, Y. An Andean-type retro-arc foreland system beneath northwest South China revealed by SINOPROBE profiling. *Earth Planet. Sci. Lett.* **2018**, *490*, 170–179.

61. Xu, C.; Zhang, L.; Shi, H.; Brix, M.R.; Huhma, H.; Chen, L.; Zhang, M.; Zhou, Z. Tracing an Early Jurassic magmatic arc from South to East China Seas. *Tectonics* **2017**, *36*, 466–492.

62. Yui, T.F.; Chu, H.T.; Suga, K.; Lan, C.Y.; Chung, S.H.; Wang, K.L.; Grove, M. Subduction-related 200 Ma Talun metagranite, SE Taiwan: An age constraint for palaeo-Pacific plate subduction beneath South China Block during the Mesozoic. *Int. Geol. Rev.* **2016**, *59*, 333–334.

63. Wang, Q.; Xu, J.-F.; Jian, P.; Bao, Z.-W.; Zhao, Z.-H.; Li, C.-F.; Xiong, X.-L.; Ma, J.-L. Petrogenesis of Adakitic Porphyries in an Extensional Tectonic Setting, Dexing, South China: Implications for the Genesis of Porphyry Copper Mineralization. *J. Pet. 2006*, *47*, 119–144.

64. Liu, X.; Fan, H.-R.; Evans, N.J.; Batt, G.E.; McInnes, B.I.A.; Yang, K.-F.; Qin, K.-Z. Cooling and exhumation of the mid-Jurassic porphyry copper systems in Dexing City, SE China: Insights from geo- and thermochronology. *Miner. Deposita* **2014**, *49*, 809–819.

65. Zhou, Q.; Jiang, Y.H.; Liao, S.Y.; Zhao, P.; Jin, G.D.; Jia, R.Y.; Liu, Z.; Xu, S.M. SHRIMP zircon U-Pb dating and Hf isotope studies of the diorite porphyrite from the Dexing copper deposit. *Acta Geol. Sin.* **2012**, *86*, 1726–1734. (In Chinese with English Abstract).

66. Gao, F.Z. Alteration of Dexing porphyry copper (molybdenum). *Shanghai Geol. 1992*, *2*, 24–35. (In Chinese with English abstract).

67. Pan, X.F.; Song, Y.C.; Wang, S.X.; Li, Z.Q.; Yang, Z.M.; Hou, Z.Q. Evolution of hydrothermal fluid of Dexing Tongchang copper-gold porphyry deposit. *Acta Geol. Sin.* **2009**, *12*, 1929–1950. (In Chinese with English abstract).

68. Rui, Z.Y.; Huang, C.K.; Qi, G.M.; Xu, Y.; Zhang, H.T. Porphyry Copper (Molybdenite) Deposits of China; Geological Publishing House: Beijing, China, 1984; pp. 242–252 (in Chinese with English abstract).

69. Jochum, K.P.; Weis, U.; Stoll, B.; Kuzmin, D.; Yang, Q.; Raczek, I.; Jacob, D.E.; Stracke, A.; Birbaum, K.; Frick, D.A.; et al. Determination of Reference Values for NIST SRM 610-617 Glasses Following ISO Guidelines. *Geostand. Geoanalytical Res.* **2011**, *35*, 397–429.

70. Audôtat, A.; Garbe-Schönberg, D.; Kronz, A.; Pettke, T.; Rusk, B.; Donovan, J.J.; Lowers, H.A. Characterisation of a natural quartz crystal as a reference material for microanalytical determination of Ti, Al, Li, Fe, Mn, Ga and Ge. *Geostand. Geoanalytical Res.* **2015**, *39*, 171–184.

71. Liu, Y.; Hu, Z.; Gao, S.; Günther, D.; Xu, J.; Gao, C.; Chen, H. In situ analysis of major and trace elements of anhydrous minerals by LA-ICP-MS without applying an internal standard. *Chem. Geol.* **2008**, *257*, 34–43.

72. Roedder, E. Fluid inclusions. *Rev. Mineral.* **1984**, *12*, 11-16.

73. Steele-MacInnis, M.; Lecumberri-Sanchez, P.; Bodnar, R.J. HokieFlincs_H₂O-NaCl: A Microsoft Excel spreadsheet for interpreting microthermometric data from fluid inclusions based on the PVTX properties of H₂O-NaCl. *Comput. Geosci.* **2012**, *49*, 334–337.

74. Rusk, B.G.; Reed, M.H.; Dilles, J.H. Fluid Inclusion Evidence for Magmatic-Hydrothermal Fluid Evolution in the Porphyry Copper-Molybdenum Deposit at Butte, Montana. *Econ. Geol.* **2008**, *103*, 307–334.

75. Ostapenko, G.T.; Tarashchan, A.N.; Mitsyuk, B.M. Rutile-quartz geothermobarometer. *Geochem. Int.* **2007**, *45*, 506–508.

76. Thomas, J.B.; Watson, E.B.; Spear, F.S.; Wark, D.A. TitaniQ recrystallized: Experimental confirmation of the original Ti-in-quartz calibrations. *Contrib. Mineral. Petrol.* **2015**, *169*, 27.

77. Acosta, M.D. Titanium in Quartz during Growth and Deformation under Hydrothermal-Magmatic Conditions. Doctoral Dissertation, University of Oregon, Eugene, OR, USA, 2020.

78. Raimbourg, H.; Famin, V.; Canizarès, A.; Le Trong, E. Fluid pressure changes recorded by trace elements in quartz. *Geochem. Geophys. Geosystems* **2022**, *23*, e2022GC010346.

79. Rusk, B.; Reed, M.; Bignall, G.; Tsuchiya, N. Natural and synthetic quartz growth and dissolution revealed by scanning electron microscope cathodoluminescence. In Proceedings of the 14th International Conference on the Properties of Water and Steam, Kyoto, Japan, 29 August–3 September 2004.

80. Rusk, B. Cathodoluminescent Textures and Trace Elements in Hydrothermal Quartz. In *Quartz: Deposits, Mineralogy and Análtyics*; Springer Geology: Berlin/Heidelberg, Germany, 2012; pp. 307–329.

81. Vasyukova, O.V.; Kamenetsky, V.S.; Goemann, K.; Davidson, P. Diversity of primary CL textures in quartz from porphyry environments: Implication for origin of quartz eyes. *Contrib. Miner. Pet.* **2013**, *166*, 1253–1268.

82. Monnier, L.; Lach, P.; Salvi, S.; Melleton, J.; Bailly, L.; Béziat, D.; Monnier, Y.; Gouy, S. Quartz trace-element composition by LA-ICP-MS as proxy for granite differentiation, hydrothermal episodes, and related mineralization: The Beauvoir Granite (Echassières district), France. *Lithos* **2018**, *320*, 355–377.

83. Tanner, D.; Henley, R.W.; Mavrogenes, J.A.; Holden, P. Combining in situ isotopic, trace element and textural analyses of quartz from four magmatic-hydrothermal ore deposits. *Contrib. Mineral. Petrol.* **2013**, *166*, 1119–1142.

84. Li, X.-H.; Klyukin, Y.; Steele-MacInnis, M.; Fan, H.-R.; Yang, K.-F.; Zoheir, B. Phase equilibria, thermodynamic properties, and solubility of quartz in saline-aqueous-carbonic fluids: Application to orogenic and intrusion-related gold deposits. *Geochim. Cosmochim. Acta* **2020**, *283*, 201–221.
85. Blount, C.W.; Dickson, F.W. The solubility of anhydrite (CaSO₄) in NaCl-H₂O from 100 to 450 °C and 1 to 1000 bars. *Geochim. Cosmochim. Acta* **1969**, *33*, 227-245.

86. Lloyd, G.E.; Freeman, B. Dynamic recrystallization of quartz under greenschist conditions. *J. Struct. Geol.* **1994**, *16*, 867-881.

87. Stipp, M.; Stünitz, H.; Heilbronner, R.; Schmid, S.M. Dynamic recrystallization of quartz: Correlation between natural and experimental conditions. *Geol. Soc. London, Spéc. Publ.* **2002**, *200*, 171-190.

88. Ashley, K.T.; Carlson, W.D.; Law, R.D.; Tracy, R.J. Ti resetting in quartz during dynamic recrystallization: Mechanisms and significance. *Am. Mineral.* **2014**, *99*, 2025-2030.

89. Nachlas, W.O.; Hirth, G. Experimental constraints on the role of dynamic recrystallization on resetting the Ti-in-quartz thermo-barometer. *J. Geophys. Res. Solid Earth* **2015**, *120*, 8120-8137.

90. Nachlas, W O.; Thomas, J.B.; Hirth, G. TitaniQ deformed: Experimental deformation of out-of-equilibrium quartz porphyroclasts. *J. Struct. Geol.* **2018**, *116*, 207-222.

91. Burnham, C.W. Magmas and hydrothermal fluids. In *Geochemistry of Hydrothermal Ore Deposits*; Barnes, H.L., Ed.; John Wiley & Sons: Hoboken, NJ, USA, 1997; pp. 63-118.

92. Fournier, R.O. Hydrothermal processes related to movement of fluid from plastic into brittle rock in the magmatic-epithermal environment. *Econ. Geol.* **1999**, *94*, 1193-1211.

93. Gustafson, L.B.; Hunt, J.P. The porphyry copper deposit at El Salvador, Chile. *Econ. Geol.* **1975**, *70*, 857-912.

94. Arancibia, O.N.; Clark, A.H. Early magnetite-amphibole-plagioclase alteration-mineralization in the Island copper porphyry copper-gold-molybdenum deposit, British Columbia. *Econ. Geol.* **1996**, *91*, 402-438.

95. Gustafson, L.B.; Quiroga, G.; Patterns of mineralization and alteration below the porphyry copper orebody at El Salvador, Chile. *Econ. Geol.* **1995**, *90*, 2-16.

96. Dilles, J.H.; Solomon, G.C.; Taylor, H.P.; Einaudi, M.T. Oxygen and hydrogen isotope characteristics of hydrothermal alteration at the Ann-Mason porphyry copper deposit, Yerington, Nevada. *Econ. Geol.* **1992**, *87*, 44-63.

97. Masterman, G.J.; Cooke, D.R.; Berry, R.F.; Walshe, J.L.; Lee, A.W.; Clark, A.H. Fluid Chemistry, Structural Setting, and Emplacement History of the Rosario Cu-Mo Porphyry and Cu-Ag-Au Epithermal Veins, Collahuasi District, Northern Chile. *Econ. Geol.* **2005**, *100*, 835-862.

98. Richards, J.P. The oxidation state, and sulfur and Cu contents of arc magmas: Implications for metallogeny. *Lithos* **2015**, *233*, 27-45.

99. Seedorff, E.; Barton, M.D.; Stavast, W.J.; Maher, D.J. Root zones of porphyry systems: Extending the porphyry model to depth. *Econ. Geol.* **2008**, *103*, 939-956.

100. Einaudi, M.T.; Hedenquist, J.W.; Inan, E.E. Sulfidation state of fluids in active and extinct hydrothermal systems: Transitions from porphyry to epithermal environments. *Spec. Publ.-Soc. Econ. Geol.* **2003**, *10*, 285-314.

101. Liang, H.Y.; Sun, W.C.; Zartman, R.E. Porphyry copper-gold mineralization at Yulong, China, promoted by decreasing redox potential during magnetite alteration. *Econ. Geol.* **2009**, *104*, 587-596.

102. Kouzmanov, K.; Pokrovski, G.S. Hydrothermal controls on metal distribution in porphyry Cu (-Mo-Au) systems. *Spec. Publ. Soc. Econ. Geol.* **2012**, *16*, 573-618.

103. Schmidt, C.; Watenphul, A.; Jahn, S.; Schäpan, I.; Scholten, L.; Newville, M.G.; Lanzotti, A. Copper complexation and solubility in high-temperature hydrothermal fluids: A combined study by Raman, X-ray fluorescence, and X-ray absorption spectroscopies and ab initio molecular dynamics simulations. *Chem. Geol.* **2018**, *494*, 69-79.

104. Brimhall, G. Deep hypogene oxidation of porphyry copper potassium-silicate protore at Butte, Montana; a theoretical evaluation of the copper remobilization hypothesis. *Econ. Geol.* **1980**, *75*, 384-409.

**Disclaimer/Publisher's Note:** The statements, opinions and data contained in all publications are solely those of the individual author(s) and contributor(s) and not of MDPI and/or the editor(s). MDPI and/or the editor(s) disclaim responsibility for any injury to people or property resulting from any ideas, methods, instructions or products referred to in the content.
85. Blount, C.W.; Dickson, F.W. The solubility of anhydrite (CaSO₄) in NaCl-H₂O from 100 to 450 °C and 1 to 1000 bars. *Geochim. Cosmochim. Acta* **1969**, *33*, 227-245.

86. Lloyd, G.E.; Freeman, B. Dynamic recrystallization of quartz under greenschist conditions. *J. Struct. Geol.* **1994**, *16*, 867-881.

87. Stipp, M.; Stünitz, H.; Heilbronner, R.; Schmid, S.M. Dynamic recrystallization of quartz: Correlation between natural and experimental conditions. *Geol. Soc. London, Spéc. Publ.* **2002**, *200*, 171-190.

88. Ashley, K.T.; Carlson, W.D.; Law, R.D.; Tracy, R.J. Ti resetting in quartz during dynamic recrystallization: Mechanisms and significance. *Am. Mineral.* **2014**, *99*, 2025-2030.

89. Nachlas, W.O.; Hirth, G. Experimental constraints on the role of dynamic recrystallization on resetting the Ti-in-quartz thermo-barometer. *J. Geophys. Res. Solid Earth* **2015**, *120*, 8120-8137.

90. Nachlas, W O.; Thomas, J.B.; Hirth, G. TitaniQ deformed: Experimental deformation of out-of-equilibrium quartz porphyroclasts. *J. Struct. Geol.* **2018**, *116*, 207-222.

91. Burnham, C.W. Magmas and hydrothermal fluids. In *Geochemistry of Hydrothermal Ore Deposits*; Barnes, H.L., Ed.; John Wiley & Sons: Hoboken, NJ, USA, 1997; pp. 63-118.

92. Fournier, R.O. Hydrothermal processes related to movement of fluid from plastic into brittle rock in the magmatic-epithermal environment. *Econ. Geol.* **1999**, *94*, 1193-1211.

93. Gustafson, L.B.; Hunt, J.P. The porphyry copper deposit at El Salvador, Chile. *Econ. Geol.* **1975**, *70*, 857-912.

94. Arancibia, O.N.; Clark, A.H. Early magnetite-amphibole-plagioclase alteration-mineralization in the Island copper porphyry copper-gold-molybdenum deposit, British Columbia. *Econ. Geol.* **1996**, *91*, 402-438.

95. Gustafson, L.B.; Quiroga, G.; Patterns of mineralization and alteration below the porphyry copper orebody at El Salvador, Chile. *Econ. Geol.* **1995**, *90*, 2-16.

96. Dilles, J.H.; Solomon, G.C.; Taylor, H.P.; Einaudi, M.T. Oxygen and hydrogen isotope characteristics of hydrothermal alteration at the Ann-Mason porphyry copper deposit, Yerington, Nevada. *Econ. Geol.* **1992**, *87*, 44-63.

97. Masterman, G.J.; Cooke, D.R.; Berry, R.F.; Walshe, J.L.; Lee, A.W.; Clark, A.H. Fluid Chemistry, Structural Setting, and Emplacement History of the Rosario Cu-Mo Porphyry and Cu-Ag-Au Epithermal Veins, Collahuasi District, Northern Chile. *Econ. Geol.* **2005**, *100*, 835-862.

98. Richards, J.P. The oxidation state, and sulfur and Cu contents of arc magmas: Implications for metallogeny. *Lithos* **2015**, *233*, 27-45.

99. Seedorff, E.; Barton, M.D.; Stavast, W.J.; Maher, D.J. Root zones of porphyry systems: Extending the porphyry model to depth. *Econ. Geol.* **2008**, *103*, 939-956.

100. Einaudi, M.T.; Hedenquist, J.W.; Inan, E.E. Sulfidation state of fluids in active and extinct hydrothermal systems: Transitions from porphyry to epithermal environments. *Spec. Publ.-Soc. Econ. Geol.* **2003**, *10*, 285-314.

101. Liang, H.Y.; Sun, W.C.; Zartman, R.E. Porphyry copper-gold mineralization at Yulong, China, promoted by decreasing redox potential during magnetite alteration. *Econ. Geol.* **2009**, *104*, 587-596.

102. Kouzmanov, K.; Pokrovski, G.S. Hydrothermal controls on metal distribution in porphyry Cu (-Mo-Au) systems. *Spec. Publ. Soc. Econ. Geol.* **2012**, *16*, 573-618.

103. Schmidt, C.; Watenphul, A.; Jahn, S.; Schäpan, I.; Scholten, L.; Newville, M.G.; Lanzotti, A. Copper complexation and solubility in high-temperature hydrothermal fluids: A combined study by Raman, X-ray fluorescence, and X-ray absorption spectroscopies and ab initio molecular dynamics simulations. *Chem. Geol.* **2018**, *494*, 69-79.

104. Brimhall, G. Deep hypogene oxidation of porphyry copper potassium-silicate protore at Butte, Montana; a theoretical evaluation of the copper remobilization hypothesis. *Econ. Geol.* **1980**, *75*, 384-409.

**Disclaimer/Publisher's Note:** The statements, opinions and data contained in all publications are solely those of the individual author(s) and contributor(s) and not of MDPI and/or the editor(s). MDPI and/or the editor(s) disclaim responsibility for any injury to people or property resulting from any ideas, methods, instructions or products referred to in the content.